MINERALS - anubih
MINERALS - anubih
MINERALS - anubih
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Fabijan Trubelja, PhD<br />
Professor emeritus, University of Sarajevo<br />
Ljudevit Barić, PhD<br />
Professor emeritus, University of Zagreb<br />
<strong>MINERALS</strong><br />
of Bosnia and Herzegovina<br />
Part 1 – Silicates<br />
ANU<br />
BiH<br />
AHY<br />
БиХ<br />
Sarajevo, 2011
SILICATES<br />
Fabijan Trubelja and Ljudevit Barić<br />
Minerals of Bosnia and Herzegovina<br />
Part 1 – Silicates<br />
Original title:<br />
Minerali Bosne i Hercegovine. Knjiga I – Silikati.<br />
Translated by Prof. Goran Kniewald,* 1 PhD<br />
Publisher:<br />
Academy of Sciences and Arts of Bosnia and Herzegovina, Sarajevo<br />
Editor:<br />
Acad. Enver Mandžić, PhD<br />
Technical revision:<br />
Prof. Goran Kniewald, PhD, Acad. Enver Mandžić, PhD<br />
DTP:<br />
Štamparija „Fojnica“, Fojnica<br />
Printed in Fojnica, Bosnia and Herzegovina,<br />
by “Štamparija Fojnica“ D.D. Fojnica, 2011<br />
Circulation:<br />
300<br />
CIP - Katalogizacija u publikaciji<br />
Nacionalna i univerzitetska biblioteka<br />
Bosne i Hercegovine, Sarajevo<br />
549.6(497.6)<br />
TRUBELJA, Fabijan<br />
Minerals of Bosnia and Herzegovina. ½Pt. ½1, Silicates /<br />
Fabijan Trubelja, Ljudevit Barić ; [translated by Goran Kniewald].<br />
- Sarajevo : Academy of Sciences and Arts of Bosnia and<br />
Herzegovina, 2011. - 356 str. : graf. prikazi ; 24 cm<br />
Prijevod djela: Minerali Bosne i Hercegovine. - Fabijan Trubelja, Ljudevit Barić: str. 6-7. -<br />
Bibliografija: str. 424-448.<br />
ISBN 978-9958-501-65-4<br />
1. Barić, Ljudevit<br />
COBISS.BH-ID 19153670<br />
* Goran Kniewald (1955, Zagreb), Senior scientist and and Head of Laboratory for Physical Trace<br />
Chemistry, Department of Marine and Environmental Research, Rudjer Boskovic Institute, Zagreb,<br />
Croatia and Professor at the University of Zagreb, Faculty of Science, Department of Geology;<br />
visiting professor or scientist at Université de Toulon-Sud-Var, France; Institute of Chemistry<br />
and Dynamics of the Geosphere, Research Center Juelich, Germany; Scripps Institution of<br />
Oceanography, University of California, USA; Max Planck Institute of Chemistry, Biogeochemistry<br />
department, Germany; Institute of Applied Physical Chemistry, Nuclear Research Center<br />
Juelich, Germany; member of American Geophysical Union, European Union of Geosciences,<br />
Geochemical Society, International Symposia on Environmental Biogeochemistry and permanent<br />
court interpreter of English, German and Serbian language.<br />
2
CONTENTS<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Page<br />
Preface ............................................................................................................ 9<br />
Historical overview of the production, use and exploration of<br />
mineral resources of Bosnia and Hercegovina ............................................. 11<br />
I The period of production and use of mineral resources .......................... 11<br />
II The period of scientific exploration and research ................................... 20<br />
Olivine ........................................................................................................ 30<br />
Garnets.......................................................................................................... 39<br />
Hibschite....................................................................................................... 48<br />
Zircon ........................................................................................................... 48<br />
Thorite .......................................................................................................... 53<br />
Andalusite..................................................................................................... 55<br />
Kyanite ......................................................................................................... 57<br />
Staurolite ...................................................................................................... 59<br />
Braunite ........................................................................................................ 60<br />
Titanite ......................................................................................................... 63<br />
Chloritoide, Ottrelite .................................................................................... 68<br />
Datolite ......................................................................................................... 69<br />
Hemimorphite............................................................................................... 71<br />
Suolunite ...................................................................................................... 72<br />
Clinozoisite – Epidote .................................................................................. 75<br />
Clinozoisite .................................................................................................. 75<br />
Epidote ......................................................................................................... 78<br />
Allanite ......................................................................................................... 85<br />
Zoisite .......................................................................................................... 87<br />
Pumpellyite .................................................................................................. 90<br />
Vesuvianite ................................................................................................... 90<br />
Axinite ......................................................................................................... 90<br />
Beryl ............................................................................................................. 91<br />
Cordierite ................................................................................................... 100<br />
Tourmaline ................................................................................................. 101<br />
Pigeonite..................................................................................................... 111<br />
Diopside and Diallag .................................................................................. 111<br />
Augite ......................................................................................................... 111<br />
Omphacite .................................................................................................. 127<br />
Enstatite, Bronzite, Hypersthene ................................................................ 128<br />
Tremolite, Actinolite .................................................................................. 136<br />
3
SILICATES<br />
Hornblende ................................................................................................. 142<br />
Glaucophane............................................................................................... 155<br />
Crocidolite .................................................................................................. 155<br />
Wollastonite................................................................................................ 157<br />
Tobermorite ................................................................................................ 158<br />
Xonotlite..................................................................................................... 159<br />
Rhodonite ................................................................................................... 164<br />
Pyrophyllite ................................................................................................ 165<br />
Talc ............................................................................................................. 166<br />
Muscovite ................................................................................................... 172<br />
Glauconite .................................................................................................. 179<br />
Phlogopite .................................................................................................. 182<br />
Biotite ......................................................................................................... 183<br />
Illite ............................................................................................................ 191<br />
Hydromuscovite ......................................................................................... 196<br />
Hydrobiotite ............................................................................................... 197<br />
Stilpnomelane ............................................................................................ 198<br />
Montmorillonite ......................................................................................... 198<br />
Beidellite .................................................................................................... 202<br />
Nontronite .................................................................................................. 204<br />
Saponite ..................................................................................................... 206<br />
Vermiculite ................................................................................................. 206<br />
Chlorite group............................................................................................. 206<br />
Kaolinite ..................................................................................................... 217<br />
Dickite ........................................................................................................ 224<br />
Nacrite ........................................................................................................ 224<br />
Chrysocolla ................................................................................................ 224<br />
Serpentine group ........................................................................................ 225<br />
Meta-Halloysite .......................................................................................... 237<br />
Sepiolite ..................................................................................................... 238<br />
Prehnite ...................................................................................................... 242<br />
Searlesite .................................................................................................... 250<br />
Nepheline ................................................................................................... 254<br />
Analcite ...................................................................................................... 254<br />
Sanidine ..................................................................................................... 256<br />
Orthoclase .................................................................................................. 258<br />
Microcline .................................................................................................. 261<br />
Anorthoclase .............................................................................................. 262<br />
Hyalophane ................................................................................................ 264<br />
4
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Plagioclase group ....................................................................................... 274<br />
Albite ......................................................................................................... 274<br />
Oligoclase .................................................................................................. 286<br />
Andesine .................................................................................................... 289<br />
Labradorite ................................................................................................. 295<br />
Bytownite ................................................................................................... 301<br />
Anorthite .................................................................................................... 306<br />
Lazurite ...................................................................................................... 308<br />
Scapolite ..................................................................................................... 308<br />
Natrolite ..................................................................................................... 309<br />
Scolecite ..................................................................................................... 311<br />
Mesolite ..................................................................................................... 313<br />
Thomsonite ................................................................................................ 313<br />
Laumontite ................................................................................................. 316<br />
Stilbite ........................................................................................................ 317<br />
Chabazite .................................................................................................... 319<br />
References .................................................................................................. 326<br />
Index .......................................................................................................... 352<br />
5
SILICATES<br />
FABIJAN TRUBELJA<br />
(Ključ near Varaždin 1927 – Split 2007)<br />
Fabijan Trubelja was born and educated in Ključ near<br />
Varaždin. In 1953, he graduated from the Faculty<br />
of Science, Department of Geology, University<br />
in Zagreb. As of 1953, he worked as an assistant<br />
lecturer for courses in mineralogy and petrology at<br />
the Faculty of Arts, University in Sarajevo. After<br />
having specialised in mineralogical and petrological<br />
research in Zagreb, he returned to Sarajevo and<br />
worked on his doctoral thesis “Petrology and<br />
Petrogenesis of the Magmatic Rocks of the Višegrad<br />
Area in Eastern Bosnia”. After having successfully defended his doctoral thesis, he<br />
was elected senior lecturer in 1959, associate professor in 1968 and full professor<br />
in 1972 at the Faculty of Science, University in Sarajevo. In 1981, he was elected<br />
corresponding member, and in 1987 full member of the Bosnia and Herzegovina<br />
Academy of Sciences and Arts.<br />
As a research worker, from the very beginning, Fabijan Trubelja started a<br />
mineralogical-petrological research of the problems of Triassic and Jurassic<br />
ultrabasic, magmatic rocks, and of the mineralogical features, genesis and<br />
classification of bauxite in Bosnia and Herzegovina, using the results of the<br />
specialist studies he had attended in Zagreb, Moscow and Leningrad. One of his<br />
most important theory contributions in mineralogy is a research into the weathering<br />
crust of the Jablanica gabbro and the emergence of bauxite matter in Herzegovina.<br />
By means of synthesising his theory knowledge and personal investigations in<br />
more than one hundred published papers, he has made a great contribution to the<br />
investigation of the geological evolution of the Dinarides.<br />
Investigations of rare minerals in Bosnia and Herzegovina served him and Ljudevit<br />
Barić as the basis for writing a major work, “Minerals of Bosnia and Herzegovina<br />
– Silicates” in 1979, which was followed by “Minerals of Bosnia and Herzegovina<br />
– Non-Silicates” in 1984. In the capacity of an associate of the Geological Institute<br />
of Bosnia and Herzegovina, he was in charge of the project “Geology of Bosnia and<br />
Herzegovina”, Book IV – “Magmatism and Metalogenia” (1978). The Geological<br />
Institute was awarded Veselin Masleša Prize for this book. As a professor at the<br />
Faculty of Science in Sarajevo and the Faculty of Mining and Geology in Tuzla, he<br />
taught mineralogy, petrography, crystallography and other courses. He also wrote<br />
university textbooks for these courses.<br />
6
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
LJUDEVIT BARIĆ<br />
(Zagreb 1902 – Zagreb 1984).<br />
Born and educated in Zagreb, Ljudevit Barić<br />
graduated from the University of Zagreb in 1927,<br />
receiving degrees in chemistry, physics and<br />
mathematics. These disciplines are fundamental<br />
to the study of mineralogy, the science for which<br />
he developed an enthusiasm already as a student.<br />
In the period 1929-1932 he went to Germany to<br />
study goniometric-methods and crystallometry<br />
with professor Victor Goldschmidt at Heidelberg<br />
where he aquired skills which he subsequently<br />
developed to utmost proficiency. Ljudevit Barić<br />
also took courses in petrological methods (with prof. Erdmannsdörfer), X-ray<br />
crystallography and structure determination methods (prof. Schiebold, Leipzig) and<br />
rotating-stage methods in microscopy (prof. Nikitin, Ljubljana, Slovenia). In 1932<br />
he was appointed as curator of the Museum of Mineralogy and Petrology in Zagreb.<br />
He received his PhD degree at the University of Zagreb in 1935, with a thesis on<br />
kyanite from Prilepac at Mt. Selečka in Macedonia.<br />
His thesis was published in extenso by the Zeitschrift für Kristallographie in<br />
1936, and his data were cited in all significant reference handbooks on optical<br />
mineralogy (Winchell, Tröger and others). He was appointed as assistant<br />
professor (1937) and associate professor (1941) at the University of Zagreb.<br />
After the II World War Ljudevit Barić was commissioned as director of the<br />
Museum of Mineralogy and Petrology in Zagreb (1954), where he worked until<br />
his retirement in 1973. As an adjunct professor of the Faculty of Science in<br />
Zagreb, he taught various courses in the field of mineralogy, and was well-known<br />
among his students as an excellent teacher.<br />
He authored more than 150 scientific and professional publications, and several<br />
books, including the two-volume treatise on the minerals of Bosnia and Hercegovina<br />
(together with Fabijan Trubelja). In 1975, a new mineral – barićite – was named<br />
after him, in honour of his significant contributions to the science of mineralogy.<br />
7
SILICATES<br />
8
Preface<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
This book is a translation of the first part of the two-volume treatise on the<br />
“Minerals of Bosnia and Herzegovina”. Book 1 of this set, dealing with silicate<br />
minerals, was originally published in Serbo-Croatian/Bosnian language in 1979.<br />
Book 2, on nonsilicate minerals, was published in 1984. When published, this<br />
set was the most comprehensive treatise on the minerals found in Bosnia and<br />
Hercegovina – as it is today.<br />
In 2005 the Academy of Sciences and Arts of Bosnia and Herzegovina<br />
decided to translate the two volumes into English and thus make this valuable<br />
encyclopaedic compilation accessible to a much wider audience of mineralogists<br />
and earth scientists. This was initiated by one of the authors-Fabijan Trubelja,<br />
professor emeritus at Sarajevo University. Sadly enough, Fabijan Trubelja passed<br />
away in 2007 and would thus, unfortunately, not see the completion of his project.<br />
The task of editorial supervision of the translation was taken over by Enver Mandžić,<br />
professor at Tuzla University and full member of the Academy of Sciences and Arts<br />
of Bosnia and Herzegovina.<br />
The style in which the two-volume set has been written reflects the<br />
foundations of the subject of mineralogy which lie in the systematic, taxonomic<br />
description of the compositions and structures of minerals and mineral groups. Even<br />
though this approach may today seem somewhat outdated, the translation follows the<br />
original text and only minor modifications have been made in cases where clarity or<br />
modern usage required this. The order in which the minerals are described follows<br />
the classic crystallochemical approach by Hugo Strunz (1966) and the formulae have<br />
also been written following his system. Even the one or two odd minerals which<br />
were subsequently rejected by the Commission on New Minerals and Mineral<br />
Names (CNMMN) of the International Mineralogical Association (IMA) have not<br />
been omitted in this translation. In the section on literature references, all titles of<br />
publications have been translated into English, except for those originally published<br />
in German or French. No new references have been added, except the one on the<br />
new mineral tuzlaite (in volume 2 – nonsilicate minerals), identified in the rock-salt<br />
deposits at Tuzla. This is the first and – up to now – only new mineral which has been<br />
found in Bosnia and Herzegovina. A recently published geological map of Bosnia<br />
has been added to the translation, and most diagrams and drawings were revised and<br />
reproduced using modern graphic tools. Several figures of thermal analysis spectra<br />
were omitted in the translation as they did not provide substantial information, or the<br />
data was duplicated in tables or otherwise.<br />
The editors wish to express their sincere gratitude to Ms. Amra Avdagić<br />
from the Academy of Sciences and Arts of Bosnia and Herzegovina who supervised<br />
the translation project on behalf of the Academy and was instrumental in the keeping<br />
9
SILICATES<br />
of the time plan. Asim Abdurahmanović edited all graphic material and produced<br />
new figures and drawings where required.<br />
The editors – Enver Mandžić and Goran Kniewald<br />
Original title and reference of the two-volume set:<br />
1. Fabijan Trubelja i Ljudevit Barić (1979): Minerali Bosne i Hercegovine. Knjiga<br />
I – silikati. Zemaljski muzej Bosne i Hercegovine, Sarajevo, 452 pp.<br />
2. Ljudevit Barić i Fabijan Trubelja (1984): Minerali Bosne i Hercegovine. Knjiga<br />
II – nesilikati.<br />
Svjetlost, Sarajevo, 571 pp.<br />
10
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Historical overview of the production, use and exploration of mineral<br />
resources of Bosnia and Hercegovina<br />
Research into the history of mining and associated use of the mineral resources<br />
of Bosnia and Hercegovina, from the early times-based upon oldest available data<br />
– has shown that mining has during all those historical periods been an important<br />
activity for the economies of the people and ethnic groups living in the area. The rich<br />
mineral resources of Bosnia and Hercegovina have also attracted conquerors and<br />
others insurgents, but has also been of utmost importance in establishing frameworks<br />
of small scale economies and living conditions of the local, autochtonous population.<br />
The following sections provide a historical overview of the exploration and<br />
use of the mineral resources of Bosnia and Hercegovina, from ancient times until the<br />
middle of the 19 th century. The period of scientific research of our minerals and rocks<br />
will also give an overview of people who have contributed to this research.<br />
I The early period of ore production and use of mineral resources 1<br />
1. Paleolithic to Roman era<br />
There are only very few written documents or archaeological findings<br />
about the early period of mining in Bosnia and Hercegovina. Neither Roman nor<br />
Greek authors have provided any descriptions of these activities. Even more recent<br />
literature dealing with early mining activities in Bosnia and Hercegovina is based<br />
rather on assumptions than on more solid proof. Nevertheless, various archaelogical<br />
artefacts including relicts of mining activities and tools belonging to similar age<br />
groups, provide an indication of the geographical distribution, scale and methods of<br />
mining activities in this area during the early period.<br />
There are three areas of importance in Bosnia and Hercegovina where more<br />
or less extensive and continuous mining activities have been taking place during<br />
ancient times, but also during the Illyrian and subsequent periods of various rulers,<br />
Roman through Austrian. Most important of these is the so called area of “central<br />
Bosnian mountains” located between the rivers Vrbas, Lašva, Neretva, Rama and<br />
their tributaries. The second one is the area of western Bosnia, bordered by the Vrbas<br />
and Una rivers, with its main orebearing formations found in the river-valleys of<br />
Sana and Japra, and their tributaries. The third area is eastern Bosnia, around the<br />
river Drina between the towns of Foča and Zvornik, the principal mining activity<br />
centered around Srebrenica. 1<br />
1 This section was written by Dr Ratimir Gašparović, professor at the Faculty of Natural<br />
Sciences and Mathematics in Sarajevo. His contribution is gratefully acknowledged.<br />
11
SILICATES<br />
Ores of various metals, including iron, are found in these areas and exploitation<br />
has been going on for more than 5000 years – from the period of prehistoric human<br />
settlers, thorugh Illyrian, Roman, Slavic, Turkish and Austrian rulers, into the present.<br />
Various metals were extracted from these ores, including antimony, nickel, arsenic,<br />
manganese, chromium, copper, zinc, lead, bismuth, tin, cadmium, mercury, gold,<br />
silver and iron. But man, especially the prehistoric man, used these ores but also other<br />
minerals like quartz which was of importance for his daily life. It was found that the<br />
choice of temporary settlements of palaeolithic man was influenced by sources of<br />
quartz material – the palaeolithic settlements in the valleys of the rivers Ukrina and<br />
Bosna were close to these sources (Benac 1964, p. 17).<br />
The mountains of central Bosnia are the most important area in Bosnia and<br />
Hercegovina where mining activities took place during the prehistoric and Illyrian<br />
periods. There are numerous remnants of mining and smeltering activity, including<br />
slag heaps, remnants of smelters, and washing sites. The most significant areas<br />
where mining took place are Mt. Vranica, the area around the township of Gornji<br />
Vakuf with tributaries of the rivers Vrbas, Bistrica and Krupa, the Lašva river valley<br />
and areas around Kreševo, Fojnica, Busovača and Vareš (Čurčić 1908, p. 86-89).<br />
Already the oldest evidence of mining during the Illyrian period shows that<br />
substantial amounts of gold were produced from the alluvial deposits of the Vrbas<br />
and Lašva rivers and their numerous tributaries. Some Illyrian tribes probably lived<br />
in the “gold areas” of central Bosnia and were engaged in gold production. Thus the<br />
Ardianes living in the Lašva river valley fought the Antariates tribe, living around<br />
Fojnica and the Vrbas, Rama and Neretvica watershed, because of the gold. The<br />
Antariates were the most powerful Illyrian tribe, and they were neither agricultural<br />
nor artisanal people. Their wealth and power was rather based on gold (Rücker 1896,<br />
p. 18). According to some more recent authors, the Illyrians were knowledgable<br />
not only about the production of gold, but also of silver, lead, iron, copper and zinc<br />
(Pašalić 1975, p. 278).<br />
The oldest iron production centers in Bosnia appeared during the Iron Age<br />
(8 th – 1 st century BC). Mining and iron working in this area was already taking place<br />
during the Bronze Age, evidence of which is provided by occurences of iron ores<br />
and production of charcoal used for smeltering. The locations of some slag heaps in<br />
mountainous areas around Fojnica and Kreševo indicate that mining was taking place<br />
here already in the pre-Roman i.e. Illyrian period, since it is well known that these<br />
tribes had their smelting camps located in well fortified and inaccessisble places.<br />
Several slag heaps, indicating the presence of smelting camps were thus found at the<br />
mountains of Vranica, Inč, Zahor, Lisina near Konjic, Karaula above Gornji Vakuf,<br />
Vilenica and Komar near Travnik, Konjuh near Olovo, Stožer west of Olovo and<br />
elsewhere (Pašalić 1975, p. 156).<br />
12
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Contemporary development of mining and ironworking occured in<br />
northwestern Bosnia around the Sana river and its tributaries. A number of artefacts<br />
(slag, moulds, tools etc.) found close to prehistoric settlements around Sanski Most<br />
indicate that extensive iron working was taking place in this area (Fiala 1899, p. 62-<br />
128). Particularly large slag heaps were found at Blagaj in the Japra river valley, and<br />
around Čela (Radimsky 1891, p. 443-444). The amount of weathered slag together<br />
with the absence of other smelting constructions in a surrounding of dense oaktrees<br />
imply a very primitive iron working process, probably one of the first such activities<br />
in Bosnia. A similar Illyrian settlement where iron working was done is located in the<br />
Gradina and Majdan area near Jajce (group of authors 1966, p. 161-163; Radimsky<br />
1893, p. 180-183).<br />
During the Bronze Age, copper mining and copper working was taking place<br />
around the settlements of Mračaj and Mačkara, southeast of Gornji Vakuf. Remnants<br />
of smetling activities were found at Mt. Gradina near the village of Varvare close to<br />
the source of the Rama river. According to several researchers of prehistoric Bosnia<br />
and Hercegovina, extensive copper working was done in the area of the Rama river<br />
(Katzer 1907, p. 23; Čurčić 1908, p. 86-89). Metalurgical activity also existed at<br />
Debelo Brdo, located on the western flanks of Mt. Trebević, where one of the major<br />
Bronze Age settlements existed around Zlatište – Soukbunar (Čurčić 1908, p. 85).<br />
2. The Roman Period (1 st – 4 th Century)<br />
When the Roman Empire became a significant military and political factor<br />
during the 3 rd century BC, its influence spread to the eastern Adriatic coast and<br />
its extensive hinterland, all the way north to the Danube. This area was inhabited<br />
by numerous Illyrian tribes, whose political and military organization was not<br />
particularly well founded. The Romans were very much aware of the geostrategic<br />
and economic potential of this region, and by conquering the area they secured their<br />
presence in the Adriatic, including important lines of communication between Italy,<br />
the Danubian basin and further on to the Middle East. The Illyrian region also had<br />
extensive resources in metal ores, timber and arable land. Immediately after their<br />
final conquest of the Illyrian lands in year 9 AD, the Romans partitioned the area<br />
into two major provinces: Dalmatia and Panonia. Most of the territory of Bosnia and<br />
Hercegovina became part of Dalmatia, while only the northernmost part, north of the<br />
line Bosanski Novi – Banja Luka – Doboj – Zvornik – Bijeljina were included into<br />
the province of Panonia.<br />
Mining activities had an important role for the economy of the Roman<br />
province of Dalmatia, since Bosnia had the most significant resources of metal ores<br />
of the entire province. Some information about mining and metal working in this<br />
part of the Roman Empire can be found in writings of several authors (Anonymous<br />
13
SILICATES<br />
1879; Plinius 1873), but most of the evidence is to be found in the field – remnants<br />
of mining and smeltering activity as well as administrative documents pertaining<br />
to mining. The first three hundred years after the Roman conquest in 9 AD were a<br />
period of peaceful economic and social development for local populations, including<br />
extensive mining activities. There is, therefore, evidence of mining and metal<br />
working from the first decades of Roman rule in Bosnia until its decline in the 4 th<br />
century. Mining and smelting of gold started immediately, this being a continuation<br />
of earlier practice, from prehistoric times, over the Illyrian period to the Roman rule.<br />
The most productive gold mines during the Roman era were those around<br />
the upper part of the river Vrbas. There is ample evidence that the diluvial deposits<br />
of Mt. Vranica were mined for gold at the following localities: Rosinje, Radovine,<br />
Devetak, Crvena Zemlja, Uložnica, Zlatno Guvno etc. The alluvial sediments of the<br />
Bistrica and Krupa brooks, tributaries of the Vrbas river close to Gornji Vakuf, have<br />
been panned for gold and large amounts of washed-out gravel and sand was found<br />
in the area. Structures containing objects related to gold mining were located nearby<br />
(Jireček 1951, p. 69; Conrad 1871, p. 220; Rücker 1896, p. 20) 2 .<br />
Extensive gold washing sites during the Roman period were located in the<br />
Lašva river valley at Vrela, Čosići, Đelilovci, where large piles of washed gravel<br />
can still be seen. Along the tributaries of Lašva river – Kaurski brook, Grovica,<br />
Večeriska, Dubravica, Dolovski brook, Krčevina brook, Panovac, Vraniska brook<br />
etc. similar larger or smaller gravel piles are located (Simić 1951, p. 117; Rückner<br />
1896, p. 18-60).<br />
The largest Roman gold washing sites were located in the Fojnička Rijeka<br />
river valley and Željeznica, tributary to the former. The washed-out material on these<br />
sites is around 15-20 meters thick, i.e. west of Gomionica (Foullon 1893, p. 46).<br />
Due to the military character of the Roman Empire, and the numerous<br />
conquests and military missions it has undertaken, the need for iron mining and<br />
working became especially great during their rule in Bosnia and Hercegovina (Pašalić<br />
1975, p. 46). During the Roman rule, mining activities increased substantially as<br />
compared to the Illyrian period – especially pertaining to iron production. Iron ore<br />
mined in Bosnia was transported to large state smeltering facilities at Sisak, Mitrovica<br />
and to Italy, due to the fact that transportation of ore from Bosnia was easier and<br />
cheaper than transport from other Roman provinces, or beyond those (Mikolji 1969,<br />
p. 18-19). Important sites of Roman iron ore mining and workings were at Bugojno,<br />
Donji and Gornji Vakuf, between Busovača and Kiseljak, at Fojnica, Kreševo, Vareš<br />
and Breza. Large amounts of iron slag originating from Roman and pre-Roman<br />
2 Plinius the elder who lived during the reign of Emperor Nero in the 1 st century AD notes<br />
that in the Gornji Vakuf area gold could be found on the ground, and sometimes as much<br />
as 50 pounds could be gathered in a single day<br />
14
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
activities was found in the vicinity of these sites. Substantial mining was done also in<br />
the western-Bosnian ore province, encompassing the watersheds of the rivers Sana,<br />
Una and Japra. Mines were located at Ljubija, Sanski Most, Blagaj, Bosanski Novi<br />
and elsewhere. Large amounts of slag was found at Ljubija (Adamuša). The local<br />
mining administration was located at Briševo near Ljubija (Pašalić 1975, p. 269;<br />
Mandić 1931, p. 35; Radimsky 1891, p. 431 and 437).<br />
Extensive iron mining was also done around Majdan and Sinjakovo, near<br />
Jajce. There are indications that copper was also mined and worked in this area<br />
during the Roman period. Today, the impact of mining during the Austro-Hungarian<br />
rule prevails in the area.<br />
Remnants of smelters can be seen in the vicinity of Mrkonjić-Grad, as well<br />
as in the town itself. This area was at a crossroads of Roman lines of communication,<br />
and it may be inferred that also here mining was important during the Roman period<br />
(Patsch 1898, p. 493).<br />
The third region important for mining activities during the Roman rule is in<br />
eastern Bosnia, the most important sites around the Jadro river valley, at Ljubovija<br />
and Srebrenica. Close to Srebrenica was the Roman township of Domavia where<br />
lead ore was being mined and smeltered. The ead ore was also the source of silver,<br />
which alongside with gold and iron was the main mining product of Bosnia at the<br />
time. Some remnants indicate possible Roman mining activities around Foča (Pašalić<br />
1975, p. 264; Pogatschnik 1890, p. 125).<br />
Mercury production from cinnabar, tetrahedrite or their decomposition<br />
products probably took place already during the Roman period in Bosnia, although<br />
precise information is lacking. Since mercury is important in collecting small gold<br />
particles, it may be expected that some mercury production was going on since the<br />
requisite ore minerals were available. This was probably done at Čemernica, north<br />
of Fojnica and at Vranak close to Kreševo (Simić 1951, p. 130).<br />
The decline of the Roman Empire in the 4 th century AD saw also a decline<br />
in mining activities in Bosnia, especially with respect to iron production. Frequent<br />
hostile insurgencies into Roman provinces by Huns, Vandals, Markomans, Alans<br />
and Goths occured during the 5 th century AD and looting was common. This also<br />
happened in Bosnia and Hercegovina, and the 300-year long rule of the Romans was<br />
terminated in the year 480 AD when the Gothic ruler Odoacar occupied Bosnia west<br />
of the Drina river.<br />
15
SILICATES<br />
16<br />
3. The Middle Ages (Early Slavic period – The State of Bosnia<br />
in the Middle Ages, 7 th Century – 1463) 3<br />
The prehistoric and Roman mining activities becan to decline in Bosnia and<br />
Hercegovina when the major movements of peoples commenced. Most of the mines in<br />
Bosnia and Hercegovina ceased their operations by the end of the 6 th century, coinciding<br />
with the insurgencies of Slavic and Avar tribesmen into the region of the Balkans, and<br />
particularly Bosnia and Hercegovina. A revival of mining in the region took place<br />
only the latter part of the Middle Ages. In the late 12 th and early 13 th centuries Bosnia<br />
was ruled by Ban Kulin, during whose reign Bosnia experienced a significant rise in<br />
terms of political issues, economy and culture. Trade between Bosnia and Dubrovnik<br />
began in this period. Businessmen from Dubrovnik were granted mining concessions<br />
in Bosnia, and their colonies and townships became important in and around mining<br />
areas – at Duboštica, Kamenica, Olovo, Srebrenica, Fojnica, Ostružica etc. During the<br />
13 th and early 14 th centuries Bosnia was ruled by Bans (a local ruler or viceroy) among<br />
which Stjepan Kotromanić II was the most important one. Bosnia flourished during his<br />
reign, with territories between the Sava river and the Adriatic coast, and the Cetina and<br />
drina rivers. A revival of mining activities takes place during this time, which coincides<br />
with a decline of mining activities in the rest of Europe. New mines were opened in<br />
numerous locations and they flourished until the end of the middle-age Bosnian state<br />
during the 15 th century. The most important mining area of those days was the central-<br />
Bosnian ore province with eight active mines producing silver, lead, copper and iron,<br />
while information on gold production is inconsistent.<br />
Silver was the most important metal produced in most of the mines in central<br />
Bosnia. Apart from the mine at Busovača which produced iron and Olovo producing<br />
lead, all other mines produced silver – the most productive ones at Fojnica, Kreševo,<br />
Dusina and Deževica (Jireček 1951, p. 69; Kovačević 1961).<br />
Gold production during the Middle Ages in Bosnia cannot be compared with<br />
Roman times, when production was considerably larger. The old gold washings were<br />
worked by Saxon miners which were invited from Erdelj and Banat by the Bans of<br />
Bosnia during the 13 th century. They re-washed those parts of the deposits which<br />
were considered to be nonfeasible for production during the Roman rule. This was<br />
the case with gold-washings at Vranica, and along the rivers Bistrica, Krupa, Vrbas,<br />
Lašva, Fojnička Rijeka and Lepenica, as well as their tributaries.<br />
Concerning iron, it can be said that middle-age Bosnia was the only state in<br />
the Balkans which was not only selfsustaining in the production of iron but also was<br />
3 The symposium ‘Mining and metallurgy in Bosnia and Hercegovina from prehistoric<br />
times to the 20th century’ was held in October 1973 in Zenica. Professor M. Vego<br />
presented a lecture on ‘The sources of information on mining in Bosnia and Hercegovina<br />
in the Middle Ages – 7th to 15th century’, p. 1-21, which we have cited here.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
able to export this commodity, mainly to Venice and the Middle East. The beginning<br />
of the 14 th century saw steady exports of iron to Dubrovnik, the Venetian republic and<br />
to southern Italy. The Bans and Kings of Bosnia maintained in their possession the<br />
mining areas around Skoplje on Vrbas, and the areas around Fojnica, Olovo and Vareš.<br />
The main production and export centers were at Visoko and Konjic (Mikolji 1969).<br />
Lead was, next to silver, the most important metal in terms of production<br />
quantities. The main production centres were at Deževica and Olovo, famous for its<br />
lead mines operated in the 14 th and 15 th centuries.<br />
The Saxon miners were especially active in producing mercury from<br />
cinnabar, and the Čemernica mine – north of Fojnica – was considered as one of the<br />
most important bosnian mercury mines (Simić 1951, p. 124).<br />
After the death of King Tvrtko at the end of the 14 th century Bosnia was<br />
involved in numerous battles for the throne, fought by a number of bosnian feudal<br />
landlords whose might arose from political, economic and military power. After a<br />
period of internal turmoil, which resulted in a steady decline of its territory, Bosnia<br />
was finally occupied by the Turks in 1463 which had started their raids and conquests<br />
already during the late 14 th century.<br />
4. Period of Ottoman rule<br />
(1463 – early geological investigations in the mid-19 th Century) 4<br />
The mining and production of metals in Bosnia, and elsewhere in the Balkan<br />
region, was revived with the advent of Ottoman rule. Production was continued using<br />
the technologies and manpower already available locally. The Saxon miners, which<br />
had been so important for maining practices in Bosnia during the Middle Age, had<br />
the most expertise. The businesspeople of Dubrovnik retained most of the mining<br />
claims. Nevertheless, there was a short period during which mining seems to have<br />
been interrupted, at the beginning of Ottoman rule. To mediate the problem, new<br />
mining regulations were introduced, including new contracts and mining concessions<br />
(Škarić 1935 and 1939; Spaho 1913, p. 133-194; Truhelka 1936).<br />
4 Most of the information about this period can be found in the following publications: A.<br />
Handžić – 1. ‘Oldest turkish sources of information on mines in Bosnia’. Lecture presented<br />
at the Symposium on Balkanology in Istanbul, 15-21.9.1973. – 2. ‘Mining and mining areas<br />
in Bosnia in the second half of the 15th century’ and the publication by R. Skender ‘Mining<br />
in Bosnia during the 16th and 17th centuries based on turkish information sources’ –<br />
presented at the Symposium ‘Mining and metallurgy in Bosnia and Hercegovina from<br />
prehistoric times to early 20th century’, held in Zenica in October 1973.<br />
17
SILICATES<br />
The first reliable information on mining in Bosnia and Hercegovina at the<br />
beginning of the Ottoman rule are derived from several regulations (canons) issued<br />
by Mehmed II the Conqueror (1451–1481) and Bayazid II (1481–1512) dealing<br />
with the mines at Srebrenica, Sasa, Crnča, Kreševo, Fojnica, Deževica, Dusina and<br />
Ostružnica. Information is provided about the exploitation of metal ores conatining<br />
silver, lead, copper and iron. During later period of Ottoman rule in Bosnia, several<br />
travellers write about mining in Bosnia, especially gold washing. First such data<br />
is given in the travelogues of Jeronim Zlatarić dated 1599, where gold washing on<br />
the Lašva river is mentioned. Grgičević (1626) and A. Đorđić (1626) mention gold<br />
washing and production around Fojnica. Both authors mention a decline in gold<br />
production, due to difficulties in exploitation and sale.<br />
Production of mercury, gold, silver and iron in Bosnia is also mentioned in<br />
the 1771 travelogue of V. Brkić, while the frenchman Chaumette de Fosse in passing<br />
through Bosnia during 1807/1808 notes its rich mineral resources, particularly gold<br />
along the rivers Bosna, Vrbas, Lašva and Drina. The mining engineer A. Conrad<br />
(1871, p. 221) mentions that people from Dubrovnik were washing gold on the river<br />
Vrbas and its tributaries as late as the 1860-ies.<br />
Based on written accounts and various administrative documents pertaining<br />
to the early period of Ottoman rule, as well as from various travel reports and similar<br />
sources, it can be seen that there were three important mining regions in Bosnia in<br />
those days: central Bosnia, eastern Bosnia and the river Drina region, and western<br />
Bosnia and the river Una region. Of some significance was alse the secondary region<br />
of the Krivaja river, northeast of central Bosnia.<br />
The principal mines which operated in central Bosnia during early Ottoman<br />
rule were the following: Fojnica – settlement and silver/mercury mine and commercial<br />
centre for silver trade; Ostružnica – iron mine, mentioned in 1349 also as a silver<br />
mine, leased to Dubrovnik merchants; Kreševo – the second largest silver mine in<br />
Bosnia, generating ca. 30% less income than the Fojnica silver mine; the somewhat<br />
smaller silver mines at Deževica and Dusina, both in the Kreševo mining area; Mt.<br />
Inač, a very important occurence of cinnabar close to Deževica, from which mercury<br />
production by means of distillation was until the Austro-Hungarian occupation of<br />
Bosnia. The mercury from Kreševo was exported to Dubrovnik. Mercury production<br />
also took place in the Kostajnica valley, southwest of Kreševo (Rimska Jama). The<br />
Oberska Rupa locality was considered to be among the most productive mercury<br />
mining areas in Bosnia during the Ottoman rule. The Rimska Jama near Vranak,<br />
some 2.5 km west of Kreševo was an important mercury mine during the Roman<br />
period (Jurković 1956a, p. 5-20), and it is probable that production continued into<br />
the Turkish times.<br />
18
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
In the northeastern part of the central Bosnian ore province the folowing<br />
mines were active: Borovica – an iron and silver mine; Vareš – iron; Dahštansko,<br />
southeast of Vareš – silver; Busovača and Pržići – iron. The town of Visoko was also<br />
in the Middle Ages known to be an important mining and trade center.<br />
The important Olovo lead mine in the Krivaja river valley was both a mine<br />
and trade center. Three smaller mines operated in the vicinity – Čičal, a lead mine<br />
which operated also during the Middle Ages (Cecegel 1382), and the Kruševo–Donje<br />
Podgrađe mine. The iron mine at Varci (today called Vruci) was first mentioned in<br />
the 16 th century.<br />
The eastern Bosnian region encompasses the Srebrenica and Zvornik area.<br />
The Srebrenica mine (and the adjacent Sasa mine), known to have produced lead and<br />
silver from ancient times, was the main source of lead and silver in this area during<br />
the Ottoman rule. Silver was the main product, along with some lead and iron. Some<br />
of these mines were leased to Dubrovnik merchants. The Srebrenica mine generated<br />
a substantial income even at the beginning of the 16 th century, althugh production<br />
agains starts to decline and the Sasa mine ceases all operation by the end of the 16 th<br />
and early 17 th century.<br />
Other mines in this area, on the left bank of the Drina river were the following:<br />
Đevanje, Mratinci and Hlapovići, Đevanje being the most important one. In early<br />
16 th century it was known as a silver and lead mine, but in 1533 the locality is only<br />
mentioned as a township and not as a mine. A production decline was also seen at<br />
Mratinci, west of Bratunci, and the mine is mentioned no more in later documents.<br />
In the Srebrenica area, the Daljegošće mine produced iron, but likewise terminated<br />
operations at the beginning of the 16 th century.<br />
Further to the south of the Srebrenica region was the area of Višegrad and<br />
Čajniče, producing iron. In the Prača river valley the following mines operated:<br />
Hladilo (Vrhprača), Čelopek, Grabovica and Busovac (Buševac). During the<br />
Ottoman rule Čajniče is mentioned in 1468 and during the 16 th century as an iron<br />
mining and trading center with some blacksmith shops and iron ore smeltering huts,<br />
although this area is not mentioned in earlier accounts to be of importance. Four<br />
mines operated also in the Goražde area: Križevo, Mrković, Kluščić and Bučje.<br />
Goražde was an important mining and trading center during early turkish rule, like<br />
Borač and Prača which both had strong links with Dubrovnik.<br />
In the region of western Bosnia, iron production was the most important<br />
one. During the 16 th and 17 th centuries the Kamengrad iron mine near Bihać was<br />
of importance. According to a turkish document from the 16 th century, there was<br />
an iron mine in this area between the forts of Ključa and Kamengrad. Another<br />
document from the early 18 th century mentions a copper mine at the village of<br />
Bušavić, close to Kamengrad.<br />
19
SILICATES<br />
There is not much information available about mining activities during the<br />
17 th and 18 th centuries (and early 19 th century). However, it is generally known that<br />
there was a steady decline in mining activities, compared to the beginning of the<br />
Ottoman rule in Bosnia and Hercegovina, or to the pre-Ottoman conditions during the<br />
Middle Ages. According to information, the silver mines in Bosnia and Hercegovina<br />
ceased production by mid-17 th century. From the late 17 th century onwards there is<br />
a steady decline in the military and economic power of the Ottoman Empire, and<br />
the decline in mining activities followed suit. However, mining and metal working<br />
never completely ceased in Bosnia and Hercegovina, as can be seen from travel<br />
reports of Hadži Kalfa, Evlija Ćelebija and A. Conrad. The devolution of mining<br />
activities in the Ottoman countries, hence also in Bosnia and Hercegovina correlates<br />
with a general degeneration of turkish economy and military power, leading to the<br />
termination of Ottoman rule in Bosnia in 1878.<br />
20<br />
II The period of scientific exploration and research 5<br />
1. The end of Ottoman rule in Bosnia and Hercegovina (1840–1878)<br />
Until the middle of the 19 th century Turkey was quite enclosed within its<br />
borders and influence from the western countries hardly existed. Then however,<br />
Turkey initiates a process of opening up – especially towards Austria and France.<br />
With permission of the turkish authorities many professional people start coming to<br />
Bosnia and Hercegovina – geologists, mining engineers, biologists, archaeologists,<br />
diplomats and military experts, initiating for the first time scientifically based<br />
investigations in the country. This approach has also included investigations of<br />
minerals and rocks in Bosnia and Hercegovina, its ores in particular.<br />
Even though ores and minerals have been exploited in Bosnia and<br />
Hercegovina for ages, it was only then that systematic scientific studies were<br />
initiated. It is interesting to note that in that period geological sciences were rather<br />
well developed, both in western Europe as well as in Russia.<br />
One of the first geologists who came to Bosnia and Hercegovina was Ami<br />
Boué. His travels in the Balkans (1836–1838) mark the advent of geological and<br />
mineralogical investigations in our latitudes. The first information on the geology of<br />
Bosnia and Hercegovina are the notes of A. Boué published in 1828 in ‘Leonhards<br />
Zeitschrift’, but most of his observations are contained in two publications: ‘Esquisse<br />
géologique de la Turquie d’Europe’ (1840) and ‘La Turquie d’Europe’ (1840a).<br />
Both of these publications contain significant scientific information and are the first<br />
account of rocks and minerals in Bosnia and Hercegovina. Ami Boué is thus rightly<br />
considered to be the founder of geological sciences in our area.<br />
5 This section is authored by F. Trubelja
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The arrival of A. Boué and other professionals, diplomats and military<br />
experts in what was then Turkey, influenced also some changes in its social and<br />
political environments and in 1878 the territory of Bosnia and Hercegovina was<br />
occupied by the Austro-Hungarian Monarchy. This state of affairs can be deduced<br />
from reports which all these named professionals brought back to Vienna. Some of<br />
these reports were also published.<br />
Other authors which have provided information on our minerals include D.<br />
Wolf, O. Sendtner (a botanist), J. Roskiewicz, M. Hantken, A. Conrad, O. Blau, K.<br />
M. Paul and others. These professionals may be regarded as forerunners to those<br />
eminent geologists from Vienna who arrived immediately before the occupation<br />
or shortly after 1878. It is interesting to note that J. Roskiewicz was a military<br />
officer, while O. Blau arrived as the Prussian consul. In his 1847 publication D.<br />
Wolf mentions the iron ores at Fojnica and mercury from Kreševo, correlating this<br />
occurence with the one at Idrija. He also described the galena from Vareš and rock<br />
salt from Tuzla.<br />
M. Hantken (1867) first described the occurence of sepiolite (sea-foam)<br />
at the Branešci locality near Prnjavor, which was already quarried and used for<br />
making pipes. In spite of Hantkens publication, scientific authorities in Vienna were<br />
reluctant to accept our sepiolite, a rare mineral species, as a separate mineral. Twenty<br />
years later B. Walter (1887) mentions the occurence in Bosnia of magnesite which is<br />
macroscopically similar to sepiolite. Our petrologist M. Kišpatić (1893, p. 99) noted<br />
with some flippancy that following Walters paper, they were ready to dismiss our<br />
sea-foam from the list of Bosnian ores.<br />
An interesting but overoptimistic account of Bosnian minerals and their<br />
economic importance can be found in several publications of A. Conrad (1866, 1870<br />
and 1871). Data from his papers was used for an evaluation of the economic potential<br />
of some of our ore-bearing regions (such as the schist mountains of central Bosnia).<br />
The mining engineer from Saxony A. Conrad worked in Bosnia during 1866–1867 on<br />
behalf of the Turkish authorities. The information he collected concerned primarily<br />
the mercury-antimony-silver containg tetrahedrites, baryte, goldbearing quartz veins<br />
and goldbearing sulfides from which gold is released due to surface weathering<br />
processes of ore bodies in central Bosnia. In these papers Conrad explains that<br />
Bosnia has a nice future, because of its rich metal ores and extensive forests.<br />
H. Sterneck (1877) published the first petrological map of Bosnia and<br />
Hercegovina and some adjacent areas.<br />
An account of this early period of investigations and reporting on the geology<br />
of Bosnia and Hercegovina is given by L. Marić (1974). He writes that “these reports<br />
were written between 1846 and 1872 with an obvious goal to provide a good account<br />
21
SILICATES<br />
of Bosnia and Hercegovina assets in ores and forests, and the economy in general.<br />
The reports also include information on communication lines such as rivers and<br />
roads – information which was shown to be of vital importance at the Congress of<br />
Berlin held in 1878. At the Congress of Berlin the Austro-Hungarian Empire was<br />
empowered to occupy Bosnia and Hercegovina, and this was done during the same<br />
year. The military occupation of Bosnia and Hercegovina also provided access to its<br />
natural resources which were needed by the Monarchy, especially the mineral and<br />
ore resources required for the industrialization of the Empire”.<br />
22<br />
2. Period of Austro-Hungarian Empire (1878–1918)<br />
Immediately following the occupation of Bosnia and Hercegovina, a whole<br />
wave of geologists and petrologists started to arrive in the Balkans – mainly from<br />
Vienna, and to a lesser extent from Budapest. The geoelogists E. Mojsisovics, A.<br />
Bittner, E. Tietze. K. M. Paul, F. Hauer and others publish significant geological<br />
publications – some of them monographs – as early as 1879 and 1880. Even today<br />
we can find in them important information about our minerals. The most extensive<br />
and most important monograph of that time was written by Mojsisovics, Tietze<br />
and Bittner (1880) entitled “Grundlinien der Geologie von Bosnien-Herzegovina<br />
(Outline of the geology of Bosnia and Herzegovina)’’. This publication covers<br />
mostly geological issues, but contains also various mineralogical and petrological<br />
information. However, most important for mineralogy is the appendix to the volume<br />
written by C. John (1880) entitled “Über krystallinische Gesteine Bosnien’s und<br />
der Hercegovina (On the crystalline rocks of Bosnia and Hercegovina)’’. In this<br />
publication the author provides data on extensive microscopic investigations (also<br />
some chemical investigations) of mostly igneous and some metamorphic rocks and<br />
minerals contained in them. As noted by the author in the introduction, most of the<br />
samples were collected by the above named authors as well as some other geologists<br />
working in the area, on behalf of the Vienna Geological Survey.<br />
John determined numerous rock-forming minerals in the muscovitecontaining<br />
granite of Mt. Motajica, in the diabase porphyres from the river Vrbas valley<br />
between Donji Vakuf and Jajce, and from the Rama river valley close to Prozor. John<br />
paid considerable attention also to the rocks and minerals of the Bosnian serpentine<br />
zone (named as such by M. Kišpatić in 1897). He thus investigated diabases, diorites,<br />
olivine gabbros, serpentinites and other rocks from this area. Detailed microscopical<br />
data is provided for effusive rocks from Maglaj, from Mt.Vranica, and from the areas<br />
around Srebrenica, Ljubovija and Zvornik. The following minerals were found in<br />
these rocks: muscovite, orthoclase, quartz, hornblende, magnetite, calcite, epidote,<br />
augite, chlorite, ilmenite, diallag, biotite, olivine, garnet, oligoclase, labradorite,<br />
anorthite, sanidine, serpentine, picotite, apatite, halite, zoisite, actinolite. For some<br />
of these minerals John gave detailed microphysiographic data.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Based on the above, John may be regarded as the founder of microscopic<br />
mineralogy and mineral chemistry in our area.<br />
Several less detailed publications appeared during this time, but they were<br />
also of great value for knowing our minerals and rocks. Papers were published by F.<br />
Schafarzik (1879), A. Rzehak (1879), H. Rittler (1878), R. Potier (1879) and K.M.<br />
Paul (1872, 1879 and 1879a). Schafarzik (1879) identified andesine in the diabase on<br />
which the Doboj fortress was erected. More recently Lj. Barić found this andesine to<br />
have high-temperature optics. K.M. Paul (1879) also identified andesine in this rock.<br />
Towards the end of the 19th century a local geologist (mineralogist and<br />
petrologist) started working in Bosnia and Hercegovina. This was Gj. Pilar, a<br />
professor of geology at the University of Zagreb. In fact, he joind the team of the<br />
austrian geologists Mojsisovics, Tietze and Bittner. It is important to note that Pilar<br />
published results of his investigations in a rather extensive paper published by the<br />
Yugoslav Academy of Sciences and Arts in Zagreb in 1882. Pilar identified various<br />
minerals in igneous and metamorphic rocks around Jajce – some of this minerals<br />
were not mentioned in earlier papers: chrysotile from Kozara, fluorite from Jajce,<br />
gypsum from Bosanski Novi. On pages 64-68 Pilar gives an account of ‘’Bosnian<br />
ores’’ known to him mentioning pyrite, baryte, arsenopyrite, chalcopyrite, cinnabar,<br />
realgar, orpiment, antimonite, tetrahedrite, tennantite, cuprite, hematite, quartz,<br />
chalcedony, picotite, chromite, magnetite, limonite, psilomelane, fluorite, calcite,<br />
dolomit, ankerite, siderite, malachite, gypsum, garnet, sepiolite and chrysotile. This<br />
list of minerals and descriptions of their parageneses was Pilar’s real contribution to<br />
topographic mineralogy.<br />
In the period between 1878 and the end of the century, the following authors<br />
provided information on our minerals: G. Primics (1881), F. Hauer (1884), A. Götting<br />
(1886), B. Walter (1887), K. Vrba (1885 and 1889), H.B. Foullon (1893, 1893a and<br />
1895), A. Rücker (1893 and 1897), F. Poech (1888 and 1900), W. Radimsky (1889),<br />
J. Grimmer (1897 and 1899) and L. Pogatschnig (1890).<br />
During this period, and later, our mineralogist and crystallographer M.<br />
Kišpatić (1893, 1897, 1900, 1902, 1904, 1904a, 1904b, 1909, 1910, 1912, 1915<br />
and 1917) also worked in Bosnia and Hercegovina. He published extensively, but<br />
his most important contribution is the monography on the rocks and minerals of the<br />
Bosnian serpentine zone (1897) which was also translated into German (1900).<br />
Kišpatić authored the monography entitled “The crystalline rocks of the<br />
serpentine zone in Bosnia’’ which is of great significance for Bosnia and Hercegovina.<br />
Here he argues on genetic issues based on microscopic investigations of ‘Bosnian<br />
serpentines’ and associated basic rocks which he termed diabase and crystalline<br />
23
SILICATES<br />
schists. His microscopic data are still valid today and have not been revised to<br />
any major extent. Based on qualitative and quantitative chemical and microscopic<br />
investigations, Kišpatić was able to identify many more minerals than found earlier<br />
by various investigators, mainly C. John. Thanks to the efforts of this tireless<br />
researcher, many minerals from this zone of igneous and metamorphic rocks in the<br />
inner Dinaride range of Bosnia were also chemically analysed (diopside, sepiolite,<br />
magnezite, broncite).<br />
Kišpatić also investigated the Tertiary-age effusive rocks from Srebrenica<br />
and from the Bosna river valley where he was able to identify numerous rockforming<br />
minerals (1904 and 1904a).<br />
At the beginning of the 20th century Kišpatić authored an important<br />
mineralogical and petrological investigation, with numerous goniometric<br />
measurements of realgar, cerrusite, anglesite, pyrite, siderite, kalcite, quartz,<br />
heulandite and beryl and he was able to identify several crystal forms on several of<br />
these minerals.<br />
Among the several publications by Kišpatić given above, we should point<br />
out the one published in 1912 where he gives data on minerals in bauxites from<br />
Duvno (Županjac) in Hercegovina. A student and coworker of Kišpatić, F. Tućan<br />
identified several minerals in the terra-rossa from the same area (1912).<br />
Next to Kišpatić, other mineralogists and petrographers working in Bosnia<br />
and Hercegovina which need to be mentioned were F. Koch (1897, 1899, 1899a,<br />
1902 and 1908) and M. Čutura (1918).<br />
Several of the earlier mentioned foreign researchers gave important<br />
contributions to the knowledge of the minerals in Bosnia. The extensive publication<br />
by B. Walter (1897) entitled “Beitrag zur Kentniss der Erzlagerstätten Bosniens<br />
(Contribution to the knowledge of Bosnian ore deposits)’’ can be regarded as our first<br />
practical mineralogy text featuring detailed descriptions of ore deposits of iron, goldbearing<br />
pyrite, chalcopyrite, manganese, gold, silver ores of Srebrenica, antimony,<br />
mercury and chrome ores. The parageneses are decribed in detail as well as their<br />
genetic implications.<br />
Several years prior to the publication of Walters text, a publication<br />
authored by the famous viennese geologist (paleontologist) and director of the<br />
Vienna Geological Survey, F. Hauer (1884) appeared. This publication, entitled<br />
“Erze und Mineralien aus Bosnien (Ores and minerals of Bosnia)’’ is based<br />
on samples of minerals amd ores which were donated to the museum in Vienna<br />
by B. Walter (samples from Čemernica, Sinjakovo, Hrmza, Vareš, Pogorelica,<br />
Srebrenica, Čevljanovići, Vranjkovci, Duboštica). Hauer was able to identify the<br />
24
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
following minerals, based on physiographic characteristics and partly their chemical<br />
composition: realgar, orpiment, antimonite, galena, sphalerite, pyrite, arsenopyrite,<br />
tetrahedrite, chalcopyrite, cinnabar, boulangerite, berthierite, cuprite, hematite,<br />
limonite, psilomelane, pyrolusite, chromite, Ni-serpentine, cerrusite, baryte, ankerite,<br />
malachite and azurite. It is interesting to note that Hauer also described the graphite<br />
schists from the iron ore deposit Smreka (Vareš). Some chemical analyses of sulfide<br />
ores from Srebrenica are also given in the paper.<br />
F. Boullon (1893) published an extensive paper on the mineral composition<br />
of schists from the central Bosnian mountains, describing some 30 mineral species.<br />
K. Vrba (1885 and 1889) has undertaken crystallographic investigations of<br />
realgar from Hrmza in the Kreševo area. He was able to identify numerous crystal<br />
forms. J. Krenner (1884) has also published some data on the realgar and orpiment<br />
from the same location. These two researchers should be regarded as the founders of<br />
our crystallography since they were the first ones to undertake such investigations.<br />
B. Baumgärtel (1904) and J. Schiller (1905) have also contributed to the<br />
knowledge of Bosnian minerals and rocks.<br />
F. Katzer has a special place in the history of mineralogical research in<br />
Bosnia and Hercegovina. His contribution is most relevant and substantial. Katzer<br />
started his investigations into the geology and mineralogy of Bosnia immediately<br />
upon his arrival in occupied Bosnia and Hercegovina in 1898. When the Geological<br />
survey in Sarajevo was established in 1912, he became its first director and he headed<br />
this institution until his death in 1925. Katzer spent most of his career in Bosnia and<br />
Hercegovina, although he spent some time in Czechia and in Brasil. Based on this<br />
fact, and his major contributions to the geological investigations in our area, he can<br />
be referred to as a Bosnian-Hercegovinian geologist (mineralogist).<br />
An evaluation of Katzers earlier publication shows that he was a most<br />
dilligent and productive researcher. However, the sheer volume of his investigations<br />
in Bosnia and Hercegovina causes a feeling of profound admiration towards his<br />
person. Among his publications on the mineralogy and ore-deposits of our areas,<br />
the following warrant mentioning: on iron ores from Vareš (1900 and 1910); goldbearing<br />
alluvial deposits of the Pavlovac creek (1901); the Glauber-salt deposit in<br />
the Jahorina tunnel (1904); pyrite and chalcopyrite deposits (1905); deposits of<br />
tetrahedrite and mercury ore (1907); manganese ores from Čevljanovići (1906);<br />
ores from Sinjakovo and Jezero (1908); Bosnian sepiolite (1909 and 1912a); arsenic<br />
ores (1912); the bauxite deposit of Domanovići in Hercegovina (1917) etc. The<br />
largest amount of data on minerals are contained in his most significant publication<br />
– Geology of Bosnia and Hercegovina (1924, 1925 and 1926).<br />
25
SILICATES<br />
An interesting feature of Katzer’s mineralogical investigations lies in the fact<br />
that he usually mentioned the combination of crystal forms he was able to identify,<br />
but seldom provided goniometric data. Due to the lack of such information, it is<br />
impossible to verify his results. The data on minerals usually included information on<br />
their hardness and density, but seldom optical information obtained by a polarizing<br />
microscope or other appropriate instrument. He gave considerable importance to<br />
quantitative chemical analysis. He describes in detail the paragenetic relationships<br />
in the investigated ore-deposits, and provides ample location sketches, profile and<br />
geological maps. Based on field observations and laboratory work, Katzer derives<br />
his conclusions on the genesis of specific mineral assemblages. His conclusions<br />
were mainly focused on the possibilities of ore and mineral exploitation, but never<br />
neglected fundamental scientific issues.<br />
Some of Katzer’s conclusions were not completely correct, when they were<br />
based only on quantitative chemical analyses of minerals. This can be clearly seen<br />
from the example of the allegedly new mineral poechite, which he “discovered”<br />
in the iron ore bodies of Droškovac and Smrika near Vareš (1911 and 1921). The<br />
relative coherence of chemical data for poechite, which Katzer mentioned several<br />
times and which made him believe that it was a new mineral, can be easily explained.<br />
It is well known that in many major ore deposits a geologist or mining engineer<br />
can, based upon his knowledge of the ore body and its characteristics, recognize<br />
those ores whose chemical composition is practically constant. In such a case the<br />
reason for this is the aggregate of several major minerals, and not neccessarily a<br />
new mineral. Further investigations concerning poechite showed this to be a mixture<br />
of goethite, hematite and quartz (and sometimes rhodochrosite). The poechite from<br />
Vareš today is a discredited mineral species (Barić and Trubelja, 1975a).<br />
Katzer (1917) made some significant conclusions regarding the genesis of the<br />
bauxites from Hercegovina, based on his research of this material from Domanovići.<br />
Katzer suggested that the material from which bauxite formed was transported from<br />
distant sources in the form of clayey silicate mud, subsequently litified into bauxite.<br />
However, he did not provide sufficient explanation for the process of bauxitization<br />
of these coastal muds. Katzer’s views on bauxite formation seem to have disagreed<br />
with current theories of bauxite formation of that time, advanced by M. Kišpatić and<br />
F. Tućan which postulate that bauxite has been formed from “red soil” (terra rossa)<br />
– this being an insoluble residue of the weathering of carbonate rocks in the karst of<br />
the Dinarides.<br />
Katzer intended to produce a systematic description of all mineral occurences<br />
in Bosnia and Hercegovina. However, due to his numerous other commitments<br />
on the geological mapping of the area, he managed only to begin this work and<br />
provided data for graphite, sulphur, gold, mercury, copper and iron only (Katzer<br />
26
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
1920). His idea was to provide a “Topographic and practical mineralogy of Bosnia<br />
and Hercegovina”. Unfortunately, this task remained unfinished, much like his other<br />
significant project on the geology of Bosnia and Hercegovina in which he wanted to<br />
compile his great expertise on the geological relationships of the country, based upon<br />
twentyfive years of intensive research.<br />
There is one more “document” of Katzer’s mineralogical research –<br />
the collection of minerals located in the State Museum in Sarajevo (Zemaljski<br />
muzej) containing all important mineral species from Bosnia and Hercegovina,<br />
and elsewhere, which Katzer obtained through direct exploration or through his<br />
international contacts and exchange. Even today this collection is frequently<br />
visited and studied by pupils, students and researchers, and is a part of Bosnia and<br />
Hercegovina’s cultural heritage.<br />
It can be said without exaggeration that, due to Katzer’s research and<br />
activities, Sarajevo was in the first quarter of the last century a significant center of<br />
geological and mineralogical research in Europe.<br />
3. Period between the two World Wars (1918–1945)<br />
Very little mineralogical research was done in Bosnia and Hercegovina<br />
during the period between the two World Wars. Katzer’s Geology, discussed in<br />
the previous chapter, was established in this period. Although this was a period of<br />
decline of geological and mineralogical research in Yugoslavia, some investigations<br />
did take place nevertheless.<br />
R. Koechlin (1922) published data on several rare minerals in the Ljubija<br />
ore deposit, and found nowhere else in Bosnia and Hercegovina – leadhillite and<br />
beudantite. These minerals are secondary products of galena weathering, and<br />
Koechlin performed crystallographic measurements on them.<br />
In the Ljubija deposit there are also occurences of rhodochrosite, investigated<br />
in detail by Lj. Barić and F. Tućan (1925). The crystallographic features of sphalerite<br />
from the same locality were investigated by M. Tajder (1936).<br />
The aforementioned book Geology authored by Katzer was translated by<br />
T. Jakšić and M. Milojković, two geologists from Bosnia and Hercegovina. At that<br />
time, this was an important contribution in the sense that information on minerals<br />
was made available to a broader public audience. Jakšić published several papers<br />
on the bauxites from Hercegovina (1927, 1934), rock salt in Tuzla (1929), arsenic<br />
minerals from Hrmza (1930, 1937) and manganese ores from Mt. Kozara near Banja<br />
Luka (1938). Another important paper on the geology and minerals of Bosnia and<br />
Hercegovina was written by M. Milojković (1929).<br />
27
SILICATES<br />
A. Polić wrote two short papers – one on magnesite from Dubnica close<br />
to Višegrad (1938) and another, dealing with manganese ores from Mt. Ozren near<br />
Sarajevo (1940).<br />
L. Marić (1927) authored an important petrological and mineralogical<br />
description of the gabbro complex of Jablanica in Hercegovina. Marić was able to<br />
identify numerous minerals in various differentiates of the gabbro, using a polarising<br />
microscope. Of particular value are the extinction angle measurement and other<br />
optical data obtained on feldspar, pyroxene, amphibole and other minerals. This data<br />
was used to obtain information on the chemical composition of these minerals. In<br />
addition to the above, Marić paid special attention to vein minerals like tourmaline,<br />
stilbite, calcite, pennine, quartz, titanite, prehnite, epidote etc. It is interesting to note<br />
that until the end of the second World War this was the only identification of prehnite<br />
(in the Jablanica gabbro) in Bosnia and Hercegovina.<br />
Important contributions to the identification of several rock-forming<br />
minerals from around Višegrad in eastern Bosnia were made by S. Pavlović (1937),<br />
in his paper on ultrabasic, basic and metamorphic rocks of Mt. Zlatibor.<br />
This short account of mineralogical and petrological research in Bosnia and<br />
Hercegovina between the two World Wars could not cover all work of all authors who<br />
were active in the area, but we hope to have given information on most important<br />
achievements. The appended reference list provides complementary information.<br />
No organized research took place in Bosnia and Hercegovina during the 2 nd<br />
World War.<br />
28<br />
4. Mineralogical research in Yugoslavia<br />
In the previous chapter we have shown that in the period between the two<br />
World Wars there was no specialized institution for mineralogical and petrological<br />
research in Bosnia and Hercegovina, and that educated mineralogists were also<br />
very few. After the end of the 2 nd World War, young geologists – educated in our<br />
universities in Zagreb, Belgrade and Ljubljana – started coming to Bosnia and<br />
Hercegovina and soon become very active with their research. In those early days<br />
these researchers worked at the Geological Survey (Geološki zavod, today called<br />
the Institute of Geology) and at the University of Sarajevo. Later on, a Department<br />
of Geology was established at the State Museum in Sarajevo, where fundamental<br />
research in geology, palaentology, mineralogy and petrology took place.<br />
The University of Sarajevo was established in 1950 and two centers for<br />
research in the field of geology were set up. One of these centers was located in
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
the Technical faculty (today called the Civil Engineering faculty), the other one<br />
in the Faculty for Philosophy (today called the Faculty of Natural Sciences and<br />
Mathematics). Courses in mineralogy, petrology and related disciplines started to<br />
be held at the Technical faculty, as well as research required by the engineering<br />
sector. Today, a well organised Laboratory for Mineralogy and Petrology is part of<br />
the Faculty of Natural Sciences and Mathematics, where research has been going on<br />
for the past twentyfive years.<br />
These centers were being equipped with modern instrumentation, however<br />
with rather limited funds. Some major and costly equipment has been acquired only<br />
recently. Even though mineralogical and petrological research is quite important<br />
for many geological fields as well as the economic sector, the limited number of<br />
researchers was not always able to respond to all requirements. An important step<br />
forward was the establishment of the Faculty of Mining in Tuzla, later reorganised<br />
into the Faculty of Mining and Geology with its independent Department of<br />
Mineralogy, Petrology and Ore Deposits.<br />
Today, organised high-level research is being done at the Geological institute<br />
in Sarajevo (Ilidža), the Faculty of Natural Sciences and Mathematics in Sarajevo<br />
and at the Faculty of Mining and Geology in Tuzla – comprising both fundamental<br />
research as well as applied investigations for the requirements of the industry and<br />
other customers. Chemical analyses, optical crystallography measurements, X-ray<br />
diffraction, IR-spectroscopy and other modern techniques form the core of these<br />
investigations.<br />
The community of geologists, mineralogists and petrologists of Bosnia and<br />
Hercegovina is comparatively small but is involved in significant research leading<br />
to important scientific results. Research is published in the Journal of the Geological<br />
institute in Sarajevo (Geološki glasnik) and in the Journal of the State Museum in<br />
Sarajevo (Glasnik Zemaljskog muzeja), as well as in other local and international<br />
journals. Much of this research has been done in collaboration with colleagues from<br />
other research centers and groups.<br />
In the period after the 2 nd World War, the mineralogists and petrologists<br />
working in Bosnia and Hercegovina have been to numerous to be mentioned<br />
individually. It would be even harder to make a lists of all their results and<br />
achievements. To this end, we would like to invite the reader to make use of the<br />
rather extensive list of references, appended to this book.<br />
29
SILICATES<br />
OLIVINE<br />
(Mg,Fe) 2<br />
[SiO 4<br />
]<br />
Crystal system and class: Orthorhombic, Rhombic-dipyramidal;<br />
Lattice ratio: a : b : c = 0.467 : 1 : 0.586 (for Mg 2<br />
SiO 4<br />
)<br />
Unit cell parameters: a = 4.76, b = 10.20, c = 5.98, Z = 4 (Mg 2<br />
SiO 4<br />
);<br />
a o<br />
= 4.82Å, b o<br />
= 10.48Å, c o<br />
= 6.11Å (fayalite Fe 2<br />
SiO 4<br />
).<br />
Properties: colour usually olivegreen (hence the name), also (Mg 2<br />
SiO 4<br />
); white<br />
(forsterite) and brown to black (fayalite). Cleavage weak and present only in Ferich<br />
members of the group. Hardness is 7-6.5, specific gravity 3.22 (Mg 2<br />
SiO 4<br />
) to<br />
4.37 (Fe 2<br />
SiO 4<br />
), common olivine 3.3-3.4. Streak is white to gray. Vitreous lustre.<br />
Refractive indices are high: Nx = 1.635-1.827 Ny = 1.651-1.869 Nz = 1.670-1.879.<br />
Birefringence is high at 0.035-0.052.<br />
X-ray diffraction data: forsterite d 2.77 (100), 2.51 (100), 2.46 (80), ASTM-card<br />
7-19; fayalite d 2.83 (100), 2.50 (70), 2.57 (50), ASTM-card 7-164.<br />
IR spectrum: 428 473 512 545 612 840 890 958 995 cm -1 (forsterite, Mt.<br />
Vesuvius, Italy); 418 475 516 612 848 898 950 1002 cm -1 (olivine, Teplice, Czech<br />
Republic).<br />
30<br />
OLIVINE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Baumgärtel (1904), Đorđević (1969a), Đurić (1963), Golub<br />
(1961), Hauer (1879), Hiessleitner (1951/52), John (1879, 1880, 1888), Karamata<br />
and Pamić (1960), Kišpatić (1897, 1900, 1904b, 1910), Majer (1962), Majer and<br />
Jurković (1957, 1958), Marić (1927, 1953), Marković and Takač (1958), Pamić<br />
(1960a, 1964, 1969a, 1970, 1971, 1972, 1972c, 1972d, 1973 and 1974), Pamić and<br />
Antić (1964), Pamić, Šćavničar and Međimorec (1973), Pamić and Trubelja (1962),<br />
Paul (1879), Pavlovich (1937), Pilar (1882), Primics (1881), Ristić, Pamić, Mudrinić<br />
and Likić (1967), Schiller (1905), Sijarić and Šćavničar (1972), Sunarić and Olujić<br />
(1968), Trubelja (1957, 1960, 1961), Trubelja and Pamić (1957, 1965), Tscherne<br />
(1892), Varićak (1966).<br />
Olivine is one of the most common and ubiquitous rock-forming minerals<br />
in Bosnia and Hercegovina. Numerous mountain ranges or parts thereof in the inner<br />
Dinarides range in Bosnia (Kozara, Borja, Skatovica, Ljubić, Ozren, Konjuh) are<br />
built of olivine rocks. These mountains spread from the northewest (Bosanski Novi<br />
area) towards southeast, close to the town of Višegrad. This area has been named<br />
“the Bosnian serpentine zone” by M. Kišpatić (1897, 1900) – here olivine is an
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
important constituent of ultrabasic and occasionally basic igneous rocks. Olivine is a<br />
constituent of peridotites and serpentinized peridotites, dunites, gabbro-peridotites,<br />
olivine-gabbros and troctolites (Figure 1).<br />
Figure 1. Map of Bosnia and Hercegovina showing the location of the<br />
“Bosnian serpentine zone”<br />
Outside the “Bosnian serpentine zone” olivine occurs in specific products of<br />
triassic magmatism (basic intrusive and dyke rocks), in the area of central-bosnian<br />
schist mountains, as well as near Jablanica and Kalinovik.<br />
Data on olivine can be found in many petrological publications and<br />
monographs, implying that the results of optical microscopy and theodolitic<br />
measurements for olivine are rather numerous and detailed.<br />
31
SILICATES<br />
1. Olivine in rocks of the Bosnian serpentine zone<br />
Mt. Kozara. First information on olivine in igneous rocks of Mt. Kozara were<br />
published in 1882 by Gj. Pilar. According to him, olivine is an important constituent<br />
of olivine gabbro. Olivine is partially or completely transformed into serpentine.<br />
The monograph by M. Kišpatić on the igneous rocks of the “Bosnian<br />
serpentine zone” provides substantial data on olivine and other rock-forming<br />
minerals (Kišpatić’s data-set on minerals of the “Bosnian serpentine zone” is quite<br />
extensive and largely composed of qualitative measurements). According to Kišpatić<br />
(1897, 1900) olivine is an essential constituent of lherzolite, troctolite and olivine<br />
gabbro. Kišpatić mentions or describes olivine in olivine gabbro of Kozaračka<br />
Rijeka, from Kotlovac stream and in the areas of Jankovića mill, Lake Benkovac,<br />
Kozarac, Omarska stream and the Bistrica river valley. In addition to olivine gabbro,<br />
Kišpatić describes olivine containing troctolites from Kotlovac stream. In gabbros<br />
from the Elkina spur, olivine is of subordinate significance. Kišpatić also describes<br />
the transition of olivine into amphibole.<br />
Olivine is the most important constituent of lherzolite rocks of Mt. Kozara.<br />
Kišpatić provides optical microscopic investigations and descriptions of olivine in<br />
lherzolites from Kozarac, from the Benkovac and Elkina spur, Mimići and from<br />
Ljučica stream. In all these rocks olivine is more or less transformed into serpentine.<br />
Detailed microscopic investigations on olivine in lherzolites, troctolites<br />
and olivine gabbros from various locations on Mt. Kozara are given in more recent<br />
investigations by Lj. Golub (1961). His data are given in Table 1.<br />
Olivine in lherzolites from Jovača stream is in the form of “eyes” in a<br />
serpentine matrix. Troctolites from Jovača stream show olivine serpentinization and<br />
exsolution of magnetite. Most of the olivine crystals are rounded due to magmatic<br />
resorption. Some of the partially preserved olivine crystals are surrounded by a single<br />
or double layer of acicular amphiboles of the tremolite-actinolite isomorphous series.<br />
The amphibole layers around olivine have formed at the contact with plagioclase.<br />
The olivine content of olivine gabbro from Jovača stream is 17.9 vol %.<br />
Rocks between the rivers Bosna and Vrbas. Numerous mountains (Prisjeka,<br />
Skatovica, Uzlomac, Borja, Čavka, Ljubić) or parts thereof located in the area between<br />
the rivers Bosna and Vrbas are composed of olivine rocks (mainly peridotites).<br />
Most of the microscopic data on olivine and other minerals comes from the already<br />
mentioned research by M. Kišpatić (1897, 1900). Olivine in rocks of this area is<br />
also mentioned in publications by other cited authors, but no detailed information is<br />
given. It is interesting to note that olivine in the olivine gabbros of Barakovac from<br />
the valley of the river Vrbanja was already determined in 1880 by John and in 1882<br />
32
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
by Pilar. According to these authors, this olivine gabbro also contains labradorite and<br />
monoclinic pyroxene. This research provided first microscopic data on the olivines<br />
from the part of the serpentine zone.<br />
Table 1. Optical axes angle and chemical composition of olivine<br />
Locality and rock type Optical axes angle 2V<br />
Chemical<br />
composition<br />
Jovača stream, lherzolite -2V = 88° (median value) 18% Fa<br />
Vrela stream, lherzolite<br />
2V = +88° to 2V = -88°<br />
(median value 2V = -89°)<br />
16% Fa<br />
Jovača stream, lherzolite -2V = 87° (median value) 21% Fa<br />
Jovača stream, troctolite -2V = 80° to 87° (median value 84°) 28% Fa<br />
Kozarački stream, olivine -2V = 84°, 86°, 80°, 85°, 80° (median value<br />
32% Fa<br />
gabbro<br />
-2V = 82°)<br />
More recently, the olivine and other rocks of this area have been<br />
investigated by V. Majer (1962) and J. Pamić (1969a and 1972c). According<br />
to Pamić, olivine is the essential constituent of the ultrabasic complex of Mt.<br />
Skatovica. It occurs as hypidiomorphic and allotriomorphic fragments, with some<br />
crystals showing effects of pressure twinning. Chemically, they are enriched in<br />
forsterite (86-100%). The optic axes angle is in the range 2V = +86° to ±90°. The<br />
olivine is moderatly to significantly serpentinized, with occasional exsolution of<br />
substantial amounts of magnetite.<br />
M. Tscherne (1892) needs to be mentioned as one of the early investigators<br />
mentioning olivine at Mt. Ljubić, occuring in association with the sepiolite formations<br />
in this area.<br />
Mt. Ozren and the Bosna river valley. Mt. Ozren is located eastwards of<br />
the Maglaj-Doboj transverse and south of the Spreča river. It is built mainly out of<br />
ultrabasic olivine-pyroxene rocks which are partially serpentinized. Olivine is an<br />
essential constituent of these rocks.<br />
Numerous authors have mentioned olivine in rocks of Mt. Ozren and in the<br />
Bosna river valley (Đorđević 1969a; Hauer 1879; Hiessleitner 1951/52; John 1879<br />
and 1880; Kišpatić 1897 and 1900; Pamić 1973, Pamić and Trubelja 1962; Paul 1879;<br />
Trubelja and Pamić 1965). The original data by Kišpatić are also quite significant<br />
for the olivines of this area also. The author has microscopically determined olivine<br />
in troctolites of Vukovac stream, in troctolites and gabbros of Krušička Rijeka,<br />
troctolite from Rakovac, and lherzolites from Riječica, Mala Prenja, Krušička Rijeka<br />
and Vukovac stream. In thin sections prepared from the abovementioned rocks,<br />
olivine was fresh or somewhat serpentinized. Occasionally – mainly in troctolites –<br />
it transforms into colourless or pale green amphibole.<br />
33
SILICATES<br />
More detailed microscopic investigations and theodolitic measurements<br />
of olivine and other minerals occuring at Mt. Ozren were performed recently by<br />
J. Pamić and F. Trubelja (1962) and F. Trubelja and J. Pamić (1965). Data on the<br />
optical axes angles are shown in Table 2.<br />
Table 2. Data for olivine from Mt. Ozren<br />
Locality and rock type<br />
Optical axes angle 2V<br />
Ostravica, dunite 2V = -89°, 89°, -86°, +86°, +87°<br />
Paklenica stream, feldspar-peridotite 2V = +89° to 2V = -85°<br />
Krivaja stream, serpentinized harzburgite 2V = +86°<br />
Malo Selište, serpentinized lherzolite<br />
no data<br />
Jadrina river, harzburgite 2V = +88°<br />
Pištala stream, lherzolite 2V = -84.5°<br />
Gostilj (774 m), lherzolite 2V = -85° to 2V = -88°<br />
V. Ostravica, harzburgite 2V = +81°, +86°, +88°<br />
The dunite from Ostravica is largely a monomineralic olivine rock with very<br />
little secondary serpentine and accessory chromite. The olivine fragments are similar<br />
in size, fresh, always fractured and partly eliptically rounded.<br />
Olivine and enstatite are the most important minerals forming the<br />
serpentinized harzburgites of the Krivaja stream. The fragments show fracturing<br />
along which the serpentinization process proceeds.<br />
The olivine in the serpentinized lherzolites of Malo Selište is largely<br />
serpentinized so that only its relicts may be found in the matrix. These relicts display<br />
a high relief, lively interference colours and wavy extinction under the microscope.<br />
Olivine in lherzolites of the Pištala stream and in harzburgites of V.<br />
Ostravica shows similar features as in other mentioned rocks. Some twinning of<br />
olivine crystals occurs.<br />
Mt. Konjuh and the Krivaja river valley. Olivine is the essential constituent<br />
of ultrabasic and basic rocks of Mt. Konjuh and those of the Krivaja river valley<br />
(Baumgärtel 1904; Hiessleitner 1951/52, Karamata and Pamić 1960; Kišpatić 1897,<br />
1900; Pamić 1970, 1974; Pamić and Antić 1964; Primics 1881; Ristić, Pamić,<br />
Mudrinić and Likić 1967; Sijarić and Šćavničar 1972; Sunarić and Olujić 1968;<br />
Trubelja 1961). Some of these authors provide information on olivine in the vicinity<br />
of the Duboštica chromite deposit.<br />
More detailed microscopic investigations of olivine occuring in this part<br />
of the “Bosnian serpentine zone” can be found in publications by Kišpatić, Pamić,<br />
Ristić and coworkers, Šćavničar and Sijarić, and Trubelja. Results of theodolitic<br />
measurements of olivine from ultrabasic and basic rocks of the SE section of Mt.<br />
Konjuh are given in Table 3 (Trubelja 1961).<br />
34
Table 3. Data on olivine from the rocks of Mt. Konjuh<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Locality, rock type<br />
Optic axes angle 2V<br />
Chemical<br />
composition<br />
Lisac (970 m), lherzolite 2V = +88°, +89° 7-10% Fa<br />
Zečji vrat (1275 m), lherzolite 2V = +83°, +87°, +85.5° almost pure Fo<br />
Grabovica stream, lherzolite 2V = +82°, +88°, +89°, +89.5° very little Fa<br />
Olovo-Kladanj road, feldspar peridotite 2V = -87°, -87.5° 20% Fa<br />
Blizanci stream, troctolite 2V = -85.5° 22.7% Fa<br />
Stupačnica stream, olivine gabbro 2V = -89.5° ---<br />
Data presented in Table 3 show that the olivine in ultrabasic rocks is very<br />
depleted in the fayalite component. On the other hand, the olivine in feldsparperidotites<br />
and gabbroid rocks contains ca. 20% fayalite which is consistent with the<br />
crystalisation and differentiation of peridotite magma from which the ultrabasic and<br />
basic rocks formed.<br />
Olivine in the lherzolite from Lisac (970 m) amounts to ca. 60% of the total<br />
mineral content of the rock. It shows fracturing and some serpentinization, with<br />
secondary magnetite exsolution along the fractures.<br />
Olivine in the lherzolite from Zečji Vrat (1275 m) shows extensive<br />
serpentinization, with exsolution of magnetite in the form of black dust in the<br />
serpentine matrix. Some olivine fragments are surrounded in a veil-like manner<br />
by enstatite.<br />
Other lherzolite rocks in the area contain olivine which has undergone<br />
varying degrees of serpentinization. Olivine in the lherzolite from the source area of<br />
Grabovica stream shows a characteristic elliptically shaped magmatic resorption of<br />
almost all mineral fragments.<br />
According to data by Ristić, Panić, Mudrinić and Likić (1967), olivine is an<br />
essential component of lherzolite and harzburgite from Mt. Konjuh, being of only<br />
secondary importance in gabbros. Some lherzolites contain almost 90% olivine.<br />
The fragments are fractured, serpentinized, with regular magnetite exsolution. The<br />
olivine is optically positive, with values of 2V = 82° to 89° which corresponds to ca.<br />
14% of fayalite content.<br />
The quantitative chemical analysis of olivine from Mt. Konjuh is given in Table 4.<br />
35
SILICATES<br />
Table 4. Chemical analysis of olivine from Mt. Konjuh<br />
1 2<br />
SiO 2<br />
42.56 40.94<br />
Al 2<br />
O 3<br />
1.04 0.69<br />
Fe 2<br />
O 3<br />
0.47 0.68<br />
FeO 10.46 12.43<br />
MgO 45.44 44.24<br />
CaO 0.28 0.42<br />
Total<br />
Spec. gravity<br />
Composition<br />
36<br />
100.25<br />
3.43<br />
88% Fo<br />
12% Fa<br />
1 – olivine, Bebrave stream; 2 – olivine, nameless stream flowing into Lašva river<br />
99.40<br />
3.51<br />
93% Fo<br />
7% Fa<br />
Ristić and coworkers provide x-ray diffraction data for olivine from<br />
Dinkovac – d 3.74 (1) 2.85 (4) 2.50 (1) 2.455 (3) 1.74 (1).<br />
As mentioned previously, olivine is also the most common constituent of<br />
the investigated harzburgites. Serpentinization of olivine is quite extensive. The 2V<br />
values are 84°, 88°, 89° these values being almost the same for the optically positive<br />
olivine from lherzolite rocks. The olivines from gabbros have similar 2V values.<br />
According to J. Pamić (1970), olivine in ultrabasic rocks from the Duboštica<br />
chromite deposit area is commonly allotriomorphic, often corroded and showing<br />
rounded edges. Its contains around 8% fayalite, and is almost always serpentinized<br />
to some degree, showing a wavy extinction in thin section. Pressure twinning is<br />
also present.<br />
Based on diffraction data of the serpentine minerals associated with<br />
occurences of magnesite at Miljevci near Kladanj, Šćavničar and Sijarić (1972)<br />
identified olivine in the serpentine paragenesis.<br />
The Višegrad area. Ultrabasic and basic olivine rocks are rather common<br />
also in the area of Višegrad in eastern Bosnia. Olivine is the dominant constituent<br />
of harzburgites and feldspar-peridotites, while of secondary importance in gabbros<br />
(Trubelja 1957, 1960).<br />
In harzburgites from the Karaula spur near Dobrun, the olivine is present<br />
only in the form of “islets” in the serpentine matrix.<br />
Olivine in harzburgites from Bosanska Jagodina in the Rzav river valley is<br />
also largely serpentinized. All fragments are elliptically corroded and sometimes<br />
completely embedded into enstatite. Some mineral fragments of olivine display<br />
distinct cleavage parallel to (010).
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The olivine in feldspar-peridotites from Bosanska Jagodina has several<br />
characteristic features. Its content in these rocks is around 50%. In thin section it<br />
is rather fresh and fractured, with magnetite in the fractures. The serpentinization<br />
process is still in its early stages. Most of the fragments are elliptically shaped and<br />
surrounded by amphibole of tremolite-actinolite composition, forming a distinct<br />
kelyphytic corona around the olivine – a textbook example of a kelyphytic reaction<br />
rim. This rim is best developed along the olivine-plagioclase contact.<br />
Table 5. Data for olivine from the Višegrad area (Trubelja 1960)<br />
Locality, rock type<br />
Optic axes angle 2V<br />
Chemical<br />
composition<br />
Bosanska Jagodina, harzburgite 2V = +89°, +83°, +86°, +83° 0-10% Fa<br />
Karaula spur (Dobrun), harzburgite 2V = +89.5° (median) 14% Fa<br />
Bosanska Jagodina, feldspar-peridotite 2V = -82° to 90° 13-17% Fa<br />
Gornji Dubovik, troctolite 2V = +87°, +86°, +84°, +89.5°, +86° 0-11% Fa<br />
Gornji Dubovik, troctolite 2V = 90°, 90°, +87°, +87.5° 13-20% Fa<br />
Mirilovići village, olivine gabbro 2V = +81°, 90°, +82°, +80° ---<br />
Rijeka (Velika Gostilja), olivine gabbro 2V = 90° (median) ---<br />
Banja stream (Lahci village), troctolite 2V = -85°, -86.5°, -87°, -88°, -89° 15-24% Fa<br />
The elliptically shaped olivine fragments are commonly embedded in<br />
monoclinic or orthorhombic pyroxene, sometimes also in amphibole or plagioclase.<br />
The olivine shows a characteristic almost perfect cleavage parallel to (100). We feel<br />
the need to stress this finding since olivine is in the mineralogical literature usually<br />
described as having no pronounced cleavage.<br />
Olivine is also the predominating constituent in troctolite from Gornji<br />
Dubovik. Almost all fragments are elliptically shaped and surrounded by plagioclase,<br />
Some fragments display a thin rim of augite. Primary magnetite is usually embedded<br />
in olivine fragments.<br />
Data on olivine in basic and ultrabasic rocks of the Višegrad area can also<br />
be found in older petrological publications (John 1880, Schiller 1905, Pavlovitsch<br />
1937). Research by M. Kišpatić must be mentioned since it made a significant<br />
contribution to our knowledge on olivine and other rock-forming minerals.<br />
Marković and Takač (1958) have more recently investigated olivine in the<br />
olivine gabbros from Bosanska Jagodina. The olivine was optically positive, the 2V<br />
values = 88°, 88.5°, 86° corresponding to 18-21% of the fayalite component.<br />
37
SILICATES<br />
2. Olivine in products of triassic magmatism<br />
Outside of the “Bosnian serpentine zone” olivine occurs in the schist<br />
mountains of central Bosnia (Bijela Gromila), in products of triassic magmatism, as<br />
well as in more basic gabbro-type rocks at Jablanica.<br />
Around Kalinovik, olivine is an important constituent of diabases and picritebasalts<br />
occuring within the triassic volcanogenic-sedimentary series (Pamić 1960a).<br />
In the basalt-type rocks the olivine is substantially serpentinized and rich in forsterite.<br />
First microscopic determinations of olivine in the schist mountains of central<br />
Bosnia were done by M. Kišpatić (1910). The olivine occurs as an accessory mineral<br />
in gabbro from a locality called Peredine Liske, close to the village of Kopilo.<br />
Majer and Jurković (1957 and 1958) perfomed microscopic investigations of<br />
an olivine gabbro from Stajište-Margetići (Novi Travnik) where olivine is a principal<br />
mineral, together with hyperstene, plagioclase and some other minerals.<br />
At Jablanica, olivine occurs as a constituent of the olivine gabbro series<br />
(John 1888; Kišpatić 1910; Marić 1927). Marić determined some optical constants<br />
characteristic of olivine. According to this author the maximum birefringence Nz<br />
– Nx = 0.035; the refractive indices measured by the immersion method are Nx ><br />
1.645 < 1.646; Nz > 1.680 < 1.695.<br />
38<br />
3. Olivine in other rocks<br />
According to scant data by Varićak (1966), olivine occcurs in amphibolites<br />
and amphibolite schists of Mt. Motajica, only in the porphyroblastic varieties. The<br />
grains are small and usually very fresh with some signs of magmatic corrosion.<br />
The optic axis angle 2V lies in the range between -82° and -86°, corresponding to<br />
chrysolite with ca. 20-30% of fayalite.<br />
Uses<br />
Olivine rock with a small content of iron, either fresh or partly serpentinized,<br />
are a valuable source material for the production of fireproof forsterite bricks.<br />
Olivine is also used as a metal casting sand, instead of quartz sand. This use is<br />
based on its high melting point -1890°C for forsterite and 1205°C for fayalite. The<br />
production of fireproof bricks requires a MgO : SiO 2<br />
ratio of around 2, meaning that<br />
the olivine should be depleted in iron. When this is not the case, the iron present in<br />
the olivine results in the formation of pyroxene which has inferior fireproof qualities.<br />
The quality of natural olivine material can be improved by the addition of magnesite.<br />
The transparent, greenish-yellow variety of olivine (peridote) is also a<br />
popular gemstone.
GARNETS<br />
The Garnet Group<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Almandine Fe 3<br />
Al 2<br />
[SiO 4<br />
] 3<br />
Pyrope Mg 3<br />
Al 2<br />
[SiO 4<br />
] 3<br />
Grossular Ca 3<br />
Al 2<br />
[SiO 4<br />
] 3<br />
Andradite Ca 3<br />
Fe 2<br />
[SiO 4<br />
] 3<br />
Uvarovite Fe 3<br />
Cr 2<br />
[SiO 4<br />
] 3<br />
Crystal system and class:<br />
Cubic, Hexaoctahedral class;<br />
Properties: garnets have no pronounced cleavage. Hardness = 6-7.5. Vitreous to<br />
resinous lustre. Colour depends on the mineral species i.e. chemical composition.<br />
Pyrope is dark red, pinkish-red, black. Almandine is red, dark red, black. Spessartine<br />
can be dark red, orange-red, brown. Grossular is yellow like honey, light green, brown,<br />
red. Andradite is yellow, greenish, dark red, black. Uvarovite has a characteristic<br />
emerald-green colour.<br />
The refractive index, specific gravity and unit cell parameters vary:<br />
n D a o<br />
(Å)<br />
Almandine 1.830 4.318 11.526<br />
Pyrope 1.714 3.582 11.459<br />
Grossular 1.734 3.594 11.851<br />
Andradite 1.887 3.859 12.048<br />
Uvarovite 1.86 3.90 12.00<br />
Grossular, andradite and uvarovite sometimes display significant birefrigence.<br />
X-ray diffraction data:<br />
d<br />
Almandine 2.57 (100) 1.54 (50) 2.87 (40)<br />
Pyrope 2.58 (100) 1.54 (100) 1.07 (70)<br />
Grossular 2.65 (100) 1.58 (90) 2.96 (80)<br />
Andradite 2.70 (100) 3.02 (60) 1.61 (60)<br />
Uvarovite 2.68 (100) 3.00 (70) 1.60 (60)<br />
IR-spectrum:<br />
cm -1<br />
Almandine 455 480 527 570 638 872 902 970 1000 1090<br />
Pyrope 460 482 530 575 820 872 900 970 1000 1080<br />
Grossular 450 470 540 618 840 860 915 960 1080<br />
Andradite 428 482 512 592 820 840 895 930 1085<br />
Uvarovite 420 455 540 609 825 840 900 945 1000<br />
39
SILICATES<br />
GARNETS IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Arsenijević (1967), Cissarz (1966), Čelebić (1967), Čutura<br />
(1918), Džepina (1970), Đorđević, Buzaljko and Mijatović (1968), Đurić and Kubat<br />
(1962), Foullon (1893), Gaković J. and Gaković M. (1973), Grafenauer (1975),<br />
Jurković (1957), Katzer (1924 and 1926), Kišapatić (1897, 1900 and 1912), Koch<br />
(1908), Kubat (1964), Magdalenić and Šćavničar (1973), Majer (1962), Marić<br />
(1965), Milenković (1966), Mojsisovicz, Tietze and Bittner (1880), Nöth (1956),<br />
Pamić (1960, 1969a, 1971, 1971a, 1972c and 1972d), Pamić and Kapeler (1970),<br />
Pamić and Maksimović (1968), Pamić, Šćavničar and Međimorec (1973), Pavlović<br />
and Ristić (1971), Pavlović, Ristić and Likić (1970), Pilar (1882), Primics (1881),<br />
Ristić, Likić and Stanišić (1968), Sijerčić (1972), Šćavničar and Jović (1961 and<br />
1962), Šibenik-Studen, Sijarić and Trubelja (1976), Trubelja and Pamić (1957),<br />
Varićak (1966), Walter (1887).<br />
Garnets belong to the group of fairly common and widely distributed<br />
rock-forming minerals in Bosnia and Hercegovina. They are most common in<br />
metamorphic rocks of the Bosnian serpentine zone, and have been studied in detail<br />
in these environments. Garnets are found both as principal and accessory minerals<br />
in igneous and metamorphic rocks of Mt. Motajica and the schist mountains of<br />
central Bosnia. Around Jablanica and Prozor the garnets occur as typical contact<br />
metamorphic minerals. In the triassic granits of Komar, garnet is incorporated in<br />
quartz grains. Being resistants and stable minerals, garnets frequently find their way<br />
into clastic sediments also.<br />
40<br />
1. Garnets in metamorphic rocks of the Bosnian serpentine zone<br />
Early information on garnets in metamorphic rocks of the Bosnian serpentine<br />
zone can be found in the paper by C. von John (Mojsisovics, Tietze and Bittner<br />
1880, p. 282). According to John, bright red garnet occurs in the Podbrđe eclogite.<br />
In thin section the garnet is colourless, surrounded by a chlorite layer formed from<br />
the garnet material. These garnets are also mentioned by Pilar (1882).<br />
A substantial amount of information on the distribution of garnets in rocks<br />
of the Bosnian serpentine zone can be found in the monograph by M. Kišpatić (1897<br />
and 1900). Through microscopic investigations of eclogites, eclogite amphibolites,<br />
amphibole eclogites, eclogite pyroxenites, amphibolites, pyroxene amphibolites,<br />
garnet pyroxenites and garnet phyllites, Kišpatić was able to determine garnets in<br />
the area of Mt. Pastirevo and Višegrad.<br />
Thin sections of rocks where garnet occurs either as an accessory or principal<br />
mineral, garnet grains are seldom colourless and idiomorphic. They are mostly<br />
pinkish to reddish in colour. Grains are of irregular shape and fractured. Inclusions
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
in garnet are frequent and consist of omphacite, rutile, zircon – while feldspars are<br />
less common. Grains often have a kelyphytic corona, consisting of omphacite or<br />
amphibole. This summarizes the data provided by Kišpatić.<br />
V. Majer (1962) mentions garnet as a constituent of garnet-gabbro and<br />
garnet-hornblendites in the area between the Vrbas and Bosna rivers. In these rocks<br />
the garnet is usually pink in colour. The amount of garnet varies within a broad<br />
range, and can sometimes comprise 90% of the total rock volume. Majer mentions<br />
a frequent kelyphytic rim around garnet grains in garnet gabbros, corroborating an<br />
earlier similar finding by M. Kišpatić. The kelyphytic rim is less common in the<br />
case of garnet hornblendites. According to Majer, the garnet gabbros and garnet<br />
hornblendites could be classified as igneous rocks, although their metamorphic<br />
origin cannot be completely excluded. To this end, no final opinion about the genesis<br />
of garnets – either as principal or accessory minerals – can be given.<br />
Almandine garnet is a constituent of the garnet amphibolite og Mt. Čavka<br />
(Đurić and Kubat 1962; Kubat 1964).<br />
According to Pamić and some other authors, garnet-containing metamorphic<br />
rocks are found in three independent parts of the Bosnian serpentine zone. The Mt.<br />
Skatovica area is located east of Banja Luka, where outcrops of amphibolite with<br />
garnet as the principal mineral occur. The second area is around Mt. Borja and Mt.<br />
Mahnjača, as already described by Kišpatić. Finally, garnet rocks at the southern<br />
flanks of the Mt. Krivaja – Mt. Konjuh metamorphic complex need mentioning. In<br />
this section of the Bosnian serpentine zone, garnet rock outcrops several kilometers<br />
in length can be found (garnet amphibolites, garnet-pyroxene amphibolite schists).<br />
In these rocks the garnet grains can be several centimeters in diameter, since they<br />
seem to be porphyroblasts with macroscopically visible rhombododecahedral and<br />
other crystal forms.<br />
Some details on garnets extracted from amphibolites can be found in the<br />
papers by Pamić (1969a, 1971 and 1972c), and – particularly – Pamić, Šćavničar<br />
and Međimorec (1973). In the largely petrographic publication “Ultramafiticamphibolitic<br />
rocks of Mt. Skatovica in the ophiolitic zone of the Dinarides”, Pamić<br />
(1969a and 1972c) provides the chemical analysis of the garnet fraction of these<br />
rock, and identifes it as a pyrope-type garnet (Table 6, column 4).<br />
Pamić, Šćavničar and Međimorec (1973) have recalculated 5 chemical<br />
analyses of garnets in terms of their end-member chemistries – the data is given in<br />
Table 6. It can be seen that the chemical compositions of garnets in amphibolitic<br />
rocks can be quite different and variable, a fact which may be related to the<br />
variable chemistry of the host rocks. In other words, there seems to be a functional<br />
interdependence between the chemical composition of the garnets on one side, and<br />
that of amphibole and plagioclase on the other side.<br />
41
SILICATES<br />
Pyrope-type garnets (Table 6, columns 3 and 4) occur in rocks of andesinelabradorite<br />
and pargasite/edenite amphibole composition. Almandines (Table<br />
6, columns 1 and 2) are rather associated with Na-andesine and chermakite-type<br />
amphiboles or “common hornblende”.<br />
X-ray diffraction data of one garnet showed that the lattice parameter a o<br />
=<br />
11.570 ± 0.003 Å, implying pyrope composition.<br />
In a detailed description of rocks from the southern flanks of Mt. Borje,<br />
which have undergone regional metamorphism, D. Džepina (1970) provides data<br />
on refractive indices, unit cell parameters and composition of several garnets from<br />
various locatlities (Table 7). The garnet compositions have been derived from the<br />
Srimadas diagram, using refractive index values and cell parameters. The garnets<br />
occur as xenoblastic grains of different sizes ranging from large porphyroblasts<br />
to microscopically small grains. A kelyphytic reaction rim is a common feature<br />
of these garnets, inferring a reaction with other minerals derived from the rock<br />
(diopside, hornblende).<br />
Table 6. Chemical composition of garnets from amphibolite rocks<br />
Sample 1 2 3 4 5<br />
SiO 2<br />
38.5 39.3 38.94 38.46 39.0<br />
TiO 2<br />
0.09 0.07 --- 0.02 0.11<br />
Al 2<br />
O 3<br />
21.4 21.7 18.61 21.70 21.4<br />
Cr 2<br />
O 3<br />
nd nd 0.10 nd nd<br />
Fe 2<br />
O 3<br />
1.89 2.62<br />
FeO 24.7 22.5 16.96 13.99 24.2<br />
MnO 0.81 0.50 0.60 0.86 0.52<br />
MgO 6.4 7.3 13.75 12.75 6.0<br />
CaO 8.9 9.5 8.90 9.45 10.1<br />
Na 2<br />
O nd nd --- 0.20 nd<br />
K 2<br />
O nd nd --- 0.14 nd<br />
H2O + nd nd --- --- nd<br />
H2O - nd nd --- --- nd<br />
P 2<br />
O 5<br />
nd nd 0.09 0.05 nd<br />
Total 100.80 100.87 99.84 100.25 101.33<br />
Pyrope 27.6 24.5 45.8 45.9 22.6<br />
Almandine 45.7 49.5 31.7 28.3 48.6<br />
Spessartine 1.1 1.8 1.1 1.4 1.1<br />
Grossular 22.4 18.9 16.3 17.3 23.1<br />
Andradite 3.2 5.3 4.8 7.1 4.5<br />
Uvarovite --- --- 0.3 --- ---<br />
Localities: 1, 2 and 4 – Mt. Skatovica; 3 – Mt. Konjuh; 5 – Mt. Čavka<br />
42
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
S. Grafenauer (1975, p. 103) identified small uvarovite grains in the well<br />
known chromite deposit at Duboštica. Here, the chromite grains are very fractured.<br />
There is a zonal distribution of uvarovite with pyrrhotite and pentlandite, in the form<br />
of grains or veins. The veins can be rather long, but only about 1 μm thick.<br />
Andradite occurs together with diopside, serpentine and chlorite at Mt.<br />
Ozren, near the village of Gornji Rakovac. The minerals were identified by X-ray<br />
diffraction (Šibenik-Studen, Sijarić and Trubelja 1976).<br />
2. Garnets in rocks of Mt. Motajica<br />
F. Koch (1908) was the first to describe the garnets in igneous and<br />
metamorphic rocks of Mt. Motajica. According to his microscopic determinations,<br />
the garnets occur mostly as accessory constituents of granite, muscovite-granite,<br />
biotite-granite/gneiss and micaschists. Granet is a principal mineral of the biotitegneisses<br />
from Studena Voda and Kamen-potok near Korbaš. It occurs in the form<br />
of red nodules. In thin section the garnet grains are fresh and easily visible due<br />
to their rough surface. The smaller grains are usually birefringent. Metamorphic<br />
transformation into chlorite is common. Inclusions in garnet grains consist of<br />
magnetite, zircon, rutile and – sometimes – biotite. The garnets contained in biotite<br />
gneisses of Hercegov Dol and Bosanski Svinjar are strongly birefringent. The<br />
garnet is colourless and fresh, but fractured.<br />
Table 7. Data on garnets from the Mt. Borje metamorphites<br />
Composition %<br />
Locality Mineral assemblage N a o<br />
Pyrope Almandine Grossular<br />
hornblende 1.767 11.64 23 37 40<br />
Crni potok<br />
diopside<br />
garnet<br />
plagioclase<br />
diopside<br />
1.772 11.57 33 46 21<br />
Velika Usora<br />
plagioclase<br />
hgornblende<br />
garnet<br />
diopside<br />
1.767 11.57 36 43 21<br />
Velika Usora<br />
hornblende<br />
plagioclase<br />
garnet<br />
Velika Usora<br />
garnet<br />
1.772 11.54 40 47 13<br />
hornblende<br />
hornblende 1.768 11.57 35 44 21<br />
Borovnica<br />
diopside<br />
garnet<br />
prehnite<br />
43
SILICATES<br />
Velika usora<br />
Velika usora<br />
hornblende<br />
garnet<br />
plagioclase<br />
rodingitized garnet<br />
rock<br />
1.772 11.59 26 48 26<br />
1.752 11.56 46 29 25<br />
F. Katzer (1924 and 1926) also mentions the garnets in rocks of Mt. Motajica.<br />
Results of more recent petrographic investigations of the Mt. Motajica garnets<br />
show that the garnets are common accessory minerals in granite, pegmatites, gneiss<br />
(amphibole and albite gneisses), cornites (biotite and pyroxene), gneissphyllites,<br />
amphibolites, amphibole schists and glaucophanites (Varićak 1966).<br />
3. Garnets in rocks around Jablanica and Prozor<br />
According to available literature data, garnets occur as products of contact<br />
metamorphism in the area south of Prozor, and in the magnetite body of Tovarnica<br />
near Jablanica (Nöth 1956; Cissarz 1956; Pamić 1960; Čelebić 1967).<br />
Garnet has also been identified in the contact zone in the Crima creek – close<br />
to the village of Lug south of Prozor. It seems to be genetically associated with the<br />
albite diabase which protrudes through the Triassic limestones and upper horizons<br />
of the Werfen series. In addition to garnet, the paragenesis contains also epidote,<br />
clinozoisite, chlorite (probably pennine), hydromica, prehnite, sericite, albite,<br />
apatite, magnetite and pyrite (Pamić 1960). Relevant changes in the composition<br />
and grain size distribution of the material impacted by contact metamorphism are<br />
given in Table 8.<br />
Table 8. Paragenesis of the contact metamorphism area south of Prozor (Pamić 1960)<br />
Locality<br />
Distance<br />
from rock<br />
(m)<br />
Grain size<br />
(mm)<br />
Garnet<br />
Epidote<br />
Clinozoisite<br />
Chlorite<br />
Hydromica<br />
Prehnite<br />
Sericite<br />
Albite<br />
Apatite<br />
Magnetite<br />
Pyrite<br />
11 140-150 ca. - - - - - - - - - - -<br />
0.001<br />
12 105-115 0.01 - - - - - - - - - - -<br />
13 ca. 10 0.05 - - - + + - - - - - +<br />
14 ca. 35 0.05-0.1 - - + - + - - - + - +<br />
15 0-10 0.1-0.6 + + - + - - - - + + -<br />
10 0-10 0.5 + - - + - - - + - + -<br />
17 ca. 45 0.05 - - + - + - - - - + -<br />
28 ca. 65 0.07 - - - - + - - - - - +<br />
29 0-10 0.05 + - - + - + + + - + -<br />
31 ca. 30 0.15 + + - + - - - - - + -<br />
44
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
In the western part of the contact zone (the Crima creek) the Triassic<br />
limestones have undergone alteration, while in the eastern part (Bare creek)<br />
mostly clayey schists of the Werfen series and marls with interlayers of limestone<br />
were affected.<br />
Grossular is found in the immediate contact with albite diabase. In the<br />
rock the grossular appears to be yellowish and only sometimes green, however<br />
it is colourless in thin section. Some grains are idiomorphic in shape, and have a<br />
high relief. With crossed polarizers the grossular is completely isotropic (i.e. dark).<br />
Fracturing is common, with calcite filling the fractures.<br />
The grossular was separated from the marble host rock by acetic acid, and<br />
analysed for chemical composition. The “end-member” compositions are shown in<br />
Table 9 (analysed by J. Pamić).<br />
Table 9. Chemical analysis and the “molecular” composition of garnet from the Crima creek<br />
SiO 2<br />
39.30 Grossular 85.5%<br />
TiO 2<br />
0.22 Pyrope 6.4%<br />
Al 2<br />
O 3<br />
20.95 Andradite 5.4%<br />
Fe 2<br />
O 3<br />
1.93 Almandine 0.5%<br />
FeO 0.32 Spessartine 0.4%<br />
MnO 0.24<br />
MgO 1.72<br />
CaO 34.66<br />
Locality: Crima creek<br />
Na 2<br />
O 0.15<br />
CO 2<br />
0.52<br />
The garnet crystals from the Crima creek locality show two crystal forms:<br />
the rhombic dodecahedron {110} and the icosatetrahedron {112}.<br />
Another occurence of garnets formed by contact metamorphism is located<br />
near the rims of the gabbro body of Jablanica (Tovarnica), where the gabbro<br />
protrudes through Triassic limestones and schists forming an elongated and<br />
irregular metamorphism zone. The paragenesis of this zone was investigated in<br />
some detail by A. Cissarz (1956) – it consists of garnets, epidote, albite, calcite,<br />
magnetite and pyrite.<br />
45
SILICATES<br />
46<br />
Figure 2. Exsolution sequence of minerals in the contact metamorphism zone of<br />
Tovarnica near Jablanica (Cissarz 1956)<br />
A garnet of andradite-grossular composition is the oldest member of the<br />
paragenesis, alongside with calcite. Magnetite, together with minor amounts of<br />
pyrrhotite and chalcopyrite also formed in the initial phase. The Tovarnica locality<br />
is known for its potential as a magnetite ore body. The scarn mineral paragenesis<br />
of the Tovarnica region has been further described by Đ. Čelebić (1967) based on<br />
earlier microscopic investigations by S. Pavlović and coworkers.<br />
J. Pamić and V. Maksimović (1968) have also identified a contact<br />
metamorphism paragenesis in sediments of Bijela, near Konjic, similar to the one<br />
in Crima creek. In addition to garnet, this paragenesis consists also of hydromica,<br />
clinozoisite, epidote and albite. The garnet grains are isometric, sometimes clearly<br />
idiomorphic, so that the crystal habit is usually observable. In thin section the garnet<br />
is colourless, has a high relief and frequently displays fracturing. It is isotropic under<br />
crossed polarizers.<br />
4. Garnets in sedimentary rocks<br />
Garnet is frequently found in sedimentary rocks, due to its mechanical<br />
stability and chemical inertness, and pertaining information can be found in numerous<br />
publications (Foullon 1893; Gaković, J. and Gaković, M. 1973; Magdalenić and
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Šćavničar 1973; Marić 1965; Pavlović and Ristić 1971; Pavlović, Ristić and Likić<br />
1970; Ristić, Likić and Stanišić 1968; Sijerčić 1972; Šćavničar and Jović 1961 and<br />
1962; Kišpatić 1912).<br />
Foullon (1893) mentions an occurence of garnet in the alluvium of Zlatno<br />
Guvno and Bijela Gomila in the schist mountains of central Bosnia.<br />
Small quantities of garnets can be retrieved from the insoluble residue of<br />
Triassic carbonates (clayey micrite, microsparite) around Glamoč, as well as in Triassic<br />
pelsparites, micrites and dolomites from Livno (Gaković and Gaković 1973).<br />
The heavy mineral fraction of Pliocene sand from the Kreka coal basin<br />
also contains garnets (Šćavničar and Jović 1961 and 1962). The garnets from<br />
the “A” horizons are pinkish in colour, irregular and angular or subangular in<br />
shape. They are isotropic and display a high relief. Based on the refractive index<br />
of 1.81-1.83, determined by the immersion method, the garnet has almandine<br />
composition. Almandine can also be found in Miocene-age clastic sediments and<br />
Eocene sandstone.<br />
Occurences of garnet in sands of the Tuzla basin are mentioned by Pavlović,<br />
Ristić and Likić (1970), Ristić, Likić and Stanišić (1968) and Sijerčić (1972).<br />
Pavlović and Ristić (1971) describe an occurence of garnet in the quartz sand<br />
and gravels at Bijela Stijena near Zvornik. Magdalenić and Šćavničar (1973) have<br />
identified garnet in the heavy mineral fraction of Miocene-age sandy calcarenites<br />
from Lupina near Kulen Vakuf.<br />
M. Kišpatić (1912) investigated garnets in bauxite from Studena Vrela<br />
(Duvno) – this research is also mentioned by L. Marić (1965).<br />
Uses<br />
Due to its hardness, absence of cleavage and irregular fracture, garnets are<br />
commonly used as abrasives. Garnets of almandine composition are most common<br />
abrasive agents, spessartine much less so. Best for this purpose are larger crystals<br />
which are ground into smaller grains and attached to paper or cloth. Such abrasive<br />
items are widely used for polishing various materials. According to literature data,<br />
about 90% of garnets produced are used as abrasives. The presence of lamellae is<br />
deleterious, since the grains are prone to split into platelike fragments under pressures<br />
attained in the abrasion process.<br />
Transparent and attractively coloured garnets are frequently used as<br />
gemstones (almandine, pyrope, uvarovite).<br />
47
SILICATES<br />
HIBSCHITE<br />
Ca 3<br />
Al 2<br />
[(Si,H 4<br />
)O 4<br />
] 3<br />
Hibschite is apparently identical with plazolite (hydrogrossular). It<br />
crystalizes in the cubic system, with unit cell dimensions of a o<br />
= 12.02-12.16 Å. Part<br />
of the SiO 4<br />
tetrahedra are substituted with OH groups. It has a vitreous lustre, and is<br />
colourless to yellowish. Hardness = 6.5, specific gravity = 3.13.<br />
X-ray diffraction data: d 2.68 (100), 3.00 (80), 1.61 (80)<br />
In Bosnia and Hercegovina hibschite has been found within the Bosnian<br />
serpentine zone, at the confluence of the creeks Omrklica and Rakovac, at Mt.<br />
Ozren. It was identified by XRD and IR-spectroscopy (Šibenik-Studen, Sijarić and<br />
Trubelja 1976).<br />
ZIRCON<br />
Zr[SiO 4<br />
]<br />
Crystal system and class: Tetragonal, ditetragonal-dipyramidal class.<br />
Lattice ratio: a : c = 1 : 0.9054<br />
Unit cell parameters: a o<br />
= 6.604, c o<br />
= 5.979, Z = 4.<br />
Properties: cleavage weak along {110}. Hardness = 7.5, specific gravity = 4.6-4.7<br />
(for crystalline varieties) decreasing to 3.9 for metamict varieties. Seldom colourless,<br />
mostly brown, redish-brown due to admixtures or inclusions. Streak is white, lustre<br />
vitreous to adamantine. Refractive indices and birefringence are high, depending on<br />
variations in chemical composition:<br />
N E<br />
= 1.96-2.02, N O<br />
= 1.92-1.96, N E<br />
– N O<br />
= 0.04-0.06<br />
Zircon is optically positive, uniaxial.<br />
X-ray diffraction data: d 3.30 (100), 4.43 (45), 2.52 (45), ASTM-card 6-0266.<br />
IR-spectrum: 438 455 618 895 1040 cm -1 (zircon, Haddan, CT, USA)<br />
48<br />
ZIRCON IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Barić (1966), Barić and Trubelja (1971), Čutura (1918),<br />
Džepina (1970), Đorđević (1969), Đorđević and Mijatović (1966), Đorđević and<br />
Stojanović (1964), Foullon (1893), Gaković and Gaković (1973), Jakšić (1927),<br />
Jovanović (1972), Jurković (1956, 1958, 1958a and 1961), Jurković and Majer<br />
(1954), Karamata (1953/54), Karamata and Pamić (1964), Katzer (1924 and 1926),<br />
Kišpatić (1897, 1900, 1904, 1904a, 1904b, 1909, 1912 and 1915), Koch (1908),<br />
Luković (1957), Magdalenić and Šćavničar (1973), Majer (1963), Majer and Jurković
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
(1958), Maksimović (1968), Marić (1965), Marić and Crnković (1961), Markov and<br />
Mihailović-Vlajić (1969), Mihailović-Vlajić (1967), Mudrinić and Janjić (1969),<br />
Pamić (1961, 1969a, 1970a, 1971a, and 1972c), Pamić and Kapeler (1970), Pamić<br />
and Olujić (1969), Pamić and Tojerkauf (1970), Pamić, Šćavničar and Međimorec<br />
(1973), Pavlović and Ristić (1971), Podubsky (1968 and 1970), Ristić, Likić and<br />
Stanišić (1968), Sijerčić (1972), Šćavničar and Jović (1961 and 1962), Šinkovec and<br />
Babić (1973), Tajder (1936, 1951/53 and 1953), Trubelja (1962a and 1963), Trubelja<br />
and Šibenik-Studen (1965), Varićak (1955, 1956 and 1966), Vasiljević (1969).<br />
In Bosnia and Hercegovina zircon is a constituent of igneous, sedimentary<br />
and metamorphic rocks, mainly as an accessory mineral. It occurs mainly in granites,<br />
albitic granitoid rocks, quartzporphyres, gneisses and pegmatites. It is also commonly<br />
found in sedimentary rocks of the schist mountains of central Bosnia, as well as<br />
in eastern and western Bosnia. In these areas it is frequently associated with ore<br />
deposits. It also occurs as a accessory mineral in the metamorphic rocks (middle and<br />
high degree of metamorphism) of the Bosnian serpentine zone. Zircon is also found<br />
in the heavy mineral fraction of the carbonate rocks of the outer Dinaride complex.<br />
Because of its mechanical stability and chemical inertness zircon is frequently found<br />
in alluvial deposits and sands, as well as in other clastic sediments.<br />
1. Zircon in the schist mountains of central Bosnia<br />
In the schist mountains of central Bosnia zircon occurs in a variety of rocks,<br />
and has been described by numerous authors: Barić and Trubelja (1971), Čutura<br />
(1918), Foullon (1893), Jurković (1956, 1958, 1958a and 1961), Jurković and Majer<br />
(1954), Trubelja and Šibenik-Studen (1965).<br />
Earliest information on the occurence of zircon in alluvial deposits and<br />
sands of numerous rivers and creeks in the schist mountains of central Bosnia can<br />
be found in the paper by Foullon (1893). On pp. 32-33 of the cited paper, the author<br />
writes that zircon is associated with most minerals present in these deposits, with the<br />
exception of tetrahedrite (in the Mačkara forest), occuring sometimes in substantial<br />
quantities. It would be interesting to verify this data. Zircon is also an accessory<br />
mineral in quartzporphyres.<br />
In his publication “Petrographic notes from Bosnia” M. Kišpatić (1904b)<br />
describes the occurence of small crystals of zircon in the chloritoid phyllites<br />
between Fojnica and Čemernica. This zircon is yellowish in colour and has strong<br />
birefringence.<br />
In the schist mountains of central Bosnia, zircon is aloa associated with ore<br />
formations at Trošnik, Vrtlasce and Banjak, as a member of the high-temperature<br />
mineral series – together with rutile, tourmaline and apatite (according to I. Jurković).<br />
49
SILICATES<br />
Zircon has been described as an accessory constituent in granitoids,<br />
quartzporphyres and diorites of the schist mountains (Čutura 1918; Jurković and<br />
Majer 1954; Majer and Jurković 1958, Trubelja and Šibenik-Studen 1965).<br />
Zircon can be rarely seen in thin sections of the altered rhyolites (hydromicaschists)<br />
found at Repovci village, west of Bradina. Occasional colourless zircon<br />
crystal sometimes have a bipyramidal shape, showing a high relief. The largest<br />
crystals were ca. 0.05 mm long and 0.017 mm thick (Barić and Trubelja 1971).<br />
50<br />
2. Motajica, Prosara, northwestern and eastern Bosnia<br />
In northwestern Bosnia, within the Paleozoic-age series of rocks in the area<br />
of the rivers Una and Sana, zircon is sometimes found as an accessory mineral in<br />
sediments and metamorphic rocks, and in the parageneses of the Ljubija ore deposit<br />
(Kišpatić 1909, Marić and Crnković 1961, Podubsky 1968). Kišpatić was able to<br />
determine zircon in association with pyromorphite, limonite, cerrusite, anglesite,<br />
quartz and siderite (the Adamuša locality near Ljubija).<br />
D. Varićak (1956) found zircon as an accessory constituent of the Mt. Prosara<br />
quartzporphyres. Most igneous and metamorphic rocks from Mt. Motajica contain<br />
zircon as an almost ubiquitous accessory mineral (Varićak 1966).<br />
According to F. Koch (1908) zircon is a characteristic accessory constituent<br />
of the Mt. Motajica granite, gneiss and pegmatite. It is also found in micaschists and<br />
amphibolites. In the Vlaknica granite zircon occurs in the form of colourless egglike<br />
grains or crystals of prismatic or dipyramidal shape, and usually forms inclusions in<br />
feldspar, quartz and biotite. Koch mentions zircon in rocks from the Osovica creek<br />
near Šeferovac. In the biotite gneisses of Studena Voda, zircon occurs as numerous<br />
smaller and larger crstals of dipyramidal shape.<br />
N. Mihailović-Vlajić (1967, pp. 194-195) gave a comparatively detailed<br />
account of zircon in various rocks of Mt. Motajica. Zircon occurs in the form of<br />
pinkish crystals 0.1-0.2 mm in size, in a combination of (100) and (111) crystal<br />
forms. Their length-to-width ratio is in the range from 1 : 2.5 to 1 : 3, in aplite-type<br />
rocks even 1 : 5. In other rock types (greisens) zircon shows (110) forms, and (311)<br />
forms (leucocratic rocks).<br />
In muscovite-granites zircon occurs as opaque or almost black crystals 0.1<br />
to 0.3 mm in size of characteristic dipyramidal shape. Sometimes the (110) crystal<br />
form in cobination with (111) can be observed. Colourless zircon is seldom present.<br />
In aplitic biotite-granites the zircon is commonly colourless or yellowish,<br />
translucent and often showing signs of corrosion. Crystals are 0.1-0.4 mm in size.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Within the main granite body there is some zircon larger than 0.2 mm.<br />
The muscovitic, leucocratic and aplitic granites contain more of the corroded and<br />
colourless zircon, and these varieties usually amount to ca. 80% of the total zircon<br />
content. These crystals are always fractured, of lesser transparency and rounded<br />
edges. Crystals are sometimes malformed or torqued.<br />
In all rock types of the Mt. Motajica granite, gasesous inclusions in zircon<br />
have been observed (mostly in muscovitic granite and greisens). Sometimes can a<br />
partial ‘overgrowth’ of zircon on metallic minerals be observed in biotitic granites.<br />
Zircon is a common accessory mineral of the Paleozoic-age sedimentary<br />
rocks and semimetamorphites of eastern and southeastern Bosnia (Podubsky 1970).<br />
3. Zircon in rocks of the Bosnian serpentine zone<br />
Zircon as an accessory constituent of rocks belonging to the Bosnian<br />
serpentine zone has been decribed by numerous authors: Džepina (1970), Đorđević<br />
and Mijatović (1966), Đorđević and Stojanović (1964), Karamata (1953/54),<br />
Karamata and Pamić (1964), Majer (1963), Pamić (1969a, 1970a, 1971a, and 1972c),<br />
Pamić and Kapeler (1970), Pamić and Olujić (1969), Pamić and Tojerkauf (1970),<br />
Pamić, Šćavničar and Međimorec (1973).<br />
The occurences of zircon, mentioned by these authors, mainly pertain to<br />
igneous and metamorphic rocks in peripheral sections of the Bosnian serpentine<br />
zone (oligoclastites, albitic granites, albitic rhyolites, albitic syenites, amphibolites).<br />
It is most common in albite granitoid rocks.<br />
4. Zircon in Tertiary-age effusive rocks and tuffs<br />
Zircon as an accessory constituent of Tertiary-age effusives and associated<br />
tuffs occurs in various parts of Bosnia and Hercegovina (Barić 1966a, Đorđević<br />
1969, Kišpatić 1904 and 1904a, Luković 1957, Tajder 1951/53 and 1953).<br />
Microscopic investigations of tuffs from the Livno area showed that small<br />
quantities of zircon are present in these rocks. Crystals are very small, in the range<br />
of ca. 0.02-0.05 mm and have a high relief (Barić 1966a).<br />
S. Luković (1957) identified zircon in the form of prismatic crystals in<br />
volcanic tuffs within Neogene-age sediments around Tuzla.<br />
In the products of Tertiary magmatism (dacites) of the Srebrenica area and<br />
the river Bosna valley, zircon is only an infrequent accessory mineral (Kišpatić 1904<br />
51
SILICATES<br />
and 1904a). In dacites from Kneževac (around Srebrenica) zircon occurs in the form<br />
of beautiful, small crystals with prismatic and dipyramidal faces. It occurs both in<br />
the rock matrix as well as included in quartz or plagioclase.<br />
Zircon occasionally occurs in tourmaline-quartz rocks around Srebrenica<br />
(Đorđević 1969).<br />
52<br />
5. Zircon in other rocks<br />
Zircon is a fairly common constituent of the insoluble residues of Triassic<br />
carbonates from the outer Dinarides in Bosnia and Hercegovina (Gaković and<br />
Gaković 1973).<br />
Due to its mechanical stability and chemical inertness, zircon often occurs<br />
in alluvial deposits and riverine sands, and in other clastic sediments. Jovanović<br />
(1972) found it in Pliocene-age sands of the Prijedor basin; Magdalenić and<br />
Šćavničar (1973) in clastic sediments of Lupina, Kulen-Vakuf; Pavlović and Ristić<br />
(1971) in the sands and gravels of Bijela Stijena near Zvornik; Ristić, Likić and<br />
Stanišić (1968) in the sands of the Tuzla basin; Sijerčić (1972) in the sands at Mt.<br />
Majevica; Šćavničar and Jović (1961 and 1962) in the sands and sandstones of the<br />
Kreka coal basin.<br />
According to B. Šćavničar and P. Jović, zircon is a common constituent<br />
of the heavy mineral fraction of Pliocene sands of the so-called “A” horizons in<br />
the Kreka coal basins. It occurs as colourless or pinkish crystals, of short prismatic<br />
shape, more seldom elongated or needlelike. The authors believe that the zircon has<br />
undergone several events of resedimentation, and that it originates from acid igneous<br />
rocks, pegmatites and gneisses.<br />
Trubelja (1962a and 1963) found zircon to be an accessory constituent of the<br />
quartzporphyres of Triassic age in the Lim river valley.<br />
In the red granites of Mt. Maglaj, zircon occurs in the form of prismatic<br />
crystal 0.8 x 0.2 mm in size, with pronounced idiomorphism. They can be easily<br />
recognized under the microscope, due to its characteristic prismatic and dipyramidal<br />
shapes (Varićak 1955).<br />
Zircon crystals have also been identified in some bauxites in Bosnia and<br />
Hercegovina (Kišpatić 1912 and 1915; Jakšić 1927; Maksimović 1968; Marić 1965;<br />
Mudrinić and Janjić 1969; Šinkovec and Babić 1973).<br />
M. Kišpatić and T. Jakšić have both identified zircon in the bauxite from<br />
Široki Brijeg (Lištica) in Hercegovina. According to Kišpatić, zircon can also be
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
found in the bauxite from Studena Vrela (Duvno). Maksimović provides data on<br />
zircon from hercegovinian bauxites, while Mudrinić and Janjić found zircon in<br />
bauxite from Vlasenica in eastern Bosnia. Šinkovec and Babić identified detritic<br />
zircons in the bauxite from Grmeč (the Oštrelj deposit), with crystals 50 μm in size.<br />
Uses<br />
Zircon is a source of the elements zirconium and hafnium. It is also used in<br />
the production of ceramics and fireproof linings. Clean and transparent zircon is also<br />
used as a gem material (yellow-red hycinth, colourless, blue).<br />
Zirconium oxide ZrO 2<br />
and metallic zirconium are widely used in nuclear<br />
reactor technology and for special alloys and glazings.<br />
THORITE<br />
Th[SiO 4<br />
]<br />
Crystal system and class: Tetragonal, ditetragonal-dipyramidal class.<br />
Lattice ratio: a : c = 1 : 0.627 (based on XRD data. The XRD and morphological<br />
orientation are different due to a 45° rotation around the vertical axis).<br />
Unit cell parameters: a o<br />
= 7.03, c o<br />
= 6.25, Z = 4.<br />
Nomenclature and synonyms: In 1828 Prior M. Esmark found a dark coloured mineral<br />
in pegmatitic veins of the augite syenite at Brevik on Lövö island (Langesundfjord,<br />
southern Norway). Berzelius discovered a new element in this mineral, and in 1829<br />
named it thorium, after the nordic god Thor. As a matter of fact, he used this name<br />
previously, in 1818, when he investigated some minerals from Falun in Sweden<br />
– but some years later realized that he was dealing with yttrium phosphate. The<br />
mineral was named accordingly thorite. In 1851 Krantz gave the name orangeite to<br />
the orange-yellow variety of thorite. The variety in which thorium is substituted with<br />
8-20% UO 3<br />
has been named uranothorite. Ferrithorite may contain up to 13% Fe 2<br />
O 3<br />
,<br />
thorogummite contains water, calciothorite contains ca. 7% CaO. In auerlite (named<br />
after the Austrian chemist Auer von Welsbach) the SiO 4<br />
is partially substituted with<br />
PO 4<br />
. In the case of macintoshite (named after the chemist J. B. Macintosh), it has<br />
been found that it is thorogummite with some uranium and cerium.<br />
Properties: The crystal structure of thorite is usually metamict, because of its<br />
radioactivity. The usual consequences are a change of colour towards black, a<br />
decrease in specific gravity, hardness and refractive indices. In fresh (nonmetamict)<br />
thorite the refractive index is 1.84, specific gravity 6.7. Such thorite is clearly<br />
birefringent and optically uniaxial-positive. The dark variety is much more common<br />
– these are optically isotropic, the refractive index decreases to ca. 1.635, density is<br />
4.1 and less, the hardness decreases from 4.5-5 down to ca. 2.5.<br />
53
SILICATES<br />
X-ray diffraction data: d 4.68 (100), 3.55 (100), 2.65 (60), ASTM-card 11-72<br />
(referenced after the Index to the X-ray powder data file, 1962, p. 364).<br />
THORITE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Markov and Mihailović-Vlajić (1969), Mihailović-Vlajić<br />
(1967), Mihailović-Vlajić and Markov (1967), Petrović (1957)<br />
J. Petrović (1957) found thorite in riverine deposits of Mt. Motajica, and<br />
inferred that thorite must be an accessory constituent of the granites in this area.<br />
More detailed information was provided by Mihailović-Vlajić and Markov (1967)<br />
and Mihailović-Vlajić (1967).<br />
The thorite from Mt. Motajica occurs as brightgreen grains, transparent and<br />
with a vitreous lustre. The surface and edges of the grains are sometimes overgrown<br />
with products of thorite hydration. These products have a darker, olivegreen colour,<br />
and have a lower transparency and lustre. In thin section, the edges of such grains<br />
appear darker and less transparent in transmitted light.<br />
The thorite has been formed during the latter magmatic events, in the<br />
intergranular spaces between quartz and feldspar grains – in the aplitic sections of<br />
the Mt. Motajica granite. This finegrained granite contains up to 4.18% (vol.) thorite,<br />
as analysed by N. Kreminac. The biotite and biotite-muscovite granites contain<br />
only traces of thorite, while it is completely absent in the overlying gneisses and<br />
amphibole-biotite granites and pegmatites.<br />
The grainsize of thorite varies in the range between 0.1-0.3 mm, seldom up to<br />
0.4 mm. In the aplitic granite thorite occurs in grains of up tom 1 mm in size. According<br />
to information provided by Mihailović-Vlajić and Markov (1967, p. 71), the thorite<br />
grains are xenomorphic, crystal faces can be observed only rarely. In a later report<br />
(Mihailović-Vlajić 1967, p. 198) the author mention that thorite occurs as crystallites<br />
or incompletely idiomorphic crystals, with a length-to-width ratio of 1 : 2.5. In the<br />
aplitic granite this ratio increases to 1 : 5. The faces {110} and {111} can be observed<br />
on some crystals. Prism faces are narrow or completely absent (Figure 3).<br />
54
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Figure 3. – Thorite from the Mt. Motajica granite (Mihailović-Vlajić 1967)<br />
In their investigations, the authors collected rock specimens of ca. 80-150<br />
kg. These were crushed and the material was used to obtain a heavy concentrate<br />
on a vibrational table. This concentrate was then fractionated using heavy liquids<br />
(bromoform, methylene iodide and Clerici's solution) or using a magnet. The obtained<br />
fractions were investigated by binocular loupe and a polarising microscope. This<br />
procedure was used to identify and retrieve thorite grains that were subsequently<br />
analysed with spectrochemical methods.<br />
According to Mihailović-Vlajić and Markov (1967, p. 76) the Mt. Motajica<br />
granite is a typical example of thorite enrichment and complementary uraninite<br />
depletion in the late magmatic phases (vein stages).<br />
There is a further brief reference to thorite in the Mt. Motajica granite by the<br />
same authors (Markov and Mihailović-Vlajić 1969, p. 257).<br />
ANDALUSITE<br />
Al 2<br />
[O|SiO 4<br />
]<br />
Crystal system and class: Orthorombic, rhombic-dipyramidal class.<br />
Lattice ratio: a : b : c = 0.982 : 1 : 0.703<br />
Unit cell parameters: a o<br />
= 7.78, b o<br />
= 7.92, c o<br />
= 5.57, Z = 4.<br />
Properties: cleavage pronounced along {110}. Hardness = 7.5, specific gravity = 3.13.<br />
Occurs in different colours – colourless, white, gray, brown, pinkish-red, green. Streak<br />
is white, lustre vitreous to resinuous. Refractive indices are high, birefringence is<br />
low.<br />
X-ray diffraction data: d 5.54 (100), 4.53 (90), 2.77 (90).<br />
IR-spectrum: 415 440 455 480 520 558 600 685 735 775 855 895 938<br />
1010 cm -1<br />
55
SILICATES<br />
ANDALUSITE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Katzer (1924 and 1926), Koch (1908), Majer and Pamić (1974),<br />
Ristić, Likić and Stanišić (1968), Šćavničar and Jović (1961 and 1962), Varićak<br />
(1966), Vasiljević (1969).<br />
According to available literature data, andalusite is not a very common rockforming<br />
mineral in Bosnia and Hercegovina. As a typical metamorphic mineral,<br />
andalusite has in a primary setting been identified only in the Mt. Motajica series,<br />
and in metamorphic shales of Mt. Borja within the Bosnian serpentine zone. As<br />
a resistant mineral, andalusite has been found in sands of the Tuzla basin and in<br />
quartzites from Podrašnica near Mrkonjić-Grad.<br />
1. Mt. Motajica<br />
Koch (1908) gave a description of two micaschists in which he was able<br />
to identify andalusite. He classified one of these rocks as a chiastolite containing<br />
micaschist, with outcrops around Vinogradac, close to Svinjar. The other rock was<br />
determined as an andalusite containing micaschist, with outcrops in the nearby<br />
Resavac creek.<br />
Andalusite is a major constituent of the Resavac micaschist. Here it<br />
occurs in the form of large grains or short prismatic crystals. Sections are usually<br />
squarelike, with rounded corners. There are two cleavage systems, at right angles<br />
to each other. It shows parallel extinction under crossed polarizers. Interference<br />
colours are vivid. Andalusite is normally colourless, but some grains are pinkishred<br />
or yellow in colour, showing strrong pleochroism. Pleochroitic colours are<br />
reddish and yellow, in thicker sections the colours are olive-green, yellow and<br />
brownish-red.<br />
Andalusite normally contains numerous inclusions. Koch determined<br />
the minerals quartz, ilmenite, biotite, muscovite and a carbonaceous material as<br />
inclusions.<br />
In his treatment of the Geology of Bosnia and Hercegovina, Katzer (1924<br />
and 1926) mentions andalusite data compiled by F. Koch.<br />
According to Varićak (1966), andalusite is an accessory constituent of some<br />
gneissphyllites and micaschists of Mt. Motajica. Thin sections of these rocks contain<br />
andalusite as colourless, sericitized grains with a well developed cleavage. Measured<br />
optic axial angles on a teodolite (rotating stage) microscope vary in the range 2V =<br />
-82° to -85°.<br />
56
2. Mt. Borja<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
In the northwestern part of the ultrabasic massif of Mt. Borja within the<br />
Bosnian serpentine zone, andalusite occurs in altered shales (Majer and Pamić<br />
1974). Andalusite grains are prismatic, their sections are square shaped. They are<br />
fresh, or into a mixture of sericite and biotite. The authors provide no further data on<br />
the andalusite from this locality.<br />
3. Andalusite in sedimentary rocks<br />
B. Šćavničar and P. Jović (1961 and 1962) have determined andalusite in the<br />
heavy mineral fraction of the Pliocene-age sands of the Kreka coal basin. It occurs<br />
almost exclusively in the gray sands underlying the coalbeds. The andalusite variety<br />
of chiastolite has also been identified. A characteristic pink pleochoritic colour is<br />
observable under the microscope. Prismatic crystals display parallel extinction and<br />
posess a negative elongation character. The authors believe that this andalusites<br />
originates from rocks impacted by contact metamorphism.<br />
In the sands of the Tuzla basin andalusite has also been determined in the<br />
heavy mineral fraction and amounts to 0.1-1.5 % (Ristić, Likić and Stanišić 1968).<br />
According to R. Vasiljević (1969) andalusite occurs in sedimentary quartzites<br />
at Podrašnica near Mrkonjić-Grad (data by S. Pavlović and D. Nikolić).<br />
Uses<br />
Andalusite is primarily used in the production of high quality fireproof<br />
materials, used mainly for automobile spark plugs. When heated, andalusite,<br />
sillimanite and disthen are transformed into mullite (3Al 2<br />
O 3<br />
.2SiO 2<br />
). This material<br />
has not only good fireproof properties but is also chemically unreactive in contact<br />
with acids, bases and HF. Minerals of the kynite (disthen) group are used in the<br />
fabrication of a SiAl alloy – silumine.<br />
KYANITE / DISTHENE<br />
Al 2<br />
[O|SiO 4<br />
]<br />
DISTHENE / KYANITE<br />
Crystal system and class: Triclinic, pinacoidal class.<br />
Lattice ratio: a : b : c = 0.9066 : 1 : 0.7102, α = 89° 58.5’, β = 101° 08.5’, γ = 105° 57’<br />
Unit cell parameters: a o<br />
= 7.10, b o<br />
= 7.74, c o<br />
= 5.57, Z = 4.<br />
Properties: cleavage perfect along {100}, very good along {010}. Parting along<br />
{010}. Hardness is variable (thus the name) = 4-7, specific gravity = 3.63. Usually<br />
57
SILICATES<br />
blue in colour, occasionally patchy colouration; green, white or gray colour are also<br />
common. Refreactive indices are high, birefringence is low.<br />
X-ray diffraction data: d 3.18 (100), 1.38 (75), 3.35 (65). ASTM-card 11-46.<br />
IR-spectrum: 442 470 512 550 572 598 610 628 630 645 720 905 952<br />
1010 1040 1640 cm -1<br />
A u t h o r s: Jakšić (1927), Kišpatić (1912 and 1915), Marić (1965), Ristić,<br />
Likić and Stanišić (1968), Sijerčić (1972), Šćavničar and Jović (1962), Tućan (1912),<br />
Vasiljević (1969).<br />
As a typical metamorphic mineral, up to now kyanite has not been found in<br />
primary rocks in Bosnia and Hercegovina. The cited authors have, however, noted<br />
its presence as an accessory constituent of clastic sediments, bauxite and terra rossa<br />
– where its presence is explained by its mechanical stability.<br />
First information on kyanite in bauxite and terra rossa was simultaneously<br />
provided by M. Kišpatić and F. Tućan. According to Kišpatić (1912 and 1915)<br />
kyanite can frequently be found in the bauxites from Studena Vrela (Duvno) and<br />
Široki Brijeg (Lištica) in Hercegovina. In the Široki Brijeg bauxite, kyanite occurs<br />
in the form of small, colourless platelets. The extinction angle in the (100) section is<br />
31-32°. Jakšić (1927) has identified kyanite at this same location.<br />
F. Tućan (1912) identified kyanite in the terra rossa near Eminovo Selo<br />
(Duvno). The data on kyanite, provided by Kišpatić and Tućan, can be found in the<br />
publication on terra rossa in dinaric karst systems by L. Marić (1965).<br />
Ristić, Likić and Stanišić (1968) have identified kyanite in the heavy mineral<br />
fraction of the sands from the Tuzla basin.<br />
T. Sijerčić (1972) determined kyanite in the heavy mineral fraction isolated<br />
from the Eocene-age flysch deposits in the western part of Mt. Majevica.<br />
According to B. Šćavničar and P. Jović (1962) kyanite occurs sporadically<br />
in the heavy mineral fraction of the Pliocene sands of the Kreka coal basin.<br />
R. Vasiljević (1969) notes the occurence of kyanite in sedimentary quartzites<br />
of Podrašnica (Mrkonjić-Grad), based on microscopic determinations by S. Pavlović<br />
and D. Nikolić.<br />
58
STAUROLITE<br />
2FeO . AlOOH . 4Al 2<br />
[O|SiO 4<br />
]<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Crystal system and class: Monoclinic (pseudo-orthorhombic), prismatic class.<br />
Lattice ratio: a : b : c = 0.471 : 1 : 0.340, β = 90°<br />
Unit cell parameters: a o<br />
= 7.83, b o<br />
= 16.62 c o<br />
= 5.65, Z = 4.<br />
Properties: cleavage very good along {010}, very good along {010}. Hardness = 7,<br />
specific gravity = 3.7-3.8. Colour is brown, streak gray. Vitreous lustre, sometimes<br />
resinuous.<br />
X-ray diffraction data: d 1.387 (100), 2.38 (50), 1.96 (50).<br />
IR-spectrum: 435 485 595 650 695 785 802 855 910 1030 1090 1170 3420<br />
cm -1 (staurolite, Scaer, Finisterre, France).<br />
A u t h o r s: Đurić (1963a), Ristić, Likić and Stanišić (1968), Šćavničar and<br />
Jović (1962).<br />
Staurolite is a comparatively rare and moderately investigated mineral<br />
in Bosnia and Hercegovina. It has been identified, together with magnetite, near<br />
Čajniče and in clastic sediments of the Tuzla basin.<br />
According to S. Đurić (1963a), the occurence of staurolite at Stravnje njive<br />
near the village of Okosovići (ca. 6 km north of Čajniče in southeastern Bosnia) is<br />
associated with the magnetite deposit. This can be seen from the microphotographs<br />
in this publication.<br />
In thin section, staurolite frequently shows the characteristic twinning in the<br />
form of a cross. It has a high relief. Measurements on a rotating-stage microscope<br />
gave an optic axial angle 2V = +88°. The vibration direction Z of the optical<br />
indicatrix is codirectional with the crystallographic axis [001]. Pleochroism: yellow<br />
for vibration direction X, almost red for direction Z. The edges of the “cross”-twins<br />
are mutually perpendicular.<br />
Magnetite, occuring near the village of Okosovići, has formed on the contact<br />
of sercite phyllites and amphibole granites. Since the genesis of magnetite is probably<br />
associated with the pneumatolytic processes following the granitization phase, we<br />
believe that this could also explain staurolite formation.<br />
Staurolite is commonly found in the Pliocene sands of the Kreka coal basin<br />
(Šćavničar and Jović 1962). Grains are irregularly shaped, of yellow or brown colour.<br />
They have a high relief, and a visible pleochroism in the range from colourless<br />
to yellow. The authors believe that the staurolite is associated with the highly<br />
metamorphic crystalline rock series. Staurolite was also determined in Miocene-age<br />
clastic sediments.<br />
59
SILICATES<br />
Ristić, Likić and Stanišić (1968) determined staurolite in the sands of the<br />
Tuzla basin. The heavy mineral fractions contains 0.5-1.8 % staurolite.<br />
Use<br />
According to H. Kirsch (1968) staurolite can be used as an abrasive material,<br />
because of its hardness. Twins in the shape of a cross make popular jewelry items in<br />
some countries.<br />
BRAUNITE<br />
Mn 2+ Mn 6<br />
4+<br />
[O8|SiO 4<br />
]<br />
Crystal system and class: Tetragonal, ditetragonal-dipyramidal class.<br />
Lattice ratio: a : c = 1 : 1.9904<br />
Unit cell parameters: a o<br />
= 9.38, c o<br />
= 18.67, Z = 3, Mn : Si = 7 : 1<br />
Properties: cleavage perfect along {112}. Hardness = 6-6.5, specific gravity = 4.72 -4.83.<br />
Colour and streak are darkbrown to black. Semimetallic lustre.<br />
X-ray diffraction data: d 2.69 (10), 1.65 (9), 1.415 (8)<br />
d 2.75 (10), 1.66 (10), 1.415 (8)<br />
IR-spectrum: 455 480 530 555 625 712 815 850 953 1015 1040 1112 cm -1<br />
BRAUNITE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Hauer (1884), Jeremić (1959), Jurković (1956), Katzer (1906),<br />
Kubat (1969), Pavlović (1890), Pavlović (1953), Poech (1888), Vujanović (1962),<br />
Walter (1887).<br />
Within the occurences of manganese minerals in Bosnia and<br />
Hercegovina, braunite is probably one of the most common minerals – together<br />
with psilomelane and other manganese ore minerals. However, more detailed<br />
information on the occurence of barunite in different parageneses is available<br />
only for the Čevljanovići area.<br />
1. Braunite in the area of Čevljanovići<br />
The earliest and somewhat scanty data on braunite occurence at<br />
Čevljanovići can be found in the publications by F. Hauer (1884), B. Walter<br />
(1887) and F. Poech (1888).<br />
In his general account on manganese ores in Bosnia, Walter (1887) maintains<br />
that braunite is of less importance in terms of quantity. However, braunite and<br />
60
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
pyrolusite are the principal components of the manganese ore at Vranjkovci. Large<br />
chunks of braunite, weighing between 1-350 kg have been found in the surrounding<br />
diluvial deposits. In a description of the Vranjkovci manganese deposit, Hauer writes<br />
that braunite was mistakenly regarded as hausmannite, but that braunite crystal were<br />
found in some geodelike formations. This was already noted by Foullon (see section<br />
on hausmannite).<br />
Katzer (1906) found no evidence for the presence of braunite, manganite or<br />
hausmannite in the Čevljanovići deposit.<br />
More recent research by S. Pavlović (1963) has identified braunite as a<br />
principal constituent of the manganese mineral parageneses found at Čevljanovići.<br />
A detailed mineralogical investigation of the Čevljanovići ore deposit<br />
(Vujanović 1963) provides a better account on the importance of manganese<br />
minerals in this area. According to this investigation, braunite is the principal mineral<br />
of primary parageneses. It is also present in the so-called thermal (regenerated)<br />
parageneses at Čevljanovići, Draževići and Mt. Ozren.<br />
Minerals belonging to the primary manganese paragenesis are the most<br />
important part of the ore which was mined here in earlier days. This ore is found in the<br />
form of veins of various thickness within the mid-Triassic volcanogenic-sedimentary<br />
series of rocks. Here, braunite is the main manganese mineral, followed in importance<br />
by cryptomelane, romanechite, hausmannite and manganite. Manganite is normally<br />
associated with these Mn minerals (Figure 4).<br />
The minerals of the primary paragenesis have sustained alteration during<br />
subsequent hydrothermal events. Some of them have recrystallized within the<br />
primary deposit – forming “thermal” braunite and other minerals of this regenerated<br />
paragenesis (romanechite, hausmannite, manganite, Mn-calcite, rodochrosite,<br />
calcite, quartz etc.).<br />
Vujanović determined the main properties of this braunite by optical<br />
microscopy and differential thermal analysis. The DTA curve shows a clear<br />
endothermic peak at 1125°C.<br />
Braunite occurs here in the form of a finegrained mass, with a grain-size<br />
range between 1 and 30 μm, apparently forming from an initial gel.<br />
The braunite posesses a weak bireflection, and a weak to clear anisotropy.<br />
Internal reflections are common, as determined by ore microscopy.<br />
61
SILICATES<br />
62<br />
Figure 4. The mineral paragenesis at Čevljanovići (Vujanović 1962)<br />
Braunite is commonly associated with cherts, and more seldom with schists.<br />
When associated with cherts, braunite occurs as irregular intergrowths or dispersed.<br />
Intergrowths withg hematite are common.<br />
According to Vujanović, braunite occurs at the following localities in the<br />
Čevljanovići area: Gornji and Donji Gojanovići, Gornji and Donji Vrgalj, Velike<br />
Šume and Grk.<br />
The genesis of braunite in primary parageneses is the same as that of<br />
psilomelane (see section on psilomelane).<br />
2. Occurence of braunite in northewestern Bosnia<br />
M. Jeremić (1959) provided very general data on braunite occurences in<br />
northwestern Bosnia. Occurences of manganese ore minerals lie along the transect<br />
Bosanska Krupa – Bužim – Velika Kladuša, and braunite appears to be the main<br />
constituent of these ores. Pyrolusite frequently occurs together with braunite.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
According to Jeremić, the main occurence of braunite is in Bužim Polje.<br />
Other localities, also for pyrolusite, are Mačkovac, Kajtezovac, Varoška Rijeka,<br />
Cenić Glavica, Lubarda and Porić Selo.<br />
3. Occurences of braunite in eastern Bosnia<br />
In eastern Bosnia, braunite is a constituent of manganese and iron<br />
parageneses, which are genetically and spatially associated only with the Mesozoicage<br />
formations in the Mioče – Strmica area, on the right banks of the Lim river.<br />
Braunite and other manganese minerals are to be found only in the Mioče area, at the<br />
localities Gornji i Donji Jelići and Jagline.<br />
4. The schist mountains of central Bosnia<br />
In the area of the schist mountains of central Bosnia, braunite occurs only in<br />
the region of Busovača, at Šuplje Bukve locality (Jurković, 1956).<br />
Use<br />
Braunite is one of the most important manganese ore minerals.<br />
TITANITE<br />
CaTi[O|SiO 4<br />
]<br />
SPHENE<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.753 : 1 : 0.854, β = 119° 43’,<br />
Unit cell parameters: a o<br />
= 6.55, b o<br />
= 8.70, c o<br />
= 7.43, Z = 4.<br />
Properties: distinct cleavage along {110}. Hardness = 6, specific gravity = 3.5.<br />
Usually brown, yellow, green or grey colour. Streak is white, lustre adamantine.<br />
X-ray diffraction data: d 3.23 (100), 2.99 (90), 2.60 (90). ASTM-card 11-142.<br />
IR-spectrum: 415 440 500 570 865 960 cm -1 (titanite, Ontario, Canada).<br />
TITANITE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Arsenijević (1967), Barić (1966a and 1970a), Cissarz (1956),<br />
Čelebić (1967), Čutura (1918), Džepina (1970), Đorđević and Mojičević (1972),<br />
Đorđević and Stojanović (1964), Đurić and Kubat (1962), Foullon (1893), John<br />
(1888), Jovanović (1972), Jurković and Majer (1954), Karamata and Pamić (1964),<br />
Katzer (1924 and 1926), Kišpatić (1897, 1900, 1904b and 1910), Koch (1908),<br />
Magdalenić and Šćavničar (1973), Majer (1963), Majer and Jurković (1957 and<br />
63
SILICATES<br />
1958), Marić (1927), Marić and Crnković (1961), Olujić, Vuletić and Pamić<br />
(1971), Pamić (1960a, 1961, 1961b, 1969a, 1971, 1971a and 1972c), Pamić and<br />
Maksimović (1968), Pamić and Papeš (1969), Pamić, Šćavničar and Međimorec<br />
(1973), Paul (1879), Pavlović and Ristić (1971), Podubsky (1968 and 1970),<br />
Ramović (1966 and 1968), Ristić, Likić and Stanišić (1968), Tajder (1953), Tućan<br />
(1912, 1922, 1930 and 1957).<br />
Titanit is a very common accessory mineral in igneous, sedimentary and<br />
metamorphic rocks. It occurs in various rocks within the Bosnian serpentine zone,<br />
also in product of Triassic and Tertiary magmatism. It can be found in rocks of<br />
Mt. Motajica and in other formations of Paleozoic age. Because of its mechanical<br />
resilience, titanite is often found in alluvial deposits and sands, as well as in other<br />
clastic sediments.<br />
1. The Bosnian serpentine zone<br />
First data on titanite, obtained by microscopical investigation, were provided<br />
by M. Kišpatić (1897 and 1900). According to this author, titanite occurs mostly in<br />
metamorphic rocks and less frequently in diabases and crystalline limestones. It is a<br />
constituent of amphibolites, pyroxene amphibolites, eclogite amphibolites, actinolite<br />
schists – all along the Bosnian serpentine zone, from Mt. Kozara to Višegrad.<br />
Titanite is a significant constituent of the pyroxene amphibolites of Ozren<br />
Manastir, near Bosansko Petrovo Selo. It comes as small or larger irregular grains,<br />
seldom pointed in shape. In thin section, this titanite is yellowish in colour with a<br />
rough surface. In other amphibolites titanite appears similar. Inclusions of rutile can<br />
sometimes be seen. In the pyroxene amphibolites of Reljevac on Mt. Ljubić, the<br />
titanite is included in amphibole grains. Its surface is again rough, with dark rims.<br />
In the porphyric diabase of Benkovačko Jezero on Mt. Kozara, ilmenite is<br />
transformed into titanite (Kišpatić 1897 and 1900). This author asserts that titanite<br />
is an accessory constituent of crystaline limestones from around Zvornik. Grains<br />
are fairly small and have a rough surface, the shape is usually pointed at both ends.<br />
Grains appera to be lined up in certain directions. In these limestones, titanite occurs<br />
together with salite (malacolite).<br />
More recent investigations also describe titanite as an accessory mineral in<br />
rock from these areas (Džepina 1970; Đorđević and Mojičević 1972; Đorđević and<br />
Stojanović 1964; Đurić and Kubat 1962; Karamata and Pamić 1964; Majer 1963;<br />
Olujić, Vuletić and Pamić 1971; Pamić 1969a, 1971, 1971a and 1972c; Pamić,<br />
Šćavničar and Međimorec 1973).<br />
64
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
2. Titanite in products of Triassic and Tertiary magmatism<br />
Occurences of titanite in products of Triassic magmatism in the area<br />
of Jablanica, Konjic and Prozor have been investigated by the folowing authors:<br />
Cissarz 1956; Čelebić 1967; John 1888; Marić 1927; Pamić 1961 and 1961b; Pamić<br />
and Maksimović 1968; Ramović 1966 and 1968; Tućan 1922, 1930 and 1957. Most<br />
of these authors refer to the titanite in the gabbro rocks of Jablanica.<br />
The titanite in the Jablanica gabbros was studied in some detail by F. Tućan<br />
and L. Marić.<br />
According to L. Marić, titanite can be observed in all thin sections of the<br />
Jablanica gabbro where it occurs as grains or irregular formations. Together with<br />
ilmenite, titanite crystallizes in the intergranular spaces of feldspar crystals. In the<br />
southern part of the Jablanica massif, titanite is common in anorthosite sequences.<br />
Beautiful titanite crystals can be found in veins of the Jablanica gabbro.<br />
These have a platlike shape along (102), yellowish-brown in colour and have an<br />
adamantine lustre (Tućan 1922, 1930 and 1957). The following crystal forms have<br />
been determined on these crystals (following the Des Cloizeaux notation): c (001),<br />
d (113), n (111), m (110), x (102), g (-7.7.20), l (-112), t (-111). Specific gravity =<br />
3.4988 at 24°C.<br />
The chemical composition of the titanite is as follows: SiO 2<br />
= 28.61; TiO 2<br />
=<br />
34.31; Al 2<br />
O 3<br />
= 6.35; Fe 2<br />
O 3<br />
= 2.34; CaO = 27.58.<br />
1922).<br />
Titanite crystals from the Jablanica gabbro are shown in Figure 5 (Tućan<br />
Figure 5. Titanite in gabbro from Jablanica (Tućan 1922)<br />
65
SILICATES<br />
Tućan explained the formation of titanite as a product of lateral secretion.<br />
However, we believe that the formation of titanite and other minerals (prehnite,<br />
zeolites) is associated with hydrothermal and postmagmatic processes which have<br />
imapcted the rocks at Jablanica. A similar theory has also been advanced by L. Marić<br />
(1927, p. 11).<br />
Pamić (1961 and 1961b) determined titanite in granites from Mt. Prenj and<br />
in quartz keratophyres from Krstac. In this latter rock, titanite has a very high relief,<br />
yellow in colour and very weak pleochroism. It is optically positive and displays<br />
vivid interference colours.<br />
Titanite in products of Triassic magmatism from around Kupres was studied<br />
by J. Pamić and J. Papeš (1969). Pamić (1960a) made a microscopic determination<br />
of titanite in similar rocks from the Kalinovik area. Accessory titanite in Triassic<br />
intrusives from the schist mountains of central Bosnia (area around Jajce, Kopilo and<br />
Bijela Gromila) was investigated by M. Čutura (1918), M. Kišpatić (1910), V. Majer<br />
and I. Jurković (1957 and 1958).<br />
Little is known about accessory titanite in products of Tertiary magmatism,<br />
but some data was provide by Barić (1966a) and Tajder (1953). Barić investigated<br />
titanite in tuffs from Livno, while Tajder studied this mineral in the Srebrenica dacites.<br />
66<br />
3. Mt. Motajica and other areas with Paleozoic-age formations<br />
Titanite is an accessory mineral in various rock formations of Mt. Motajica<br />
(Koch 1908; Katzer 1924 and 1926; Varićak 1966).<br />
Koch determined titanite mainly in metamorphic rocks (biotite gneisses,<br />
micaschists, amphibolites) where it occurs after being tranformed from ilmenite. In<br />
the andalusite micaschists from Resavac creek near Svinjar, the titanite is of yellow<br />
colour, with strong pleochroism and birefringence. In thin section, both irregular and<br />
wedge shaped grains can be observed.<br />
D. Varićak described titanite as a frequent accessory mineral in granite,<br />
granite porphyres, rhyolite, gneiss, amphibolite and other rocks. This author has<br />
not done further research concerning titanite, because of its minor importance as an<br />
accessory constituent.<br />
M. Arsenijević (1967, p. 88 and 91) determined the content of tin (1340 g/<br />
ton) and niobium (1900 g/ton) in titanite contained in the Mt. Motajica granite.<br />
According to Kišpatić (1904b) titanite forms finegrained aggregates in the<br />
porphyric diabase from Sinjakovo (Mrkonjić-Grad).
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Jurković and Majer (1964) established that titanite occurs together with<br />
some other contact metamorphic minerals minerals at the contact of albite rhyolite<br />
and Paleozoic-age limestones at Alinovci, near Jezero (Jajce).<br />
Titanite occurs rather infrequently in the keratophyres in the Trešanica gorge<br />
near Bradina in Hercegovina (Barić 1970a). This titanite has a high relief, and is<br />
often associated with leucoxene.<br />
Accessory titanite occurs in Paleozoic sediments and altered sediments of<br />
northwestern and eastern Bosnia (Marić and Crnković 1961; Podubsky 1968 and<br />
1970). According to Podubsky, titanite occurs much more frequently in rocks of<br />
northwestern Bosnia than in those of its eastern part.<br />
4. Titanite in other rocks<br />
According to F. Tućan (1912) titanite is a constituent of terra rossa from<br />
Eminovo Selo near Duvno, together with quartz, muscovite, epidote, zoisite, kyanite,<br />
tourmaline, rutile and calcite.<br />
It is comparatively scarce in the heavy mineral fraction of Miocene-age sand<br />
and calcarenites from Lupina near Kulen-Vakuf (Magdalenić and Šćavničar 1973).<br />
Č. Jovanović (1972) described titanite in Pliocene-age sands of the Prijedor<br />
basin, where it was determined by Z. Sijerčić in the heavy mineral fraction.<br />
Titanite occurs in three different horizons in the Pliocene-age sands of the Kreka<br />
coal basin, however in small quantities (Šćavničar and Jović 1962). It is characterised<br />
by a high relief, strong birefringence and vivid (blue and yellow) interference colours.<br />
It has incomplete extinction, is optically positive, and has a strong dispersion of optic<br />
axes. It probably originates from granites or metamorphic rocks. These authors have<br />
also identified titanite in Eocene sandstones and Miocene clastic sediments.<br />
Pavlović and Ristić (1971) have found titanite in the heavy mineral fraction<br />
of the coarse quartz sand in the Bijela Stijena deposit near Zvornik.<br />
The content of titanite in the heavy mineral fraction of sands from the Tuzla<br />
basin is ca. 0.2-1 % (Ristić, Likić and Stanišić 1968).<br />
C. M. Paul (1879) determined titanite in diabases from Mt. Majevica.<br />
Use<br />
When titanite is available in substantial quantities, it can be used for the<br />
extraction of titanium metal.<br />
67
SILICATES<br />
CHLORITOID<br />
Fe 2<br />
2+<br />
AlAl 3<br />
[(OH) 4<br />
|O 2<br />
|(SiO 4<br />
) 2<br />
]<br />
OTTRELITE<br />
Mn 2<br />
AlAl 3<br />
[(OH) 4<br />
|O 2<br />
|(SiO 4<br />
) 2<br />
]<br />
Crystal system and class: Monoclinic, occasional triclinic symmetry within the<br />
same crystal (chloritoid).<br />
Properties: distinct cleavage along {011}, weaker along {110}. Colour is greenishblack<br />
to black. Lustre is vitreous. Hardness more than 6, specific gravity = 3.4-3.6.<br />
X-ray diffraction data for chloritoid:<br />
Triclinic d 4.449 (100), 2.456 (90), 1.5804 (80)<br />
Monoclinic d 4.449 (100), 2.963 (90), 1.5813 (80)<br />
IR-spectrum: 450 518 552 590 612 672 750 805 870 908 962 1105 1650<br />
2980 3340 3450 cm -1 (chloritoid, Galgenberg near Leoben, Austria).<br />
68<br />
CHLORITOID IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Foullon (1893), Katzer (1924 and 1926), Kišpatić (1904b),<br />
Šćavničar and Jović (1962), Tajder and Raffaelli (1967), Tućan (1957).<br />
Since some of the referenced publications do not distinguish chloritoid from<br />
ottrelite, we have placed both mineral names and their formulas in the title of this<br />
section. Chloritoid occurs in Bosnia and Hercegovina in the schist mountains of<br />
central Bosnia and in the clastic sediments of the Kreka coal basin.<br />
1. Schist mountains of central Bosnia<br />
Earliest information on the occurence of chloritoid in the so-called “ottrelite<br />
schists” from Čemernica can be found in the publication by H.B.v. Foullon (1893,<br />
p. 3), although the author did no further investigations of this mineral. On the<br />
other hand, M. Kišpatić gives in his “Petrographic notes from Bosnia” (1904b) a<br />
rather detailed macroscopic and microscopic description of chloritoid, a significant<br />
and frequent constituent of the “chloritoid phyllites located between Fojnica and<br />
Čemernica” (pages 44-47). According to Kišpatić, this chloritoid has a platelike<br />
habit, black in colour with an almost metallic lustre – macroscopically very similar<br />
to biotite. In crushed samples of rock, chloritoid platelets can be seen – these have<br />
a hexagonal shape and the basal pinacoid (001), the prism (110) and pinacoid (010)<br />
can be recognized. The platelets are 0.3-0.5 mm in diameter.<br />
In the referenced publication, Kišpatić also gives a desciption of the<br />
microphysiographic characteristics of chloritoid: it has characteristic pleochroism
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
in blue-green (X), blue (Y) and yellow-green (Z) colour. Sections parallel to the c<br />
axis have angular extinction of 20°. The measured maximum birefringence Nz –<br />
Nx = 0.011.<br />
Katzer, in his ‘Geology of Bosnia and Hercegovina’ (1924 and 1926) gives<br />
an account of the schist mountains of central Bosnia and the distribution of “ottrelite<br />
schists” (pages 109-113). Katzer’s description of chloritoid is quite similar to the<br />
earlier description given by Kišpatić. Nevertheless, Katzer writes that chloritoid<br />
platelets sometimes are as large as 9.8 mm in diameter. Katzer was somewhat poetic<br />
in comparing these chloritoid platelets with stars shining on a dark night’s sky<br />
(Katzer 1926, p. 112).<br />
Katzer also mentions the chloritoid-containing schists at Čemernica,<br />
between the antimonite mine and the Povitine creek; near Ščitovo, Putljevac creek<br />
and Bukovica forest. Similar schists occur also in the Busovača area, and elsewhere.<br />
More data on chloritoid in the schist mountains of central Bosnia can<br />
be found in the more recent publication by M. Tajder and P. Raffaelli (1967).<br />
According to these authors, chloritoid occurs in quartz-muscovite schists in the<br />
form of porphyroblasts some 2 mm in diameter. Crystals have a shortprismatic<br />
shape with a basal pinacoid. In thin section, a bluegreen pleochroism can be<br />
observed, as well as twinning parallel to the base, good cleavage, high indices of<br />
refraction and a strong r > v dispersion in convergent light. The authors did not<br />
identify the location from which the chloritoid was obtained, but refer to Katzer’s<br />
data on the distribution of these schists.<br />
2. Occurences in the Kreka coal basin<br />
B. Šćavničar and P. Jović (1962) have determined small quantities of<br />
chloritoid in the heavy mineral fraction of Pliocene-age sand from the Kreka<br />
coal basin. Chloritoid has also been found in Eocene sandstones of this area. The<br />
maximum content of chloritoid in the heavy mineral fraction was 5.3%.<br />
DATOLITE<br />
CaB[OH|SiO 4<br />
]<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 1.264 : 1 : 0.632, β = 90° 9’,<br />
Unit cell parameters: a o<br />
= 9.66, b o<br />
= 7.64, c o<br />
= 4.83, Z = 4.<br />
Properties: datolite has no distinct cleavage. Hardness = 6.5, specific gravity = 3.0.<br />
Colourless and transparent, pale-green or yellowish, occasionaly white and milky.<br />
69
SILICATES<br />
Streak is white, lustre vitreous.<br />
X-ray diffraction data: see table in text.<br />
IR-spectrum: 455 478 505 533 550 578 692 788 853 885 930 955 965<br />
1015 1050 1102 1260 3490 cm -1<br />
A u t h o r s: Đorđević and Stojanović (1972 and 1974), Trubelja, Šibenik-<br />
Studen and Sijarić (1975, 1975a and 1976).<br />
Datolite occurs in Bosnia and Hercegovina in basic rocks of the Bosnian<br />
serpentine zone mostly as a gangue mineral. It was first mentioned by Đorđević and<br />
Stojanović (1972) but the authors gave no information on the locality. Two years<br />
later the same authors provide a more detailed account on datolite which occurs in<br />
diabase rocks at Bojići near Hrvaćani and Banja Luka. The mineral association also<br />
contains some zeolite minerals and calcite. Datolite crystalizes within thin veinlets<br />
in the rock (Đorđević and Stojanović 1974).<br />
This comparatively rare mineral was determined by the authors using optical<br />
microscopy, XRD and thermal analysis.<br />
In thin section, datolite appears in the form of densely packed grains of<br />
ca. 1 mm in size, showing a high relief and vivid interference colours. Frequent<br />
intergrowths with natrolite and calcite can be observed.<br />
X-ray diffraction data for datolite from Bojići are given in Table 10. They<br />
correspond well with the ASTM-card 11-70 data.<br />
Figure 6. DTA curve of datolite and natrolite. Sample from Bojići, near Banja Luka<br />
(Đorđević and Stojanović 1974)<br />
70
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The DTA curve of a mixture of datolite and natrolite (Figure 6) shows a strong<br />
endothermic peak at 710°C, and two weaker peaks at 860°C and 920°C. Datolite<br />
was also determined during the investigation of mineral associations in veins of<br />
the diabase-spilitic rocks of Mt. Ozren (Šibenik-Studen, Sijarić and Trubelja 1976;<br />
Trubelja, Šibenik-Studen and Sijarić 1975, 1975a and 1976). It occurs together with<br />
prehnite and rhipidolite in outcrops along the road leading from Gornji Rakovac to<br />
Gornja Bukovica. Datolite and the associated minerals were identified by XRD.<br />
Table 10. X-ray diffraction data for datolite, Bojići near Banja Luka<br />
Datolite, Bojići Datolite, ASTM-card 11-70<br />
d (Å) I d (Å) I<br />
6.02 10 5.98 7<br />
4.85 20 4.83 16<br />
3.76 40 3.763 45<br />
3.41 45 3.404 30<br />
3.11 100 3.114 100<br />
2.98 40 2.986 35<br />
2.86 40 2.855 65<br />
2.52 50 2.524 30<br />
2.41 15 2.409 9<br />
The genesis of datolite crystallizing in veinlets within basic rocks of the<br />
Bosnian serpentine zone is probably related to hydrothermal processes involving<br />
solutions enriched in boron.<br />
HEMIMORPHITE<br />
Zn 4<br />
[Si 2<br />
O 7<br />
|(OH) 2<br />
] . H 2<br />
O<br />
A u t h o r s: Jurković (1961a), Katzer (1924 and 1926), Koechlin (1922),<br />
Kunštek (1940), Tajder (1936), Tućan (1930, 1957)<br />
In 1853 Kenngott gave hemimorphite its names, because of its distinctly<br />
hemimorphic shape, characteristic for crystals of this minerals (greek – hemi, half<br />
and morphe, form). It has orthorhombic symmetry, rhombic-pyramid class.<br />
Hemimorphite is a very rarely occuring mineral in Bosnia and Hercegovina.<br />
To this date it has been identified only in the iron ore mine of Ljubija near Prijedor.<br />
First crystallographic data were provided by R. Koechlin (1922). Other authors only<br />
give reference to Koechlin’s data. In 1917 Koechlin obtained two small samples<br />
from the Ljubija mine and determined that the grey-white aggregates on limonite<br />
were a mixture of hemimorphite and smithsonite.<br />
71
SILICATES<br />
The hemimorphite crystals are up to 2 mm long, and have a platelike shape<br />
along {010}. Koechlin’s measurements of two crystals identified the presence of the<br />
following crystal forms: a {010}, m {110}, θ {102}, s {101} and t {301}. The shape<br />
of the crystal is shown in a drawing (Figure 7).<br />
Figure 7. Crystal of hemimorphite from the Ljubija iron mine (Koechlin 1922)<br />
The presence of the two Zn-bearing mineral, hemimorphite and smithsonite,<br />
can be explained by the weathering of sphalerite contained in the siderite ore from<br />
Ljubija (Koechlin 1922). This sphalerite was again later mentioned by Tućan (1930),<br />
while Tajder (1936) provides a crystallographic and chemical analysis.<br />
Jurković (1961a, p. 162), in his exhaustive account of the iron minerals of<br />
Ljubija, lists hemimorphite as a mineral formed during hypergenic processes.<br />
Use<br />
Hemimorphite can be used for zinc production, when it occurs in larger<br />
quantities.<br />
SUOLUNITE<br />
Ca 2<br />
H 2<br />
[Si 2<br />
O 7<br />
] . H 2<br />
O<br />
A u t h o r s: Đorđević and Stojanović (1972), Stojanović (1973), Stojanović,<br />
Đorđević and Đerković (1974).<br />
Suolunite is a very rare mineral (hydrated calcium silicate) in Bosnia and<br />
Hercegovina. It was first determined in the Banja Kulaša region in the Bosnian<br />
serpentine zone and mentioned by Đorđević and Stojanović (1972), but without<br />
72
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
precise data on the location of the occurence. Stojanović (1973) published detailed<br />
X-ray diffraction data on suolunite occuring in the diabase rock from Kulaš. A<br />
chemical and thermal analysis of this suolunite were also done. One further report<br />
by Stojanović, Đorđević and Đerković (1974) also mentions suolunite from the same<br />
locality, occuring together with tobermorite.<br />
Table 11. X-ray diffraction data for suolunite from Kulaš.<br />
d (Å) measured I d (Å) calculated hkl<br />
5.12 20 5.107 111<br />
4.96 8 4.961 040<br />
4.856 220<br />
4.13 100 4.129 131<br />
3.70 5 3.704 240<br />
3.174 80 3.173 151<br />
3.120 4 3.118 311<br />
2.873 022<br />
2.851 65 2.849 331<br />
2.843 260<br />
2.784 5 2.784 400<br />
2.681 50 2.680 420<br />
2.642 30 2.642 202<br />
2.552 38 2.553 222<br />
2.498 40 2.498 171<br />
2.479 10 2.480 080<br />
2.473 12 2.471 351<br />
2.428 10 2.428 440<br />
2.331 15 2.332 242<br />
2.270 2 2.266 280<br />
2.224 40 2.223 062<br />
2.130 460<br />
2.108 20 2.109 371<br />
2.076 15 2.076 511<br />
2.063 20 2.064 262<br />
2.034 10 2.035 191<br />
1.998 10 1.999 422<br />
1.991 30 1.991 531<br />
1.958 4 1.960 113<br />
1.889 10 1.8881 133<br />
1.887 25 1.8880 442<br />
1.866 2 1.8693 2 10 0<br />
1.850 30 1.8521 480<br />
1.8481 551<br />
1.824 4 1.8245 620<br />
1.808 8 1.8087 282<br />
73
SILICATES<br />
1.806 10 1.8078 391<br />
1.763 12 1.7647 153<br />
1.758 10 1.7550 313<br />
1.737 3 1.7385 640<br />
1.7373 462<br />
1.706 12 1.7074 1 11 1<br />
1.701 10 1.7025 333<br />
1.679 10 1.6814 571<br />
1.6556 0 10 2<br />
1.651 8 1.6538 0 12 0<br />
1.619 3 1.6187 660<br />
1.6178 173<br />
1.615 15 1.6160 4 10 0<br />
1.610 16 1.6103 353<br />
1.5869 2 10 2<br />
1.584 18 1.5853 2 12 0<br />
1.5788 602<br />
1.577 10 1.5764 482<br />
1.564 3 1.5665 3 11 1<br />
1.558 5 1.5592 622<br />
1.533 8 1.5333 711<br />
1.515 3 1.5163 591<br />
1.504 15 1.5045 642<br />
1.498 18 1.5012 004<br />
Suolunite from Kulaš near Doboj occurs in cracks in the diabase rocks, at a<br />
depth of 45 meters, in veinlets and aggregates. Crystals are transparent, colourless or<br />
yellowish. The thickness of the veins is 2-8 mm.<br />
In thin section the suolunite is colourless, and crystals have an elongated<br />
shape. Optical constants for soulunite are as follows: Nz = 1.6227; Ny = 1.6199;<br />
Nx = 1.6120; -2V = > 30°.<br />
Unit cell dimensions (after H.F.W. Taylor) are: a o<br />
= 11.13, b o<br />
= 19.82, c o<br />
= 6.00 Å,<br />
space group Fdd2.<br />
R. Veličković determined the chemical composition of suolunite: SiO 2<br />
= 43.35%<br />
CaO = 42.22% H 2<br />
O = 14.05%<br />
Specific gravity = 2.631<br />
Spectral analysis revealed the presence of the following elements: Mg, Al, K, N, S,<br />
Ti, Cr, Mn, Fe, Li, B, F, Na, P, Cl, V, Ni, Co, Zn, Sr, Ba and others.<br />
The DTA curve of suolunite shows a strong endothermic peak at 390°C,<br />
implying water loss and a transformation into xonotlite. The exothermic reaction<br />
peak at 810°C corresponds to a transformation into β-wollastonite (Stojanović,<br />
Đorđević and Đerković 1974).<br />
74
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Concerning the genesis of suolunite and tobermorite, the referenced<br />
authors believe that the two minerals were formed by hydrothermal processes. The<br />
temperature was comparatively low (ca. 175°C) and tobermorite was the first to<br />
crystallize, followed by suolunite.<br />
CLINOZOISITE – EPIDOTE<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Clinozoisite and epidote are similar minerals, differing in the amount of iron<br />
present in them. Their axial ratios and unit cell dimensions are very similar. Epidote<br />
contains a greater amount of trivalent iron substituting aluminum (isomorphic<br />
substitution). While clinozoisite contains up to 10 mol.% of Fe, epidote (pistazite)<br />
contains 10-30%. Consequently, the refractive indices and birefringence of epidote<br />
is greater than those of clinozoisite.<br />
Properties: perfect cleavage along {001}. Hardness = 7. Specific gravity = 3.3-3.6<br />
(increases with Fe content). Colour is greenish to greenish-grey (clinozoisite);<br />
yellow, brown-green to black (epidote). Streak is white (greyish-white), lustre is<br />
vitreous. Optical constants are as follows:<br />
epidote Nx = 1.720-1.734, Ny = 1.724-1.763, Nz = 1.734-1.779<br />
Nz – Nx = 0.014-0.045<br />
clinozoisite Nx = 1.710-1.723, Ny = 1.715-1.729, Nz = 1.719-1.734<br />
Nz – Nx = 0.005-0.011<br />
X-ray diffraction data for epidote: d 2.872 (100), 1.635 (85), 2.393 (85)<br />
X-ray diffraction data for clinozoisite: d 2.884 (100), 1.631 (65), 2.385 (65)<br />
IR-spectrum: 455 520 570 650 720 838 860 885 950 1040 1080 1115 3360 cm -1<br />
CLINOZOISITE<br />
Ca 2<br />
Al 3<br />
[O|OH|SiO 4<br />
|Si 2<br />
O 7<br />
]<br />
A u t h o r s: Džepina (1970), Đorđević and Mojičević (1972), Katzer (1924<br />
and 1926), Kišpatić (1910), Pamić (1957, 1960, 1960a, 1961a, 1961b, 1962, 1969a,<br />
1971, 1971a, 1972a and1972d), Pamić and Buzaljko (1966), Pamić and Maksimović<br />
(1968), Pamić and Papeš (1969), Pamić, Šćavničar and Međimorec (1973), Pamić<br />
and Tojerkauf (1970), Podubsky (1968 and 1970), Sijerčić (1972a), Simić (1966),<br />
Šibenik-Studen (1972/73), Tajder and Raffaelli (1967), Trubelja (1957 and 1960),<br />
Trubelja and Pamić (1957 and 1965), Varićak (1966).<br />
Minor quantities of clinozoisite in Bosnia and Hercegovina occur in igneous<br />
and metamorphic rocks. Inspite of its wide distribution, there is a very limited<br />
75
SILICATES<br />
amount of detailed data on this mineral. Clinozoisite is mentioned only in those<br />
papers dealing with the petrography of igneous rocks of the spilite-keratophyre<br />
association, and rocks from the Bosnian serpentine zone.<br />
1. Mid-Triassic spilite-keratophyre association<br />
Epidote and clinozoisite can be found in the products of mid-Triassic<br />
magmatism in the Jablanica and Prozor regions (Pamić 1960, 1961a and 1961b). It<br />
occurs frequently in albite diabases of the Crima creek near the village of Lug. Here,<br />
after being transformed from plagioclase, it forms a mixture with prehnite, calcite<br />
and sericite.<br />
Clinozoisite is also a member of contact parageneses at the same locality.<br />
Here it is associated with the central sections of the contact zone, and occurs in the<br />
form of irregular and patchy aggregates within a finegrained marble. In thin section,<br />
interference colours are low, the optic axial angle 2V = +64° to +83°.<br />
Clinozoisite also occurs in the doleritic gabbroid rocks near Kukavica village<br />
on Kupres (Pamić and Papeš 1969).<br />
There is an occurence of clinozoisite at the contact of mid-Triassic igneous<br />
rocks with limestones at Bijela near Konjic (Pamić and Maksimović 1968).<br />
Clinozoisite is a frequent constituent of the products of the mid-Triassic<br />
magmatism in the area of Ilidža – Kalinovik (Pamić 1957, 1960a and 1962), and<br />
around Čajniče (Pamić and Buzaljko 1966).<br />
76<br />
2. The Bosnian serpentine zone<br />
Clinozoisite seems to be a comparatively frequent constituent of igneous<br />
and metamorphic rocks of the Bosnian serpentine zone and the surrounding diabasechert<br />
formations – Džepina (1970), Đorđević and Mojičević (1972), Pamić (1969a,<br />
1971, 1971a, 1972a and1972d), Pamić, Šćavničar and Međimorec (1973), Pamić<br />
and Tojerkauf (1970), Podubsky (1968 and 1970), Sijerčić (1972a), Šibenik-Studen<br />
(1972/73), Trubelja (1957 and 1960), Trubelja and Pamić (1957 and 1965).<br />
As a typical vein-filling mineral, clinozoisite frequently occurs in gabbroid<br />
rock from the Višegrad area (Trubelja 1957 and 1960). Its formation is associated<br />
with hydrothermal events during which the hydrothermal solutions reacted with<br />
primary ferromagnesian silicates, followed by an exsolution of clinozoisite, prehnite,<br />
zeolites, chlorite and others.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
At Pavitina (Suha Gora), clinozoisite crystallized in veins of up to 2 cm thick.<br />
It is usually pink in clour, but also yellow-green (epidote). Clinozoisite frequently<br />
forms needle-like, radial aggregates.<br />
In thin section, clinozoisite has a high relief, with characteristic interference<br />
colours of blue and lavender. Following optical constants were measured on a<br />
rotating stage microscope:<br />
c : X = 2 3.5° 2° ---<br />
-2V = 88.5° 86.5° 79° 83°<br />
According to the measured optical constants, the mineral is partly clinozoisite,<br />
partly epidote (pistazite).<br />
A monomineralic aggregate of pink clinozoisite has been found at Lahci,<br />
near Višegradska Banja. In thin section, this clinozoisite is optically positive,<br />
2V = 85¼°, 85°, 77°. Needlelike and finegrained aggregates regularly display<br />
lavender interference colours.<br />
Clinozoisite and epidote are frequently found in basic igneous and some<br />
metamorphic rocks (amphibolites) from Vareš, Zavidovići and Maglaj (Pamić 1972a).<br />
A finegrained aggregate consisting of prehnite, clinozoisite and calcite has<br />
formed as a result of retrograde metamorphism of basic plagiocalese in amphibolite<br />
rocks of Mt. Skatovica (Pamić 1969a). Pamić determined clinozoisite in amphibolites,<br />
diabases and spilites around Rudo (Pamić 1972d).<br />
3. Clinozoisite in other rocks<br />
M. Kišpatić (1910) determined clinozoisite and epidote in gabbro-diorite<br />
rocks of Bijela Gromila, south of Travnik. The same fincing was made by F. Katzet<br />
(1924 and 1926).<br />
M. Tajder and P. Raffaelli (1967) described clinozoisite in altered porphyrekeratophyres<br />
of the schist mountains of central Bosnia.<br />
Podubsky (1968 and 1970) determined clinozoisite and epidote to be regular<br />
accessory minerals occuring in the Paleozoic-age metamorphites of eastern and<br />
northwestern Bosnia. Their presence in Carbon-age rocks is of particular interest.<br />
Clinozoisite is a rather frequent constituent of rocks of Mt. Motajica<br />
impacted by contact metamorphism. As concerns igneous rocks, only lamprophyres<br />
contain clinozoisite (Varićak 1966). Here, clinozoisite occurs either as an essential<br />
77
SILICATES<br />
or accessory constituent of the following rocks: amphibole gneisses, biotite and<br />
pyroxene cornites, hornblendites, amphibolites and amphibole schists, albiteactinolite-epidote<br />
schists and glaucophanites.<br />
Clinozoisite is present in amphibolites and amphibole schists in quantities<br />
up to 6.5%. It can be an essential constituent of glaucophanites. Optic axial angles<br />
2V = +86°, c : X = 3°.<br />
EPIDOTE<br />
Ca 2<br />
(Fe 3+ ,Al)Al 2<br />
[O|OH|SiO 4<br />
|Si 2<br />
O 7<br />
]<br />
A u t h o r s: Arsenijević (1967), Barić (1970a), Behlilović and Pamić (1963),<br />
Cissarz (1956), Čelebić (1967), Čutura (1918), Džepina (1970), Đorđević (1958 and<br />
1969), Đorđević and Stojanović (1972), Đurić (1963a), Foullon (1893), Gaković<br />
and Gaković (1973), Jovanović (1972), Jurković (1954a, 1956, 1957 and 1962a),<br />
Jurković and Majer (1954), Karamata (1957), Katzer (1924 and 1926), Kišpatić<br />
(1897, 1900, 1904, 1904b, 1910 and 1912), Koch (1908), Magdalenić and Šćavničar<br />
(1973), Majer (1963), Majer and Jurković (1957 and 1958), Marić (1927 and 1965),<br />
Milenković (1966), Mojsisovics, Tietze and Bittner (1880), Nöth (1956), Pamić<br />
(1957, 1960, 1960a, 1961a, 1961b, 1962, 1963, 1969, 1969a, 1971, 1971a and 1972a),<br />
Pamić and Buzaljko (1966), Pamić and Kapeler (1969), Pamić and Maksimović<br />
(1968), Pamić and Papeš (1969), Pamić and Trubelja (1962), Pavlović, Ristić and<br />
Likić (1970), Petković (1961/62), Podubsky (1968 and 1970), Podubsky and Pamić<br />
(1969), Ramović (1957, 1963, 1966 and 1968), Ristić, Likić and Stanišić (1968),<br />
Sijerčić (1972 and 1972a), Simić (1966 and 1968), Šćavničar and Jović (1961 and<br />
1962), Šćavničar and Trubelja (1969), Šibenik-Studen and Trubelja (1967), Šibenik-<br />
Studen, Sijarić and Trubelja (1976), Tajder (1951/53 and 1953), Tajder and Raffaelli<br />
(1967), Trubelja (1960, 1962a, 1963a, 1963c, 1966a, 1969, 1971a, 1972 and 1972a),<br />
Trubelja and Miladinović (1969), Trubelja and Pamić (1957 and 1965), Trubelja and<br />
Sijarić (1970), Trubelja and Slišković (1967), Trubelja and Šibenik-Studen (1965),<br />
Trubelja, Šibenik-Studen and Sijarić (1974), Tućan (1912, 1928, 1930 and 1957),<br />
Varićak (1956, 1957, 1966 and 1971), Živanović (1963).<br />
In Bosnia and Hercegovina, epidote is a common mineral of igneous,<br />
sedimentary and metamorphic rocks. It is usually formed by metamorphosis –<br />
regional, contact or hydrothermal is commonly associated with rocks impacted by<br />
such metamorphism. It occurs frequently in the form of thin veinlets crystallizing in<br />
fractures or similar spaces. It is an essential constitutent of epidote schists.<br />
In spite of its common occurence, detailed data on epidote is very scanty.<br />
Many petrographic publications do mention epidote, but with no reference to its<br />
optical, chemical, thermal and other analytical data.<br />
78
1. Epidote in igneous and metamorphic rocks<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Oldest data on the occurence of epidote in igneous and metamorphic rocks<br />
of Bosnia and Hercegovina can be found in the paper by C. v. John (Mojsisovics,<br />
Tietze and Bittner 1880). The author made a microscopic determination of epidote<br />
in a coarsegrained diorite from Kladanj, in effusive rocks from Srebrenica, and in<br />
diabase porphyrites of the Vrbas river valley between Donji Vakuf and Jajce as well<br />
is in other rocks from this area. The epidote is green or greenish-yellow in colour.<br />
In all mentioned rocks the epidote is associated with late- or post-magmatic<br />
phases, formed by transformation of ferromagnesian silicates and plagioclase.<br />
According to John, biotite is the source of epidote in effusive rocks of from Srebrenica.<br />
M. Kišpatić (1897, 1900, 1904, 1904a and 1904b) made microscopic<br />
determinations of epidote in various rocks of the Bosnian serpentine zone, in products<br />
of Tertiary-age volcanism around Srebrenica and the Bosna river valley as well as in<br />
schists from other regions.<br />
Epidote occurs frequently in basic igneous rocks (gabbro, diabase) of the<br />
Bosnian serpentine zone. It can be found in diabases from Doboj, Mt. Majevica, and in<br />
the troctolite from Ravni Potok. Plagioclase is the source of epidote in the troctolite.<br />
Kišpatić determined epidote in metamorphic rocks of the Bosnian<br />
serpentine zone from several localities. Zoisite is found much less frequently.<br />
In amphibolites from Mehmedov creek the few epidote crystals are elongated<br />
and fractured. Epidote and amphibole are essential constituents of the epidote<br />
amphibolite from Raljevac on Mt. Ljubić. Here it occurs in the form of colourless,<br />
irregular or (rarely) elongated grains.<br />
According to more recent investigations of the Bosnian serpentine zone,<br />
epidote occurs in limited quantities in basic igneous rocks and amphibolites. Data<br />
on epidote can be found in publications of the following authors: Džepina (1970),<br />
Đorđević and Stojanović (1972), Đorđević (1958), Majer (1963), Pamić (1969a, 1971,<br />
1971a and 1972a), Pamić and Kapeler (1969), Pamić and Trubelja (1962), Trubelja<br />
(1960), Trubelja and Pamić (1965), Trubelja, Šibenik-Studen and Sijarić (1974).<br />
According to Trubelja (1960), in the Višegrad area epidote occurs together<br />
with labrador and albite in gabbropegmatites of Banja creek, near Višegradska Banja<br />
– the crystals are prismatic and have a high relief. Together with albite and prehnite,<br />
they are usually incorporated into a finegrained saussurite matrix. It is of hydrothermal<br />
genesis. Epidote (pistazite) occurs together with clinozoisite at Pavitine (Suha gora).<br />
79
SILICATES<br />
According to Pamić (1972a) iron-rich epidote crystallizes in veins within<br />
basic rocks in the areas of Vareš, Zavidovići and Maglaj. Epidote is accompanied by<br />
clinozoisite. The authors provides XRD data for the epidote from Vareš.<br />
Epidote and clinozoisite occur together also in the metamorphic rock series<br />
on the southern flanks of Mt. Ozren, near Kobilovac (Pamić 1971).<br />
We have recently published information about epidote from several localities<br />
within the Bosnian serpentine zone (Trubelja, Šibenik-Studen and Sijarić 1974).<br />
Epidote occurs together withe prehnite and calcite on the southeastern flanks of Mt.<br />
Konjuh, in the area called Karaule (creek Blizanci).<br />
Epidote is also found in the form of thin yellowish veinlets in the valley<br />
of the Trnava creek on the northern flanks of Mt. Kozara. These veinlets can be<br />
observed very well in the dolerite from Gornji Podgradci.<br />
M. Kišpatić (1904a) determined epidote microscopically in dacite from<br />
Protin Han (Srebrenica). This epidote sometimes occurs as quite large crystals.<br />
In the effucive rocks outcropping in the valley of the Bosna river, epidote<br />
occurs at sevela localities (Kišpatić 1904).<br />
M. Tajder (1953) describes epidote occuring in altered schists and normal<br />
and propilitized effusive rocks of Tertiary age in the Srebrenica region. Epidote in<br />
the Srebrenica paragenesis was also mentioned by M. Ramović (1963).<br />
According to M. Kišpatić (1904), epidote occurs in greenschists from Polom<br />
and Lonjina on the river Drina, as well as chlorite schists from mVilenica near<br />
Travnik. Here, epidote occurs in finer or larger grains. There is a substantial quantity<br />
of epidote in chlorite schists outcropping between Fojnica and Čemernica. Here the<br />
epidote is finegrained, colourless or yellow in colour. Interference colours are vivid<br />
in thin section.<br />
Epidote is also present in various rocks from Mt. Motajica and Mt. Prosara<br />
(Koch 1908; Katzer 1924 and 1926; Varićak 1956, 1957 and 1966).<br />
F. Koch determined epidote microscopically in granites, gneisses,<br />
micaschists and amphibolites. In the Mt. Motajica granite the epidote is of green<br />
colour. In the gneiss of Studena Voda it occurs either as individual crystals or as<br />
aggregates. It formed as a result of tourmaline and orthoclase metamorphosis. It<br />
is yellow in colour, quite pleochroitic and has a strong birefringence. The epidote<br />
in biotite schists of Puljane Kose has the same properties as in the previously<br />
described rock, and is altered biotite.<br />
80
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Numerous data on epidote and clinozoisite from Mt. Motajica was given by<br />
Varićak (1966). The granitoids, contact-metamorphic rocks and surrounding rock<br />
series contains epidote both as an essential or accessory constituent.<br />
The quantity of epidote in the chlorite-epidote schists amounts to ca. 20%.<br />
The epidote in granitoid rocks is normally of hydrothermal or pneumatolitic genesis.<br />
Rocks altered by contact metamorphism always contain some epidote. Occasionally,<br />
the quantity of epidote is significant, like in albite-actinolite-epidote schists.<br />
According to Varićak (1956 and 1957), epidote occurs in carbonate schists,<br />
green rocks and quartz-porphyres of Mt. Prosara.<br />
Čutura (1918) mentions epidote in various igneous rocks of southwestern<br />
Bosnia. It occurs in the form of aggregates – together with sericite – in granitoid<br />
rocks of Mt. Komar. Both minerals were formed from feldspar. Epidote is also<br />
found in basic effusive rocks from Babino Selo, as well as in similar igneous rocks<br />
around Jajce.<br />
Epidote is a common constituent of igneous rocks from other areas of the<br />
schist mountains of central Bosnia (Jurković 1954a; Jurković and Majer 1954;<br />
Kišpatić 1910; Majer and Jurković 1957 and 1958; Šibenik-Studen and Trubelja<br />
1967; Trubelja and Šibenik-Studen 1965).<br />
Epidote and zoisite are constituents of the albite rhyolite from Sinjakovo.<br />
They also occur at the contact of this albite rhyolite and Paleozoic-age limestones at<br />
Alinovac, near Jezera. The mineral association located closest to the contact consists<br />
mainly of chlorite, actinolite and epidote (Jurković and Majer 1954). In a rather<br />
similar series of magmatites in the Janj creek, close to the village of Perkovići near<br />
Jezera, epidote was identified by XRD and IR-spectroscopy (Šibenik-Studen, Sijarić<br />
and Trubelja 1976). The IR spectrum of this epidote is shown in Figure 8.<br />
Figure 8. IR-spectrum of epidote, Perkovići near Jezera<br />
(Šibenik-Studen, Sijarić and Trubelja 1976).<br />
81
SILICATES<br />
Epidote and zoisite are constituents of the augite-labrador andesite from<br />
Orašin, southeast of Bakovići (Jurković 1954a).<br />
The gabbro-dioritic rocks of Bijela Gromila also contains epidote and zoisite<br />
(Kišpatić 1910; Majer and Jurković 1957 and 1958). A detailed microscopic study of<br />
epidote from Tovarnica was done by L. Marić (1927). This epidote is associated with<br />
magnetite. He also investigated the epidote contained in gabbros from the confluence<br />
area of the Rama and Neretva rivers. At Tovarnica, epidote of a yellow-green<br />
colour occurs together with calcite and quartz. In thin section, epidote grains are<br />
rounded or slightly elongated. Some grains are brownish-green in colour and have<br />
a stronger pleochroism and higher refractive indices than the yellowish-green ones.<br />
The pleochrotoic colours are: X = yellowish, Z = greenish-brown. The difference in<br />
pleochroitic colours is a consequence of a variable amount of trivalent iron. Cleavage<br />
is distinct in the case of elongated grains. Occasionally epidote is accompanied by<br />
chlorite. Marić believes that the epidote is of secondary genesis. M. Ramović (1968,<br />
p. 168) also mentions epidote from this locality.<br />
The genesis of epidote and other minerals occuring at the contact of the Jablanica<br />
gabbros and surrounding carbonates and other sediments (Tovarnica near Jablanica) has<br />
been studied by several authors (Cissarz 1956; Nöth 1956; Čelebić 1967).<br />
According to A. Cissarz (1956), the gabbroic rocks have impacted the<br />
surrounding rocks (in the southwestern flanks of the gabbro body) through contact<br />
metamorphism. The paragenesis also contains epidote, which crystallized during<br />
the later stages of the paragenesis. The amount of epidote is substantial and thus<br />
one of the main constituents of the paragenesis, together with garnet, calcite and<br />
magnetite (see Figure 2).<br />
According to Čelebić (1967) the epidote, together with zoisite and other<br />
accessory minerals at the Tovarnica locality comprose a contact-metasomatic<br />
paragenesis. Sometimes, a zonal interchange between epidote and magnetite can be<br />
observed, resulting in a ‘zebra-like’ texture. Its colour is olivegreen to yellowish, and<br />
single-mineral aggregates are frequent (epidosite). The grainsize is in the range from<br />
several micrometers to several millimeters.<br />
In the Jablanica and Prozor areas, the spilite-keratophyric rock series<br />
sometimes contain also clinozoisite in addition to epidote (Pamić 1960, 1961a and<br />
1961b). In the case of keratophyres, small epidote grains are dispersed in the rock<br />
mass. The epidote is yellowish, with a very high relief, and intereference colour in<br />
thin section are vivid. The average optic axial angle value 2V = +70°.<br />
At the contact zone, in Crima creek near the village of Lug south of Prozor,<br />
epidote is a constituent of the contact paragenesis together with garnet, albite,<br />
82
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
chlorite, clinozoisite, prehnite, magnetite and other minerals. Grains are irregularly<br />
shaped, elongated crystals are infrequent. Relief is high. Pleochroitic colurs: X =<br />
light-yellow, Y = Z = greenish-yellow. Elongated grains have a parallel extinction.<br />
In thin section, intereference colours are high, +2V = 68° (iron-rich epidote).<br />
Epidote also occurs in mid-Triassic age magmatites around Kupres,<br />
Borovica (Vareš), Tjentište, Čajniče, Zvornik, along the transect Ilidža-Kalinovik<br />
and elsewhere (Behlilović and Pamić 1963; Đurić 1963a; Karamata 1957; Pamić<br />
1957, 1962, 1963 and 1969; Pamić and Buzaljko 1966; Pamić and Papeš 1969;<br />
Simić 1966 and 1968; Trubelja 1962a, 1963, 1963a, 1969 and 1972a; Trubelja and<br />
Miladinović 1969; Trubelja and Slišković 1967).<br />
The epidote in keratophyres from the Trešanica gorge (near Bradina in<br />
Hercegovina) contains some 30 mol.% of Fe III (Barić 1970a). It occurs as irregular<br />
grains ca. 0.1 mm in diameter, within or outside the hornblende matrix. Pleochroitic<br />
colours are light- to vivid-yellow, with occasional green overtones. Sometimes a<br />
single epidote crystal has distinctly different sections. Interference colours are vivid.<br />
The optic axial angle varies in the range 2V = -69.5° to -74.5°.<br />
In the vicinity of Tarčin, in the Crna Rijeka river valley near Gunjani village,<br />
beautiful epidote crystals were discovered in fractures of igneous rocks (Šibenik-<br />
Studen, Sijarić and Trubelja 1976). Some crystals are up to 10 cm long and 5 mm thick,<br />
the colour is greenish to yellow-brown and different sectors of one crystal can have<br />
different colouration. The epidote was determined by XRD and chemical analysis.<br />
The epidote from Crna Rijeka has the following chemical composition<br />
(analyst M. Janjatović):<br />
SiO 2<br />
= 38.03 TiO 2<br />
= --- Al 2<br />
O 3<br />
= 28.90 Fe 2<br />
O 3<br />
= 7.18<br />
CaO = 24.30 H 2<br />
O + = 2.29 H 2<br />
O - = 0.16 Total = 100.86<br />
Epidote is a regular accessory constituent of the Paleozoic-age rock series<br />
in northwestern Bosnia (consisting of semimetamorphites and metamorphites).<br />
Of particular interest is the occurence of epidote and clinozoisite in Carbon-age<br />
rocks (Podubsky 1968). Substantial concentrations of epidote occur in epidotized<br />
metasandstones and metamorphised igneous rock in the area of the Ljubija ore<br />
deposits (Podubsky and Pamić 1969).<br />
Rocks impacted by metamorphic processes (epidotization, chloritization,<br />
albitization) are frequent in the mid-Carbon-age rock formations of eastern Bosnia<br />
(Podubsky 1968 and 1970; Katzer 1924 and 1926). Epidote and clinozoisite are<br />
normally present as accessory minerals in sediments, semimetamorphites and<br />
metamorphites, but occasional enrichments in epidote have been identified in rocks<br />
around Šutorina Rijeka and Mlječvanska Rijeka.<br />
83
SILICATES<br />
More recently, data on epidote in altered porphyrite-keratophyres and other<br />
schists in the schist mountains of central Bosnia have been published (Tajder and<br />
Raffaelli 1967; Trubelja and Sijarić 1970).<br />
According to Tajder and Raffaelli, the stilpnomelane-bearing albite-epidote<br />
schists from Neretvica creek, epidote occurs in the form of large, almost idiomorphic<br />
grains, crystallizing in veinlets present in the rock. A significant variance in the<br />
mineral and chemical composition is characteristic of these veins (quartz-epidotecalcite;<br />
quartz with a minor amount of calcite, stilpnomelane, epidote and chlorite;<br />
chlorite, epidote, stilpnomelane; stilpnomelane-epidote-chlorite with a minor amount<br />
of calcite and quartz).<br />
2. Epidote in sedimentary rocks<br />
In contrast to the amount of data on epidote in igneous and metamorphic<br />
rock, information on epidote in sedimentary rocks is very scanty – Foullon (1893),<br />
Gaković and Gaković (1973), Jovanović (1972), Katzer (1924 and 1926), Kišpatić<br />
(1912), Magdalenić and Šćavničar (1973), Marić (1965), Pavlović, Ristić and Likić<br />
(1970), Ristić, Likić and Stanišić (1968), Sijerčić (1972), Šćavničar and Jović (1961<br />
and 1962), Tućan (1912).<br />
According to Foullon (1893), epidote sometimes occurs in mineral<br />
concentrates in formations in the schist mountains of central Bosnia.<br />
Epidote was also identified in the insoluble residue of Triassic-age carbonates<br />
from the outer Dinarides (Gaković and Gaković 1973).<br />
Epidote is a frequent accessory mineral in quartz sands and other<br />
sedimentary rocks of the Tuzla basin (Pavlović, Ristić and Likić 1970; Ristić,<br />
Likić and Stanišić 1968).<br />
Z. Sijerčić found epidote in the heavy mineral fraction of the Eocene-age<br />
flysch deposits on the western flanks of Mt. Majevica. Based on this identification,<br />
Jovanović (1972) determined epidote also in the heavy fraction of the Pliocene-age<br />
sands in the Prijedor basin.<br />
According to B. Šćavničar and P. Jović (1961 and 1962), epidote occurs in<br />
several horizons of the Pliocene-age sands of the Kreka coal basin, especially the<br />
B and C horizons. The grains are irregular in shape, yellowish-green in colour and<br />
have a vitreous lustre. It has a high relief, strong pleochroism and vivid interference<br />
colours. It is almost always associated with zoisite – both minerals originate from<br />
metamorphic rocks. Epidote also occurs in Eocene-age sandstones in this area.<br />
84
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Z. Magdalenić and B. Šćavničar (1973) have identified epidote in clastic<br />
rocks around Kulen Vakuf.<br />
M. Arsenijević (1967) analysed the epidote from Mt. Motajica granitoids<br />
for their Sn and Nb content and found ca. 100 g Sn/ton and 900 g Nb/t as maximum<br />
concentrations.<br />
M. Kišpatić (1912) microscopically identified epidote in the bauxites from<br />
Studena Vrela (Duvno), while Tućan (1912) found it in terra rossa from Eminovo<br />
selo. Marić (1965) gives reference to both authors in his paper.<br />
Use<br />
Green-coloured epidote (pistazite) can be used as a gemstone.<br />
ALLANITE<br />
Ca(Ce,Th)(Fe 3+ ,Mg,Fe 2+ )Al 2<br />
[O|OH|SiO 4<br />
|Si 2<br />
O 7<br />
]<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 1.5507 : 1 : 1.7684, β = 115° 01’,<br />
Unit cell parameters: a o<br />
= 8.98, b o<br />
= 5.75, c o<br />
= 10.23, Z = 2.<br />
Synonyms: the mineral belongs to the epidote group. It was first discovered<br />
on Greenland by Gieseke. It was analysed in 1810 by Thomson, a chemist in<br />
Glasgow, and named after the scottish mineralogist Allan. Berzelius called it<br />
orthite (greek orthos, upright) because crystals found in the Finbo mine (near<br />
Falun, Sweden) had an orthogonal shape. He also used the name pyrorite<br />
because some crystals – when heated – would continue smoldering (because<br />
of the bitumonous matter present). This was particularly true for crystal found<br />
at Kararfvet in the Falun area. Other names which have been used at various<br />
times: ksantorite (greek ksanthos, yellow), bodenite (after Boden, in Sachsen,<br />
Germany), muromonite (latin muro, wall, and mons, mountain) after the<br />
Mauresberg mine near Marienberg in Sachsen, tautolite (greek tautos, same and<br />
lithos, stone), bucklandite (after Buckland, a professor at Oxford).<br />
The name bagrationite came to be as follows. The russian count Bagration<br />
found black, opaque crystals of a mineral in the Akhmatovskij mine, in the Zlatoust<br />
area of the Ural mountains. They were first investigated by Koksharov in 1847 and<br />
named bagrationite. Subsequently, Koksharov (1858) realized that there was no<br />
difference between “bagrationite” and allanite, based on measurement of the angles<br />
between crystal faces.<br />
The name wasite was used for a very weathered allanite found at Rönsholm<br />
island near Stockholm. In 1863 Bahr believed that this mineral contained a new<br />
85
SILICATES<br />
element (wasium). Bahr wanted to name both the element and the mineral after the<br />
swedish royal dynasty of Wasa.<br />
X-ray diffraction data: d 2.91 (100), 2.92 (90), 2.86 (50); d 2.90 (10), 1.64<br />
(9), 2.70 (7); d 2.91 (10), 1.64 (8), 3.47 (6).<br />
A u t h o r s: Markov and Mihailović-Vlajić (1969), Mihailović-Vlajić<br />
(1967), Varićak (1966).<br />
Up to now, in Bosnia and Hercegovina allanite has been found only in the<br />
granite rocks of Mt. Motajica. According to Varićak (1966) allanite is an accessory<br />
mineral in normal granite, leucocratic granite and granite-porphyres. In the latter<br />
rock, allanite is of a primarily zonal structure. Twinning along (100) is rare. The<br />
interfacial angle between the faces (100) and (001) is 115°. The following optic data<br />
has been obtained in thin section:<br />
Nx : c = 35.5°, Nz : a = 55-60°, 2V = -74° to -75°<br />
Pleochroitic colours are as follows: Nx = yellowish-greenish-brown; Nz =<br />
darkbrown-reddish.<br />
According to Mihailović-Vlajić (1967, p. 196) four varieties of allanite are<br />
present in the Mt. Motajica granite.<br />
a) the dark to black variety of allanite is most common. The somewhat elongated<br />
crystals have a prismatic shape, and are between 0.1 and 0.5 mm long. Their<br />
surface is sometimes covered with an earthy alteration crust.<br />
b) a red-brownish variety of allanite is present in biotite-gneisses and leucocratic<br />
granite. It is usually xenomorphic.<br />
c) a pinkish-brown variety occurs in pegmatites. The occasionally present crystals<br />
are shortprismatic in shape with a visible cleavage. Grains are partly covered on<br />
the surface with an alteration crust.<br />
d) the brown-reddish variety of xenomorphic allanite with a resinuous lustre and<br />
conchoidal fracture surfaces occurs only in some parts of the muscovite-granite<br />
formation. An alteration crust is usually present. This allanite is more radioactive<br />
than the first three varieties, and contains ca. 1750 ppm (0.175%) of niobium. Six<br />
samples have been analyzed for trace elements – data is given in Table 12.<br />
Allanite has been retrieved from rock samples of more than 100 kg in weight<br />
(Mihailović-Vlajić 1967, p. 192), the same way as for thorite.<br />
In a later paper, Markov and Mihailović-Vlajić (1969, p. 257) confirm the<br />
occurence of allanite in Mt. Motajica granites.<br />
86
Use<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Hisinger named in 1811 this mineral cerine, because of its cerium content.<br />
Table 12. Concentration of trace elements in allanites from the Mt. Motajica granite<br />
(Mihailović-Vlajić 1967)<br />
Biotitegneiss<br />
Main granite<br />
body<br />
Muscovitegranite<br />
Finegrained<br />
granite<br />
Pegmatite Muscovitegranite<br />
Sample number<br />
94.991 95.012 95.219 94.990 95.223 33.600a<br />
Mn 3500 ppm 3160 ppm 3160 ppm --- 4000 ppm 1%<br />
Pb 60 39 134 25 100 60<br />
V 170 316 720 170 --- 500<br />
Ga 40 40 90 50 90 12<br />
Sn --- 37 50 --- --- 80<br />
Nb --- --- --- --- --- 1750<br />
Y 1200 660 790 1200 4000 600<br />
Yb + + + + + +<br />
Dy + - - + - -<br />
Er + - - + - -<br />
La 1% 1% 1% 1% 1% 1%<br />
Ce + + + + + +++<br />
Zr 300 1000 1000 600 631 600<br />
Ni - - 5 - - 9<br />
Cr 140 - - 60 - 80<br />
Co - - 11 - - -<br />
Cu 7 4 32 7 20 40<br />
Sc 300 340 340 400 400 340<br />
Ba 30 traces 700 140 355 400<br />
Sr 80 650 2240 800 1130 2500<br />
ZOISITE<br />
Ca 2<br />
Al 3<br />
[O|OH|SiO 4<br />
|Si 2<br />
O 7<br />
]<br />
Crystal system and class: Orthorhombic, rhombic-dipyramidal class.<br />
Lattice ratio: a : b : c = 2.879 : 1 : 1.791<br />
Unit cell parameters: a o<br />
= 16.24, b o<br />
= 5.58, c o<br />
= 10.10, Z = 4.<br />
Properties: perfect cleavage along {001}. Hardness = 6.5, specific gravity = 3.3.<br />
Colour is gray, sometimes pink or green. Streak is white, lustre vitreous (pearly on<br />
cleavage planes). Refractive indices are high, birefreingence medium to small.<br />
X-ray diffraction data: d 2.703 (100), 2.869 (100), 1.615 (75)<br />
IR-spectrum: 410 443 470 512 575 595 620 655 695 715 755 780 865 900<br />
975 1040 1115 3140 cm -1<br />
87
SILICATES<br />
A u t h o r s: Čelebić (1967), Džepina (1970), Đorđević (1958), Golub (1961),<br />
Jurković (1954a), Jurković and Majer (1954), Karamata and Pamić (1964), Katzer<br />
(1924 and 1926), Kišpatić (1897 and 1900), Magdalenić and Šćavničar (1973),<br />
Majer (1962), Majer and Jurković (1957 and 1958), Mojsisovicz, Tietze and Bittner<br />
(1880), Pamić (1971), Petković (1961/62), Ristić, Panić, Mudrinić and Likić (1967),<br />
Šćavničar and Jović (1962), Trubelja (1960 and 1966a), Trubelja and Pamić (1965),<br />
Varićak (1966), Vasiljević (1969).<br />
Zoisite is one of those rock-forming minerals which have not been sufficiently<br />
investigated in Bosnia and Hercegovina, and only a limited amount of data is available.<br />
It occurs mainly in metamorphic rocks, either as an essential mineral (zoisite schists)<br />
or as an accessory. Some igneous rocks, which have sustained alteration, do contain<br />
zoisite. Some zoisite has been found to occur in sedimentary rock, but very limited<br />
information is available.<br />
1. Zoisite in metamorphic and igneous rocks<br />
The first determinations of zoisite in hornblende-zoisite schists, from<br />
Čemlija around Zvornik, were done by John (Mojsisovics, Tietze and Bittner 1880).<br />
In some schists the zoisite dominates with respect to hornblende, in other rocks the<br />
opposite is the case. The zoisite is of a white or red colour.<br />
The zoisite amphibolite from Mamići (Kalesija), studied by Kišpatić (1897<br />
and 1900) is very similar to the schists from Zvornik investigated by John. In the<br />
Mamići amphibolite, zoisite is colourless and very refractive. In thin section, the<br />
grains have an irregular shape and two cleavage systems are visible. Birefringence is<br />
low, as are the gray interference colours. This epidote shows parallel extinction.<br />
Katzer (1924 and 1926) mentions zoisite in rock from the area of the<br />
Kamenica river, south of Zvornik. The zoisite and amphibolite rocks are probably<br />
altered basic magmatites.<br />
Zoisite is an essential mineral of the amphibole-zoisite schists from the<br />
Krušik creek, near Boljanići village at Mt. Ozren (Trubelja and Pamić 1965).<br />
Outcrops of zoisite-bearing rocks are located 400 to 500 m upstream, towards the<br />
village of Konopljište. Zoisite and an amphibole from the termolite-actinolite series<br />
are the only two rock-forming minerals. For zoisite, 2V = +54° to 60°. Refractive<br />
indices are higher than those of the amphibole, so is the relief. Extinction is parallel,<br />
and cleavage clearly visible.<br />
Zoisite and epidote are also found in similar schists on the southern flanks of<br />
Mt. Ozren, near Kobilovac (Pamić 1971).<br />
88
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
According to microscopic investigations by D. Džepina (1970), zoisite occurs<br />
in basic rock altered by regional metamorphism (southern flanks of Mt. Borja).<br />
The following authors have mentioned zoisite in igneous rocks of the bosnian<br />
serpentine zone: Đorđević (1958), Golub (1961), Karamata and Pamić (1964), Majer<br />
(1962), Ristić, Panić, Mudrinić and Likić (1967), Trubelja (1960 and 1966a).<br />
Accessory zoisite occurs in some granites at Mt. Motajica (Varićak 1966).<br />
Zoisite and epidote occur in gabbro-dioritic rocks of Bijela Gromila, south of<br />
Travnik (Majer and Jurković 1957 and 1958). They also occur in the augite-labradorcontaining<br />
andesites of Orašin, southeast of Bakovići (Jurković 1954a)<br />
Zoisite and epidote are constituents of the albite rhyolite from Sinjakovo.<br />
They are also found at the contact of this rock and Paleozoic-age limestones at<br />
Alinovac, near Jezera (Jurković and Majer 1954).<br />
Zoisite, epidote and some ither minerals are constituents of the<br />
metasomatically altered contact paragenesis within the magnetite body of Tovarnica,<br />
near Jablanica (Čelebić 1967). This zoisite occurs as coarse grains.<br />
M. Petković (1961/62) mentions zoisite in the spilite rocks at Borovica (Vareš).<br />
2. Zoisite in sedimentary rocks<br />
Very limited information is available on zoisite in the heavy mineral fractions<br />
of clastic sediments (Magdalenić and Šćavničar 1973; Šćavničar and Jović 1962).<br />
Zoisite (together with tourmaline and epidote) has been identified as an<br />
essential constituent of Miocene-age sandy calcarenites from Lupina near Kulen<br />
Vakuf (Magdalenić and Šćavničar 1973). B. Šćavničar and P. Jović (1962) identified<br />
zoisite in the Pliocene-age sands of the Kreka coal basin, within several horizons.<br />
R. Vasiljević (1969) describes the zoisite occurence in sedimentary quartzites<br />
at podrašnica (Mrkonjić Grad), based on microscopic determination by S. Pavlović<br />
and D. Nikolić.<br />
89
SILICATES<br />
PUMPELLYITE<br />
Ca 2<br />
(Al,Mg,Fe 2+ ) 3<br />
[(OH) 2<br />
|SiO 4<br />
|Si 2<br />
O 7<br />
]<br />
Pumpellyite has monoclinic symmetry. It is a member of the epidote group<br />
of minerals. Hardness = 5.5, specific gravity = 3.2. Bluish-green colour. It is best<br />
determined by x-ray diffraction: d 2.90 (100), 2.74 (50), 3.79 (40).<br />
A u t h o r s: Trubelja, Šibenik-Studen and Sijarić (1974, 1975 and 1975a),<br />
Šibenik-Studen, Sijarić and Trubelja (1976).<br />
Pumpellyite has only recently been discovered in Bosnia and Hercegovina –<br />
at Vareš and Jablanica where it is associated with Triassic-age magmatites. At Vareš,<br />
it occurs together with prehnite in veins and amygdales of altered melaphyres. It has<br />
been identified by XRD (Trubelja, Šibenik-Studen and Sijarić (1974, 1975 and 1975a).<br />
Pumpellyite occurs together with chlorite, amphibole and stilbite in veins of<br />
the gabbro at Jablanica (Ploče quarry). Pumpellyite and the other mentioned minerals<br />
have formed on stilbite (Šibenik-Studen, Sijarić and Trubelja 1976). The minerals<br />
were identified by XRD.<br />
VESUVIANITE<br />
Ca 10<br />
(Mg,Fe) 2<br />
Al 4<br />
[(OH) 4<br />
|(SiO 4<br />
) 5<br />
|(Si 2<br />
O 7<br />
) 2<br />
]<br />
Vesuvianite (idocrase) occurs at a single locality only in Bosnia and<br />
Hercegovina – in the rodingite-altered basic garnet-bearing rocks at Mt. Borja<br />
(between the bridge at Velika Usora and Crkvena). It was discovered by Džepina<br />
(1970). According to this author, vesuvianite is accompanied by hydrogarnet, calcite,<br />
epidote, zoisite, serpentine, chlorite and ksonotlite.<br />
AXINITE<br />
Ca 2<br />
(Mn,Fe)Al 2<br />
[BO 3<br />
|Si 4<br />
O 12<br />
|OH]<br />
The only information about axinite in Bosnia and Hercegovina was provided<br />
by T. Jakšić in an unpublished study of arsenic ores at Hrmza near Kreševo (Jakšić<br />
1930), where he claims that axinite occurs in these ores. He maintained that “this is a<br />
mineral which was previously been regarded as fluorite”. According to Barić (1942,<br />
p. 43), this claim was not supported by any kind of evidence. In a microscopic study<br />
of these ores, Barić determined an optically isotropic mineral with a refractive index<br />
below the one of Canada balm. The violet colouration of the mineral is patchy. The<br />
determined properties do not correspond to axinite (see fluorite).<br />
90
BERYL<br />
Be 3<br />
Al 2<br />
[Si6O18]<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Crystal system and class: Hexagonal, dihexagonal-dipyramidal class.<br />
Lattice ratio: a : c = 1 : 0.4985.<br />
Unit cell parameters: a o<br />
= 9.23, c o<br />
= 9.19, Z = 2.<br />
Synonyms: none, except for gemquality varieties – emerald, aquamarine, vorobievite<br />
or morganite, heliodor, golden beryl, goshenite or rosterite, bixbiite, green aquamarine<br />
(more information in the section on the use of beryl).<br />
Properties: weak cleavage along the base (pinacoid). The fracture surface is irregular<br />
or scalelike. Hardness = 7.5-8, specific gravity = 2.63-2.80. Refractive indices: ω =<br />
1.57-1.60, ε = 1.56-1.59. Lustre is vitreous. Occurs colourless or in various colurs.<br />
Transparency is variable.<br />
X-ray diffraction data: d 2.87 (100), 3.25 (95), 7.98 (90). ASTM-file 9-430.<br />
IR-spectrum: 415 440 497 530 595 655 685 745 810 (918) 975 1025 1086<br />
1210 cm -1<br />
A u t h o r s: Barić (1960), Gojković and Nikolić (1967), Katzer (1924 and<br />
1926), Kišpatić (1902), Koch (1899, 1902 and 1908), Markov and Mihailović-Vlajić<br />
(1969), Mihailović-Vlajić (1967), Mikinčić (1955), Nikolić (1962 and 1963), Pilar<br />
(1882), Ristić, Antić-Jovanović and Jeremić (1965), Trubelja and Pamić (1957),<br />
Varićak (1966).<br />
In Bosnia and Hercegovina, Mt. Motajica is the only location where beryl<br />
has been found. It occurs in pegmatite veins in the granite quarry between the villages<br />
of Vlaknica and Brusnik, upstream of the Bosanski Kobaš village. This granite was<br />
first described by John (Mojsisovics, Tietze and Bittner 1880), and two years later<br />
by Pilar (1882). There is no mention of beryl at Mt. Motajica in these papers. Beryl<br />
was first mentioned by Koch (1899, 1902 and 1908, p. 4). Koch did his investigation<br />
on material deposited at the Museum of Mineralogy and Petrology in Zagreb – the<br />
material comes from the Veliki Kamen quarry near Vlaknice village. The material<br />
from this quarry was used for road construction and the Sava river embankment;<br />
beryl-bearing pegmatite veins were found in this granite. Koch provides only<br />
inconsistent information as to how the material arrived in the museum in Zagreb.<br />
In one place Koch claims that the material was collected by Pilar himself (Koch<br />
1899, p. 1). The same information can be found in the paper by Barić (1960, p. 71).<br />
However, in his later paper (Koch 1908, p. 1) the author maintains that Pilar did not<br />
visit Mt. Motajica and that the material was brought to Pilar by the surveyor Uhlig –<br />
and that Koch used these specimens in his investigations. Pilar (1882, p. 15) indeed<br />
notes this gift, but does not mention beryl. Katzer (1924 and 1926) maintains that a<br />
pegmatite “nest” with beautiful beryl crystals was open in the quarry for more than<br />
91
SILICATES<br />
40 years. Katzer believes that several samples of these crystals – which Koch used<br />
for his studies – were saved by surveyor Uhlig.<br />
According to Koch, two varieties of beryl occur at Mt. Motajica – colourless<br />
and a coloured variety. The coloured one is of a bluish-green colour, and larger<br />
crystals are fairly translucent. Smaller crystals have a fair degree of transparency.<br />
The crystals are in all cases elongated parallel to [0001], and crystals 10 cm long<br />
and 4-5 cm thick were found. The lower size range is 6-7 mm in lenght and 3-5 mm<br />
in thickness. Only the crystal faces of the basal pinacoid {0001} and the protoprism<br />
{101-11} can be observed. The pinacoid faces occur more frequently and have<br />
irregular etching marks. Larger crystals often have numerous fractures and cracks,<br />
what lowers their transparency. The cracks have nonspecific directions, and are<br />
seldom parallel to the basal pinacoid. Attempts to cleave the crystals result in an<br />
uneven cleavage – part of the cleavage surface is parallel to {0001}, while the other<br />
part is uneven.<br />
The colourless variety occurs less frequently than the coloured one. This<br />
variety occurs as crystal aggregates (while the coloured variety occurs rather as<br />
solitary crystals) always separated from the coloured type. The colourless and<br />
transparent crystals have a short-prismatic shape and are usually 1.5-2 mm long and<br />
thick, although the largest crystals are 5-6 mm long and 2-3 mm thick. Some can<br />
only be seen with the aid of a loupe. The smaller the crystals are, the more elaborate<br />
is the combination of crystal forms. Sections perpendicular to the axis [0001] are<br />
usually not perfect hexagons – the crystals are mostly elongated along one co-axis.<br />
Basal cleavage can normally not be seen on these crystals. Koch measured 5 crystals<br />
and identified – in addition to {0001} and {10-11} – also the following crystal forms:<br />
{10-11}, {11-21} and {31-41}. Koch used the lattice ratio a : c = 1 : 0.49886 (the<br />
value established for beryl by Kokšarov). Koch also mentions a deuteroprism<br />
{11-20} but provides no further information on this form.<br />
Koch described his measurements in great detail, but provided very little<br />
quantitative data. He concludes that the beryl from Mt. Motajica is optically biaxial,<br />
hence certainly of lower that hexagonal symmetry, probably monoclinic or triclinic. He<br />
maintained that the beryl consists of lamellae which have oblique extinction, and that<br />
the apparently hexagonal habit of the crystals is a consequence of a mimetic twinning<br />
of these lamellae. In convergent light, the center of the dark cross is concentrically<br />
surrounded by coloured fringes (isochrome rings). When the crystal is rotated, the<br />
dark cross disintegrates into two hyperbolae only slightly separated so that their dark<br />
blue fringes remain in contact. The separation of the hyperbolae is smaller in the<br />
central section than towards the rim of the thin section. The fine striation on the prism<br />
faces should, according to Koch, be regarded as twinning striae.<br />
92
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Liquid inclusions in beryl from Mt. Motajica are very common. Two phase<br />
(gas bubble) inclusions occur most frequently, those without the gas bubble are rarer.<br />
The smallest gas-bubble inclusions are circular with an average diameter of 0.0023<br />
mm. For the larger ones, the size range is 0.1978-0.437 mm (length) and 0.0506-0.0092<br />
mm (width). The inclusions are located along the edges of the pinacoid {0001} and<br />
the prism {10-10}. The elongation direction of the inclusions is always parallel with<br />
the edges.<br />
The gas-bubble inclusions are immobile, even when the thin sections<br />
are moved or shaken. Upon heating, the gas bubbles become smaller and finally<br />
disappear, and become again visible when the thin section cools down. According to<br />
Koch, the gas in the bubbles is – without any doubt – carbon dioxide CO 2<br />
.<br />
Solid inclusions are muscovite, sometimes with clearly visible crystals.<br />
A chemical analysis, done by Koch on fresh samples of coloured and<br />
colourless beryl. The results of the analysis are given in Table 13.<br />
Three years later, Kišpatić (1902) also writes about this beryl. In the zone<br />
between {0001} and {10-11} he identified one further very narrow face with a<br />
blurred signal. He measured an angle of 3° 4’ between the normal of this face and the<br />
one for the basal pinacoid. He therefore concluded that this was a new crystal form<br />
for beryl {1.0.-1.12}. It should be noted that the measured angle of 3° 4’ would better<br />
correspond to {1.0.-1.11}. The polar distance for this form, when the lattice ratio a :<br />
c = 1 : 0.49886 is applied for beryl, is 2° 59’ i.e. only 5’ less than the value measured<br />
by Kišpatić. However, a calculation for the form {1.0.-1.12} gives a polar distance of<br />
2° 45’ and this fact was also noted by Kišpatić. The difference between the measured<br />
and calculated value is 0° 19’, and since Kišpatić agreed that the reflection from<br />
this face was rather blurred, we maintain that there is insufficient evidence for the<br />
attribution of the form {1.0.-1.12} to beryl.<br />
Table 13. Chemical composition of beryl from Mt. Motajica<br />
Coloured beryl<br />
Colourless beryl<br />
SiO 2<br />
65.735 65.685<br />
Al 2<br />
O 3<br />
14.581 14.688<br />
BeO 11.483 11.550<br />
Fe 2<br />
O 3<br />
(FeO) 2.838 2.682<br />
CaO 0.320 0.309<br />
MgO 0.447 0.428<br />
K 2<br />
O 0.387 0.325<br />
Na 2<br />
O 0.773 0.681<br />
H 2<br />
O 0.188 0.178<br />
Loss on ignition 2.533 2.362<br />
Total 99.285 99.888<br />
93
SILICATES<br />
Spectrographic analysis of beryl from Mt. Motajica<br />
Ristić, Antić-Jovanović and Jeremić (1965) published data on a qualitative<br />
spectrographic analysis of the Mt. Motajica beryl (with a semiquantitative estimate<br />
after Hasler-Harvey)<br />
Mg 0.3-3% Sr 0.003-0.3% Cr 0.0001-0.0016% V 0.001-0.01% Cu 0.0003-0.003%<br />
Ca 0.1-1% Ba --- Mn 0.03-0.3% Fe 0.3-3% Co, Ni ---<br />
There was no evidence for the presence of Ti, Zn, Sc, Cd, W, Pb, Sn, Y, Ta, Nb.<br />
The same authors ran a plame photometric analysis on alkali elements, using<br />
a Beckman photometer, and obtained the following: Li = 0.001%, Na = 0.62%, K =<br />
0.10%, Rb = 0.009%, Cs = 0.093%.<br />
According to these analyses and information provided by Koch, it appears<br />
that the beryl from Mt. Motajica contains a very limited amount of alkalies. An<br />
uptake of these elements into the beryl structure is accompanied by a substitution<br />
of Si with Al in the SiO 4<br />
tetrahedra and an increase in the anionic charge. The large<br />
cations of the alkali elements occupy positions within the structural channels of<br />
beryl, parallel to its [0001] axis. One beryl from Madagascar contained as much as<br />
11% of CsO.<br />
Recent research<br />
Lj. Barić (1960) made some further research on the beryl from Mt. Motajica.<br />
On several collected samples he identified small, colourless or bluish beryl crystals<br />
as overgrowths on smoky quartz. The beryl crystal were 3-4 mm long and 1-2 mm<br />
thick. They have an elongated shape, parallel to [0001], a feature common to beryl.<br />
Crystal with a thicker platy habit, parallel to the basal pinacoid, were found on some<br />
samples only. The crystals had developed numerous terminal faces at their ends.<br />
Barić made measurements on 23 crystals and identified many forms which were<br />
previously unknown for the Mt. Motajica beryl: {0001}, {10-10}, {11-20}, {10-11},<br />
{11-23}, {11-22}, {22-43}, {11-21}, {7.5.-12.12} (a new general form for beryl)<br />
{21-31}, {31-41}, {51-61}, {11.2.-13.2}, {19.1.-20.1}. The faces of the forms<br />
{0001} and {10-10} are usually the best developed ones. Faces of the deuteroprism<br />
are narrow in all cases. In the cas of the various hexagonal dipyramids, {10-11} and<br />
{11-21} are most prominent. The average lattice ratio for this beryl, based on 23<br />
individual measurements is a : c = 1 : 0.4985. A beryl crystal from Mt. Motajica is<br />
depicted in Figure 9.<br />
94
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Figure 9. Beryl from Mt. Motajica (Barić 1960)<br />
As concerns the optical properties of the Mt. Motajica beryl, Barić investigated<br />
15 thin sections of beryl parallel to {0001} and determined by conoscopic microscopy<br />
that the beryl was uniaxial and negative, as opposed to Koch’s conclusion. The view<br />
that the beryl had lower symmetry due to mimetic twinning was not supported by<br />
Barić’s measurements. The twinning observed by Koch is probably a twinning of<br />
several individual hexagonal crystals.<br />
Refractive indices were measured on two crystals in Na-light:<br />
ω = 1.5755 ω = 1.5758<br />
ε = 1.5691 ε = 1.5695<br />
the corresponding maximum birefringence value being 0.0063. This birefringence<br />
was also measured using a compensator, and the value was 0.0066.<br />
The specific gravity (determined by the suspension method) is 2.683 and<br />
2.687. Control measurements using a Berman-type microbalance gave s.g. values of<br />
2.677, 2.67 9<br />
and 2.69 5<br />
.<br />
Low refractive indices and a comparatively low specific gravity determined<br />
for the Motajica beryl are in accordance with chemical analysis data indicating low<br />
concentrations of alkali metals.<br />
The beryl-bearing pegmatite nest in the Veliki Kamen quarry near Vlaknica<br />
was quickly destroyed (Katzer 1926, p. 72) and for some time it seemed that no<br />
more beryl would be found (Kišpatić 1902, p. 50). However, beryl was again found<br />
as operations in the quarry continued. Katzer writes that when he visited this area in<br />
1909, together with his assistant I. Turina, they found a fragment of a large bluish<br />
bery crystal on a waste dump. In the Brusnik creek, they also found a block of granite<br />
which had a thin vein with crystals of beryl and quartz in it. Katzer maintained that<br />
beryl was not uncommon in this part of the Mt. Motajica area. The mentioned vein<br />
95
SILICATES<br />
from the Brsunik area was only 3 cm thick, and the beryls were ca. 2-5 mm long<br />
and of a short-prismatic habit, with a combination of hexagonal prosm and basal<br />
pinacoid usually visible. These beryl crystals had a honey-yellow colour, while only<br />
some were bluish and fully transparent. These blusih crystal had a vitreous lustre –<br />
the yellow ones appeared rather dull and the crystal faces seemed to be etched. This<br />
gives them a greasy lustre and less transparency.<br />
Greenish-blue beryl crystals several centimeters long can be found in the<br />
quarry even today.<br />
If we attempt to describe the genesis and formation of beryl in the Mt.<br />
Motajica area (but also elsewhere in the world), we must note the fact that beryl<br />
occurs in veins in granite. This implies that the granites formed from a granite-type<br />
magma. The crystallization of granite happens on the surface of larger plutonic<br />
granite formations. This surficial part of the granite body is frequently cracked<br />
and fractured due to cooling contractions, possible degassing processes and<br />
tectonics. These fractures could have been filled by very hot (gaseous or liquid)<br />
magmatic differentiates containing substantial amounts of silica, water vapour and<br />
other volatiles – leading to the formation of pegmatites (greek pegma, pegmatos –<br />
strongly bound).<br />
According to the ideas of the famous Russian mineralogist Fersman, such<br />
pegmatites – in the form of dykes and veins – crystallized in a temperature range<br />
between 800° and 400°. The cooling process results in an initial crystallization<br />
around the rims of such a vein or cavity, and progresses later towards the interior.<br />
In this way, cavities and veins can be completely filled up with crystallized matter.<br />
Those closer to the edges and rims are older, the ones towards the central parts are<br />
younger in age. Occasionally very large crystal can form in such conditions, and<br />
intergrowths of quartz and feldspar are common. Intergrowths of dark quartz and<br />
light-coloured feldspar sometimes results in what is called Hebrew stone (hebraic<br />
pegmatite or graphic granite).<br />
In some cases the central sections of cavities and veins remain hollow, and<br />
large crystals of quartz and feldspar can grow from the walls of these cavities. If the<br />
granite magma contained volatiles like boron, fluorine, alkali elements and beryllium,<br />
the pegmatites may contain crystals of tourmaline, topaz, various micas, beryl etc.<br />
This is a possible explanation for the formation of beryl in the Mt. Motajica area.<br />
The pegmatite veins of the Motajica granite normally consist of feldspar, quartz,<br />
muscovite and beryl – while tourmaline, albite, talc, fluorite, pyrite and psilomelane<br />
are accessories (Koch 1899, p. 1).<br />
Varićak (1966, p. 101) notes that beryl is a component of the quartz veins<br />
in the Mt. Motajica area, that it occurs as idiomorphic shortprismatic crystals of<br />
60 x 30 mm in diameter. The commonly occuring quartz relicts in and around the<br />
96
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
beryl crystals are a strong indication that their crystallization happend in the later,<br />
metasomatic phases of the alteration process (Varićak 1966, p. 104).<br />
Nikolić (1962 and 1963) maintained that the Motajica beryl was formed by<br />
two different processes. A limited amount of beryl formed in the pegmatite phase,<br />
while the main quantities of bery are the result of metasomatism (albitization).<br />
Mihailović-Vlajić (1967, p. 202) and Markov and Mihailović-Vlajić (1969,<br />
p. 257) briefly mentioned beryl in the Mt. Motajica pegmatites.<br />
Gamma spectrometry was applied for uranium and thorium determination in<br />
the beryls from the quarry at Mt. Motajica. The green-blue beryls carry 2.1 g/ton of<br />
uranium and 1.2 g/ton of thorium. This is an average of 3 individual measurements<br />
(S. Gojković and D. R. Nikolić 1967).<br />
Use<br />
Clear and transparent beryl is termed gem-quality beryl and is widely<br />
used as a gemstone in jewelry. Emerald is particularly popular as a gem – this is a<br />
largely transparent variety of green colour, the colour being due to trace amounts<br />
of chromium. The greek name for emerald is smaragdos (greek smaragdos =<br />
green stone), but the etymology of the names smaragdos and beryllos are not well<br />
understood. Light green varieties of emerald contain 0.15-0.2 % of chromium as<br />
Cr 2<br />
O 3<br />
, the darker coloured varieties 0.5-0.6 %. The beautiful green colour reminds<br />
one of spring meadows. Pliny the Elder/Plinius Secundus (23-79 AD), who died<br />
during the eruption of Mt. Vesuvius on 25 August 79, wrote in his “Historia Naturalis”<br />
that emerald is an excitement for our eyes because no other colour in nature is as<br />
vivid as the green colour of emerald. Emerald emanates its glow far and wide, and<br />
even seems to give its colour to the surounding air.<br />
Completely transparent and flawless crystals are so rare that they attain<br />
fantastic prices, even surpassing the value best-quality diamonds. The American<br />
Gem Society listed prices (for the year 1960) for emeralds between 1 and 8 carats,<br />
which amounted to 250-5000 dollars per carat. The price of larger and flawless<br />
crystals rises faster than their weight. Large emeralds are literally priceless. One<br />
famous emerald is the one which was presented to the Duke of Devonshire by the<br />
Brazilian Emperor of Brazil Dom Pedro I, in 1831. The natural crystal is a highly<br />
included, deep-green hexagonal prism, terminated on one end with an irregular<br />
fracture surface, and a hexagonal base on the other. It is ca. 6 cm high and 5 cm in<br />
diameter (see Figure 10).<br />
97
SILICATES<br />
Figure 10. The Duke of Devonshire emerald<br />
This beautiful crystal is one of the most famous emeralds in the world, with<br />
a weight of 1383.95 carats (5 carats = 1 gram). It was found in the famous Colombian<br />
emerald mine of Muzo. Another famous crystal of 24 carats is in the Russian Royal<br />
Treasury. The French traveller and jeweler Tavernier (1605-1689) writes that he<br />
saw – among other jewels – some 60 emeralds on the throne of the Grand Moghul<br />
Emperor of India. Each of these emeralds had around 60 carats. Another wonderful<br />
gem is the 24.38 ct “Napoleon” emerald, which Napoleon presented in 1800 to his<br />
wife Josephine de Beauharnais.<br />
Because of its beauty, transparency and resilience against external influences,<br />
magic and healing powers have been attributed to emerald (and other gemstones as<br />
well). Native populations of Peru have allegedly regarded an emerald, as large the<br />
egg of an ostrich, as a deity. The russian author Aleksandar I. Kuprin (1870-1930)<br />
wrote that snakes and scorpions would not approach a person wearing an emerald.<br />
Some fascinating jewellery with emeralds is kept in the Victoria and Albert<br />
Museum in London i.e. a collier with 12 emeralds and a matching set of earrings, each<br />
set with 2 magnificent emeralds. Every emerald in the jewellery set is surrounded<br />
with diamonds, which enhance the beauty of the emeralds even more. It is a “fin de<br />
18 eme siecle” masterpeices of a Russian jeweller. Precious pieces of art and jewellery<br />
with emeralds are kept in the treasury of the Zagreb cathedral.<br />
Emeralds were first mined in the ancient mines (2000 B.C. – 1200 A.D.)<br />
of the Eastern desert in Egypt, east of Aswan and near the Red Sea (Wadi Gimal,<br />
Wadi Nuqrus, Wadi Sikait, Gebel Zubara, Gebel Umm Kabu). The mines were<br />
98
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
rediscovered in 1818 (thousands of open pits and underground workings). Egypt<br />
was the source of almost all emerald in ancient times. Emerald material was found in<br />
mummies of the Pharaohs, and Empress Cleopatra had her portraits made in emerald<br />
(as gifts for high-ranking persons). The mines in Egypt were worked also during the<br />
Roman times, and continued by the Arabs and Turks. Today, most of the emerald<br />
comes from Colombia – from the famous mines at Muzo, Chivor and Cosquez. Other<br />
sources are northern Transvaal in the Republic of South Africa, Zimbabwe (Southern<br />
Rhodesia), India, Brasil, Australia and Russia (previously the Soviet Union – the<br />
emerald mines along the right banks of the Takovaya river in the Ural mountains).<br />
Aquamarine, the blue to greenish-blue variety of beryl, is also a popular<br />
gemstone. The name aquamarine comes from Latin (aqua = water, mare = sea),<br />
because the colour of aquamarine reminds of the colour of the sea. The biggest<br />
aquamarine ever mined was found in a pegmatite vein near the city of Marambaia,<br />
Minas Gerais, Brazil, in 1910. It weighed over 110 kg, and its dimensions were 48.5<br />
cm long and 42 cm in diameter. It was fragmented into smaller pieces which were<br />
cut into gems, and this single aquamarine crystal satisfied the world demand for this<br />
gem for three years.<br />
Morganite (or vorobievite) is a red to pinkish-violet beryl with a high<br />
caesium and lithium content (Cs 2<br />
O = 3.10; Li 2<br />
O = 1.39; H 2<br />
O = 1.92). Crystals are<br />
usually of a pyramidal shape, sometimes tabular (vorobievite). Apparently, morganite<br />
(vorobievite) was first found in the mines near the village of Lipovaya, northeast of<br />
Sverdlovsk in the eastern part of the Ural mountains. Vernadsky proposed that it<br />
be named after the Russian mineralogist V. I. Vorobiev (1875–1906) who did first<br />
crystallographic measurements of ther mineral. It was later also found on Madagascar,<br />
near the town of Maharitra, in the valley of the Sahatony river, and in the Pala area<br />
of San Diego county in southern California. Upon recommendation of the American<br />
mineralogist and gemmologist George F. Kunz, the name morganite was adopted in<br />
USA, in memory of the collector J. Pierpont Morgan.<br />
The colourless, transparent variety of beryl – called goshenite (after the<br />
locality Goshen, Massachussetts, USA) – is also a popular gemstone. The name<br />
heliodor (greek helios = sun, doros = gift) was given to a golden yellow variety of<br />
beryl first found in the Rössing mine on the Swakopmund – Windhoek railway line<br />
in Southwest Africa (now Namibia). Similar in colour is the golden beryl from Serro<br />
Juiz de Fora, Minas Gerais, Brazil and from USA (Litchfield, Massachussetts and<br />
Amelia Court, Virginia). In general, the coloured varieties of beryl make popular and<br />
beautiful gemstones, if these are sufficiently transparent and free from flaws.<br />
Aquamarine, morganite, goshenite, heliodor, golden beryl etc. are popular<br />
gemstones because of their beautiful, warm colours. Their hardness – greater than<br />
quartz – is also a property which makes the suitable for use as gems in jewellery.<br />
99
SILICATES<br />
Today, beryl is used not only as a gemstone and in jewellery, but also for<br />
other purposes. Large, nontransparent crystals, i.e. material which is not of gemstone<br />
quality is used in Spain as door-posts. Rolff reported in 1994 that a beryl crystal<br />
weighing ca. 200 tons was found in the state of Paraiba in Brasil. Another large<br />
crystal 9 m long and weighing 61 tons was found near Keystone in the Black Hills<br />
of South Dakota (USA). A beryl crystal found in a pegmatite near Albany, Maine<br />
(USA) was 5.5 m long and 1.2 m thick – the estimated weight was 18 tons.<br />
Beryl is also used as an ore in the production of beryllium metal. This is a<br />
silver-grey coloured metal, brittle at room temperature. The specific gravity is 1.81,<br />
melting point at 1285°C. Beryllium is lighter than aluminium which has a specific<br />
gravity of 2.712. It is used in industry in the production of beryllium bronzes and<br />
other alloys. An alloy containing 2.0% Be, 0.5% Co and 0.1% Si, the rest being<br />
copper, is used for the production of highquality wires and spirals. The wrought<br />
high strength alloys contain 1.6 to 2.0% beryllium and approximately 0.3% cobalt.<br />
The cast, high-strength alloys have beryllium concentrations up to 2.7%. The high<br />
conductivity alloys contain 0.2-0.7% beryllium and higher amounts of nickel and<br />
cobalt. These alloys are used in applications such as electronic connector contacts,<br />
electrical equipment such as switch and relay blades, control bearings, housings for<br />
magnetic sensing devices, non sparking applications, small springs, high speed plastic<br />
molds and resistance welding systems. Cast beryllium coppers are frequently used<br />
for plastic injection molds. The cast materials have high fluidity and can reproduce<br />
fine details in master patterns. Their high conductivity enables high production<br />
speed, while their good corrosion and oxidation resistance promotes long die life.<br />
A mixture of beryllium and radium was used as a neutron generator in<br />
nuclear chemistry laboratories, since beryllium releases a neutron and transforms to<br />
carbon when bombarded by alpha particles.<br />
The occurence of beryl at Mt. Motajica is interesting only for mineralogical<br />
reasons, and is of no other significance.<br />
CORDIERITE<br />
Mg 2<br />
Al 3<br />
[AlSi 5<br />
O 18<br />
]<br />
Crystal system and class: Orthorhombic, rhombic dipyramidal class.<br />
Lattice ratio: a : b : c = 1.748 : 1 : 0.954<br />
Cell parameters: a o<br />
= 17.13, b o<br />
= 9.80, c o<br />
= 9.35, Z = 4<br />
Properties: poor cleavage along {010}, parting parallel to {001}. Hardness = 7,<br />
specific gravity = 2.55-2.75 and increases with increasing iron content. Colour is<br />
light blue to blue violet, also colourless, grey, brown or yellow. Refractive indices<br />
100
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
also increase with increasing Fe content. RI very close to those of Canada balm.<br />
Birefringence is small, increases with increasing Fe content.<br />
X-ray data: depent on structure ordering (Tröger 1967, p. 355 and 358)<br />
d 8.58 (100), 3.05 (85), 4.09 (73) – mid temperature variety<br />
d 3.04 (100), 8.53 (69), 3.37 (47) – low temperature variety<br />
d 8.49 (100), 4.10 (54), 3.04 (54) – high temperature variety<br />
IR spectrum: 415 434 448 487 515 577 675 768 925 965 990 1023 1105 1170<br />
1650 cm -1<br />
Cordierite is a typical constituent of metamorphic rocks. In Bosnia and<br />
Hercegovina it occurs only in the cornite rocks of Mt. Motajica (Varićak, 1966).<br />
According to this author, cordierite is a significant constituent of biotite cornites<br />
which form the inner part of the contact zone.<br />
Cordierite occurs here mostly in the form of individual grains, and only<br />
occasionally shows cyclic twinning. The grains are small and not quite suitable for<br />
further microscopic investigations. Its alteration product is muscovite (sericite). The<br />
compositional percentage of cordierite in the cornites is rather variable within a<br />
range 0-20%.<br />
Apart from cordierite, the following minerals are present in the cornites:<br />
quartz, acidic plagioclase, garnet, tourmaline, apatite, zircon, magnetite, hematite,<br />
ilmenite and titanite (all accessory minerals).<br />
The genesis of the cornites of the inner part of the contact zone at Mt. Motajica<br />
is mainly bound to thermal alteration, but sometimes also to alkaline metasomatic<br />
alteration (Varićak 1966, p. 122 and 123).<br />
Clear blue cordierite is frequently used as a gemstone.<br />
TOURMALINE<br />
XY 3<br />
Z 6<br />
[(BO 3<br />
) 3<br />
│Si 6<br />
O 18<br />
│(OH) 4<br />
]<br />
The complicated chemical composition of tourmaline can be defined<br />
by the general formula as given above, where X is occupied by large ions like<br />
Na and Ca, Y is occupied by Mg, Li, Al, Fe 2+ , Mn, while Al, Fe 3+ , Ti 3+ , Cr 3+ are<br />
present at position Z. The significant variation in chemical composition results in<br />
a corresponding variation in properties (unit cell parameters, axial ration, optical<br />
properties, specific gravity).<br />
101
SILICATES<br />
Crystal system and class: Trigonal, ditrigonal-pyramidal class.<br />
Lattice ratio: a : c = 1 : 0.446 – 1 : 0.453<br />
Cell parameters: a o<br />
= 15.84-16.03, c o<br />
= 7.10-7.25, Z = 3<br />
Nomenclature: the varieties of tourmaline have different names and refers mainly<br />
to colour. The name tourmaline originates from the sinhalese language (turamali),<br />
and was first used for zircon. The name torumaline was first mentioned by Garmann<br />
in his book Curiöse Speculationes bei Schlaflosen Nächten – von einem Liebhaber<br />
der immer gern Speculiert (Curious speculations during sleepless nights – by a<br />
connosieur who likes speculating), Chemnitz and Leipzig 1707, p. 269. This name<br />
was used for the orange-red variety brought from Sri Lanka (Ceylon) by the Dutch<br />
in 1703. The name schorl was already used in Europe for the dark coloured variety<br />
of the mineral. The czech name of škoril or skoril is based on schorl (Katzer 1926,<br />
p. 68). Nowadays this name is used for the dark iron-rich variety. Achroite (greek<br />
ahroos = colourless) is a colourless or faintly greenish tourmaline which shown<br />
no pleochrosim in thin section. Achroite crystals from the island of Elba (thus the<br />
name elbaite) are often dark coloured at one end – such varieties are referred to as<br />
negro’s head. Rubelite (latin rubellus – reddish) or siberite (after Siberia) or apyre<br />
(greek apyros – fireproof, since it does not melt under a blowpipe) is red tourmaline,<br />
indigolite is blue, verdelite (italian verde – green) is green. Crystals which are red<br />
on one end are called turkish head in Brazil. The chrome-rich varieties from the<br />
Ural mountains are deep green. Dravite is the magnesium rich variety (brownish to<br />
greenish in colour) found in the gneiss rocks at Dobrava near the city of Dravograd<br />
in Slovenia. The mineralogist Tschermak gave this variety this name in honour of the<br />
river Drava. The black tourmaline from Kragerö in Norway is sometimes referred<br />
to as africite (greek afrizo – to foam) because it foams when heated with a blowpipe<br />
Properties: cleavage along {11-20} and {10-10} is very weak. The colour of<br />
tourmaline depends on its chemical composition. Refractive indices vary – No<br />
1.639-1.692, Ne 1.620-1.657, maximum birefringence is 0.017-0.046, specific<br />
gravity 3.0-3.25. Mohs hardness is 7-7.5. Crystals can be fully transparent to opaque.<br />
Tourmaline has distinct pyro- and peizoelectric properties. In his abovenamed book,<br />
Garmann notes that the tourmaline brought to Europe by the Dutch in 1703 at first<br />
attracts the ash of burning peat, but releases it immediately thereafter. Because of<br />
this, the Dutch called it Aschentrecker, meaning one who attracts ash. A similar, but<br />
unsuccessful attempt at nomenclature was by Ž.Vukasović in 1864 when he wanted<br />
to name tourmaline „vucipepeo“ (ash-attracter).<br />
102<br />
TOURMALINE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Čelebić (1967), Đorđević (1969), Foullon (1893), Gaković and<br />
Gaković (1973), Jakšić (1927), Jeremić (1963 and 1963a), Jurković (1954, 1956,<br />
1958, 1958a, 1961 and 1962), Jurković and Majer (1954), Jović (1965), Katzer
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
(1924 and 1926), Kišpatić (1912 and 1915), Koch (1899 and 1908), Magdalenić<br />
and Šćavničar (1973), Marić (1927 and 1965), Marić and Crnković (1961), Markov<br />
and Mihailović-Vlajić (1969), Mihailović-Vlajić (1967), Mudrenović and Gaković<br />
(1964), Pavlović (1962, 1963 and 1964), Pavlović, Ristić and Likić (1970), Podubsky<br />
(1968 and 1970), Primics (1881), Ramović (1957), Ristić, Likić and Stanišić (1968),<br />
Šćavničar and Trubelja (1969), Tajder and Raffaelli (1967), Tućan (1911 and 1912),<br />
Varićak (1966), Zarić, Đorđević and Vilovski (1971).<br />
1. Mt. Motajica<br />
It seems that Koch (1899 and 1908) was the first to describe tourmaline<br />
from a pegmatite vein mainly composed of feldspar, quartz, muscovite and beryl. In<br />
addition to tourmaline, the other accessory minerals are stilbite, talc, fluorite, pyrite<br />
and psilomelane. This vein was found in the Veliki Kamen quarry near Vlaknica.<br />
According to Koch, the mineral is black, occuring in the form of aggregates<br />
attached to the feldspar. Koch maintains that this tourmaline is brittle and parts<br />
easily along {0001}, and that good cleavage can be seen under the miscroscope.<br />
It appears that Koch misinterpreted parting for cleavage in this case. Zonation can<br />
be seen along the [0001] axis. A blue-grey to yellow-brown colour can be seen in<br />
thin section. Koch also mentions pleochroism which cannot be interpreted with<br />
known optical properties of tourmaline. For the blue-grey tourmaline he notes<br />
the following pleochroism – a = yellowish-grey // c = darkgrey. For the yellowbrown<br />
tourmaline the pleochroism is a = reddish-yellow // c = black. The first<br />
argument against the obeservations made by Koch is that absorption along the c<br />
axis = [0001] i.e. for the extraordinary ray, would be stronger than for the ordinary<br />
ray. This situation has never been identified for tourmaline, and all observations<br />
indicate the opposite case, i.e. pleochroism O > E.<br />
The second argument against Kochs observation lies in the fact that<br />
he described the second vibrational direction as being in the plane of the three<br />
crystallographic axes perpendicular to [0001]. Such a specification is incorrect in<br />
terms of optical theory. The absorption for this vibrational direction is independent<br />
of its propagation within the plane perpendicular to [0001], as long as it is confined<br />
to this plane. Therefore, the description of the pleochroism of tourmaline from the<br />
Veliki Kamen pegmatite as given by Koch could probably be corrected in saying<br />
that the pleochrosim is as follows – along [0001] yellowish-gray to reddish-brown //<br />
perpendicular to [0001] bluish-grey to black, as is the case for schorl.<br />
In a later report Koch (1908, p. 4) writes that tourmaline occurs only<br />
infrequently in the granite of Veliki Kamen, and then incorporated into feldspar<br />
and quartz. However, tourmaline is common in the pegmatite veins of this granite,<br />
contrary to Koch’s statements (1899, p. 12).<br />
103
SILICATES<br />
Tourmaline of a bluish colour occurs in the muscovite granite in the Brusnik<br />
quarry. It is of a very fine grain and is usually contained within orthoclase (Koch<br />
1908, p. 5). It can be sometimes seen in the biotite granite-gneiss from Židovski<br />
potok (Koch 1908, p. 6). Some sections of the muscovite gneiss from Studena<br />
Voda contain considerable amounts of pink tourmaline with a strong pleochroism<br />
(Koch 1908, p. 7). Pegmatite veins, ca. 1 cm thick, are common within this gneiss<br />
and they are mainly composed of black tourmaline, dark quartz, sometimes also<br />
orthoclase. The thin and needlelike tourmaline crystals appear like a fabric and are<br />
often incorporated in the quartz. They show high pleochroism.<br />
The highly weathered biotite gneiss from the Osovica creek near Šeferovac<br />
contains minor amounts of tourmaline in the form of thick hexagonal or prismatic<br />
crystals of deep pink colour (Koch 1908, p. 10). Koch (1908) also mentions tourmaline<br />
in micaschists of Mt. Motajica – in the biotite schists of Puljana kosa, and from the<br />
Manastirica and Osovica creeks near Šeferovac. In thin section these tourmalines are<br />
bluish or greenish-blue and display strong dichroism. Short prismatic crystals are<br />
found in Manastirica creek and Šeferovac, some of them have terminal pyramidal<br />
forms. Substantial amounts of tourmaline can be found in the micaschists outcropping<br />
between Galešna kosa and Vinograc near Davor (Koch 1908, p. 15). Some crystals<br />
have terminal pinacoid or pyramidal forms, sometimes a hemimorphic habit. Thin,<br />
needlike crystals can occasionally be seen – these are often bent or broken.<br />
The chiastolite schists of Vinograc contains greenish-blue, prismatic<br />
tourmaline crystals of a hemimorphic habit and with a characteristic parting. Koch<br />
mentions that larger crystals contain some finegrained black carbon-like material.<br />
This finding also warrants caution, as it seems more likely that this material are<br />
opaque iron minerals which are frequently found in a dispersed form in alteredosed<br />
schists (Tröger 1967, p. 192). Koch also mentions significant amounts of tourmaline<br />
in the argillaceous schists in Osovica creek. The crystals are very small, sometimes<br />
displaying terminal faces. They are mainly of a brown colour, but also pink and<br />
violet sections can be seen indicating a variable dichroism. Zonal structure of the<br />
crystals is common.<br />
Koch’s data have been referenced by Katzer (1924 and 1926) who mentions<br />
that black tourmaline is a frequent accessory mineral of the Mt. Motajica granite.<br />
Sometimes, ‘tourmaline stars’ (radial aggergates of needlelike crystals) can be seen.<br />
Using the Fersman diagrams for granites and pegmatites (1932, p. 320<br />
and 361; 1939, p. 258-259), the conclusion can be made that the fractionation of<br />
tourmaline in the Mt. Motajica granite occurred within a broad range of temperatures.<br />
The ‘tourmaline stars’ (schorl) indicate a high fractionation temperature (ca. 800 °C,<br />
around boundary conditions for the magmatic/epimagmatic phases). The prismatic<br />
104
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
tourmaline noted by Koch imply lower temperatures, i.e. the pegmatitic phase of<br />
the pneumatolite sequence (ca. 600°C). Even lower temperatures were suitable for<br />
the formation of transparent brown, green and pink tourmalines, while the needlike<br />
shorls of the Galešina kosa schists formed during the hydrothermal stage (temperatures<br />
around and below 400°C).<br />
Ramović (1957, p. 38) briefly mentions black tourmaline in pegmatite veins<br />
at Vlaknica quarry, occuring in association with feldspar, quartz, beryl, fluorite,<br />
pyrite, zeolite and molybdenite.<br />
Varićak (1966, p. 64-165) describes tourmaline as a significant constituent<br />
of pegmatites and pneumatolites in normal granite, leucocratic granite, aplite<br />
granite, granitic porphyres and vein rocks. The torumaline contained in these vein<br />
rocks (Varićak 1966, p. 101) has strong pleochroism – darkgreen (ordinary ray),<br />
brownish-pinkish (extraordinary ray). Grains are up to 15 x 3 mm in size. Markov<br />
and Mihailović-Vlajić (1969, p. 256) note that tourmaline is widely distributed in the<br />
Mt. Motajica pegmatites.<br />
2. Brestovsko<br />
Jurković (1954) mentions tourmaline as a constituent mineral of the<br />
actinolite-epidote schists at Hrastovi hill near Brestovsko in the schist mountains of<br />
central Bosnia. These schists feature a barite vein with an average thickness of 30-40<br />
cm (the range being 10-100 cm). This schist forms part of a transitional pneumatolite<br />
to hydrothermal ore-body, and displays significant alteration features, including the<br />
presence of tourmaline. However, the barite also contains another tourmaline phase<br />
which crystallized within a higher temperature range. This ‘older’ tourmaline occurs<br />
in the form of short prismatic crystals in a size range between 8 x 35 to 50 x 200µm.<br />
Microscopic investigations on mostly idiomorphic grains revealed the presence of<br />
typical cracks. The crystals usually have pyramidal terminal faces, while sections<br />
perpendicular to the c axis have trigonal habit. Extinction is parallel, the pleochroism<br />
is very intense – pinkish-brown parallel to the c axis, and dark green perpendicular<br />
to the c axis. In reflected light, the tourmaline has a stronger degree of reflection<br />
than barite and quartz. Bireflection is significant (light grey parallel to c, dark grey<br />
perpendicular to c). The ore body underwent significant tectonic activity, which is<br />
the reason for the orientation of tourmaline (also magnetite and pyrite) parellel to the<br />
flanks of the vein.<br />
Jeremić (1963a, p. 32) notes that in the Potplane – Kreševo area tourmaline<br />
occurs less frequently and that it is related to the Palaeozoic-age barite ore body.<br />
Small quantities of tourmaline are also present – together with magnetite and other<br />
high-temperature minerals – in the Podljetovik – Brestovsko barite formation.<br />
105
SILICATES<br />
3. Vrtlasce – east of Fojnica, Trošnik – south of Fojnica and Čemernica<br />
Jurković (1958a, p. 311) describes the occurrence of tourmaline in the flanks<br />
of the ore vein at the Vrtlasce ore body near the village of Klisac, where it comes<br />
as a primary mineral in dark grey sericite-quartz schists, chlorite schists and sericitecontaining<br />
quartzporphyres. The alteration process resulted in the formation of<br />
tourmaline, rutile, sericite, quartz and albite. The same author believes that tourmaline<br />
is the high-temperature primary mineral in the Trošnik ore body near Fojnica, where<br />
the tourmaline occurs together with rutile, zircon and apatite, although a microscopic<br />
investigation of these rocks did not reveal the presence of tourmaline.<br />
Jurković (1956 and 1962, p. 143, 149) also identified tourmaline in the<br />
antimonite ore body in the area of Čemernica creek, 3 km north of Fojnica in quartz<br />
veins within schist rocks. Most rocks in the Zahor ore complex – the Završće creek<br />
area, Donje Selo (Ormanov creek) and Selišće – are significantly tourmalinized.<br />
4. Banjak and Hrmza<br />
Jurković (1961, p. 205) identified tourmaline as a common mineral in the<br />
realgar- and auripigment-containing formations, where it occurs in the flanks of the<br />
ore body. The tourmaline crystals are prismatic, in a size range between 10 x 60 µm<br />
and 40 x 150 µm. Pleochroism is strong – dark green parallel to c, light brown<br />
perpendicular to c.<br />
Jurković (1961, p. 221) noted a similar occurrence of tourmaline at the Hrmza<br />
ore body. The prismatic tourmaline crystals are associated with rutile, sometimes<br />
also fluorite.<br />
5. Mt. Vranica<br />
Foullon (1893, p. 7) mentions torumaline as a very rare accessory mineral in<br />
the quartz-porphyres of Mt. Vranica, with no mention of precise locations where it<br />
was found. The small and ill-formed crystals are of a dark blue colour in transmitted<br />
light. This information was later referenced by Katzer (1926, p. 185). Foullon also<br />
identified tourmaline in the mining concentrates left over at the abandoned mine of<br />
Crvena zemlja, as well as in the clayey soils from the northern flanks of Nadkrstac,<br />
in the sand from the stream sediment of the Ljuti potok creek, in the clays of Tješilo<br />
near Fojnica and in the sands from a limestone-hole called Bosanska Idrija on Mt.<br />
Zec where cinnabar was mined (Foullon 1893, p. 32 and 33). This tourmaline is<br />
brownish-pink in colour, displaying sharp edges of its hemimorphic crystals. Due to<br />
the fact that Foullon found such tourmalines in all schists from the area (i.e. Rosin,<br />
Čemernica) his conclusion was that it was genetically associated with the schists.<br />
106
6. Alinovci near Jezero<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Jurković and Majer (1954, p. 224) noted an occurrence of tourmaline in the<br />
10-30 cm thick vein at the contact of a schistlike rhyolite (quartzporphyre) and limestone.<br />
According to these authors, the amount of tourmaline is highest in the central portion<br />
of the contact vein, diminishing towards the sections closer to the contact. They also<br />
mention tourmaline in the barite deposits of the schist mountains of central Bosnia,<br />
at Kolovoje (Deževica), Ljetovik (Kiseljak) and Brestovsko (Busovača), as well as at<br />
the antimonite-sphalerite ore body at Selišće (Fojnica) and the pyrrhotite-cassiterite<br />
deposit at Vrtlasce (Fojnica). According to these authors, the presence of tourmaline<br />
in these formations indicates a close relationship between Permian magmatic activity<br />
resulting in the formation of the quartzporphyres and the mentioned ore bodies.<br />
Tourmaline in rocks of the schist mountains of central Bosnia was also<br />
mentioned by Šćavničar and Trubelja (1969) and Tajder and Raffaelli (1967).<br />
7. The Jablanica gabbro and Tovarnica<br />
Marić (1927, p. 53) identified short prismatic torumaline crystals within<br />
cracks in the weathered protions of the gabbro, at their contact with Werfen-age<br />
schists, near the village of Čehar on the left bank of the Neretva river. The inner<br />
surfaces of these cracks are covered with green epidote crystals, intergrown with<br />
tourmaline. The formation of these minerals is related to intense weathering of both<br />
rock types. Marić (1927, p. 55) dismisses the possibility of a contact-metamorphic<br />
zone in this area, even though igneous rocks are in close proximity.<br />
Cissarz (1956) later found that a zone of contact metamorphism was<br />
evidently present, especially on Tovarnica (a more detailed description of this are<br />
was given in the section on garnets).<br />
During a geological mapping campaign in this area (Pavlović 1962, 1963 and<br />
1964), tourmaline and wollastonite were identified in the magnetite-bearing section of<br />
the metamorphic contact-zone. The tourmaline occurs in the form of regular hexagonal<br />
prismatic crystals up to 3 mm in size and bluish-grey in colour, displaying strong<br />
pleochroism. This information was later corroborated by Čelebić (1967, p. 97-99).<br />
8. Srebrenica<br />
Đorđević (1969) identified tourmaline-bearing rocks within an area od 2<br />
km 2 at the Srebrenica mine. The younger dacite and andesite rocks are affected by<br />
alteration processes (mainly sericitization, kaolinization, calcitization, silification)<br />
contain tourmaline as well as the older Palaezoic-age metasandstones and<br />
argillaceous schists).<br />
107
SILICATES<br />
The tourmaline-quartz containing rocks show a high degree of silification<br />
and thus macroscopically resemble proper quartzites. The rocks are usually very<br />
hard with a cavernous texture, grey or greyish-yellow in colour. Veins composed of<br />
quartz and tourmaline intersect these host rocks in various directions. Microscopic<br />
investigations of these mostly dark veins show a microgranitic matrix with<br />
occasionally corroded quartz crystals and tourmaline, probably implying alteration<br />
of older dacites. More finegrained rocks without phenocrystals and composed of<br />
quartz, tourmaline and mica are also found. The amount of tourmaline in some thin<br />
sections approaches 70%.<br />
Tourmaline usually occurs in the form of radial aggerates. Prismatic crystals<br />
are comparatively rare, although – when found – their size is in the range of 0.1<br />
to 1 mm. It displays uniaxial-negative optical properties, with parallel extinction.<br />
Pleochroism is distinct – greyish-blue to dark blue. Refractive indices, established<br />
by the immersion method are Ne = 1.625, No = 1.648. Small prismatic crystals with<br />
no discernible pleochroism can also be found. The presence of tourmaline was also<br />
determined by XRD, DTA and spectrographic measurements.<br />
The 0.1-0.2 size fraction of tourmaline showed endothermic peaks at 150°C,<br />
and between 430 and 480°C and 750-770°C indicating a loss of water upon heating.<br />
A broad endothermic peak at 950-1000°C implies a loss of B 2<br />
O 3<br />
.<br />
X-ray diffraction using Cu Kα1<br />
radiation (λ = 1.540 A) and a Ni filter indicates<br />
a rubelite (Li tourmaline) composition for the tourmaline.<br />
The B content, established by spectrographic techniques, is around 10000<br />
ppm (1%).<br />
9. South-western Bosnia<br />
In south-western Bosnia tourmaline occurs in sedimentary rocks as an<br />
authigenic mineral. In the area around Kulen-Vakuf tourmaline was found in the<br />
Permian-age sandstones and red clastic rocks with gypsum. Tourmaline was identified<br />
in the heavy mineral fraction and is present in amounts ca. 0.1-1.5%. Magdalenić<br />
and Šćavničar (1973, p. 141) established that this heavy mineral fraction consists<br />
primarily of zircon and tourmaline. The authigenic greenish or bluish tourmaline<br />
frequently grows upon older tourmaline, parallel to the c axis = [0001] and in the<br />
same optical orientation. Individual crystals of authigenic green tourmaline are less<br />
frequently found. The older tourmaline fractions are usually abraded and subangular,<br />
with no terminal faces. Their size is in the range 0.05-0.20 mm. Their colour is<br />
mostly brownish, sometimes brownish-green, with a black carbon-like filling of<br />
some hollow crystals. In this case also, this black material probably are opaque<br />
iron minerals (see the section on Koch’s investigations of the tourmaline from Mt.<br />
Motajica). This tourmaline has strong pleochroism (O = dark brown, dark green<br />
108
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
to black, E = brown, greenish-brown). Refractive indices are No = 1.645-1.648,<br />
Ne = 1.624-1.627. The autigenic tourmaline commonly occurs in the form of<br />
composite, rod-like crystals which grow at different growth rates so that their<br />
terminal faces show a sawtooth-like habit. The optic character is negative, the<br />
refractive indices being No = 1.646 ± 0.001, Ne = 1.621 ± 0.001. The pleochroism is<br />
fairly strong – O = intense green or dark bluish-green, E = pale green or pale brown.<br />
The ratio of detrital and authigenic tourmaline varies in the range 1:0.2 to 1:4.5.<br />
The newgrown sections of the tourmaline are completely preserved, inspite<br />
of their delicate texture, indicating that they grew in the same position in which they<br />
are found today. There are no indications that this tourmaline formed elsewhere and<br />
was redeposited in quartz sandstones.<br />
Jović (1965) identified authigenic tourmaline in the heavy mineral fraction of<br />
Miocene-age sandy calcarenites from Lupina near Kulen-Vakuf. Epidote and zoisite<br />
are further common constituents of this fraction. The core of the detrital tourmalines<br />
is mostly green, while the overgrowth of authigenic tourmaline shows a pale blue or<br />
no colour at all. The crystal faces of authigenic tourmaline are sometimes slightly<br />
pitted on the surface. The occurrence of authigenic tourmaline in Miocene sediments<br />
of the Kulen-Vakuf area should be understood in terms of the hydrothermal activity<br />
of boron.enriched groundwaters (Magdalenić and Šćavničar 1973, p. 119). The<br />
boron enrichment is probably related to the underlying evaporites in the area.<br />
10. Tourmaline in other rocks<br />
Kišpatić (1912, p. 539) identified tourmaline in bauxites of Studena Vrela<br />
near Županjac. The tourmaline grains are ca. 0.05 x 0.015 in size and display distinct<br />
pleochroism – O = blue, E = colourless to grey.<br />
Tućan (1912, p. 424) found tourmaline as an accessory mineral in dark red<br />
and yellowish crljenica soil (terra rossa) near Eminovo Selo, close to Županjac. The<br />
attractive short-prismatic and hemimorphic crystals are up to 0.1 mm in size and<br />
display the following pleochroism – O = greenish or brownish, E = colourless, light<br />
green to light brown. In a later paper Kišpatić (1915, p. 54) briefly describes the<br />
finding of tourmaline in bauxite from the hill on which the abbey of Lištica (Široki<br />
Brijeg) in Hercegovina is located, noting that tourmaline is ubiquitously present,<br />
but in minor amounts. Jakšić (1927, p. 95) describes the location of the finding as<br />
Dubrava Greda, south-east from the abbey, at Stražnica (362 m a.s.l.).<br />
According to Tućan (1911, p. 798) the source of tourmaline in terra rossa<br />
and bauxite of our karst regions are the limestones and dolomites which contained<br />
small amounts of tourmaline as an accessory, primary and authigenic mineral. Tućan<br />
(1912, p. 405) believes that the red soil (terra rossa) is nothing but the insoluble<br />
residue which remains after the weathering and erosion of these limestones and<br />
109
SILICATES<br />
dolomites. Kišpatić (1912) maintained that terra rossa and bauxite are identical, due<br />
to the similarity of their mineral compositions. In his treatise of terra rossa, Marić<br />
(1965) also notes the tourmalines identified by Kišpatić and Tućan.<br />
Some small, prismatic tourmaline crystals were found in the insoluble residue<br />
of limestone from Varoški potok, the left tributary of the Zalomska river between<br />
Kifina Sela and Gacko in Hercegovina. They show well preserved crystal forms,<br />
indicating very little or no transport at all (Mudrenović and Gaković 1964, p. 143).<br />
This location has also been described by J. Gaković and M. Gaković (1973, p. 137).<br />
Marić and Crnković (1961, p. 144 and 156) found some crushed tourmaline<br />
crystals in the dark Paleozoic-age schists of the Brdo surface mine in the mining<br />
area of Ljubija.<br />
Podubsky (1968) also notes the occurrence of tourmaline in Paleozoic<br />
rocks of north-western Bosnia – as an accessory mineral in argilaceous schists and<br />
metasandstones of lower Palezoic age (Carbon-aged rocks at Mala Rijeka close<br />
to Trnova), in the Permian-Triassic sandstones and schists as well as sediments of<br />
lower Triassic age – sandstones and schists containing feldspar, hematite, limonite,<br />
quartz and sericite (Podubsky 1968, p. 174-189).<br />
Podubsky (1970) gives similar information also for eastern Bosnia. Here<br />
the Paleozoic-age phyllites and phyllite-schists, clay schists and metasandstones<br />
contain tourmaline an accessory mineral. The biotite-tourmaline-epidote-quartzamphibole<br />
schists of Mlječvanska Rijeka were apparently formed by alteration o<br />
tuffs (Podubsky 1970, p. 160-169).<br />
Pavlović, Ristić and Likić (1970, p. 232 and 235) described the heavy mineral<br />
fraction (ca. 1.5%) of quartz sands from the Miladije and Bukinje ore bodies in the<br />
Tuzla basin, noting that about half of this fraction consists of opaque minerals and<br />
picotite, while the rest is composed of tourmaline, iron oxides, epidote, amphiboles,<br />
garnets, rutile, pyroxene and other minerals. Likewise, the heavy mineral fraction<br />
of the sarmatian-pontian sands of the Tuzla basin, contains 2.7-4.1 % tourmaline<br />
(Ristić, Likić and Stanišić 1968).<br />
Irregular and corroded grains of tourmaline are the accessory mineral phase<br />
of sandstones outcropping near Banja Slatina, some 10 km north-east of Banja Luka<br />
(Zarić, Đorđević and Vilovski 1971, p. 217). The tourmaline has distinct pleochroism<br />
in pale green and dark green colours.<br />
It is interesting to note that the earliest information on tourmaline was provided<br />
by Primics (1881) related to its occurrence in extrusive rocks around Žepče and Maglaj.<br />
110<br />
The various coloured varieties of tourmaline are regularly used as gems.
PIGEONITE<br />
(Mg, Fe 2+ , Ca) 2<br />
[Si 2<br />
O 6<br />
]<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Cell parameters: a o<br />
= 9.69 -9.71, b o<br />
= 8.92 - 8.96, c o<br />
= 5.24-5.25, β = 108° 33’<br />
Properties: pigeonite is the term for an isomorphous series between clinoenstatite<br />
and diopside. The main difference from other pyroxenes is the small optic axial<br />
angle which shows a large variation range; +2V = very small to 40°.<br />
X-ray data: almost identical with clinoenstatite (Tröger 1967, p. 388)<br />
A u t h o r s: Pamić (1957), Simić (1964), Šibenik-Studen and Trubelja (1967<br />
and 1971).<br />
Pigeonite, a member of the monoclinic pyroxene minerals, has not been<br />
studied in any detail in Bosnia and Hercegovina. Pamić (1957) notes that pigeonite<br />
occurs together with augite and other minerals in dolerites (diabases) of Donja<br />
Grkarica on Mt. Bjelašnica. As opposed to augite which has an angle 2V = + 58°<br />
and an extinction angle of 44°, pigeonite has a substantially smaller 2V angle = +<br />
36°, and an extinction angle of 32°. Simić (1964) noted similar optical constants for<br />
pigeonite in basic igneous rocks from the Rača creek near Sarajevo. The 2V angle of<br />
this pigeonite is 36°, the extinction angle c : Z = 37°.<br />
Šibenik-Studen and Trubelja (1971) identified pigeonite phenocrystals in dense<br />
porhyric diabase from the locality of Kovačići, on the eastern part of Mt. Konjuh. The<br />
same authors made a microscopic identification of pigeonite in basalts of the village of<br />
Đihanići in the valley of the river Vrbas, between Donji Vakuf and Jajce.<br />
DIOPSIDE<br />
CaMg [Si 2<br />
O 6<br />
]<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 1.092 : 1 : 0.589; β = 105° 50’<br />
Cell parameters: a o<br />
= 9.73, b o<br />
= 8.91, c o<br />
= 5.25, Z = 4<br />
Properties: pronounced cleavage parallel to {110}, with occasionally distinct parting<br />
along {100} or {001}. A variety of diopside with very clear parting along {100}<br />
was earlier referred to as diallage, which was also the variety enriched in Al and<br />
Fe. Hardness is 6, the specific gravity 3.25-3.55 and increases with Fe content. The<br />
varieties depleted in Fe are colourless or white, or dark green to black (hedenbergite)<br />
when enriched with Fe. Lustre is vitreous. Streak white to grey. Refractive indices<br />
are high: Nx = 1.650-1.698 Ny = 1.657-1.706 Nz = 1.681-1.727<br />
X-ray data: d 2.99 (100), 2.53 (40), 2.89 (30) – ASTM-card 11-654<br />
IR-spectrum: 405 475 512 635 672 868 925 970 1080 cm -1<br />
111
SILICATES<br />
DIOPSIDE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Baumgärtel (1904), Džepina (1970), Foullon (1893), Golub<br />
(1961), Katzer (1924 and 1926), Kišpatić (1897, 1900, 1904b), Majer (1962), Marić<br />
(1927), Pamić (1969a, 1970, 1971, 1971a, 1972, 1972c, 1972d, 1973 and 1974),<br />
Pamić, Šćavničar and Međimorec (1973), Pamić and Trubelja (1962), Ristić, Pamić,<br />
Mudrinić and Likić (1967), Schiller (1905), Sijarić and Šćavničar (1972), Tajder<br />
(1953), Trubelja (1960, 1961), Trubelja and Pamić (1965), Varićak (1966).<br />
Diopside is widely distributed in Bosnia and Hercegovina, mainly within<br />
the Bosnian serpentine zone (BSZ), where it is an important constituent of basic and<br />
ultrabasic as well some metamorphic rocks.<br />
Outside of the BSZ diopside is often the predominant mineral of some<br />
differentiates of the gabbro complex near Jablanica, as well in certain dacites around<br />
Srebrenica. Diopside has also been found in rocks at Mt. Motajica.<br />
Available information on diopside is still relatively scant and incomplete,<br />
although the mineral is mentioned in numerous articles dealing with various<br />
petrographic issues in Bosnia. The reason for this probably lies in the fact that<br />
researchers were unable to precisely determine monoclinic pyroxenes solely on<br />
the basis of microscopic investigations. Therefore, numerous publications make<br />
reference to diopside-diallage or some other similar nomenclatorial combination.<br />
112<br />
1. Diopside in rocks of the Bosnian serpentine zone<br />
Kišpatić (1897, 1900, 1904b) investigated microscopically numerous<br />
samples of serpentine-peridotite rocks (lherzolites) originating from the Bosnian<br />
serpentine zone (BSZ), finding diopside in all of these rocks. According to this author,<br />
diopside is the dominant mineral in lherzolites from various localities at Mts. Kozara,<br />
Uzlomac, Borje, Ljubić and Ozren as well as around the town of Višegrad. Diopside<br />
also occurs in troctolites at Snagovo near Zvornik and in pyroxene amphibolites<br />
from Mt. Borje.<br />
The treatise by Kišpatić (1897 and 1900) deals mainly with microscopic<br />
determinations of diopside, but contains also two quantitative chemical analyses of<br />
this mineral (Table 14)<br />
Table 14. Chemical composition of diopside from the Bosnian serpentine zone<br />
Sample 1 Sample 2<br />
SiO 2<br />
50.62 50.84<br />
Al 2<br />
O 3<br />
3.98 0.42<br />
FeO 7.20 7.17
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
CaO 19.39 21.48<br />
MgO 15.76 16.54<br />
Cr 2<br />
O 3<br />
traces traces<br />
Loss on ignition 3.20 4.23<br />
Sample 1: green diopside from the Milakovac chromium mine<br />
Sample 2: green diopside from lherzolite rock, Pobilje, Vareš<br />
100.15 100.68<br />
Diopside in the pyroxene amphibolite of Mt. Borja is of a colourless or green<br />
variety, occuring as large foliated crystals (Kišpatić 1904b). It has no pleochroism.<br />
The extinction angle is 41°, maximum birefringence Nz – Nx = 0.027.<br />
Golub (1961) provides some more recent data about diopside in ultrabasic<br />
rocks of Mt. Kozara. The diopside in lherzolite samples from Jovača creek is of<br />
a finely crystalline variety and a variable 2V angle in the range +54° – +57°. The<br />
average value of the extinction angle is 37.8°. In lherzolites from the Vrela creek,<br />
diopside has an average 2V angle of +54º, and an extinction angle c : Z = 37°. It<br />
shows a good prismatic cleavage and parting along [100].<br />
Majer (1962) found minor amounts of monoclinic pyroxene with diopside<br />
characteristics in amphibole and garnet gabbros, as well as hornblendites in the BSZ<br />
section between the Bosna and Vrbas rivers.<br />
Pamić (1969a, 1972c) identified an omphacite-type diopside in the<br />
amphibolites of Mt. Skatovica. This diopside has an elevated 2V angle between +60°<br />
and +62° and an extinction angle of 36° to 43°. Diopside from metamorphic rocks<br />
often has distinct pleochroism in different saturations of green. Greenish diopside<br />
of the omphacite type (enriched with the jadeite molecule) occurs also in pyroxene<br />
schists which outcrop on Mt. Skatovica together with the amphibolites and peridotites.<br />
According to Pamić, diopside in ultrabasic rocks has somewhat different properties<br />
than the one in amphibolites – the ultrabasic diopside has no pleochroism and a 2V<br />
angle in the range +53° to +55°. Pamić, Šćavničar and Međimorec (1973) published<br />
the results of three chemical analyses of diopside from metamorphic rocks (Table 15):<br />
Table 15. Chemical composition of clinopyroxene from Mt. Skatovica and Mt. Čavka<br />
Sample 1 Sample 2 Sample 3<br />
SiO 2<br />
51.2 51.1 49.9<br />
TiO 2<br />
0.38 0.45 0.60<br />
Al 2<br />
O 3<br />
6.1 5.8 6.3<br />
FeO 8.3 10.6 10.7<br />
MnO 0.09 0.09 0.11<br />
MgO 11.3 10.5 10.5<br />
113
SILICATES<br />
CaO 20.4 18.2 20.4<br />
K 2<br />
O 0.03 0.03 0.03<br />
Na 2<br />
O 1.7 2.8 1.4<br />
99.50 99.57 99.94<br />
Composition Di 62<br />
Hd 26<br />
Jd 12<br />
Di 56<br />
Hd 24<br />
Jd 20<br />
Di 59<br />
Hd 31<br />
Jd 10<br />
Samples 1 and 2: Mt. Skatovica, Banja Luka; Sample 3: Mt. Čavka, Teslić<br />
Džepina (1970) found diopside to be the dominant mineral of the garnetbearing<br />
metamorphic rocks from the souther flanks of Mt. Borja. A microscopic<br />
study showed that in thin section the diopside is colourless to pale green, while the<br />
more intensely coloured varieties have a larger percentage of the jadeite molecule.<br />
Peripheral alteration into hornblende can sometimes be seen. This author maintains<br />
that diopside is a component of different parageneses found in various locations.<br />
For example, the paragenesis of the Crni potok creek is of the hornblende-diopsidegarnet-plagioclase<br />
type; that of Velika Usora is a diopside-plagioclase-hornblendegarnet<br />
paragenesis; while that of Borovnica is of the hornblende-diopside-garnetprehnite<br />
type.<br />
Pamić (1971a) found diopside to be a common mineral in amphibolites<br />
associated with ultrabasic rocks in the Krivaja – Konjuh area.<br />
Baumgärtel (1904) identified a green chromediopside in the lherzolites of<br />
Duboštica. Pamić (1970) provides a more detailed account and chemical analysis<br />
data of this diopside – SiO 2<br />
= 51.11, TiO 2<br />
= 0.15, Al 2<br />
O 3<br />
= 0.68, Fe 2<br />
O 3<br />
= 1.16,<br />
Cr 2<br />
O 3<br />
= 0.81, FeO = 2.19, MnO = 0.15, MgO = 18.80, CaO = 22.42, Na 2<br />
O = 1.24,<br />
K 2<br />
O = 0.38, H 2<br />
O - = 0.27, Total = 99.96<br />
Pamić maintains that chromdiopside often is the only indicator of chromite<br />
ore deposits. It is of minor importance in the Rakovac area, but occurs frequently at<br />
Borak, Šabanluke and other localities around Duboštica. It is easily recognized by<br />
its shining, almost emerald-green colour. However, chromamphibole is of a very<br />
similar colour, and when the two minerals occur together macroscopic identification<br />
may prove difficult. The chromediopside sometimes forms monocrystals of<br />
centimeter length, with clear parting along the pinacoid. Pleochroism can be seen<br />
only sometimes, in thicker thin sections. The 2V angle is +63°, the extinction angle<br />
38°, and the maximum birefringence Ny – Nx = 0.033.<br />
Sijarić and Šćavničar (1972) have made XRD determinations of diopside<br />
in numerous serpentinized peridotites from Mt. Konjuh which are associated with<br />
the Miljevica magnezite veins. Ristić et al. (1967) have performed microscopic<br />
determinations and chemical analyses of monoclinic pyroxene from the Dinkovac<br />
114
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
lherzolites. Their chemical composition is as follows – SiO 2<br />
= 48.98, TiO 2<br />
= 0.10,<br />
Al 2<br />
O 3<br />
= 4.01, Fe 2<br />
O 3<br />
= 1.96, FeO = 5.61, MnO = 0.10, CaO = 20.43, Na 2<br />
O = 0.12,<br />
H 2<br />
O - = 0.75.<br />
Trubelja (1961) gives data on diopside in ultrabasic rocks from the southeastern<br />
part of Mt. Konjuh. Here, diopside is the dominant mineral in the lherzolites<br />
from the locality of Lisac (970 m a.s.l.) and Zečji vrat, as well from the source area<br />
of the Grabovica creek. In thin section, most of the diopside grains in the Lisac<br />
lherzolite display clear prismatic cleavage and parting along (100) or (010). The<br />
extinction angle, measured on several grains, has a stable value of 42°. The diopside<br />
is optically positive – 2V angle measurements on three grains gave the following<br />
values: 56°, 57° and 61.5°. The monoclinic pyroxene from the locality of Zečji Vrat<br />
has properties characteristic of diopside. However, measurements in thin section<br />
revealed the presence of grains with a small 2V angle, thus indicating that they<br />
belong to the isomorphous series of diopside-clinoenstatite. For diopside, 2V = 47.5°<br />
and 52.5°, c : Z = 32.5°.<br />
Diopside from Grabovica displays clear prismatic cleavage and parting along<br />
(100) and (010). The angle between the cleavage planes (110) : (1-10) = 86.5°, the<br />
extinction angle is 39° to 43°, the measured 2V angle varies in the range +56° to +60°.<br />
Pamić (1974) determined an iron-rich diopside in gabbro-type rocks of the<br />
Krivaja – Konjuh ultrabasic complex. This diopside has a 2V angle = +56° to +58°,<br />
c : Z = 40-46°.<br />
Diopside (diallage) is very common in the ultrabasic rocks of Mt. Ozren.<br />
This diopside has the following optical properties: c : Z = 38-40°, average 2V angle<br />
is +60º. It has prismatic cleavage and parting along (100). Based on microscopic<br />
determinations, diopside was found in the following rocks: serpentinized harzburgite<br />
in the Krivaja creek, serpentinized lherzolite from Malo Selište, harzburgite from<br />
Jadrina river valley, lherzolite from Pištalo creek, lherzolite from Gostilje. More<br />
detail can be found in the publications by Kišpatić (1897, 1900), Pamić and Trubelja<br />
(1962), Trubelja and Pamić (1965) and Pamić (1973).<br />
Trubelja (1960) determined clinoenstatite-diopside in the Lahci basalts near<br />
Višegradska Banja. In thin section, distinct cleavage and very narrow parting lamellae<br />
can be seen. The measured 2V angles are in the range 47.5-62°, the c : Z extinction<br />
angles = 30-44°. The twinning angle (100) : (1-10) is 90°. In many cases the pyroxene<br />
core is surrounded with amphibole, indicative of the process of uralitization.<br />
In Bosnia and Hercegovina salite (diopside enriched in Fe 2+ ) occurs only<br />
in BSZ and on Mt. Motajica. Kišpatić (1897, 1900) determined salite in pyroxene<br />
amphibolites. It occurs less frequently in amphibole pyroxenites, actinolite schists<br />
115
SILICATES<br />
and crystalline limestone. Kišpatić identified pyroxene amphibolite on the following<br />
locations: Rudine creek, Reljevac, Ozren Manastir, Mala Bukovica, Velika Bukovica,<br />
Ravna Rijeka near Duboštica. Salite was also found in the Buletić amphibole<br />
pyroxenite, the actinolite schists outcropping between Dragovac and Prisjeka and in<br />
the crystalline limestones of Salkići. Kišpatić (1897) found that salite occurs together<br />
with titanite in this limestone. The c : Z angle is 38°.<br />
Salite is often found to be a significant constituent of pyroxene amphibolites,<br />
where – in thin section – the grains are colourless or pale green. Diopside (salite) is<br />
found in the pyroxene cornites of Mt. Motajica (Varićak 1966).<br />
116<br />
2. Diopside in rocks outside the Bosnian serpentine zone<br />
Marić (1927) determined diopside and other pyroxenes (augite, hyperstene)<br />
in the Jablanica gabbro rocks. The extinction angle of this diopside is 38°, the<br />
pleochroism Nz = pale yellow, Nx = brownish-yellow. Maximum birefringence =<br />
0.023, 2V is ca. 60°.<br />
Tajder (1953) identified diopside in certain extrusive rocks around<br />
Srebrenica – the dacites from the village of Diminići and the Kiselica creek.<br />
In the Diminići dacite diopside is so uncommon that it could be identified only<br />
in some thin sections in the form of idiomorphic, prismatic, colourless crystals<br />
with good cleavage. The extinction angle is 36-38°. On the other hand, diopside<br />
is a significant constituent of the Kiselica dacite, where it occurs in the form of<br />
idiomorphic, prismatic crystals of ca. 0.3 x 0.1 mm in size. The colour is pale green<br />
and it has a high relief. The extinction angle is 38°, 2V = 59-60°. Twinning can<br />
be seen on some crystals. A carbonate corona is present in some cases indicating<br />
hydrothermal alteration.<br />
Foullon (1893) mentioned diopside in ore concentrates in the schist<br />
mountains of central Bosnia.<br />
DIALLAGE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Brajdić (1964), Đorđević (1958, 1960), Golub (1961), Hauer<br />
(1879), John (1879, 1880, 1888), Kišpatić (1897, 1900), Pamić (1971, 1972), Pamić<br />
and Antić (1964), Pamić and Trubelja (1962), Pilar (1882), Primics (1881), Ristić,<br />
Pantić, Mudrinić and Likić (1967), Schiller (1905), Trubelja (1957, 1960, 1961),<br />
Trubelja and Pamić (1965).<br />
In Bosnia and Hercegovina diallage is a ubiquitous mineral in gabbroid<br />
rocks of the Bosnian serpentine zone (BSZ). John (1888) is the only author who<br />
mentions this mineral in the Jablanica gabbro in Hercegovina.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
1. Diallage in rocks of the Bosnian serpentine zone (BSZ)<br />
Hauer (1879) and John (1879) provide the first data on diallage in the olivine<br />
gabbro rocks in the Bosna river valley, between Maglaj and Žepče. Samples of these<br />
rocks were collected by Anton Rzehak and microscopic determinations were done<br />
by John. More detailed data can be found in the subsequent publication by C. John<br />
(1880). In additon to data on diallage from the Maglaj-Žepče olivine gabbros, John<br />
investigated also similar rocks from Barakovac in the Vrbanja river valley, troctolites<br />
and gabbros from the Višegrad area. Diallage is a significant constituent in all of the<br />
mentioned rocks.<br />
Diallage is very common in the olivine gabbros from Višegrad. Its colour<br />
is brown with a metallic lustre; the cleavage is alomost perfect. In thin section<br />
the diallage is mostly fresh and often incorporates large crystals of feldspar and<br />
olivine. John paid a lot of attention to the alteration products of diallage, pointing<br />
out that hornblende is the most common alteration product. The darker variety<br />
of diallage, common in olivine gabbro, alters into brown hornblende, which has<br />
strong pleochroism. The lighter diallage varieties alter mostly into fibrous, almost<br />
colourless hornblende.<br />
Pilar (1882) also provides a description of diallage in gabbro-type rocks<br />
from Vrbanja/Barakovac near Banja Luka and from Mt. Kozara.<br />
Early microscopic determinations of diallage in rocks of the BSZ were done<br />
by Primics (1881), Schiller (1905) and Kišpatić (1897, 1900). Kišpatić investigated<br />
the entire BSZ, while Primics and Schiller confined their research on the Duboštica<br />
and Višegrad areas only.<br />
Substantial research on these rocks was done after the II World War, and a<br />
considerable amount of microscopic and other data can be found in various petrologic<br />
treatises. Golub (1961) provides a significant set of microscopic measurements of<br />
diallage in the rocks of Mt. Kozara. Here, diallage is a constituent of troctolite,<br />
olivine gabbro, actinolite gabbro – rocks which have extensive outcrops on the<br />
southern flanks of Mt. Kozara.<br />
The diallage (3.5 vol.%) from Jovača creek troctolite shows good cleavage<br />
and parting. The average 2V angle value is +60°, the extinction angle is 42.5°. In<br />
the Jovača olivine gabbros diallage is of a light pinkish colour, quite pleochroitic (Z<br />
= pinkish, Y = reddish, X = pinkish-red. The angle between cleavage planes<br />
is 88.5-89.5°. The extinction angle based on several measurements lies in the<br />
range 40-42°, while the 2V angle = 56-58°. The maximum birefringence Nz – Nx =<br />
0.0277, while the partial birefringences are as follows: Nz – Ny = 0.0219 and Ny –<br />
Nx = 0.0058. This optical data indicate that the diallage is enriched with titanium.<br />
117
SILICATES<br />
Reddish-brown platelike inclusions can be seen within the cracks resulting from<br />
parting, and this material is probably hematite.<br />
The diallage from the olivine gabbros of the Kozara creek has similar<br />
optical characteristics as the one previously described. It shows prismatic cleavage<br />
and parting. The extinction angle is 42-44°, 2V° +60° (average value of six<br />
individual measurements). The maximum birefringence, measured on two grains,<br />
is Nz – Nx = 0.0271 and 0.0273. The pleochroitic colours are Z = pale red, Y =<br />
yellowish-red, X = pinkish-red. In the gabbros of Kozara creek the diallage has<br />
a pinkish-grey colour and a weak pleochroism. The 2V angle lies in the range<br />
59-60°, the extinction angle is 36-38°. It has less inclusions than the former<br />
diallage. The diallage contained in the actinolite gabbro has similar 2V angles,<br />
while the extinction angles are somewhat lower.<br />
Pamić and Trubelja (1962) and Trubelja and Pamić (1965) have determined<br />
diallage in the gabbro-type rocks of Mt. Ozren. Microscopic determinations, using<br />
the Fedorov method on a rotating stage, provided data of the fundamental optical<br />
constants. Diallage in the olivine gabbro from Paklenica has a 2V angle of +59°, an<br />
extinction angle of 46°. The angle between the two sets of cleavage lamellae is 87.5º.<br />
More recent petrographic investigations of the gabbro-type rocks of Mt.<br />
Konjuh, the Krivaja river valley and the Duboštica area were done by Pamić and<br />
Antić (1964), Ristić et al. (1967), Brajdić (1964) and Trubelja (1961). Thus, Trubelja<br />
(1961) and Brajdić (1964) found diallage to be a constituent of olivine and uralite<br />
gabbros, gabbro-diorites and gabbro-pegmatites of the Mt. Konjuh complex. In the<br />
olivine gabbros from the Stupančica creek close to the village of Bjeliš, the diallage<br />
is fresh and has a poikilitic structure with enclosed small grains of rhombic pyroxene.<br />
Almost all investigated grains show good prismatic cleavage and pinacoidal parting.<br />
The average 2V angle is +56°, the c : Z extinction angle = 40.8°. B 1/2<br />
twinning can<br />
be observed on some grains.<br />
In the uralite gabbros, which are located immediately next to the olivine<br />
gabbro, diallage has undergone alteration into uralite, and can be identified only in<br />
some central sections of the uralite phylla. A similar situation is encountered in the<br />
case of gabbro-diorite where diallage has altered both into uralite and chlorite.<br />
Within the ultrabasic complex of Mt. Konjuh, differentiation of some<br />
crystalline gabbro-pegmatite can be observed. The diallage grains in such rocks<br />
are often several centimeters in diameter. Brajdić (1964) determined diallage in a<br />
pegmatite vein from Bjeliš, near Olovo. This diallage has an extinction angle of<br />
40-41°, and 2V angle of +56°. Parting along (100) is clearly visible. Almost all grains<br />
are affected by alteration processes (uralitization).<br />
118
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Ristić et al. (1967) investigated the gabbro-pegmatites from Katranička river<br />
at Mt. Konjuh. XRD data of diallage is as follows: d 2.99 (10) 2.51 (9) 2.12 (6)<br />
1.68 (8) 1.42 (7).<br />
Đorđević (1958, 1960) determined microscopically diallage from the basic<br />
intrusive rocks from the Vareš area. He found diallage in gabbros, anorthosites and<br />
gabbro-pegmatites. The extinction angle of this diallage is 42-43° but can also be<br />
much smaller (28°) in which case it is probably pigeonite. The authors data from the<br />
paper published in 1960 are more detailed. The diallage grains are some 4.5 x 3.5 mm<br />
in size, and display distinct parting along (100). Pleochroitic colours are very weak.<br />
The 2V angle lies in the range 48-60°, the c : Z extinction angle = 36-42°. Maximum<br />
birefringence of 0.0296 was measured on one grain. Table 16. shows the chemical<br />
analysis data.<br />
Table 16. Chemical analysis data and ion formula units of diallage from basic rocks (Vareš)<br />
Diallage (gabbro)<br />
Diallage (gabbro-pegmatite)<br />
SiO 2<br />
47.26 Si = 1.753 41.29 Si = 1.565<br />
TiO 2<br />
0.60 Ti = 0.016 0.75 Ti = 0.023<br />
Al 2<br />
O 3<br />
5.32 Al = 0.231 9.40 Al = 0.419<br />
Fe 2<br />
O 3<br />
2.60 Fe 3+ = 0.072 3.17 Fe 3+ = 0.091<br />
FeO 4.46 Fe 2+ = 0.138 7.90 Fe 3+ = 0.250<br />
MnO 0.09 Mn = 0.02 0.12 Mn = 0.004<br />
MgO 19.00 Mg = 1.049 19.65 Mg = 1.109<br />
CaO 17.57 Ca = 0.696 11.40 Ca = 0.462<br />
Na 2<br />
O 0.93 Na = 0.066 0.82 Na = 0.066<br />
K 2<br />
O 0.51 K = 0.023 0.36 K = 0.017<br />
H2O + 1.94 4.88<br />
H2O - 0.24 0.67<br />
100.52 100.41<br />
The diallage from the gabbro-pegmatite has considerably larger grains<br />
(15 x 12 mm). The 2V angle is in the range +47-60°, the extinction angle 37-48°. The<br />
maximum birefringence measured on one grain is 0.02877.<br />
The above chemical analysis shows a fairly high amount of water in both<br />
diallage samples, particularly in the gabbro-pegmatite which is an indication that this<br />
diallage has undergone substantial alteration.<br />
Trubelja (1957, 1960) established that diallage is a common mineral of the<br />
basic intrusive rocks from the Višegrad area. It occurs in small amounts in troctolites,<br />
while its percentage in normal and olivine gabbro is higher. The gabbro-pegmatites<br />
of this area also contain diallage. In uralite gabbros diallage is substantially altered<br />
into amphibole.<br />
119
SILICATES<br />
The gabbros from the village of Pijavice contain mostly plagioclase and<br />
diallage. The diallage shows characteristic parting along (100) and, to a lesser extent,<br />
along (010). In this section it is of pale green colour, and often surrounded by uralite.<br />
Some grains show evidence of cracking or bending. Twinning is not common. The<br />
extinction angle is 40-43°, the 2V angle lies in the range +58-62°. The olivine gabbros<br />
from the village of Mirilovići contain diallage which has clear prismatic cleavage<br />
and parting along (100). Some grains show alteration effects into bastite and brown<br />
hornblende. Its 2V angle lies in the range 53-61°, the extinction angle = 39.3-44.3°.<br />
The olivine gabbros from Rijeka near Velika Gostilja contain pyroxenes<br />
with pronounced characteristics of diallage, including clear parting along the (100)<br />
pinacoid and less pronounced prismatic cleavage. Grains mostly represent individual<br />
crystal but twinning is occasionally present according to the B 1/2<br />
law. In this case,<br />
both twins share common crystallographic axes [001] and [010]. The angles between<br />
the Z and X vibrational directions of the optical indicatrix are 81° which corresponds<br />
to the extinction angle value multiplied by two. The diallage grains are 1-2 mm in<br />
diameter. The extinction angle lies in the range 38-42°, the 2V = 48.5-56.5°.<br />
The troctolites from Lahci village in the valley of the Banja creek contain ca.<br />
3 vol.% of diallage. It has identical constants with the previously described diallages.<br />
The gabbro-pegmatite vein within the harzburgite rock series of Karaula<br />
Kosa near Dobrun, the diallage grains, grey to dark green in colour, often attain sizes<br />
of more than 10 cm in length. It displays perfect parting along (100) – crystal faces of<br />
this form have a strong light reflectance capacity. This parting is so conspicuous that<br />
it resembles the cleavage pattern of micas. Thin sections, when cut parallel to (100)<br />
have a parallel extinction, while one of the optic axes is almost perpendicular to this<br />
face. The prismatic cleavage is perfect, and parting along (010) is often very good.<br />
The extinction angle lies in the range 37.5-43º, the +2V angle is 57.5-59.5º. The<br />
grains are mostly fresh but sometimes show alteration into finegrained uralite. Other<br />
alteration products include chlorite and bastite. Olivine and magnetite inclusions<br />
have been observed in this diallage. The chemical composition of very clear<br />
grains is as follows (analyst: F.Trubelja): SiO 2<br />
= 49.13, TiO 2<br />
= 0.60, Al 2<br />
O 3<br />
= 4.78,<br />
Fe 2<br />
O 3<br />
= 1.08, Cr 2<br />
O 3<br />
= 0.15, FeO = 3.89, MnO = 0.25, MgO = 16.85, CaO = 19.79,<br />
Na 2<br />
O = 1.15, K 2<br />
O = 0.01, H 2<br />
O + = 2.05, H 2<br />
O - = 0.50, Total = 100.23<br />
120<br />
The somewhat elevated percentage of water is the result of alteration processes.<br />
The albite-bearing gabbro-pegmatites from Višegradska Banja contain<br />
diallage which shows signs of mechanical stress and deformation. Parting is clearly<br />
visible. Larger diallage grains, sometimes altered into chlorite and amphibole, are<br />
often surrounded with microbreccias. The optical values of this diallage are as follows:<br />
the c : Z extinction angle lies in the range 41-45°, the +2V angle = 53.5-54°. A partial<br />
Ny – Nx birefringence has been measured as 0.003-0.005.
2. Diallage in the gabbro from Jablanica<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
John (1888) has given a detailed account of the diallage contained in the<br />
gabbro series from Jablanica in Hercegovina. In thin section this diallage is of a<br />
light brown colour and shows very weak pleochroism. Prismatic cleavage and<br />
pinacoidal parting is clearly visible. The measured extinction angle is 45°. Inclusions<br />
of hornblende, biotite, magnetite and hematite are present in diallage grains.<br />
AUGITE<br />
(Ca,Na) (Mg,Fe 2+ ,Fe 3+ ,Ti,Al) [(Si,Al) 2<br />
O 6<br />
]<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio and Cell parameters: almost identical to diopside.<br />
Properties: pronounced cleavage parallel to {110}, as is the case with all pyroxenes.<br />
Other properties are similar to those of diopside.<br />
X-ray data: d 2.99 (100) 1.62 (100) 1.43 (100) – ASTM-card 3-0623<br />
IR-spectrum: 410 465 477 515 637 676 860 875 915 970 1070 1630 3425 cm -1<br />
AUGITE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Barić (unpublished data), Čelebić (1967), Čutura (1918), Golub<br />
(1961), Hauer (1879), John (1879, 1880, 1888), Jurković (1954a), Karamata (1953,<br />
1957, 1960), Karamata and Pamić (1960), Katzer (1903, 1924, 1926), Kišpatić (1897,<br />
1900, 1904b, 1910), Majer and Jurković (1957, 1958), Marić (1927), Pamić (1957,<br />
1960, 1960a, 1961a, 1961b, 1962, 1963, 1969, 1969a, 1971, 1971a, 1972c, 1972d),<br />
Pamić and Antić (1964), Pamić and Buzaljko (1966), Pamić and Jurić (1962), Pamić<br />
and Kapeler (1969, 1970), Pamić and Maksimović (1968), Pamić and Papeš (1969),<br />
Pamić and Trubelja (1962), Paul (1879), Petković (1961/62), Pilar (1882), Ramović<br />
(1957), Ristić, Pamić, Mudrinić and Likić (1967), Schafarzik (1879), Sijerčić<br />
(1972a), Simić (1964, 1966), Šibenik-Studen and Trubelja (1967, 1971), Trubelja<br />
(1960, 1961, 1962, 1962a, 1963, 1966a, 1972/73), Trubelja and Miladinović (1969),<br />
Trubelja and Pamić (1957, 1965), Trubelja and Slišković (1967), Trubelja and<br />
Šibenik-Studen (1965), Tućan (1928, 1957), Varićak (1966).<br />
Augite is a rock forming mineral with a complex chemical composition.<br />
In Bosnia and Hercegovina augite is quite ubiquitous, particularly in vein-type and<br />
effusive basic and intermediary igneous rocks such as diabase, spilite, porphyrite<br />
and keratophyres. Augite-bearing rocks have a regional distribution along the entire<br />
Bosnian serpentine zone (BSZ), and its peripheral sections known as the diabasechert<br />
series.<br />
121
SILICATES<br />
Augite is also an important constituent in the rocks resulting from Triassicage<br />
magmatic events. These rocks are to be found in numerous locations in Bosnia<br />
and Hercegovina. Diabases, spilitic rocks, porphyrites, keratophyres and other rock<br />
belonging to spilite-keratophyre series of mid-Triassic age are located mainly in the<br />
Vrbas river valley, at Kupres, and in the Konjic – Jablanica – Prozor area. These<br />
rocks are alos to be found in the Borovnica – Vareš – Čevljanovići area, in southeastern<br />
Bosnia near Čajniče and Tjentište, as well as in the Ilidža – Kalinovik area.<br />
A substantial amount of literature data is available for augite, both in older<br />
and in more recent publications. The information provided is based mainly on<br />
microscopic determinations, including rotating-stage measurements.<br />
122<br />
1. Augite in rocks of the Bosnian serpentine zone (BSZ) and the<br />
diabase-chert series (DCS)<br />
The earliest data on augite occurences in rocks of the BSZ and its peripheral<br />
parts were provided by Hauer (1879), John (1879, 1880), Kišpatić (1897, 1900,<br />
1904b), Paul (1879), Pilar (1882) and Schafarzik (1879). The mineral augite was<br />
determined mainly by microscopic methods in transmitted polarized light. Some of<br />
the above authors provide also quantitative measurements – i.e. Kišpatić (1904b, p.<br />
53) gives optical constants for augite in the diabase-porphyrite from Dobrljin:<br />
c : Z = 41° Nz – Nx = 0.020 2V = +56°<br />
A large amount of data can be found in the treatise by Kišpatić (1897, 1900).<br />
He determined and measured augite in numerous rock samples from Mts. Kozara,<br />
Prisjeka, Skatovica, Uzlomac, Borja, Ljubić, Ozren, from the Bosna river valley<br />
and the Višegrad area. He established that the augite has commonly altered into<br />
amphibole and chlorite. This alteration process and transformation of augite into<br />
amphibole is so widespread that augite completely disappears and transforms into<br />
fibrous amphibole.<br />
A number of papers published after the II World War contain qualitative<br />
and quantitative data on augite: Golub (1961), Karamata and Pamić (1960), Pamić<br />
and Kapeler (1969), Pamić and Trubelja (1962), Ristić, Pamić, Mudrinić and Likić<br />
(1967), Šibenik-Studen and Trubelja (1971), Trubelja (1960, 1961, 1962, 1966a,<br />
1972/73), Trubelja and Pamić (1965).<br />
a) Bosanski Novi area and Mt. Kozara<br />
Trubelja (1962) finds that augite is contained in the spilitic rocks in the northwestern<br />
part of BSZ. In addition to augite, titanoaugite is an important constituent<br />
of the biotite-spilite from Torić creek. In thin section and when the nicols are not in
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
a crossed position, the titanoaugite has a vivid violet colour which is characteristic<br />
for this mineral. The +2V angle lies in the range 48-52.5°. The extinction angle is<br />
comparatively large at 48-50°. Some alteration into chlorite was noticed.<br />
Golub (1961) identified augite in the uralite gabbros from Kozarački creek<br />
on Mt. Kozara. Most of the augite here is altered and transformed into uralite. Parting,<br />
so characteristic for diallage, is missing while the cleavage lamellae intersect at<br />
an angle of 89.5°. The augite is colourless to pale green, the extinction angle is<br />
39-42.5º, the +2V angle is 46-52º. The coarsegrained augite from the Kotlovača<br />
creek gabbro-pegmatite is fractured and weathered, of a pale green colour and very<br />
weak pleochroism. The extinction angle is 41-43º, the +2V angle 56-59º. Augite<br />
from diabase from this same area has an extinction angle of 45°. Pamić and Kapeler<br />
(1969) made similar measurements on these augites.<br />
Trubelja (1966a) found that augite-bearing diabase-dolerite rocks have<br />
a wide distribution on the northern flanks of Mt. Kozara. Much of the augite is<br />
transformed into amphibole or chlorite (i.e. in the Bukovica and Trnova creeks).<br />
The dolerites from Trnova creek carry augites as rather large individual crystals<br />
showing a substantial degree of alteration into amphibole. In thin section, good<br />
prismatic cleavage can be seen. Pleochroism is either very weak or completely<br />
absent. The +2V angle = 50°, the extinction angle is 42°. Plagiocale and augite are<br />
the predominant minerals in the diabases found in the source area of the Bukovica<br />
creek. The augite grains are irregular in shape and fill the intergranular space of<br />
the plagioclase. Most of the augite is chloritized or uralitized. Prismatic cleavage<br />
is visible, the +2V angle is 56°.<br />
b) Mt. Ozren, Mt. Konjuh and the Doboj area<br />
Pamić and Trubelja (1962) and Trubelja and Pamić (1965) identified augite<br />
to be a common constituent of diabases and spilitic rocks in the peripheral parts<br />
of the large peridotite-serpentine complex of Mt. Ozren. It was microscopically<br />
determined in the porpyric amphibole-dolerite from the Krivaja creek, in the spilitc<br />
rocks from Rakovac, Brezica and Konopljište villages. In the Krivaja series, the<br />
augite in amphibole-dolerite rock is considerably altered to uralite, and relicts of<br />
augite are encountered only occasionally.<br />
At Konopljište, augite and albite are the predominant minerals in the spilites.<br />
Augite normally occupies the space between prismatic albite grains. It is frequently<br />
fresh and there is only minor alteration into chlorite and amphibole. The augite is<br />
colourless to pale brownish, the pleochroism is weak, and prismatic cleavage is a<br />
characteristic feature. The +2V angle, measured in convergent light, is 56°. Grains<br />
which are sectioned perpendicular to the c axis have octogonal shapes with distinct<br />
prismatic cleavage lamellae. The relief and interference colours are much higher<br />
123
SILICATES<br />
than those of albite and other minerals in the rock. Augite in other spilitic rocks has<br />
the same or very similar microphysiographic characteristics – the c : Z angle is 38-40º,<br />
+2V = 56-60°.<br />
Augite is also the principal mineral of diabases from Mt. Konjuh (Trubelja<br />
1961, Šibenik-Studen and Trubelja 1971). In thin sections prepared from dolerites<br />
from the Blizanci creek, the augite is almost colourless but heavily included with dark<br />
inclusions. Prismatic cleavage and parting along (001) and (010) is distinct. The +2V<br />
angle (measured on several grains) lies in the range 58-59.5°, the extinction angle is<br />
42°. Augite grains are commonly surrounded with green or brown hornblende. Some<br />
alteration into acicular or foliated uralite occurs.<br />
Ristić et al. (1967) determined augite in the gabbroid veins of Mt. Konjuh.<br />
The +2V angle lies in the range 54-63°, the extinction angle is 40-44°.<br />
John (1879, 1880), Hauer (1879) and Schafarzik (1879) found augite to<br />
be an important mineral component of diabase on which the old fortress of Doboj<br />
(Gradina) is erected. The determination of augite is largely due to the efforts of C.<br />
John. This well known petrographer and microscopist maintained that augite had<br />
the structure of diallage (John 1879). Recently, Barić (unpublished results) made<br />
microscopic measurements (using a Fedorov-type rotating stage) on augite from the<br />
Gradina diabase. Measurements made on six individual grains gave a +2V angle<br />
in the range of 47-52¼°, and the c : Z extinction angle 39-43¼°. A red > violet<br />
dispersion of optic axes was determined in convergent light.<br />
c) the Višegrad area<br />
Kišpatić (1897, 1900) and Trubelja (1960 and 1972/73) provide data on<br />
augite in rocks from the Višegrad area in eastern Bosnia. Augite in diabases matrices<br />
is here also mostly converted into uralite. On the other hand, the prehnitized diabase<br />
(on the road Višegrad – Dobrun) the augite is fresh.<br />
2. Augite in products of Triassic magmatism<br />
a) Schist mountains of central Bosnia – Konjic, Jablanica and Prozor<br />
Augite is an important constituent of gabbros, diorites, diabases, andesites and<br />
other rocks in the schist mountains of central Bosnia. Jurković and Majer (1957, 1958)<br />
provide data on augite which occurs in rocks of the gabbro-dioritic complex of Bijela<br />
Gromila south of Travnik. Augite in diorite from a location near the village of Kopila<br />
is largely idiomorphic and of a greenish colour. Twinning along (100) is common. The<br />
+2V angle lies in the range 51-56°, the extinction angle is in the range 40-43°.<br />
124
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Marić (1927) identified augite in a gabbro rock series in the southern part of<br />
the Jablanica complex. It has a weak pleochroism (Z = pale brown, X = greyish). The<br />
extinction angle is 44°, the +2V = 59° 50’, and the maximum birefringence is 0.025.<br />
One of the measured grains showed a higher extinction angle of 45° 20’.<br />
Jurković (1954a) finds that in the augite-labrador bearing andesite of Orašin<br />
(south of Bakovići) augite occurs as small grains, although some of these are ca. 1<br />
mm in size. In thin section the augite grains have isometric or octogonal shapes and<br />
carry magnetite inclusions. Some augite grains are surrounded by plagioclase. Ten<br />
grains were used for measurement – the +2V angle lies in the range 50-62° while<br />
the c : Z extinction angle varies from 42° to 50°. Some twinning along (100) is<br />
observed. Some augite grains have a zonal texture. Metamorphic alteration results in<br />
a conversion of augite to chlorite and calcite.<br />
Trubelja and Šibenik-Studen (1965), Šibenik-Studen and Trubelja (1967)<br />
and Pamić and Papeš (1969) describe augite in rocks from the Kupres and Bugojno<br />
areas and from the Vrbas river valley between Donji Vakuf and Jajce. Here, augite<br />
is an important constituent of spilitic rocks, porphyr-diabase, andesite and trachyte.<br />
Augite is commonly altered into chlorite.<br />
In the area of Konjic, Jablanica and Prozor, augite occurs as a common<br />
constituent of rocks which are products of Triassic magmatism, such as basalts,<br />
diabases, spilites, keratophyrs etc. Data on augite and other minerals in these rocks<br />
can be found in publications by Katzer (1903), Čelebić (1967), Čutura (1918), John<br />
(1880, 1888), Kišpatić (1910), Pamić (1960, 1961a, 1961b), Pamić and Maksimović<br />
(1968) and Tućan (1928).<br />
Tućan (1928) microscopically determined augite in the Vrata andesite. The<br />
augite is often idiomorphic in shape and shows sharp egdes of crystal faces. Some<br />
grains were rather large (3.59 x 1.83 mm) in size, with some zonation present. The<br />
extinction angle is 44°, the Ny refractive index = 1.7099, the Nz – Nx maximum<br />
birefringence = 0.0262, the +2V angle = 59° 51’.<br />
Substantial information on augite in various igneous rocks from this area<br />
can be found in the publications by J. Pamić. His investigations showed that augite<br />
in basalts is commonly allotriomorphic and that octogonal shapes are comparatively<br />
rare. Twinning along (100) is often present, and the angle between twinning lamellae<br />
is typically 87.5°. In thin section the augite grains have a pale green colour. The<br />
+2V angle is in the range 54-60°, while the c : Z extinction angle varies in the<br />
range 40-48°. Interference colours are usually high. In andesites (i.e. the andesite<br />
from Vrata near Sovići) the augite has very similar microphysiograpic features to<br />
the augite described above. The main difference lies in the fact that alteration of<br />
augites in andesites is more pronounced than in basalts. The alteration process can<br />
125
SILICATES<br />
result in a more or less complete conversion of augite to chlorite (pseudomorphic<br />
chlorite). Augite in spilitic rocks has a +2V angle of 59° and an extinction angle of<br />
44°. Progressive alteration of augite to chlorite is also typical for spilites.<br />
126<br />
b) the Borovica, Vareš and Čevljanovići area and the Sarajevo district<br />
Karamata (1953, 1960), Pamić (1963), Petković (1961/62) and Ramović<br />
(1957) identified augite as one of the important constituents of Triassic effusive rocks<br />
and veins of Vareš and adjacent areas. It is interesting to note that Kišpatić (1897)<br />
made no determination of augite in the melaphyrs around Vareš, but points out that<br />
some vacuoles in these rocks are shaped like augite or plagioclase crystals (which<br />
may have been destroyed as a result of surface weathering). Karamata also identified<br />
phenocrystals of augite in the basic effusive rocks of Vareš. In thin section these<br />
augites are colourless and have distinct cleavage, and often contain inclusions<br />
of plagioclase crystals. Measurements of optical constants provide following<br />
values: the +2V angle is in the range 51-53.5°, the c : Z extinction angle is in the<br />
range 36-43°. The largest augite phenocrystal was 2.88 x 2.70 mm in size.<br />
Augite is likewise an important constituent of Triassic diabases and spilites<br />
from the Čevljanovići area. Pamić measured a +2V angle of 52° and an extinction<br />
angle of 41°, these being averages of several measurements.<br />
The effusive rocks of the Sarajevo district also have augite as a significant<br />
mineral constituent (Pamić 1957, 1960a, 1962) and Simić (1964, 1966). Augite in<br />
dolerites (diabases) from Donja Grkarica is mostly allotriomorphic and thin sections<br />
reveal distinct prismatic cleavage. The average angle between cleavage planes is<br />
86.5°. Twins along (100) are uncommon. In thin section this augite is colourless; the<br />
average value for the +2V angle is 58° and 44° for the extinction angle. The augite in<br />
the Govnište dolerites has similar characteristics (+2V = 59º and c : Z = 42°). Both<br />
of these localities are on the north-eastern flanks of Mt. Bjelašnica.<br />
Simić (1964, 1966) determined augite in the basic effusives at Babin Dol<br />
and Durmiševica on Mt. Bjelašnica, and in the basic igneous rocks in the area of the<br />
Rača creek, north of Sarajevo.<br />
Pamić (1962) identified augite in the spilites from the Godinja village near<br />
the source of the Željeznica river. Here augite occurs together with albite, but in<br />
considerably smaller amounts compared to the plagioclase. The augite grains are<br />
very small, allotriomorphic to hipidiomorphic in shape. In thin section this augite is<br />
colourless and fractured; the extinction angle is in the range 41-45°.<br />
Pamić (1960a) determined augite to be an important and common mineral<br />
in the Kalinovik diabases, picrite-diabases and basalt-andesite rocks. On the other<br />
hand, the effusive rocks bearing alkaline plagioclase, contain almost no augite.
c) South-eastern Bosnia<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Trubelja (1962a, 1963), Pamić and Buzaljko (1966), Trubelja and Slišković<br />
(1967) and Trubelja and Miladinović (1969) determined augite as a significant<br />
constituent in the products of Triassic magmatism in the area of Tjentište, Sutjeska<br />
and Čajniče in SE Bosnia. The andesites at Crvene Prljage, south of the village<br />
of Čurevo and in the Hrčavka river valley contain augite. At Janjina Rijeka, near<br />
Čajniče, the andesites contain augite phenocrystals. Some grains display typical<br />
cleavage features. The +2V angle is in the range 58-60°, the extinction angle is<br />
between 38-40° and there is no pleochroism. Augite grains are partly or completely<br />
altered into chlorite.<br />
Augite was also determined in thin sections of dacites (quartzporphyrites)<br />
from Crni Potok and in crystalline tuffs from Ponikve in the Čajniče area.<br />
3. Other occurrences of augite<br />
Varićak (1966) identified augite in the amphibolites and amphibole schists<br />
of Mt. Motajica. The determination of augite is based on 2V and c : Z measurements.<br />
The extinction angle is 42-42.5° and the +2V angle in the range 53-60°.<br />
Karamata (1957) found that augite occurs, but is not very common, in<br />
keratophyrs from the Zvornik region. The augite is always altered into chlorite. The<br />
+2V angle is 61° and the extinction angle = 43-44°.<br />
OMPHACITE<br />
(Ca,Na) (Mg,Fe 2+ ,Fe 3+ ,Al) [Si 2<br />
O 6<br />
]<br />
Omphacite is a variety of augite which occurs mainly in highly altered<br />
schists i.e. eclogites.<br />
In Bosnia and Hercegovina omphacite occurs in metamorphic rocks of the<br />
Bosnian serpentine zone (BSZ). Kišpatić (1897, 1900) made first determinations of<br />
omphacite in eclogite rocks from Mts. Skatovica and Mahnjača and the Kruševički<br />
creek, as well as in the eclogite pyroxenite of Ravna Rijeka and Vidaković creek.<br />
Omphacite occurs as irregular grains in the amphibole eclogite from Mt.<br />
Skatovica. In thin section it is almost completely fresh and of a pale green colour,<br />
and prismatic cleavage is well developed. The Mt. Skatovica eclogite contains a<br />
significant amount of omphacite.<br />
The eclogite amphibolite of Ravni Potok contains small amounts of a green<br />
monoclinic pyroxene. According to Kišpatić, this pyroxene is omphacite or salite.<br />
127
SILICATES<br />
Omphacite is a fairly common mineral in the metamorphic rocks of the<br />
Višegrad area. It is the predominant mineral in the eclogite pyroxenite from Vidaković<br />
creek. It is of a lush green colour and is sometimes included in garnet. The omphacite<br />
in the Kruševički creek eclogite is similar to the one described above.<br />
The Ravna rijeka eclogite pyroxenite contains omphacite in the form of<br />
smaller and larger grains of a green colour. There is no pleochroism and no clear<br />
cleavage, while the extinction angle is large.<br />
Pamić (1969a, 1971a, 1972c) and Pamić and Kapeler (1970) provide more<br />
recent data on the occurrence of omphacite in the BSZ, particularly the amphibolites<br />
and eclogites of Mt. Skatovica and from the Vijake – Vareš area, as previously<br />
described by Kišpatić.<br />
Pamić and Kapeler (1970) also note that the clinopyroxene in amphibolites<br />
of the Krivaja – Konjuh complex is probably omphacite. In thin section, this mineral<br />
has a pale green colour and distinct pleochroism. The +2V angle is in the range of<br />
60-61.5°, the extinction angle 39-42°.<br />
Tućan (1957), in his famous textbook of mineralogy, mentions the same<br />
locations for omphacite as Kišpatić.<br />
128<br />
ENSTATITE<br />
Mg 2<br />
[Si 2<br />
O 6<br />
]<br />
BRONZITE<br />
(Mg,Fe) 2<br />
[Si 2<br />
O 6<br />
]<br />
HYPERSTHENE<br />
(Fe,Mg) 2<br />
[Si 2<br />
O 6<br />
]<br />
Crystal system and class: Orthorhombic, rhombic dipyramidal class.<br />
Lattice ratio and Cell parameters: vary with chemical composition<br />
Properties: the orthorhombic pyroxenes enstatite, bronzite and hypersthene have a<br />
distinct prismatic cleavage as well as parting developed along the pinacoids. They<br />
represent an isomorphous series between MgSiO 3<br />
and FeSiO 3<br />
. The colour depends<br />
on the chemical composition. Enstatite contains up to 5% FeO and its colour is<br />
grey, brownish or greenish. Bronzite contains 5-15% FeO and is of brown colour.<br />
Hypersthene contains more than 15% FeO and is usually dark green to black.<br />
Hardness = 6, specific gravity = 3.2-3.9 and increases with increasing iron content.<br />
The streak is white to grey, lustre is vitreous (bronze-like in the case of bronzite).<br />
Refractive indices also increase with increasing Fe content, usually in the range<br />
1.65-1.78.
X-ray data:<br />
Enstatite: d 2.873 (100) 3.168 (50) 2.470 (45)<br />
d 3.17 (100) 2.87 (87) 2.49 (51)<br />
ASTM-card 7-216<br />
Hypersthene: d 3.14 (100) 1.47 (80) 2.86 (60)<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
IR spectrum:<br />
Enstatite: 410 460 505 535 655 695 722 745 763 852 908 940 1020<br />
1056 1180 1640 cm -1<br />
Bronzite: 410 455 508 540 565 650 695 722 745 860 930 1015 1065<br />
1125 cm -1<br />
Hypersthene: 408 456 508 536 562 635 650 692 725 760 855 872 895 945<br />
1028 1070 cm -1<br />
ENSTATITE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Đurić and Kubat (1962), Golub (1961), Majer (1962), Pamić<br />
(1969a, 1970, 1971, 1972, 1972c, 1972d), Pamić and Antić (1964, 1968), Pamić,<br />
Šćavničar and Međimorec (1973), Pamić and Trubelja (1962), Primics (1881),<br />
Ristić, Pamić, Mudrinić and Likić (1967), Schiller (1905), Sijarić and Šćavničar<br />
(1972), Simić (1966), Sunarić and Olujić (1968), Šćavničar and Jović (1961, 1962),<br />
Trubelja (1957, 1960, 1961), Trubelja and Pamić (1965).<br />
Enstatite occurs almost exclusively in ultrabasic rocks of the Bosnian<br />
serpentine zone (BSZ) – in peridotites and serpentinized peridotites. Since these<br />
rocks have a wide regional distribution in Bosnian inner Dinarides, so is the amount<br />
of enstatite substantial. Together with olivine and monoclinic pyroxene, enstatite is<br />
an important mineral of all bosnian ultrabasic rocks. It occurs in the lherzolites and<br />
harzburgites of north-western, central and eastern Bosnia. Enstatite also occurs in<br />
the ultrabasic rocks of Mt. Kozara, and those of BSZ between the rivers Bosna and<br />
Vrbas. It can be present in very substantial amounts in peridotites of Mts. Ozren,<br />
Konjuh and other areas of the central ophiolite zone. Enstatite is an important mineral<br />
in lherzolites and harzburgites of eastern Bosnia in the Višegrad area.<br />
Outside of BSZ, enstatite occurs in the alkaline effusive rocks at Mt.<br />
Bjelašnica.<br />
The information available on enstatite is not overwhelming, although enstatite<br />
is among the most omnipresent rock-forming minerals of the BSZ. Perhaps the main<br />
reason for this lies in the fact that earlier researchers considered enstatite to be bronzite<br />
(i.e. Kišpatić 1897, 1900). Microscopic investigations of orthorhombic pyroxenes<br />
– without the use of a Fedorov-type rotating stage and no data on their chemical<br />
composition – were insufficient for discriminating between enstatite and bronzite.<br />
129
SILICATES<br />
Consequently, data on enstatite can be found only in papers published after the II World<br />
War. It is, however, interesting to note that Primics (1881) was the only one to identify<br />
enstatite, in ultrabasic rocks from the Krivaja-Duboštica area. This determination is<br />
most probably the first identification of this mineral in the ultrabasic rocks of Bosnia.<br />
1. Mt. Kozara<br />
Golub (1961) microscopically determined enstatite in the lherzolites from<br />
Jovača and Vrela creeks on Mt. Kozara. In the Jovača lherzolite, enstatite occurs<br />
as grains of more than 1 cm in diameter. Cleavage is not distinct, but parting along<br />
(010) is usually present. Some alteration of enstatite into bastite and talcum is<br />
usually seen within the parting fractures. The +2V angle is in the range 78-84°. The<br />
2V angle measurement implies that this enstatite contains about 9% of the FeSiO 3<br />
component. In thin section enstatite has a parallel extinction and the angle between<br />
the two prismatic cleavage planes is 87.5-88.5°.<br />
In the Vrela lherzolite, enstaite also occurs in the form of large grains. Again,<br />
cleavage is not distinct but parting along (010) is visible. The measured +2V angle<br />
is in the range 80-90°, indicating a 11% enrichment with FeSiO 3<br />
.<br />
In the described<br />
rocks, enstatite can be easily recognized with the naked eye.<br />
2. The area between the Vrbas and Bosna rivers<br />
Đurić and Kubat (1962), Majer (1962), Pamić (1969a, 1972c), Pamić and<br />
Antić (1968), Pamić, Šćavničar and Međimorec (1973) provide data on enstatite<br />
in the ultrabasic rocks of the spacious area between the rivers Vrbas and Bosna.<br />
Peridotites and their serpentinized product belong to the most widespread rocks in<br />
this area. Particularly interesting are the porphyric varieties of peridotites where<br />
large (up to 3 cm) enstatite grains occur within a cryptocrystalline olivine matrix.<br />
Majer (1962) found the quantity of enstatite in these rocks to be variable.<br />
The ultrabasic rocks of Mt. Skatovica are often associated with amphibolites.<br />
Enstatite is an important constituent of these rocks, and has an average 10% of<br />
FeSiO 3<br />
, and a +2V angle of 85°. Enstatite commonly alters into serpentine (Pamić<br />
1969a, 1972c; Pamić, Šćavničar and Međimorec 1973).<br />
Pamić and Antić (1968) found enstatite to be a signficant constituent of<br />
serpentine-websterites and harzburgites in the area of Teslić and Prnjavor on Mt.<br />
Čavka. In thin section the enstatite is of hipidiomorphic shape and platelike habit.<br />
It is colourless and displays clear prismatic cleavage and an angle of 87° between<br />
the cleavage planes. The measured +2V angles of around 80° indicate about 8% of<br />
FeSiO 3<br />
in the enstatite molecule.<br />
130
3. Mt. Ozren and Mt. Konjuh<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Pamić (1970), Pamić and Antić (1964), Pamić and Trubelja (1962), Primics<br />
(1881), Ristić, Pamić, Mudrinić and Likić (1967), Sijarić and Šćavničar (1972),<br />
Sunarić and Olujić (1968), Trubelja and Pamić (1965) provide data about enstatite<br />
which occurs in the ultrabasic rocks of Mt. Ozren and Mt. Konjuh. Here, together<br />
with olivine, enstatite is the predominant mineral in these rocks.<br />
Trubelja and Pamić (1965) have invesetigated in detail the peridotite<br />
rocks of Mt. Ozren, including the enstatite which is an important constituent of<br />
the lherzolites, harzburgites and their intermediates. The enstatite from the Velika<br />
Ostravica harzburgite shows in thin section low interference colours. It has a well<br />
developed prismatic cleavage; the extinction is parallel. Some grains have inclusions<br />
of olivine or thin lamellae of a monoclinic pyroxene. The +2V angle of 78.5° was<br />
measured in convergent light.<br />
Enstatite is the predominant mineral in the serpentinized harzburgite from<br />
the Krivaja creek. It is usually allotriomorphic, less frequently hipidiomorphic.<br />
The prismatic cleavage is well developed, as is parting along (010). Thin twinning<br />
lamellae can be seen under crossed nicols in most grains, parallel to the pinacoid<br />
face. The average +2V angle is 79° corresponding to 10% FeSiO 3<br />
. Some grains show<br />
signs of alteration into serpentine.<br />
The lherzolite from the Pištalo creek contains large enstatite grains which<br />
can be seen with the naked eye. Next to olivine, enstatite is the second most<br />
important mineral constituent of this rock. It has a lamellar structure which makes<br />
measurements on the rotating stage rather difficult. The +2V angle is 88°. Occasional<br />
alteration into bastite was observed. Enstatite in other rocks of the Mt. Ozren series<br />
has similar properties to the one described above.<br />
Several authors referenced earlier have investigated the enstatite contained<br />
in ultrabasic rocks of the Krivaja – Mt. Konjuh complex. Pamić and Antić (1964)<br />
found that enstatite is a constituent of the lherzolite lenses within the Gostovička<br />
Rijeka (close to Zavidovići) series of gabbroid rocks. The +2V angle of this enstatite<br />
is 90° (14% FeSiO 3<br />
).<br />
Pamić (1970, 1971) determined that enstatite is an important mineral in the<br />
ultrabasic rocks of the Krivaja complex, associated with the Duboštica chromium<br />
ore body. Enstatite is the predominant mineral in single-mineral pyroxenites (veinlike<br />
formations), such as the enstatite-dunite rock from the Tribija river valley.<br />
Enstatite is often closely associated with chromite ore of the Duboštica area,<br />
in which case it has a characteristic honey-yellow colour. The grainsize of these<br />
enstatites is usually 0.5-1 mm.<br />
131
SILICATES<br />
Trubelja (1961), Ristić et al. (1967), Sijarić and Šćavničar (1972) provide<br />
data on the enstatite in ultrabasic rocks from Mt. Konjuh. Trubelja (1961) found<br />
that enstatite is less common than olivine in the Lisac lherzolite. The grains show<br />
perfect prismatic cleavage, and parting along (010) – as well as very thin lamellae<br />
of monoclinic pyroxene. Some enstatite grains are altered to bastite, while many of<br />
them contain olivine inclusions. Wavy extinctions can be observed on most enstatite<br />
grains. The measured +2V angle is 83-85°. In the case of enstatite from the Zečji<br />
Vrat (1275 m a.s.l.) lherzolite, the +2V angle is 83-86° corresponding to 10.5-12%<br />
FeSiO 3<br />
. The angle between the two cleavage planes (110) : (1-10) is 89°.<br />
Enstatite grains up to 1 cm in diameter occur in the Grabovica creek<br />
enstatite. A wavy extinction is commonly observed in thin section. Inclusions of<br />
monoclinic pyroxene and polisynthetic lamellae are parallel to (010). Olivine<br />
inclusions in enstatite are a common feature, impying that the enstatite is a reaction<br />
product of magmatic processes involving previously crystallized olivine (Trubelja<br />
1961). Sijarić and Šćavničar (1973) have determined enstatite by X-ray diffraction<br />
in numerous samples of ultrabasic rocks from Miljevac on Mt. Konjuh.<br />
132<br />
4. The Višegrad area<br />
Trubelja (1957, 1960) found enstatite to be a common and important<br />
constituent of ultrabasic rocks in the area of Višegrad. It is commonly found in<br />
harzburgites of Bosanska Jagodina (river Rzava valley). Thin sections of the mineral<br />
show low interference colours and parting along (010), and parallel inclusions of<br />
monoclinic pyroxene – much like in enstatites in other rocks of the BSZ. Alteration<br />
of enstatite to bastite is a common feature and many grains have retained enstatite<br />
only in their cores. The measured +2V angle is in the range 79.5-88° corresponding<br />
to 9-13 % FeSiO 3<br />
. The harzburgite from Karaula Kosa near Dobrun contains<br />
enstatite which has very similar properties to the one described above. However,<br />
some pressure twinning of enstatite has been observed in several samples. The +2V<br />
angle is in the range 74-86° corresponding to 7.5-12% FeSiO 3<br />
.<br />
Enstatite grains can be observed with the naked eye in ultrabasic rocks from<br />
the Višegrad area – due to its bronze colour and semimetallic lustre.<br />
Pamić (1972d) investigated the enstatite in lherzolites from the area of Rudo<br />
(valley of the river Lim). This enstatite contains some 7% FeSiO 3<br />
(based on +2V<br />
measurements).<br />
5. Enstatite in other areas<br />
Simić (1966) reports on enstatite occurrences outside of the BSZ, mainly in<br />
basic extrusive rocks of Triassic age on Mt. Bjelašnica (the localities of Durmiševica<br />
and Gornja Grkarica). The measured +2V angle is in the range 54-58°, refraction
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
indices Nz = 1.664, Nx = 1.565 ± 0.002, maximum birefringence Nz – Nx = 0.008.<br />
The enstatite is colourless and almost idiomorphic.<br />
Enstatite is also a constituent of some clastic sedimentary rocks. Šćavničar<br />
and Jović (1961,1962) found enstatite in Pliocene sands of the Kreka coal basin,<br />
using powder XRD, but provide no further information. Ristić et al. (1968) report<br />
on the occurrence of enstatite in sands from the Tuzla basin. We believe that in<br />
both cases the enstatite originates from the ultrabasic rocks of adjacent areas of the<br />
Bosnian serpentine zone.<br />
BRONZITE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Baumgärtel (1904), Hiessleitner (1951/52), Kišpatić (1897,<br />
1900), Pavlović (1899), Roskiewicz (1868), Tscherne (1892), Walter (1887).<br />
Early publications mention bronzite as an important constituent of the rocks<br />
in the Bosnian serpentine zone (BSZ). Hiessleitner (1951/52) describes bronzite<br />
occurrences in rocks of the chromium ore-body of Duboštica and Krivaja (p. 94),<br />
based on earlier papers by Walter (1887), Baumgärtel (1904) and Kišpatić (1897,<br />
1900). The largest amount of relevant information pertaining to bronzite occurrences<br />
in BSZ can be found in the two publications by Kišpatić. He maintained that bronzite<br />
is an important mineral constituent of all lherzolites – from Mt. Kozara in the northwest<br />
to the Višegrad area in the south-east. It needs to be mentioned that in the<br />
period when Kišpatić (but also earlier investigators) did their research, it was not<br />
possibly do differentiate between bronzite and enstatite only by microscopy. Results<br />
of more recent investigations – based on 2V angle measurements on a Fedorov-type<br />
rotating stage – indicate that most of what was determined as bronzite is, in fact,<br />
enstatite. Thus, bronzite probably occurs less frequently in bosnian ultrabasic rocks<br />
than previously believed (by Kišpatić).<br />
Kišpatić (1897) made a chemical analysis of the orthorhombic pyroxene<br />
hosted in the Pobilje lherzolite (near Vareš):<br />
SiO 2<br />
56.00<br />
Al 2<br />
O 3<br />
0.72<br />
FeO 8.98<br />
CaO 0.59<br />
MgO 32.44<br />
LOI 1.77<br />
Total 100.50<br />
The results of this analysis indicate that the Pobilje lherzolite indeed<br />
contains bronzite, since FeO is above 5%. The obvious conclusion, based on this<br />
example, is that a chemical analysis is a prerequisite (in additon to optical data) for<br />
a determination of orthorhombic pyroxenes.<br />
133
SILICATES<br />
Roskiewicz (1868) was apparently the first to mention bronzite in rocks of<br />
the BSZ, in the Vareš area (referenced by Kišpatić 1897, p. 96).<br />
Tscherne (1892) described the occurence of sepiolite on Mt. Ljubić near<br />
Prnjavor, mantioning the occurrence of bronzite in surrounding sepiolite rocks.<br />
HYPERSTHENE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Katzer (1924, 1926), Kišpatić (1897, 1900, 1904b, 1910),<br />
Majer and Jurković (1957, 1958), Marić (1927), Pamić (1971, 1971a), Pamić and<br />
Kapeler (1970), Pamić, Šćavničar and Međimorec (1973), Primics (1882), Ramović<br />
(1961,1962,1966), Schiller (1905), Tajder (1953), Trubelja (1960, 1961)<br />
In Bosnia and Hercegovina hypersthene occurs in some rocks of the Bosnian<br />
serpentine zone (BSZ), in certain Triassic igneous rocks and in andesite-dacite rocks<br />
in the area of Srebrenica.<br />
Kišpatić (1897, 1900, 1904b, 1910), Pamić (1971, 1971a), Pamić and<br />
Kapeler (1970), Pamić, Šćavničar and Međimorec (1973), Primics (1882), Ramović<br />
(1961,1962,1966), Schiller (1905), Trubelja (1960, 1961) report on hypersthene<br />
occurrences in basic and ultrabasic rocks of the BSZ – olivine gabbros, lherzolites<br />
and amphibolites.<br />
Hypersthene occurs in products of Triassic magmatic events in rocks of the<br />
schist mountains of central Bosnia – Bijela Gromila, as well as in the Jablanica<br />
gabbro complex. Several authors have reported on the above – Katzer (1924, 1926),<br />
Kišpatić (1910), Majer and Jurković (1957, 1958), Marić (1927).<br />
Kišpatić (1904a), Tajder (1953) and Ramović (1961, 1962, 1966) have<br />
determined hypersthene in in Tertiary andesites and dacites from the Srebrenica areas.<br />
1. The Bosnian serpentine zone (BSZ)<br />
The already referenced publications by Kišpatić provide most information<br />
on the occurrence of hypersthene in igneous and metamorphic rocks of the BSZ. He<br />
made microscopic determinations of hypersthene in the pyroxene amphibolite of<br />
Velika Bukovica on Mt. Ozren, in the olivine gabbro from Gostovići, in the eclogite<br />
amphibolite of Ravanka (near Gornje Vijake and Vareš). It is likely that hyperesthene<br />
also occurs in the lherzolite from the Ljučica creek on Mt. Kozara.<br />
Kišpatić (1897) found that the hypersthene in the Velika Bukovica<br />
amphibolite has poor cleavage but strong pleochroism. The hypersthenes from the<br />
134
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Ravanka eclogite amphibolite, and from the Turjački creek olivine gabbros have<br />
similar properties. The hypersthene from Turjački creek displays distinct pleochroism<br />
in brownish-red, yellowish-red and green-grey colours (Kišpatić 1897).<br />
Trubelja (1960) found that the feldspar-peridotite from Bosanska Jagodina<br />
contains only small amounts of hypersthene. In thin section, this hypersthene<br />
displays distinct psimatic cleavage and parting along (010). Some alteration into<br />
brown hornblende is visible. The measured -2V angle is 82-84°.<br />
Schiller (1905) determined hypersthene in gabbro from Višegrad. It is<br />
optically negative and contains at least 15% FeSiO 3<br />
.<br />
Trubelja (1961) mentions an ocurrence of hypersthene in the olivine gabbro<br />
from Stupčanica creek, near the village of Bjeliš on Mt. Konjuh. The negative 2V<br />
angle of 86° was measured on one hypersthene grain included in a diallage crystal.<br />
Pamić (1971, 1971a), Pamić and Kapeler (1970), Pamić, Šćavničar and<br />
Međimorec (1973) identified minor amounts of hypersthene (ca. 5-15%) in the<br />
amphibolites of the Krivaja – Konjuh metamorphic complex. Hypersthene is<br />
associated with alkaline plagioclase, garnet and edenite-pargasite hornblende.<br />
Pleochroism is distinct in thin section. The negative 2V angle of 63° and 64°<br />
corresponds to 40% FeSiO 3<br />
.<br />
Pamić (1971) found variable amounts of hypersthene in amphibolite schists<br />
in the souther part of Mt. Ozren.<br />
2. Hypersthene in Triassic intrusive rocks<br />
Kišpatić (1910), Katzer (1924, 1926), Majer and Jurković (1957, 1958)<br />
provide data on the occurrence of hypersthene in gabbro-diorite rocks of Bijela<br />
Gromila, near Travnik. Majer and Jurković (1957, 1958) found that the diorite of<br />
Kopile contains plate-like grains of hypersthene which display distinct pleochroism<br />
(Nz = greenish, Nx = pinkish-red). The measured 2V angle is -66° corresponding to<br />
ca. 25% FeSiO 3<br />
. Inclusions of plagioclase are common. Some alteration to uralite<br />
was observed. Hypersthene was also found in diorites from the source area of the<br />
Zasenjak creek. Here the hypersthene is highly altered.<br />
Kišpatić (1910) was the first to report on the occurrence of orthorhombic<br />
pyroxene in the gabbro rocks of the Jablanica complex. No further details on<br />
the mineral were given in this paper. Marić (1927) investigated the minerals in<br />
these rocks and found that hypersthene was an important constituent of basic<br />
rocks in the central parts of the massif. Hypersthen occurs together with olivine<br />
and diopside. Pleochroism is distinct in thin section (Nz = redish-brown, Nx =<br />
135
SILICATES<br />
colourless to grey). The maximum birefringence has a value of 0.019. The grains<br />
are elongated along the c axis, and sections parallel to (100) have a platelike habit.<br />
Some circumferential alteration of the grains (into hornblende and chlorite) was<br />
observed. Dispersed inclusions of magnetite are common. In one thin section of<br />
the gabbro from Bukov Potok on the left bank of the Neretva river, hypersthene<br />
grains completely enclose olivine.<br />
3. Hypersthene in the effusive rocks of Srebrenica<br />
Kišpatić (1904a) provide the first data on the occurrence of hypersthene<br />
in the products of Triassic magmatism in the Srebrenica area. Hypersthene was<br />
microscopically determined in andesite rocks from Potočari, Sikirić and Crveni Potok.<br />
In the Sikirić andesite, hypersthene is fairly common – particularly in the<br />
rock groundmass while phenocrystals are rare. In thin section the grains have a<br />
columnar habit with distinct prismatic cleavage and cross-fracturing. No pleochroism<br />
and a low birefringence were determined. Kišpatić’s measurement of the 2V angle of<br />
-50° indicates an FeSiO 3<br />
content of 54%. Hypersthene in Potočari andesite has quite<br />
similar properties. A maximum birefringence of 0.014 was measured.<br />
Tajder (1953) provides data on hypersthene occurrences in his treatise on<br />
the effusive rocks of Srebrenica. It was found only in the bytownite dacite from the<br />
village of Diminići, and then only in minor amounts in the form thin idiomorphic<br />
crystals. Alterations into biotite, chlorite and amphibole were observed. Some<br />
hypersthene grains are completely converted to chlorite.<br />
TREMOLITE<br />
Ca 2<br />
Mg 5<br />
[Si 8<br />
O 22<br />
] (OH) 2<br />
ACTINOLITE<br />
Ca 2<br />
(Mg,Fe 2+ ) 5<br />
[Si 8<br />
O 22<br />
] (OH,F) 2<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.545 : 1 : 0.292; β = 104° 42’ – tremolite<br />
a : b : c = 0.544 : 1 : 0.295; β = 105° 00’ – actinolite<br />
Cell parameters: a o<br />
= 9.84, b o<br />
= 18.05, c o<br />
= 5.575, Z = 2 – tremolite<br />
a o<br />
= 9.86, b o<br />
= 18.11, c o<br />
= 5.34, Z = 2 – actinolite<br />
Properties: perfect cleavage parallel to {110}, with occasionally distinct parting<br />
along one of the pinacoids. In terms of chemical composition, an isomorphous series<br />
between the Mg end-member (tremolite) and the Fe end-member (ferrotremolite).<br />
136
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The white to grey tremolite, in which a small amount of Mg can be substituted with<br />
Fe, converts into green actinolite. The chemistry of the isomorphous series is much<br />
more complex due to other possible substitutions resulting in the formation of other<br />
amphiboles i.e. hornblende. The specific gravity is given as 2.98-3.35, but increases<br />
with the iron content. The streak is white, the lustre vitreous. The refractive indices<br />
are moderately high, increasing with the iron content. The birefringence shows a<br />
small increase with an increase of Mg.<br />
X-ray data: actinolite d 2.709 (100) 3.120 (70) 2.535 (55)<br />
tremolite d 1.438 (10) 1.047 (9) 2.710 (8)<br />
IR-spectrum: actinolite (405) 425 445 462 507 540 645 660 686 758 920<br />
952 1000 1060 1105 3430 3540 3654 3668 cm -1<br />
tremolite 410 425 455 470 515 532 550 646 670 690 723 757<br />
924 955 995 1020 1105 1640 cm -1<br />
TREMOLITE AND ACTINOLITE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Baumgärtel (1904), Džepina (1970) , Golub (1961), Jurković<br />
(1954, 1956, 1957), Jurković and Majer (1954), Katzer (1924, 1926), Kišpatić<br />
(1897, 1900), Koch (1908), Kubat (1964), Majer (1962, 1963), Maksimović and<br />
Antić (1962), Marić (1927), Mojsisovics, Tietze and Bittner (1880), Pamić (1969a,<br />
1971, 1974), Pamić and Kapeler (1969), Pilar (1882), Primics (1881), Šćavničar<br />
and Jović (1962), Šibenik-Studen and Trubelja (1971), Šibenik-Studen, Sijarić and<br />
Trubelja (1976), Tajder and Raffaelli (1967), Trubelja (1960, 1961, 1963a, 1966a),<br />
Trubelja and Pamić (1965), Trubelja and Sijarić (1970), Varićak (1957, 1966, 1971).<br />
Tremolite, actinolite and other members of the isomorphous series are very<br />
common rock-forming minerals in Bosnia and Hercegovina. Nevertheless, these<br />
minerals have not been researched to any great extent. The available data is based<br />
only upon microscopic determinations or measurements of 2V and c : Z angles<br />
done using a Fedorov-type rotating stage. These minerals are often referred to just<br />
as ‘amphiboles’ or – with slightly more precision – ‘amphiboles of the tremoliteactinolite<br />
isomorphous series’. Detailed accounts of these minerals are very scarce.<br />
The available data on the tremolite-actinolite series has been published mainly<br />
in papers dealing with the petrology and mineralogy of the Bosnian serpentine zone<br />
(BSZ), where these minerals contribute to the composition of basic and ultrabasic<br />
intrusive rock, as well as some metamorphites<br />
Outside the BSZ, the tremolite-actinolite minerals occur in the metamorphic<br />
rocks of Mt. Motajica and Mt. Prosara and in the rocks of the schist mountains of<br />
central Bosnia. The are also found in Triassic igneous rocks (the Jablanica gabbro<br />
complex and the granites of Čajniče) and in some clastic sedimentary formations.<br />
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SILICATES<br />
1. The Bosnian serpentine zone (BSZ)<br />
Tremolite in rocks of the BSZ has been mentioned by several authors –<br />
Baumgärtel (1904), Kišpatić (1897, 1900), Golub (1961), Maksimović and Antić<br />
(1962). Kišpatić determined tremolite in the olivine gabbros from Vodoplav on Mt.<br />
Ljubić, in the troctolites from Krušička Rijeka on Mt. Ozren and the troctolites from<br />
Ravni creek and from the village of Lahci near Višegradska Banja. Tremolite also<br />
occurs in actinolite schists in Vidakovićev Potok near Višegrad. In most of these rocks<br />
tremolite formed as an alteration product of plagioclase, in the presence of olivine.<br />
Tremolite is usually colourless and without pleochroism in thin section. The<br />
results of more recent investigations give rise to our doubts that Kišpatić dealt only with<br />
pure tremolite in all cases, and not with the isomorphous series tremolite-actinolite.<br />
Golub (1961) did microscopic investigations of troctolites and uralitized<br />
gabbros from Mt. Kozara in which he was able to identify tremolite. In the Jovača creek<br />
troctolite, tremolite is prismatic, acicular or fibrous. No pleochroism was observed<br />
in thin section, it is colourless but with a high relief. Measurements on two larger<br />
grains showed the mineral to be optically biaxial and negative. The extinction angle<br />
in unoriented sections was 17° or less. Tremolite and actinolite were also identified in<br />
the corona around olivine grains in the uralite gabbro from Kotlovača creek.<br />
Baumgärtel (1904) determined tremolite in the secondary incrustations<br />
within fractures in the ultrabasic rocks of the Duboštica area.<br />
The amphiboles of the tremolite-actinolite series are mostly formed as a<br />
result of pyroxene alteration into uralite or as products of the reaction between<br />
olivine and alkaline plagioclase.<br />
The tremolite-actinolite amphiboles are important constituents of gabbros,<br />
olivine gabbros, uralite gabbros, feldspar-peridotites and some harzburgites from<br />
the Višegrad area (Trubelja 1960). The harzburgites from Bosanska Jagodina<br />
in the Rzava river valley carry tremolite and actinolite which were formed<br />
by uralitization of enstatite and amphibolization of olivine. A keliphytic rim<br />
indicates a reaction process between olivine and relicts of weathered plagioclase.<br />
In thin section tremolite grains display distinct prismatic cleavage. The measured<br />
extinction angle c : Z is 20°. Tremolite and actinolite in the feldspar-peridotites<br />
of Bosanska Jagodina were here also formed by alteration of hypersthene and<br />
diallage into uralite or by alteration of olivine. The tremolite and actinolite are<br />
located within the keliphytic corona around pyroxene and olivine. The negative<br />
2V angle is 86-87°.<br />
Needlelike tremolite/actinolite occurs in the olivine gabbro from Rijeka<br />
– Velika Gostilja, at the contact of olivine and plagioclase grains. They are also<br />
138
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
important constituents of the uralite gabbro from Smrijeće. Here they were formed<br />
by the alteration of diallage into uralite. There are so few relicts of pyroxene in the<br />
rock that we can conclude that the process of uralitization is more or less complete.<br />
In thin section, it appears that the alteration process prgressed in steps – the first<br />
step would be the formation of a thin keliphytic rim at the contact of pyroxene and<br />
plagioclase; the second step would involve the uralitization of the whole grain. The<br />
2V angle was determined to be -88°, the extinction angle = 13°.<br />
Tremolite and actinolite were found in the gabbro rocks from the village of<br />
Pijavice. The negative 2V angle was determined as 80.5-81.5°, the extinction angle<br />
= 19°. Prismatic cleavage is distinct, while twinning along (100) can be seen on<br />
some grains only.<br />
Trubelja (1961) identified the amphiboles of the tremolite-actinolite series in<br />
the diabases of Mt. Konjuh. These amphiboles and plagioclases are the predominant<br />
minerals of the porphyric diabase from the Blizanci creek. In thin section they are<br />
mostly pale green in colour, sometimes with a hint of blue. Some grains are pale<br />
brownish, and these display distinct pleochroism. Prismatic cleavage is apparent<br />
on homogeneous grains – the angle between the two cleavage planes is 57°; the<br />
extinction angle lies in the range 8¼-12¼°; the negative 2V angle is 87°.<br />
Šibenik-Studen and Trubelja (1971) determined the tremolite-actinolite<br />
amphibole in diabase from the village of Kovačići. They occur in two different<br />
modes – either as independent ‘nests’ or as alteration rims around augite grains. In<br />
both cases the amphiboles are the results of augite uralitization. Pamić (1974) reports<br />
on the presence of tremolite-actinolite amphiboles in gabbros from the Krivaja –<br />
Konjuh complex of ultrabasic rocks.<br />
Trubelja and Pamić (1965) found that this type of amphiboles are significant<br />
constituents of some igneous and metamorphic rocks of the Mt. Ozren series.<br />
Tremolite-actinolite amphiboles in the amphibole-zoisite schists from Krušik<br />
creek (near the village of Boljanići) are colourless or pale green in thin section,<br />
with no apparent pleochroism but dislaying distinct prismatic cleavage. The grains<br />
are comparatively large and fresh, making them appropriate for rotating stage<br />
measurements. The negative 2V angle is 86-88°, the extinction angle 17¼° to<br />
18¼°. These amphiboles seldom occur as homogeneous grains in the spilites from<br />
Konopljišt, rather forming pale green, fibrous aggregates.<br />
Trubelja (1966a) and Pamić (1969a, 1971, 1972c) report on the occurence of<br />
amphiboles in rocks on Mt. Kozara, Mt. Skatovica and in other parts of the BSZ.<br />
C. John (referenced in Mojsisovics et al. 1880) was apparently the first<br />
investigator to report the occurrence of actinolite in Bosnia – he determined it<br />
139
SILICATES<br />
microscopically in the amphibolite from Rudo. His findings were confirmed some<br />
years later by Primics (1881), Pilar (1882) and Kišpatić (1897, 1900) who identified<br />
actinolite in rocks throughout the BSZ. Golub (1961) determined actinolite in<br />
numerous basic rocks in the southern part of Mt. Kozara. In the actinolite gabbros<br />
from Kotlovača creek, actinolite is important as a constituent mineral and either<br />
builds up the alteration ‘corona’ around olivine grains, or occurs as granular or<br />
radiating aggregates with apparent pleochroism (Z = pale green, Y = yellowishgreen,<br />
X = colourless). The maximum extinction angle which could be measured on<br />
some grains was never in excess of 20°. The negative 2V angle = 66°. Actinolite in<br />
the Jovača troctolite is also pleochroitic with the same colour as given above.<br />
Golub determined amphiboles of the actinolite-hornblende series in uralite<br />
gabbros from Kozarački creek and in the Kotlovača gabbro-pegmatite. The amphiboles<br />
are only in part primary minerals, while the rest formed by alteration ofmonoclinic<br />
pyroxene. In thin section, the primary amphiboles are present as allotriomorphic<br />
grains (2-3 mm in size) showing distinct prismatic cleavage. Pleochroitic colour are<br />
Z = greenish, Y = yellowish-green, X = yellowish. The c : Z extinction angle is 22°,<br />
the negative 2V angle = 74°.<br />
The uralite gabbros from Kozarački creek contain amphiboles which again<br />
belong to the actinolite-honblende series. They formed by alteration of augite into<br />
uralite. Pleochroism is quite strong (Z = bluish-green, Y = green, X = pale green).<br />
The negative 2V angle was measured on two larger grains (grain I -2V = 88°, c : Z = 19°,<br />
grain II -2V = 85°, c : Z = 18°).<br />
Pamić and Kapeler (1969) report on the occurrence of actinolite in the<br />
gabbro-dolerite rocks at Mt. Kozara.<br />
Majer (1962) and Kubat (1964) note the occurrence of actinolite in the BSZ,<br />
in the area between the Vrbas and Bosna rivers. Trubelja (1960) determined actionlite<br />
microscopically in basic rocks from the Višegrad area. This author maintains that<br />
actinolite forms by alteration of monoclinic pyroxene into uralite, and that actinolite<br />
occurs mainly in diabase-doleritic rocks. The actinolite in diabase (dolerite) from<br />
the Rzava river (near Višegrad) is greenish in colour, with distinct pleochroism (Z<br />
= brownish-green, Y = dark green, X = light green). Prismatic cleavage is good, the<br />
angle between the two cleavage planes is 56°. The c : Z extinction angle is in the range<br />
15.3-16.8°, the negative 2V angle in the range 74.5-75.3°. B1/2 twinning = ^ (100) was<br />
observed. Similar properties have the actinolites from other rocks.<br />
140<br />
2. Mt. Motajica and Mt. Prosara<br />
Koch (1908), Katzer (1924, 1926) and Varićak (1966) report on actinolite in<br />
rocks of Mt. Motajica. Koch described the actinolite schists from Osovica creek (near
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Šeferovac) where actinolite occurs in the form of fibrous aggregates. It is colourless<br />
or pale green in thin section; pleochroism is weak but apparent – in pale green and<br />
blue-green. The extinction angle is somewhat greater than 15°. This actinolite was<br />
also noted by Katzer (1924, 1926).<br />
Varićak (1966) reports on the presence of actinolite in amphiboles and<br />
amphibole schists of Mt. Motajica. Actinolite is an important constituent of<br />
metamorphic rocks which belong to the 'facies of green rocks' which is ubiquitous –<br />
although in small masses only – at Mt. Prosara (Varićak 1957).<br />
3. The schist mountains of central Bosnia<br />
Jurković (1954, 1956, 1957), Jurković and Majer (1954), Tajder and Raffaelli<br />
(1967), Trubelja and Sijarić (1970) and Varićak (1971) determined actinolite in rocks<br />
of the schist mountains of central Bosnia.<br />
Tajder and Raffaelli (1967) maintain that actinolite is an important constituent<br />
of green schists. The actinolite is green-blue in colour with strong pleochroism.<br />
This iron-rich actinolite appears to be similar to the green-blue hornblende of the<br />
epidote-amphibolite facies. the hornblende, however, has higher concentrations of<br />
Al and Na than actinolite. Since distinguishing between these two amphiboles is not<br />
straightforward, it is possible that amphibole schists belong to the epidote-amphibolite<br />
facies, not to the 'facies of green rocks'. On the other hand, the paragenesis of pelitic<br />
schists which are associated with the amphibole schists, provides more arguments<br />
for the 'green rock' theory. Other important constituents of green schists are quartz,<br />
chlorite, epidote and magnetite.<br />
Jurković (1954, 1956) noticed the presence of actinolite in the pneumatolytichydrothermal<br />
baryte vein near the village of Hrastovi and Brestovsko. The baryte has<br />
formed within an extensively altered actinolite-epidote schist. Jurković determined,<br />
in thin section, that the actinolite occured in a coxcomb texture with tiny prismatic<br />
grains up to 0.3 x 0.7 mm in size, or as radiating, acicular aggregates. The actinolite<br />
has perfect cleavage parallel to [001] – in basal sections the two cleavage planes<br />
intersect at at angle of 124°. The extinction angle c : Z is 11-14°. Pleochroism is<br />
strong (Z = dark green, X = greenish-yellow).<br />
Jurković and Majer (1954) investigated the occurrence of actinolite in<br />
altered rhyolites (quartzporphyres) from Busovača, Kreševo and Fojnica. These<br />
authors also note the formation of actinolite by contact metamorphosis at the albiterhyolite/Paleozoic<br />
limestone interface, from Alinovci near Jajce.<br />
Šibenik-Studen, Sijarić and Trubelja (1976) report the occurrence of<br />
actinolite asbestos at Tarčin near Crna Rijeka. The fibrous aggregate was determined<br />
141
SILICATES<br />
as actinolite by X-ray diffraction, chemical analysis and IR-spectroscopy. The<br />
chemical analysis was done by M. Janjatović – SiO 2<br />
= 50.96; TiO 2<br />
= 0.22; Al 2<br />
O 3<br />
= 3.05;<br />
Fe 2<br />
O 3<br />
---; FeO = 5.52; CaO = 11.47; MgO = 22.43; K 2<br />
O ---; Na 2<br />
O = 0.40; H 2<br />
O - =<br />
0.69; H 2<br />
O + = 5.57; Total = 100.41<br />
4. Other occurrences<br />
Marić (1927) determined actinolite in the Jablanica gabbro. Šćavničar and<br />
Jović (1962) found actinolite to be a common mineral in Pliocene-age sands of the<br />
Kreka coal basin.<br />
Use<br />
Amphiboles of the tremolite-actinolite series can form fibrous aggregates<br />
(amphibole asbestos). These materials have been used widely as fire-proof<br />
fabrics, insulators, building blocks, additives in car-brake linings etc. Due to their<br />
environmental impact and extremely detrimental effect on human health, asbestos<br />
materials are being phased out of all industrial or technical applications.<br />
HORNBLENDE<br />
Ca 2<br />
[(Mg 4<br />
,Fe 4<br />
2+<br />
)(Al,Fe 3+ )] [Si 7<br />
AlO 22<br />
] (OH) 2<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.548 : 1 : 0.296; β = 105° 44’ (for common hornblende)<br />
Cell parameters: a o<br />
= 9.87, b o<br />
= 18.01, c o<br />
= 5.33 different for other varieties of hornblende<br />
Properties: perfect cleavage parallel to {110}, hardness = 6, specific gravity is given<br />
as 3.0-3.4, but increases with the iron content. The colour is dark green, brown<br />
or black. The streak is white, the lustre vitreous. The refractive indices are fairly<br />
high, birefringence is moderate. Hornblende belongs to the group of monoclinic<br />
amphiboles. The chemical composition of hornblende is variable and complex, so<br />
that trace elements – like titanium and others – frequently enter into its structure.<br />
The varieties of hornblende have different names such as edenite, ferro-edenite,<br />
tchermakite, pargasite, hastingsite etc.<br />
X-ray data: substantial differences depending on variety of hornblende (see Tröger<br />
1967, p. 423-473 and other handbooks)<br />
IR-spectrum: common hornblende 445 505 540 635 655 695 725 778 880 900<br />
990 1010 1110 1146 cm -1 basalt hornblende (415) 465 510 630 680 740 (908) 955<br />
980 1050 1650 cm -1<br />
142
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
HORNBLENDE IN BOSNIA AND HERCEGOVINA<br />
A u t h o r s: Barić (1970a), Behlilović and Pamić (1963), Boué (1870),<br />
Čutura (1918), Džepina (1970), Đorđević (1958, 1960), Đurić and Kubat (1962),<br />
Foullon (1893), Golub (1961), Hlawatsch (1903), John (1880, 1888), Katzer (1903,<br />
1924, 1926), Kišpatić (1897, 1900, 1904, 1904a, 1904b, 1910), Koch (1908),<br />
Kubat (1964), Majer (1962, 1963), Majer and Jurković (1957, 1958), Marić (1927),<br />
Marković and Takač (1958), Mojsisovics, Tietze and Bittner (1880), Pamić (1960,<br />
1963, 1969a, 1970, 1971, 1971a, 1972c, 1972d, 1973, 1974), Pamić, Dimitrov and<br />
Zec (1964), Pamić and Kapeler (1969, 1970), Pamić, Šćavničar and Međimorec<br />
(1973), Pamić and Trubelja (1962), Paul (1897), Pavlović (1889), Pavlović and Ristić<br />
(1971), Ramović (1957, 1961, 1962, 1963, 1966, 1968), Roskiewics (1868), Simić<br />
(1964, 1966), Šćavničar and Jović (1962), Šćavničar and Trubelja (1969), Šibenik-<br />
Studen (1972/73), Tajder (1953), Trubelja (1957, 1960, 1961, 1963, 1963a, 1963c,<br />
1966a), Trubelja and Pamić (1956, 1965), Varićak (1957, 1966), Walter (1887).<br />
In Bosnia and Hercegovina hornblende is one of the most common and<br />
ubiquitous rock-forming minerals. Hornblende is a constituent mineral of numerous<br />
igneous and metamorphic rocks, even in some sedimentary ones. Several varieties of<br />
hornblende occur in different basic, intermediate i acidic igneous rocks from many<br />
areas in Bosnia and Hercegovina. They occur both in intrusive and effusive rocks.<br />
Some hornblende types and varieties are characteristic and essential constituents of<br />
many amphibolites and amphibolite schists of the Bosnian serpentine zone (BSZ).<br />
The author has encountered some difficulty in writing this chapter on<br />
hornblende, because many petrographic publications do not refer to hornblende as<br />
a separate mineral species – rather as a member of the amphiboles. This implies<br />
that data – by which we could distinguish between the various types of hornblende<br />
– is relatively scarce.<br />
1. Hornblende in rocks of the Bosnian serpentine zone<br />
C. John (1880) was the first (or certainly one of the first) investigators who<br />
microscopically determined hornblende in rocks of the Bosnian serpentine zone<br />
(BSZ). This author reports occurrences of hornblende in diorites from Čelinci<br />
and Kladanj, epidiorites from the Maglaj area and Barakovac in the Vrbanja river<br />
valley. Fibrous brown hornblende occurs in the gabbros from Višegrad (of which<br />
John published a chemical analysis – table 17). The hornblendes in gabbros<br />
and olivine gabbros from Višegrad formed by alteration of diallage. Different<br />
diallage grains results in the formation of different hornblende varieties. For<br />
example, diallage of a dark colour converts into brown, very pleochroitic<br />
hornblende, while lightly coloured diallage results in the formation of fibrous,<br />
almost colourless hornblende.<br />
143
SILICATES<br />
Table 17. Chemical composition of hornblende from the area of Višegrad<br />
Plumose hornblende<br />
Fibrous hornblende<br />
SiO 2<br />
50.22 50.50<br />
Al 2<br />
O 3<br />
5.64 5.90<br />
FeO 21.79 21.78<br />
CaO 12.42 12.30<br />
MgO 9.81 9.55<br />
LOI 1.17 1.20<br />
101.05 101.23<br />
Kišpatić (1897, 1900) provides a substantial amount of data derived from<br />
microscopic measurements of amphiboles from various rocks of the BSZ. It is<br />
interesting to note that Kišpatić never mentioned hornblende as a separate mineral<br />
entity. The authors hesitation in this respect is difficult to percieve since we know<br />
that the various amphiboles could have been distingusihed and classified by their<br />
extinction angles in thin section. In the cited publication, Kišpatić paid particular<br />
attention to microscopic determinations of various metamorphic rocks from the BSZ,<br />
in which amphiboles are essential – and sometimes the only constituent minerals.<br />
In a separate publication with the title ‘Petrographic notes from Bosnia’<br />
Kišpatić (1904) also provided numerous results of microscopic determinations of<br />
amphiboles, without distinguishing their types and varieties.<br />
Kišpatić reports results of two chemical analyses for 3-4 cm long columnar<br />
amphibole crystals from Nemila in the Bosna river valley (Table 18). The analyst<br />
was F. Tućan.<br />
Table 18. Chemical analysis of amphibole from Nemila, Bosna river valley<br />
1 2<br />
SiO 2<br />
44.37 44.63<br />
Al 2<br />
O 3<br />
24.66 24.97<br />
Fe 2<br />
O 3<br />
6.79 1.78<br />
FeO n.d. 4.51<br />
MgO 8.55 8.81<br />
CaO 11.09 11.31<br />
H 2<br />
O 3.49 3.36<br />
Total 98.95 99.37<br />
A substantial amount of data based on microscopic determination and<br />
chemical analyses of hoirnblendes from BSZ was collected and published in the<br />
period after the II World war.<br />
Marković and Takač (1958) determined pale green and weakly pleochroitic<br />
hornblende in rocks of the Višegrad area. Trubelja (1957, 1960) investigated the<br />
144
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
hornblende in olivine gabbros from Bosanska Jagodina where the hornblende is an<br />
alteration product of pyroxenes. This author maintains that hornblende occurs mostly<br />
as an essential constituent (in some cases only as an accessory mineral) of feldsparperidotites,<br />
troctolites, olivine gabbrosand diabase-doleritic rocks. Hornblende has<br />
a characteristic mode of occurrence in veins such as pegmatites and hydrothermal<br />
veins in the Višegrad area.<br />
Green and brown hornblende occurs in the feldspar-peridotites of Bosanska<br />
Jagodina in the Rzav river valley. In thin section the brown hornblende is highly<br />
pleochroitic (Z = brown, X = pale brown), the c : Z extinction angle is 19.3°. Prismatic<br />
cleavage is good and the angle between the two cleavage planes is 57.3°. Another<br />
hornblende grain in the same thin section has following properties: pleochroism (Z<br />
= light bluish, X = pale green); the extinction angle is 22.5°.<br />
Some hornblende formed as a result of pyroxene alteration into uralite, in<br />
troctolites from Gornji Dubovik and olivine gabbros from Mirilovići.<br />
Amphiboles (hornblende) are predominant minerals in the Banja Potok<br />
diabases near Višegradska Banja. Here also they are products of pyroxene alteration.<br />
Pyrite and ilmenite inclusion are common. Pleochroism is strong (Z = bluish-green,<br />
X = light green). Hornblende grains are homogeneous and the measured extinction<br />
angle is in the range 19.8-25.5°, the negative 2V angle is in the range 72-82°.<br />
Hornblende occurring in dolerites from the Rzav valley river, on the Dobrun<br />
– Smrijeće road, displays distinct pleochroism (Y = light brown, X = light green).<br />
The extinction angle is 22°, the negative 2V angle is in the range 79-82.5°.<br />
At Suha Gora (Pavitine) the hornblende is associated with clinozoisite and<br />
prehnite. The grains are columnar or foliated and display distinct prismatic cleavage.<br />
Prismatic faces are observed on columnar crystals. Measurements done on a rotating<br />
stage gave following values: the c : Z extinction angle is in the range 9-24.5°, the<br />
negative 2V angle 73-82°. Plewochroism is distinct (Z = pale green, X = light green).<br />
A cleavage plane was used for angle measurement with a reflexion goniometer. The<br />
angle between the prism faces was measured<br />
(110) : (1-10) = 55° 09’<br />
The occurrence of hornblende and associated minerals in the rocks at<br />
Pavitine should be understood in terms of postmagmatic processes which followed<br />
the extrusion of basaltic rocks through older gabbro series.<br />
Green hornblende, occurring at the Lahci gabbro quarry, formed under<br />
similar paragenetic conditions as the one at Suha Gora. This hornblende has<br />
foloowing optical constants: the c : Z extinction angle is in the range 11-23º, the<br />
145
SILICATES<br />
negative 2V angle between 86° and 88.5°. Twinning (B1/2 = ^ [100]) is common;<br />
pleochroism (Z = bluish-green, X = light green).<br />
Pamić, Šćavničar and Međimorec (1973) made a detailed investigation of<br />
various hornblendes from amphibolitic rocks of the BSZ. Microscopy, chemical<br />
analysis and X-ray diffraction methods were employed in this study. Seven samples<br />
of hornblende from amphibolites of Mt. Skatovica near Banja Luka (sample<br />
numbers 0, 1, 1’, 2, 4, 5 and 7), three hornblende samples from the Krivaja – Konjuh<br />
amphibolites (sample numbers 8, 9 and 10) and one sample from the amphibolite<br />
schists near Rudo (sample number 11). The research methods used (measurement<br />
of optical constants on a rotating stage, chemical analyses and other procedures)<br />
including structural formula calculations, enabled the authors to determine several<br />
types and varieties of hornblende. The authors findings are as follows:<br />
2V angle<br />
Extinction angle c : Z<br />
Brown hornblende -77.5° 16.5°<br />
Green hornblende -84.5° 19.3°<br />
Pargasite hornblende +86° 19°<br />
In addition to the above results, the authors were able to distinguish several transitional<br />
varieties of hornblende – i.e. green-edenite hornblende, green-brown hornblende etc.<br />
The chemical analysis of 11 hornblende samples is given in Table 19.<br />
Calculated formula units are given in Table 20. Table 21 gives the composition<br />
of the hornblende samples, defined by their end-member percentages. The ‘pure’<br />
hornblendes or end-member varieties can be clearly distinguished from ‘composite’<br />
types. For example, sample no. 10 is a pure pargasite (from a corundum-bearing<br />
amphibole schist). The 2V angle of this pargasite is +83°, the extinction angle is<br />
18.5°, the refractive index 1.670 ± 0.005. The pargasite is completely colourless in<br />
thin section.<br />
Sample no. 8 is interesting because of its comparatively high Ti content<br />
(5.35% TiO 2<br />
) and was therefore classifies as kersutite or titanium-pargasite. This<br />
amphibole was also extracted from amphibole schists of the Krivaja – Konjuh<br />
metamorphic complex. The 2V angle is -77°, the extinction angle 16°, the refractive<br />
index 1.670 ± 0.005. Pleochroitic colours are X = Y = light grey, Z = light brown.<br />
Pamić (1970) identified green edenite-hornblende (chromium-amphibole)<br />
in rocks of the chromium ore body at Duboštica. This hornblende could, however,<br />
be identified only on two localities – Borak and Šabanluke where it occurs in the<br />
form of foliated and finegrained aggregates in alternating layers with chromite. In<br />
thin section this hornblende is completely colourless and displays distinct prismatic<br />
cleavage. The angle between the two cleavage planes is 124°. The 2V angle is -86°<br />
146
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
to -86.5°, the extinction angle is 18-19°. It chemical composition is as follows:<br />
SiO 2<br />
= 50.47; TiO 2<br />
= 0.03; Al 2<br />
O 3<br />
= 5.17; Cr 2<br />
O 3<br />
= 0.33; Fe 2<br />
O 3<br />
= 2.79; FeO = 6.79;<br />
MnO = 0.07; MgO = 17.92; CaO = 13.42; Na 2<br />
O = 1.40; K 2<br />
O = 0.23; H 2<br />
O + = 1.56;<br />
H 2<br />
O - = 0.01; Total = 110.19<br />
The following ionic numbers (formula units) were calculated: Si + Al = 8.00;<br />
Al + Cr + Fe 3+ + Fe 2+ + Mn + Mg = 5.14; Ca + Na + K = 2.48; OH = 1.47<br />
Table 19. Chemical composition of amphiboles from the Bosnian serpentine zone<br />
0 1 1’ 2 4 5 7 8 9 10 11<br />
SiO 2<br />
43.5 45.71 39.5 45.48 42.28 42.28 46.75 38.52 44.80 41.92 42.51<br />
TiO 2<br />
1.7 0.33 0.09 0.08 0.22 0.03 0.34 5.35 0.77 --- 0.35<br />
Al 2<br />
O 3<br />
12.7 12.45 15.7 11.38 13.25 9.81 6.34 13.55 8.48 15.47 14.70<br />
Fe 2<br />
O 3<br />
6.9 1.46 7.6 6.20 2.29 5.51 1.70 5.69 3.35 3.69 1.04<br />
FeO 6.4 13.44 7.5 4.15 11.46 3.34 6.75 7.48 10.40 3.71 7.86<br />
MnO 0.09 0.29 0.04 0.19 0.28 0.01 0.11 0.24 0.26 0.08 0.11<br />
MgO 12.90 10.08 11.2 15.80 12.58 21.96 20.67 10.87 18.17 17.05 17.81<br />
CaO 11.0 11.20 11.2 12.72 14.76 11.90 12.50 12.70 9.48 14.00 10.60<br />
Na 2<br />
O 2.1 2.46 3.3 1.09 0.92 1.20 1.48 2.51 1.81 2.96 1.94<br />
K 2<br />
O 0.43 0.10 0.23 0.16 0.19 0.68 0.14 0.71 --- 0.43 0.28<br />
H 2<br />
O + n.d. 1.21 n.d. 2.43 1.39 2.98 2.45 1.98 1.71 0.92 1.99<br />
H 2<br />
O - n.d. 0.39 n.d. 0.32 0.13 0.42 0.53 0.21 0.53 0.15 0.52<br />
P 2<br />
O 5<br />
n.d. 0.16 n.d. 0.04 0.16 0.09 0.09 --- --- 0.10 0.18<br />
Total 97.72 99.28 96.36 100.04 99.91 100.49 99.85 99.81 99.76 100.48 99.89<br />
Table 20. Structural formulas of amphibole – based on 230 atoms<br />
Sample 0 1 2 4 5 7 8 9 10 11<br />
Na 0.49 0.470 0.132 0.269 0.164 0.416 0.718 0.509 0.811 0.542<br />
A K 0.08 0.018 0.029 0.034 0.126 0.026 0.013 0.073 0.052<br />
Ca 0.060 0.355 0.511 0.511 0.364 0.36 0.298 0.118 0.250<br />
Ca 1.74 1.765 1.896 1.974 1.328 1.560 1.993 1.176 2.00 1.350<br />
X<br />
Na 0.09 0.229<br />
Fe 2+ 0.20 0.006 0.104 0.026 0.408 0.440 0.007 0.825 0.650<br />
Mg 0.264<br />
Ca 0.013<br />
Mn 0.01 0.034 0.023 0.034 0.017 0.030 0.041 0.007 0.014<br />
Fe 2+ 0.58 1.648 0.397 1.386 0.378 0.923 0.438 0.444 0.297<br />
Y Mg 2.80 2.202 3.394 2.756 4.501 4.465 2.410 3.929 3.606 3.817<br />
Ti 0.19 0.038 0.012 0.029 0.005 0.046 0.297 0.105 0.048<br />
Fe 3+ 0.75 0.159 0.672 0.248 0.489 0.048 0.636 0.366 0.393 0.153<br />
Al 0.48 0.881 0.490 0.518 0.407 0.016 0.537 0.623<br />
Ti 0.300<br />
Fe 3+ 0.115 0.138<br />
Z Al 1.69 1.281 1.442 1.774 1.684 1.083 1.962 1.496 2.049 1.874<br />
Si 6.31 6.719 6.558 6.226 6.201 6.779 5.783 6.504 5.951 6.126<br />
H 2<br />
O 0.595 1.168 0.685 1.447 1.184 0.983 0.827 0.434 0.956<br />
147
SILICATES<br />
Table 21. Composition of amphiboles expressed as end-member ratios<br />
Sample #<br />
Composition<br />
0 Ed 16.6<br />
Pa 36.9<br />
Ts 32.1<br />
Ho 14.4<br />
1 Ed 34.5<br />
Pa 13.7<br />
Ts 14.7<br />
Ho 37.1<br />
(Ed 26.3<br />
Pa 21.1<br />
Ts 18.0<br />
Ho 23.4<br />
Gl 11.2)<br />
1’ Pa 26<br />
Ts 28<br />
Gl 10<br />
2 Ed 12.1<br />
Pa 9.6<br />
Ts 34.9<br />
Ho 43.4<br />
4 Ed 14.7<br />
Pa 50.9<br />
Ts 26.7<br />
Ho 7.7<br />
5 Ed 16.4<br />
Pa 64.0<br />
Ts 15.6<br />
Ho 4.0<br />
7 Ed 63.0<br />
Pa 17.6<br />
Ts 4.3<br />
Ho 15.1<br />
8 Kersutite (titanium-pargasite 84%)<br />
9 Ed 40.9<br />
Pa 38.4<br />
Ts 10.1<br />
Ho 10.6<br />
10 Pa 100.0<br />
11 Ed 10.7<br />
Pa 74.1<br />
Ts 13.4<br />
Ho 1.9<br />
Ed = edenite (ferro-edenite); Pa = pargasite (ferro-pargasite, Mg-hastingsite); Ts =<br />
tschermakite (ferro-tschermakite); Ho = common hronblende; Gl = glaucophane.<br />
The unit cell parameters of the investigated hornblendes are given in Table 22.<br />
Table 22. Unit cell parameters of amphiboles (Pamić, Šćavničar and Međimorec 1973)<br />
Sample # * a 0<br />
(Å) b 0<br />
(Å) c 0<br />
(Å) β (º) V 0<br />
(Å 3 )<br />
2 9.810 18.039 5.282 105.13 902.34<br />
3 9.811 17.998 5.267 105.27 897.15<br />
5 9.833 17.994 5.269 105.29 899.26<br />
6 9.863 18.106 5.295 105.17 912.61<br />
7 9.800 18.019 5.270 105.19 898.10<br />
8 9.892 18.085 5.347 105.23 923.01<br />
9 9.814 18.010 5.269 105.22 898.65<br />
10 9.783 17.973 5.278 104.96 894.81<br />
11 9.796 17.998 5.273 105.28 897.38<br />
* Chemical analysis was not done on samples No. 3 and 6 (loc. Mt. Skatovica, Banja Luka)<br />
In a short preliminary report on amphibolites in the Krivaja – Konjuh area<br />
Pamić (1971a) notes the folowing amphiboles: brown hornblende, green hornblende,<br />
edenite and pargasite.<br />
Pamić and Kapeler (1970) microscopically determined pargasite-hornblende<br />
to be an essential constituent of schists and corundum-bearing amphibolites from<br />
Donja Vijaka near Vareš. In thin section this hornblende is colourless, the measured<br />
+2V angle is in the range 76-78º, while the extinction angle varies between 15°<br />
and 21º. Macroscopically, the hornblende has an emerald-green colour. The green<br />
hornblende has following optical constants: the 2V angle is negative and in the range<br />
-76° to -80°, c : Z = 13-20°. The pargasite-edenite hornblende has a negative 2V<br />
angle of -87° to -88°, and is colourless in thin section.<br />
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<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Pamić (1974) notes the occurrence of brown hornblende in gabbro-type<br />
rocks of the Krivaja – Konjuh ultrabasic complex, but provides no further data.<br />
Đorđević (1958, 1960) studied in some detail the occurrence of hornblende<br />
in basic rocks of the Vareš area. In the coarse-grained amphibole gabbro hornblende<br />
is present in the form grains from 2.7 x 1.0 mm to 12 x 3 mm in size. It is of a<br />
dark green colour, or somewhat paler in the case of weathered grains. Following<br />
observations were made in thin section: pleochroism (Z = green, Y = yellow-green,<br />
X = pale yellow-green); the negative 2V angle is in the range -77° to -88° ; the<br />
extinction angle c : Z is in the range 12.5-23.5°. The angle between the (110) and<br />
(1-10) cleavage planes is 125.5°.<br />
The hornblende contained in finegrained amphibole gabbro occurs as crystals<br />
up to 0.3 mm in size, and has a dark green colour. In thin section, the observed<br />
pleochroitic colours are Z = green, Y = yellow-green, X = pale yellow. The negative<br />
2V angle is in the range -83° to -89°, the extinction angle is in the range 12-15.5°.<br />
The measured (110) : (1-10) is 125°. The chemical composition of this hornblende<br />
is given as: SiO 2<br />
= 42.73; TiO 2<br />
= 1.25; Al 2<br />
O 3<br />
= 14.22; Fe 2<br />
O 3<br />
= 6.05; FeO = 9.27;<br />
MnO = 0.18; MgO = 13.02; CaO = 9.05; Na 2<br />
O = 0.92; K 2<br />
O = 0.52; H 2<br />
O + = 2.90;<br />
H 2<br />
O - = 0.21; Total = 100.32<br />
Based on the above chemical analysis, the structural formula of the<br />
hornblende is (Ca 1.419<br />
Mg 0.363<br />
Fe 2+ 0.145 Na 0.131 K 0.048 Mn 0.022 ) 2.127 (Mg 2.483 Fe2+ 0.992 Al 0.727<br />
Fe 3+ 0.662 Ti 0.136 ) 5 - (Si 6.267 Al 1.733 ) 8 O 22 (OH) 2<br />
The end-member percentages of the analyzed hornblende are as follows:<br />
ferro-tschermaikte 31.5%; ferro-hastingsite 4.0%; hastingsite 14.0%; tschermakite<br />
22.5%; Mg-gedrite 23.5%; Fe-gedrite 1.0%; kupferite 3.5%.<br />
The chemical composition of hornblende from the finegrained amphibole<br />
gabbro is given as (Đorđević 1960, p. 115): SiO 2<br />
= 41.16; TiO 2<br />
= 2.00; Al 2<br />
O 3<br />
=<br />
13.70; Fe 2<br />
O 3<br />
= 1.83; FeO = 7.88; MnO = 0.14; MgO = 17.83; CaO = 10.23; Na 2<br />
O<br />
= 1.57; K 2<br />
O = 0.66; H 2<br />
O + = 2.54; H 2<br />
O - = 0.47; Total = 100.01<br />
Based on the above chemical analysis, the structural formula of the<br />
hornblende is (Ca 1.618<br />
Mg 0.583<br />
Na 0.441<br />
Fe 2+ 0.146 K 0.122 Mn 0.017 ) 2.927 (Mg 3.327 Fe2+ 0.827 Al 0.423<br />
Ti 0.220<br />
Fe 3+ 0.203 ) 5 - (Si 6.061 Al 1.939 ) 8 O 22 (OH) 2<br />
The end-member percentages of the analyzed hornblende are as follows:<br />
ferro-tschermaikte 3.3%; ferro-hastingsite 10.0%; hastingsite 36.7%; tschermakite<br />
17.1%; Mg-gedrite 21.2%; Fe-gedrite 5.4%.<br />
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SILICATES<br />
The genesis of amphibole formation in amphibolites and amphibole schists<br />
is closely related to the formation of the entire mineral association in these rocks.<br />
At this stage we cannot provide a final theory on the genesis of amphibolites or the<br />
amphiboles contained in them. The occurence of corundum in some of these rocks<br />
makes things even more difficult. The amphibolites could be products of regional but<br />
also of contact metamorphism. It needs to be said that both edenite and pargasite are<br />
typical minerals for contact metamorphism.<br />
Trubelja (1961) determined brown and green hornblende in the olivine<br />
gabbros from Stpčanica creek, near the village of Bjeliš. In thin section, the green<br />
hornblende is pleochroitic in the colours Z = light green, X = dark green; the extinction<br />
angle is 17.5°. The brown hornblende has the following pleochroitic colours – Z =<br />
light brown, X = dark brown; the extinction angle is 17° , the 2V angle is -75° . Both<br />
hornblendes have good cleavage. Overgrowths on diallage are common. Brown<br />
and green hornblende also occurs in the dolerites from the Blizanci creek, where<br />
overgrowths upon augite are frequently observed. The author maintains that these<br />
overgrowths and reaction rims are the consequence of magmatic melts reacting with<br />
previously crystallized augite, so that he considers the amphiboles (hornblendes)<br />
to be primary minerals formed in a normal sequential crystallization process. The<br />
brown hornblende has a 2V angle of -79° while the extinction angle is 26.8°. For the<br />
green hornblende these values are – extinction angle = 18.8°, pleochroism Z = light<br />
green, X = light green.<br />
Trubelja and Pamić (1965) and Pamić (1973) found hornblende to be a<br />
common mineral also in the basic rocks at Mt. Ozren. Hornblende is an essential<br />
constituent of the porpyric amphibole-dolerites from the Krivaja creek. In thin section<br />
the hornblende is pleochroitic (Z = yellow-brown, Y = yellowish, X = light yellow).<br />
The average 2V angle is -65°, the c : Z extinction angle = 18°. The hornblende<br />
formed by alteration from augite.<br />
The pyroxene amphibolites of Gornja Bukovica carry fresh and homogeneous<br />
brown hornblende. Pleochroism is Z = brown, X = light brown. The 2V angle = -77°,<br />
the extinction angle c : Z = 14°.<br />
Amphiboles from the amphibolic dunites from Vijenac (east of Mt. Ozren)<br />
were microscopically determined as hornblende with an increased kersutite content<br />
(Pamić 1973). The 2V angle = -81° to -82°, the extinction angle c : Z = 13-17°.<br />
The amphibole is probably the source of Ti (TiO 2<br />
= 1.05%). The same hornblende<br />
occurs also in the harzburgite from this locality. Pamić also mentions peridotites<br />
with pargasite (?) hornblende with these constants: 2V angle = -86° to -88°, the<br />
extinction angle c : Z = 18° to 22°.<br />
150
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Majer (1962) provides some additional information on amphiboles in igneous<br />
and metamorphic rocks of the BSZ. Green and black hornblende is an essential<br />
constituent of amphibole gabbros, garnet-bearing gabbros and hornblendites.<br />
Majer classifies these rocks as igneous, although others believe them to be typical<br />
metamorphic rocks.<br />
Majer (1963) identified hornblende to be the dominant mineral of albite<br />
granite, present in the form of pebbles within the diabase-chert series. Such pebbles<br />
are abundant near the village of Prisoje on the Doboj – Banja Luka railroad. The<br />
hornblende grains are columnar, the extinction angle is 14°. Pleochroism is bluegreen<br />
to greenish-yellow.<br />
Đurić and Kubat (1962) and Kubat (1964) have investigated the copper<br />
mineralizations on Mt. Čavka, finding hornblende in garnet-bearing amphibolites.<br />
Its extinction angle is 18°, the 2V angle -88°.<br />
Hornblende is an essential mineral in numerous igneous rocks of Mt. Kozara,<br />
as observed by Golub (1961) and Trubelja (1966a). Hornblende occurs in the diabases<br />
from the Bukovica creek and dolerites from Trnava creek. In both cases the hornblende<br />
seems to have formed by alteration of augite. Pleochroism is Z = greenish-brown, X =<br />
pale greenish-brown. The 2V angle = -69°, the extinction angle c : Z = 12°<br />
2. Hornblende in products of Triassic magmatism<br />
Many authors mentioned at the beginning of this chapter have reported on<br />
the presence of hornblende in various products of Triassic magmatism. Roskiewics<br />
(1868) and Boué (1870) provide the earliest accounts.<br />
Marić (1927) made detailed determinations of hornblende occurring in<br />
gabbro-type rocks of Jablanica gabbro complex. He found hornblende to be the<br />
third most common mineral in these rocks, i.e. after feldspar and pyroxene. Green<br />
hornblende is closely associated with monoclinic pyroxene, and overgrowths<br />
are a common feature. Replacement of pyroxene by hornblende is sometimes so<br />
extensive (or even complete) that psudomorphic hornblende is frequently observed.<br />
Green hornblende also has the propensity to replace augite, and this is the case in<br />
rocks outcropping between Zlato and the Tovarnica magnetite mine, and around the<br />
confluence of the Rama and Neretva rivers.<br />
Hornblende’s prismatic cleavage can best be observed in longitudinal sections.<br />
Pleochroism – Z = greenish, Y = brownish-yellow, X = pale yellow. Maximum<br />
birefringence = 0.022. The green hornblende is much more common than the yellowbrown<br />
variety which occurs in the central part of the massif. This hornblende is also<br />
optically negative like the green variety, but the extinction angle is larger.<br />
151
SILICATES<br />
Green hornblende with somewhat different optical characteristics occurs in in<br />
the northern part of the massif, along the right bank of the Neretva river. The grains are<br />
0.15 x 0.005 mm in size. Pleochroism – Z = greyish-green, Y = brownish-yellow, X =<br />
pale yellow. The maximum birefringece is slightly smaller, at Nz – Nx = 0.019.<br />
Large hornblende crystals can be found in fractures and cracks within the<br />
gabbro rock at Bukov Pod. The columnar hornblende crystal are up to 10 cm long and<br />
1.5 cm thick. They are of a dark green colour – fresh cleavage planes have a metallic<br />
lustre. Prismatic cleavage can be observed macroscopically on some crystals. The<br />
hornblende from the Jablanica massif has been described with more or less detail<br />
by a number of other authors (Hlawatsch, 1903; John 1888; Katzer 1903; Kišpatić<br />
1910; Ramović 1968; Roskiewics 1868).<br />
Data on hornblende occuring in various igneous rocks in the schist mountains<br />
of central Bosnia can be found in publications by the following authors – Barić<br />
(1970a), Čutura (1918), John (1888), Katzer (1924, 1926), Kišpatić (1910), Majer<br />
and Jurković (1957, 1958), Mojsisovics et al. (1880).<br />
Majer and Jurković (1957, 1958) determined the green hornblende in the<br />
gabbro-dioritic massif of Bijela Gromila, south of Travnik. John (1888) made a<br />
microscopic determination of hornblende from the diorite rocks between Donji Vakuf<br />
and Jajce, as well as from the Tešanica (probably Trešanica) diorite from Bradina in<br />
Hercegovina.<br />
Barić (1970a) also reports a determination of the Bradina hornblende, a<br />
common hornblende from a keratophyre rock from Trešanica cliff. We are not quite sure<br />
whether John referred to this hornblende or not. The hornblende occurs as phenocrysts<br />
in the keratophyre and has a distinct pleochroism – Z = green, Y = pale yellowishgreen,<br />
X = colourless to pale yellow. The 2V angle was measured on two hornblende<br />
grains (using a rotating stage, on a section where both optic axes were visible) and lies<br />
in the range -74° to -74.5° with a red > violet dispersion of optic axes. The 2V angle<br />
was measured on several other sections which showed only one optic axis, and the<br />
measured values are in the range from -73° to -77.5°. The optical extinction angle c : Z<br />
varies in the range 14.3° to 18.7°. Twinning along (100) is rarely observed.<br />
Data on hornblende in products of Triassic magmatism in other parts of<br />
Bosnia and Hercegovina is relatively scarce (Behlilović and Pamić 1963; Boué 1870;<br />
Pamić 1960, 1963; Simić 1963, 1964; Trubelja 1963, 1963a) although hornblende<br />
appears to be a common mineral in these rocks.<br />
Trubelja (1963a) measured optucal constants on hornblende from the<br />
amphibolic granites of the Čajniče area (village of Dublje). The measured 2V angle<br />
= -78.5° to -84°, the optical extinction angle is 15-16°.<br />
152
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
3. Hornblende in products of Tertiary magmatism<br />
Hornblende is an essential constituent of volcanic rocks in the area of<br />
Srebrenica. This area was investigated in detail by M.Tajder and relevant information<br />
is provided in his treatise on the petrology of this area (Tajder 1953). This publication<br />
contains extensive information about optical properties of hornblende, derived mainly<br />
from measurements of the optical axis angle, the extinction angle and determination<br />
of pleochroism.<br />
The amphibole dacites of Diminići village contain amphiboles in the form of<br />
common hornblende. The average c : Z extinction angle is 17°, the 2V angle is in the<br />
range -85° to -88°. Twinning along (100) is fairly common. Pleochroism is strong, in<br />
yellow and brown.<br />
Dacites at Kiselica creek contain green hornblende as idiomorphic,<br />
hipidiomorphic and irregularly shaped elongated crystals up to 1.4 x 0.7 mm in size.<br />
Pleochroism in yellow-green and dark green is distinct. The extinction angle c : Z =<br />
16°, the 2V angle = -82°. Green hornblende also occurs in amphibole dacites in the<br />
area of Srebrenica.<br />
John (1880), Kišpatić (1904a), Pavlović (1889) and Walter (1887) report<br />
on hornblende occurrences in Tertiary effusive rocks in the Srebrenica area. John<br />
(1880) determined optically the hornblende contained in the trachytes of Šušnjara, in<br />
the quartzpropilites of Srebrenica, the Ljubovija dacite and the hornblende andesites<br />
of Zvornik. Kišpatić (1904a) corrected John’s findings with regard to the trachyte<br />
from Šušnjara, maintaining that the rock is a hypersthene andesite (Kišpatić does not<br />
distinguish between various amphiboles in his publication). The hornblendes from<br />
Srebrenica were also studied by Ramović (1957, 1961, 1962, 1963 and 1966).<br />
The Tertiary effusive rocks outcropping in various locations in the Bosna<br />
river valley carry hornblende which is often an essential constituent of these rocks.<br />
Data on these hornblendes can be found both in older and more recent publications<br />
John (1880), Kišpatić (1904), Paul (1879), Trubelja and Pamić (1956, 1965). John<br />
(1880) microscopically determined hornblende in the trachyte upon which the<br />
Maglaj fortress is erected. Trubelja and Pamić (1956, 1965) determined brown and<br />
green hornblende in the amphibole dacite near the village of Parnice and the town<br />
of Maglaj. The hornblendes occur as regular idiomoprhic crystals, also as foliated<br />
aggregates. Some grains show evidence of magmatic resorption. Zonar structure is<br />
often observed in thin section. Twinning is according to the B 1/2<br />
= ^ (100) system.<br />
Such twins are characteristic insofar as the individual crystals share the vibration<br />
direction (Y), the crystallographic axis c [001] and the prismatic cleavage. The<br />
extinction angle c : Z is in the range 18-19.9°, the 2V angle is 75° to 83°. Pleochroism<br />
is in green and greenish-yellow.<br />
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SILICATES<br />
4. Hornblende in rocks of Mt. Motajica and Mt. Prosara<br />
Not much data is available on hornblende at Mt. Motajica and Mt. Prosara.<br />
The first report is by C. John (1880) on hornblende in the granites of Mt. Motajica.<br />
Here, hornblende is common and sometimes an essential constituent of various<br />
metamorphic rocks. Koch (1908) reports about the occurence of amphiboles in<br />
the Kamen Potok amphibolite (near Kobaš) but gives no further details about its<br />
mineralogical classification, although it is probably hornblende since the optical<br />
extinction angle he measured is 23°.<br />
Varićak (1966) gives a fairly detailed account of the hornblende occurrence<br />
in amphibole gneisses, honblendites, amphibolites and amphibole schists of<br />
Mt. Motajica. Hornblende in amphibole gneisses is quite pleochroitic (Z = dark green, Y<br />
= green, X = pale yellow-green). The extinction angle c : Z = 18.5°, the 2V angle = -80°.<br />
The hornblendites carry hornblende which is also strongly pleochroitic (Z =<br />
greenish-brown, Y = olive-green, X = pale yellow-brown), but grains with different<br />
pleochroitic colours are also present. It is interesting to note that hornblendes with<br />
different pleochroisms also have different optical constants and the range of values<br />
is considerable (extinction angles are in the range 15-17.5°, the 2V angles are in the<br />
range between -70° and -86°).<br />
Hornblendes in amphibolites and amphibole schists also have distinct<br />
pleochroism (Z = olive-green, Y = yellow-green, X = pale yellowish-green). The c :<br />
Z = 17.5-19.5°, the 2V angles are -74° to -85°.<br />
At Mt. Prosara hornblende occurs infrequently and only in the so-called<br />
'green rocks' (Varićak 1957).<br />
154<br />
5. Hornblende in other rocks<br />
According to John (1880), hornblende is an essential constituent of<br />
amphibole-zoisite schists at Zvornik and the amphibolites from Rudo. Information<br />
on the occurrences of hornblende in sedimentary rocks in Bosnia and Hercegovina is<br />
scant, and refers mainly to the Tertiary age Tuzla basin and the quartz-sand deposit<br />
at Zvornik (Šćavničar and Jović 1962; Pavlović and Ristić 1971). The Pliocene sands<br />
of the Kreka coal basin carry hornblende and actinolite withn the B and C horizons.<br />
Šćavničar and Jović determined the hornblende to be pleochroitic i green and browngreene.<br />
The angle of oblique extinction is is between 18° and 20°. The hornblendes<br />
originate from metamorphic rocks of the 'facies of green rocks' and amphibolites.<br />
The 'Bijela Stijena' deposit of quartz sand from the area of Zvornik carries<br />
hornblende as a constituent of the heavy mineral fraction (Pavlović and Ristić 1971).<br />
No further information is provided.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Hornblende has been identified in the insoluble residue of some carbonate<br />
rocks in Hercegovina (Gaković and Gaković 1973).<br />
GLAUCOPHANE<br />
Na 2<br />
[(Mg 3<br />
,Al 2<br />
) [Si 8<br />
O 22<br />
] (OH) 2<br />
A u t h o r s: Foullon (1895), Kišpatić (1897, 1900, 1902, 1904b), Pamić,<br />
Šćavničar and Međimorec (1973), Pavlović and Milojković (1958), Tajder and Herak<br />
(1972), Tućan (1919, 1930, 1957), Varićak (1966).<br />
Glaucophane belongs to the group of alkaline amphiboles.<br />
H.B. Foullon (1895) authored first information about glaucophane in Bosnia<br />
and Hercegovina. Foullon compared the chemical composition of the glaucophane<br />
asbestos of Halilovac in western Bosnia with the same mineral from the greek<br />
island of Rhodos, which he referred to as rhodusite. Kišpatić (1902) investigated<br />
the same material some years later, confirming that it was a fibrous glaucophane i.e.<br />
glaucophane asbestos. Pavlović and Milojković (1958) use the name krokydolite<br />
(alternative spelling is crocydolite) and krokydolite asbestos for this mineral.<br />
Kišpatić (1897, 1900) in his well known treatise about rocks of the Bosnian<br />
serpentine zone mentions a single occurrence of glaucophane only, in the olivine<br />
gabbro from Omarski creek at Mt. Kozara. An amphibole resembling glaucophane<br />
occurs in the greenschists of Polom on the Drina river.<br />
Varićak (1966) finds glaucophane to be an essential constituent of<br />
glaucophanites at Mt. Motajica, in the area of Mramorje, where they are associated<br />
with albite gneisses. Microscopic investigations showed the glaucophane to have<br />
a short prismatic habit, and a distinct cleavage along (110). The angle between the<br />
two cleavage planes is 124.5°. Some alteration into chlorite, albite and epidote<br />
was observed. The pleochroism is – Z = blue to blue-violet, Y = pale indigo-blue,<br />
X = colourless. The optical axis plane is parallel to (010). the average extinction<br />
angle = 6°, the 2V angle = 34°. The described glaucophanite contains also epidote,<br />
clinozoisite, garnets, ilmenite and titanite.<br />
CROCYDOLITE – RIEBECKITE<br />
Na 2<br />
[(Fe 3<br />
2+<br />
Fe 2<br />
3+<br />
) [Si 8<br />
O 22<br />
] (OH) 2<br />
A u t h o r s: Foullon (1895), Grimmer (1897), Joksimović (1903) Kišpatić<br />
(1902), Pavlović and Milojković (1958), Tućan (1919, 1930, 1957).<br />
The term crocydolite is today used for the fibrous variety of the mineral<br />
riebeckite, a member of the amphibole group (Deer, Howie and Zussman 1963).<br />
155
SILICATES<br />
There is only one known occurrence of crocydolite in Bosnia and<br />
Hercegovina, near Halilovac in the Japra river valley. Some information about this<br />
crocydolite has been recently published by Pavlović and Milojković 1958, based<br />
upon XRD, optical microscopy and differential thermal analysis (DTA). Chemical<br />
analysis of two samples was also done.<br />
Older publications (Foullon 1895; Grimmer 1897; Kišpatić 1902) considered<br />
this material to be asbestos, glaucophane asbestos or simply ‘blue asbestos’ becuase<br />
of its bluish colour. According to these authors, limited amounts of this material (soft<br />
as cotton) were mined at Halilovac – in ancient times but also after the II World War.<br />
Macroscopically, the crocydolite asbestos from Halilovac occurs in a<br />
complex, filiform, silky aggregate. The length of the silky-thin fibers is 1-7 cm. The<br />
fibers are soft, flexible (pliable) but tough. Pavlović and Milojković have determined<br />
the density of the material = 3.249 and approximate refractive indices (n = 1.620 for<br />
Na-light). The glass melt of the material, prepared by melting in an electric arc, had<br />
a refractive index n = 1.609. Powder XRD data are given in Table 23:<br />
Table 23. X-ray diffraction data of the crocydolite asbestos from Halilovac<br />
I d (Å) I d (Å)<br />
10 8.7 2 2.32<br />
3 4.98 3 2.17<br />
6 4.58 2 2.06<br />
8 3.44 1 2.01<br />
3 3.28 2 1.65<br />
8 3.13 1 1.61<br />
2 3.03 3 1.58<br />
2 2.81 2 1.51<br />
10 2.73 1 1.30<br />
2 2.61 3 1.29<br />
4 2.54<br />
A comparison of the XRD data for the Halilovac crocydolite with literature<br />
data reveals some differences in the d values. The authors believe this to be a<br />
consequence of variations in the chemical composition.<br />
Several chemical analyses of the crocydolite asbestos from Halilovac have<br />
been published (Table 24).<br />
156<br />
The structural formula of crocydolite from Halilovac is given below:<br />
(Si 7.35<br />
Al 0.62<br />
) 7.97<br />
(Fe 3+ 1.60 Fe2+ 0.91 Mg 2.00 Ca 0.39 ) 4.90 (Na 2.32 K 0.26 ) 2.58 (OH 2.76 O 21.24 ) 24.00<br />
The crocydolite asbestos from Halilovac, as named by Pavlović and<br />
Milojković (1958), has a somewhat different chemical composition from ‘normal’
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
crocydolite (riebeckite) since it contains more magnesium. It could be defined as a<br />
Mg-crocydolite, approaching glaucophane from the chemical point of view. However,<br />
the paragenesis and origins of the crocydolite are not quite clear. The authors write<br />
“ ... we found that the underlying structure is composed of granular gypsum and<br />
some dolomite. The overlying layer is composed of ill-smelling, black, bituminous<br />
limestone. In between is a fractured, clayey mass impregnated with water up to 2 m<br />
thick, with aggregated soft asbestos material of a dirty green colour. Other portions<br />
of these aggregates are brick-red, which is the colour of the clay. This entire clayey<br />
mass reminds us of a land-slide’’.<br />
In our opinion, the description of the paragenesis and other available information<br />
is still insufficient to explain the origin of this rare and interesting occurrence.<br />
Table 24. Chemical analysis of the crocydolite asbestos, Halilovci<br />
1 2 3 4 5 impure<br />
6 pure<br />
SiO 2<br />
54.10 52.35 54.51 54.65 50.28 50.22<br />
Al 2<br />
O 3<br />
--- 5.47 2.68 2.53 3.75 3.59<br />
Fe 2<br />
O 3<br />
15.75 15.36 13.60 15.34 12.41 14.54<br />
FeO 7.33 --- 7.33 6.66 7.53 7.46<br />
MgO 12.60 10.39 10.60 10.95 8.46 9.19<br />
CaO 1.44 --- 2.59 1.13 2.41 2.46<br />
Na 2<br />
O 5.40 --- 5.47 5.33 8.59 8.24<br />
K 2<br />
O 0.45 4.37 0.38 0.78 3.71 1.46<br />
CO 2<br />
0.09 --- 0.59 0.23 --- ---<br />
Water --- 4.18 --- --- --- ---<br />
LOI 2.81 6.07 2.09 2.43 2.83 2.84<br />
99.98 98.19 99.84 100.03 99.97 100.00<br />
Source: 1. Foullon 1895 (analyst L. Schneider), 2. Grimmer 1897 (analyst S. Bošnjaković),<br />
3. and 4. Kišpatić 1902, 5. and 6. Pavlović and Milojković 1958 (analyst R. Milojković).<br />
WOLLASTONITE<br />
Ca 3<br />
[Si 3<br />
O 9<br />
]<br />
Wollastonite is a typical mineral of contact metamorphism. It occurs very<br />
rarely in Bosnia and Hercegovina. There is only one known occurrence of wollastonite<br />
– in the magnetite ore deposit at Tovarnica near Jablanica (Čelebić 1967). Here, the<br />
wollastonite is either incoporated in garnets and epidotes or included in the kornite<br />
silicate matrix.<br />
Wollastonite is widely used in the manufacture of ceramics and refractories,<br />
and as filling agent in paint.<br />
157
SILICATES<br />
TOBERMORITE<br />
Ca 5<br />
Si 6<br />
[O,OH] 18<br />
.5H 2<br />
O<br />
Crystal system and class: Orthorhombic, disphenoidal class.<br />
Lattice ratio: a : b : c = 1.542 : 1 : 3.083<br />
Cell parameters: a o<br />
= 11.3, b o<br />
= 7.33, c o<br />
= 22.6 Z = 4<br />
Properties: very finegrained, white mass. Refractive index Ny = 1.558<br />
A u t h o r s: Đorđević and Stojanović (1972), Stojanović (1973), Stojanović,<br />
Đorđević and Đerković (1974).<br />
Tobermorite is a rare hydrated calcium silicate and only occurrence has been<br />
identified in Bosnia and Hercegovina – at Banja Kulaša in the Bosnian serpentine<br />
zone (Stojanović 1973; Stojanović, Đorđević and Đerković 1974). Suolunite also<br />
occurs at this locality.<br />
Tobermorite occurs in diabases, at depths between 40 and 95 m, in the<br />
form of thin veins and globular aggregates. One variety is crystalline tobermorite<br />
of an acicular, radiating habit with needles ca. 3 mm long growing from the inner<br />
surfaces of nodular geodes. The other variety is microcrystalline tobermorite in the<br />
form of thin veins with a layered texture. Individual tobermorite grains can in such<br />
aggregates be identified only under the microscope. In thin section tobermorite is<br />
colourless and displays parallel extinction. The refractive index is greater than that<br />
of Canada balm.<br />
Powder XRD data of both crystalline and microcrystalline (11 Å tobermorite)<br />
varieties are given in Table 25. Some differences in the intensities have been observed.<br />
Table 25. Powder XRD data of tobermorite from Banja Kulaši (Stojanović et al. 1974)<br />
Crystalline<br />
tobermorite<br />
ASTM-card<br />
10-373<br />
Microcrystalline<br />
tobermorite<br />
ASTM-card<br />
19-1364<br />
d (Å) I d (Å) I d (Å) I d (Å) I<br />
11.5 100 11.3 100 11.5 100 11.3 80<br />
5.74 10 5.72 8 5.67 4<br />
5.55 5 5.55 90 5.55 4<br />
5.46 30 5.46 25 5.48 25<br />
3.82 25 3.84 20 3.78 8 3.78 6<br />
3.63 6 3.64 8<br />
3.55 30 3.57 70 3.54 20 3.53 20<br />
3.32 8 3.34 20 3.32 20 3.31 18<br />
158
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
3.24 20<br />
3.08 30 3.11 70 3.08 80 3.08 100<br />
2.97 30 2.99 70 2.97 60 2.98 65<br />
2.86 60 2.86 10<br />
2.82 80 2.83 100 2.82 30d 2.82 40<br />
2.80 10 2.80 40<br />
2.72 15 2.75 20 2.72 10 2.73 10<br />
2.52 20 2.53 60 2.52 15 2.52 12<br />
2.44 10 2.45 50 2.44 20 2.43 10<br />
2.31 25 2.32 70B 2.30 20 2.297 8<br />
2.29 50 2.29 60 2.28 20 2.266 14<br />
The two varieties of tobermorite also demonstrate different behaviour if<br />
heated for the purpose of identifying possible phase changes (thermal analysis).<br />
Chemical analysis of the Banja Kulaši tobermorite: SiO 2<br />
= 54.19; CaO = 40.70;<br />
H 2<br />
O + = 13.55<br />
Some of the calcium is due to the presence of admixed calcite. The presence of K, Al,<br />
Mg, Na, Ti, Cr, Fe, Sr, Li, Be and other elements was determined by spectrochemical<br />
analysis.<br />
According to Stojanović et al. (1974) the Banja Kulaši tobermorite is<br />
of hydrothermal origin. Tobermorite (and subsequently suolunite) crystallized<br />
at comparatively low temperatures (around 175°C), in an alkaline (high pH)<br />
environment.<br />
XONOTLITE<br />
Ca 6<br />
[Si 6<br />
O 17<br />
] (OH) 2<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 2.332 : 1 : 0.958; β ~ 90º (based on unit cell)<br />
Cell parameters: a o<br />
= 16.56, b o<br />
= 7.34, c o<br />
= 7.04 Z = 2<br />
Nomenclature and synonyms: named after the discovery site of the mineral Tetela<br />
de Xonotla in the state of Puebla in Mexico. Taylor (1954) determined that xonotlite<br />
is identical with the mineral jurapaite which was identified as a new mineral from<br />
Crestmore, near Riverside in California (Eakle 1921).<br />
Properties: fibrous mineral. Properties are discussed in the section on its occurrence<br />
in Bosnia.<br />
A u t h o r s: Džepina (1970), Đurić and Nikolić (1969), Majer and Barić<br />
(1973), Trubelja (1971b, 1972/73, 1975).<br />
159
SILICATES<br />
1. The Teslić region<br />
Xonotlite was first identified in Bosnia and Hercegovina in 1965/66 by Dušan<br />
Džepina, during a field-work assignment related to his diploma (baccalaureate)<br />
thesis. His task was to collect samples from Mt. Borje (near Teslić) for mineralogical<br />
and petrological investigations. The xonotlite he found occurs in a rodingitized<br />
metamorphic garnet-bearing rock (Džepina 1970, p. 138-139). The colour is snowywhite,<br />
sometimes with pale pink overtones and a silky-vitreous lustre. It forms fibrous<br />
and radiating aggregates in cracks and vacuoles 1-3 cm in size within the rock. In thin<br />
section, xonotlite is optically biaxial and positive, with a parallel extinction. Cleavage<br />
is apparent and parallel to the axis of the fibrous crystals. Džepina reports the following<br />
refractive indices: Nz = 1.593, Nx = 1.584, birefringence Nz – Nx = 0.009.<br />
The powder diffraction data obtained by Džepina (assisted by S. Đurić) is<br />
given in Table 26.<br />
Table 26. Powder XRD data for xonotlite from Teslić<br />
I d (Å) I d (Å)<br />
5 6.88 7 2.66<br />
1 6.49 2 2.63<br />
6 4.24 5 2.497<br />
2 3.91 4 2.326<br />
7 3.71 4 2.241<br />
7 3.23 7 2.032<br />
10 3.08 8 1.942<br />
8 2.82 3 1.833<br />
Đurić and Nikolić (1969) made some further determinations on the material<br />
provided by Džepina. XRD data was used to calculate the unit cell dimensions:<br />
a o<br />
= 16.80, b o<br />
= 7.34, c o<br />
= 7.05; β approximately 90°<br />
The specific gravity is 2.57. The authors also did a differential thermal<br />
analysis of the material. The mineral appears to release water at 830°C (there is a<br />
small endothermic peak in the DTA curve at this temperature). Thermogravimetry<br />
was used to establish the rate of loss-of-water. The inflexion of the TGA curve at<br />
830°C corresponds to a loss of 2.24-2.41% of water. The general appearance of the<br />
curve implies a continuous release of water which could be moisture trapped within<br />
the fibrous aggregate of xonotlite.<br />
Chemical analysis of the xonotlite from Teslić gave the following percentages:<br />
SiO 2<br />
= 48.65; TiO 2<br />
= 0.02; Al 2<br />
O 3<br />
= 0.23; FeO = 0.42; MgO = 0.21; CaO = 46.53;<br />
Na 2<br />
O = 0.04; H 2<br />
O 1000° = 3.84; H 2<br />
O 100° = 0.33; Total = 100.27<br />
The calculated structural formula for this xonotlite is:<br />
(Ca 6.06<br />
Mg 0.03<br />
Fe 0.04<br />
) 6.13<br />
Si 5.91<br />
Al 0.03<br />
O 18.00<br />
x 1.02H 2<br />
O<br />
160
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
In the calculation the authors took into consideration only the 2.50% water,<br />
determined by thermal analysis to be constitutional (crystal) water. Traces of V, Ba<br />
and Mn were determined by spectrochemical methods.<br />
Đurić and Nikolić (1969) regard the xonotlite from Mt. Borja near Teslić to<br />
be the last product of the autometamorphism of basic and ultrabasic rocks.<br />
2. The Višegrad region<br />
Two separate occurrences of xonotlite have up to now been identified<br />
in the area around Višegrad. One occurrence is on the Višegrad-Dobrun road ca<br />
1.5 km from Višegrad. The second occurrence of xonotlite is in the diabases of<br />
Bosanska Jagodina.<br />
The occurrence of xontlite at Višegrad was first reported by Trubelja (1971b,<br />
1972/73, 1975). Xonotlite here occurs in prehnitized diabases in the form of thin veins<br />
(several mm up to 1 cm thick) and fillings of cracks and cavities in the rock mass. It<br />
forms white, fibrous aggregates – the fibres are subparallel to parallel with the walls<br />
of the cavities. In thin section, the needle-like crystals are elongated parallel to the<br />
b axis (010), and the exctintion is parallel also. The mineral is optically positive and<br />
either uniaxial or the 2V angle is very small.<br />
Refractive indices were determined using the immersion method, in sodium<br />
light. Nz = 1.589 ± 0.002, Nx = 1.570 ± 0.002. Therefore, the birefringence<br />
Nz – Nx = 0.010.<br />
The specific gravity (determined by picnometry) is 2.746 g/cm 3 (at 18°C).<br />
The xonotlite was also studied by thermal analysis – the DTA curve shows two<br />
endothemic peaks (at 820°C, and a weal peak at around 700°C). Trubelja (1972/73,<br />
1975) believes this to be a dehydroxilation of xonotlite and its conversion to<br />
wollastonite.<br />
The infra-red absorption spectrum (400-4000 cm -1 ) of the xonotlite from<br />
Višegrad is given in Figure 11. Characteristic absorption maxima, related to the<br />
vibrations of Si-O and O-H bonds, are given in Table 27.<br />
Table 27. Absorption maxima in the IR spectrum of xonotlite from Višegrad<br />
cm -1<br />
410 635 928 1065<br />
537 671 975 1203<br />
611 741 1010 3618<br />
161
SILICATES<br />
Figure 11. IR spectrum of xonotlite fromVišegrad (Trubelja 1972/73)<br />
Based on the above determinations, and the presence of the 3618 cm -1<br />
peak, Trubelja (1972/73, 1975) concludes that this xonotlite formed during the<br />
hydrothermal phase, at comparatively low temperatures. The 711 cm -1 absorption is<br />
probably due to admixed calcite.<br />
Powder XRD investigations of the xonotlite were done using both the film<br />
technique and diffractometry.<br />
XRD data obtained by the film technique are given in Table 28. The data<br />
corresponds to d and intensity values for xonotlite in the literature.<br />
Table 28. XRD data for xonotlite fromVišegrad (film technique)<br />
Nr. d (Å) I relative<br />
Nr. d (Å) I relative<br />
1 8.525 w 17 1.838 vs<br />
2 7.00 s 18 1.824 mm<br />
3 4.25 s 19 1.774 mm<br />
162
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
4 3.91 mm 20 1.749 m<br />
5 3.632 s 21 1.707 s<br />
6 3.495 w 22 1.679 m<br />
7 3.227 s 23 1.637 mm<br />
8 3.09 vvs 24 1.597 m<br />
9 2.822 vs 25 1.575 m<br />
10 2.690 vs 26 1.519 ms<br />
11 2.622 w 27 1.421 w<br />
12 2.503 s 28 1.390 ms<br />
13 2.331 m 29 1.334 w<br />
14 2.245 m 30 1.319 mm<br />
15 2.036 vs 31 1.3055 mm<br />
16 1.987 vs 32 1.2520 m<br />
Intensities were estimated visually.<br />
A comparison of the XRD data with ASTM-card 3-0568 shows some<br />
differences in the intensities of certain lines, particularly the most characteristic<br />
ones. For example, the d = 3.09 line has an intensity 100 in the ASTM-card, but was<br />
of low intensity in our diffractogram. We have the opposite case with the line at d =<br />
7.00 Å. These variations, and those observed using the diffraction vs. film technique,<br />
may be explained by preferred orientation of the samples.<br />
Chemical analysis (analysts F. Trubelja and M. Janjatović) of xonotlite gave<br />
following reults:<br />
SiO 2<br />
= 49.79; CaO = 46.37; Na 2<br />
O = 0.20; H 2<br />
O + = 3.50; H 2<br />
O - = 0.27; Total = 100.13<br />
The corresponding structural formula is Ca 5.91<br />
Na 0.02<br />
(OH) 2.72<br />
Si 5.92<br />
O 17.00<br />
Xonotlite from the Višegrad region is of hydrothermal origin. Hydrothermal<br />
waters circulated through the host rocks induced the alteration of alkaline plagioclase<br />
and the migration of certain ions into the hot hydrothermal solutions. The comparatively<br />
high concentration of calcium and silica in these solutions facilitated the crystzallization<br />
of xonotlite, but also of prehnite and zeolites (Trubelja 1972/73, 1975).<br />
At Bosanska Jagodina, xonotlite also crystallizes within cracks and cavities<br />
in the diabase host rock (left bank of the Rzav river, in the abandoned quarry). This<br />
xonotlite was also investigated by XRD and IR spectroscopy.<br />
All identified occurrences of xonotlite in Bosnia are within the Bosnian<br />
serpentine zone. Majer and Barić (1973) have reviewed the then available data on<br />
xonotlite from Bosnia.<br />
163
SILICATES<br />
RHODONITE<br />
CaMn 4<br />
[Si 5<br />
O 15<br />
]<br />
Crystal system and class: Triclinic, pinacoidal class.<br />
Lattice ratio: a : b : c = 0.625 : 1 : 0.541<br />
α = 85° 10’ β = 94° 04’ γ = 111° 29’<br />
Cell parameters: a o<br />
= 7.99, b o<br />
= 12.47, c o<br />
= 6.75 Z = 2<br />
Properties: perfect cleavage along {001} and {100}. Hardness = 5.5-6.0. Specific<br />
gravity = 3.4-3.68. Colour is pink, pinkish-red, brownish-red. Streak is white, lustre<br />
vitreous.<br />
X-ray data: d 2.77 (100) 2.98 (65) 2.92 (65) – ASTM-card 13-138<br />
IR-spectrum: 415 455 495 507 537 563 578 650 670 695 723 876 902<br />
920 950 1003 1035 1064 1160 3440 3660 cm -1<br />
A u t h o r s: Jurković (1956), Katzer (1906, 1907, 1924, 1926)<br />
Rhodonite is an exceptionally rare mineral in Bosnia and Hercegovina.<br />
Accoridng to available literature, rhodonite occurs only in two locations – in the ore<br />
province of Bitovnja (locality Budišna Ravan) and in the area of Čevljanovići.<br />
The rhodonite from Budišna Ravan was first mentioned by F. Katzer (1907,<br />
1924, 1926). Katzer maintains that the origin of this rhodonite is related to a variety<br />
of igneous rock which he named quartzporphyrfelsite.<br />
Jurković (1956) roports that the locality of Budišna Ravan is 15 km<br />
north-west of Konjic and 8 km north-east of Ostrožac, between the creeks Klisac<br />
and Vranjić. This locality is known for its occurrence of the mineral tetrahedrite.<br />
Other minerals are also found here (malachite, azurite, psilomelane, pyrolusite<br />
and rhodonite).<br />
Katzer (1906) is the only author to report on the occurrence of rhodonite<br />
at Čevljanovići. His report deals with manganese mineralizations, and he believes<br />
rhodonite to be a very rare mineral.<br />
164
PYROPHYLLITE<br />
Al 2<br />
[Si 4<br />
O 10<br />
] (OH) 2<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.577 : 1 : 2.084; β = 99° 55’<br />
Cell parameters: a o<br />
= 5.15, b o<br />
= 8.92, c o<br />
= 18.59 Z = 4<br />
Properties: good cleavage on {001}. The lamellar crystals are flexible but inelastic.<br />
Hardness is 1-1.5. Colour is white or pale yellow, red or brownish (from admixed<br />
iron oxides). Streak is white, lustre pearly on cleavage planes.<br />
X-ray data: d 3.05 (100) 9.16 (40) 4.46 (40)<br />
IR-spectrum: 420 465 485 522 542 580 627 815 837 855 910 951 1070<br />
1121 1635 3440 3640 3668 cm -1<br />
A u t h o r s: Barić and Tajder (1955, 1956), Barić and Trubelja (1971,<br />
1975), Čelebić (1967), Čičić (1975), Muftić and Čičić (1969), Podubsky (1955),<br />
Simić (1972), Tajder and Herak (1972).<br />
Only one occurrence of pyrophyllite is known today in Bosnia and<br />
Hercegovina, near the village of Parsovići in the Konjic area. Simić (1972) reports<br />
on the presence of pyrophyllite in early Triassic clastic rocks near Sarajevo, but is<br />
not sure if it is pyrophyllite or hydromica-muscovite.<br />
The pyrophyllite at Parsovići is one of the essential constituents of the<br />
pyrophyllite schists where the mineral association comprises also quartz, dolomite,<br />
calcite, kaolinite, muscovite, gypsum and some other less abundant minerals.<br />
Pyrophyllite, quartz and the carbonate minerals are essential constituents of the rock<br />
and their percentage varies in different sections of the deposit. This pyrophyllite<br />
schist body was discovered some twenty years ago when first publications on this<br />
mineral became available (Barić and Tajder 1955, 1956; Podubsky 1955). It was<br />
discovered in the valley of the Šćukovac creek, a tributary of the Neretvica river.<br />
The schist was investigated microscopically and by chemical analysis by Barić and<br />
Tajder who found that the following minerals were present in the schist: quartz<br />
= 44.2%; pyrophyllite = 35.3%; carbonates = 3.9% and limonite = 1.3%. Čelebić<br />
(1967) found the percentage of pyrophyllite to be 58.86%.<br />
Simultaneously with the first paper by Barić and Tajder (1955), Podubsky<br />
(1955) also published a report on the pyrophyllite from Parsovići. He found<br />
that the schist contained quartz, illite (muscovite, sericite), some carbonate and<br />
montmorillonite, in addition to pyrophyllite. The determination was based on DTA<br />
and XRD data. The paper contains 3 DTA curves and one diffraction pattern. The<br />
presence of montmorillonite was not confirmed by powder XRD analysis (diffraction<br />
analysis by S. Šćavničar and K. Kranjc).<br />
165
SILICATES<br />
Microscopy of the pyrophyllite in thin section, done by Barić and Tajder,<br />
showed that pyrophyllite had a high birefringnce (and displayed vivid interference<br />
colours) and that the refractive index was greater than that of Canada balm. The<br />
grains display parallel extinction and have a positive character of elongation.<br />
Čelebić (1967) believes that these pyrophyllite schists are of Permian age,<br />
representing a lateral equivalent of the red schistose sandstone facies. Their origin is<br />
supposedly hydrothermal.<br />
Muftić and Čičić (1969) report that the pyrophyllite schists were mined<br />
since 1963, for the requirements of paper, ceramics and rubber industries, as well<br />
as for the production of plant protection chemicals. Čičić (1975) estimates that the<br />
quantity of pyrophyllite schist is around 15 million tons. He mentions pyrophyllite<br />
from the village of Repovac, but the rock was shown to be a hydromuscovite schist<br />
(Barić and Trubelja 1971, 1975).<br />
Use: Pyrophyllite is an important industrial mineral. It is used in the<br />
manufacture of ceramics (tiles), refractories, fillers, plastics, rubber, paint,<br />
insecticides and glass. Dense varieties of pyrophyllite (also known under the names<br />
agalmatolite or pagodite) have been used in China since ancient times for carvings<br />
and similar purposes.<br />
166<br />
TALC<br />
Mg 3<br />
[Si 4<br />
O 10<br />
] (OH) 2<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.578 : 1 : 2.067; β = 100°<br />
Cell parameters: a o<br />
= 5.27, b o<br />
= 9.12, c o<br />
= 18.85 Z = 4<br />
Properties: good cleavage on {001}. The lamellar crystals are flexible but inelastic.<br />
Hardness is 1, specific gravity = 2.82. Colour is pale green, white or grey. Streak is<br />
white, lustre pearly on cleavage planes. Refractive indices are generally above thos<br />
of Canada balm. Birefringence is high.<br />
X-ray data: d 9.34 (100) 3.12 (100) 4.66 (90)<br />
IR-spectrum: 428 445 457 466 537 674 (700) 1020 1050 1640 3435<br />
3655 3670 cm -1<br />
A u t h o r s: Čičić (1975a), Đorđević (1969a), Đurić (1968), Golub<br />
(1961), Ignjatović (1973), Ilić (1954), Jakšić (1938a), Jurković (1956), Karamata<br />
(1953/54), Katzer (1924, 1926), Kišpatić (1897, 1900), Koch (1899), Majer and<br />
Jurković (1957, 1958), Maksimović and Antić (1962), Muftić and Čičić (1969),<br />
Pamić (1970, 1970a, 1971), Pamić and Olujić (1974), Podubsky (1955), Ristić,<br />
Panić, Mudrinić and Likić (1967), Soklić (1957), Šćavničar and Trubelja (1969),<br />
Trubelja and Pamić (1965), Vakanjac (1962, 1964).
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Occurrences of talc in Bosnia and Hercegovina are not common. Talc<br />
occurs mostly in the Bosnian serpentine zone (BSZ) where its origin is related to<br />
the alteration of femic minerals (olivine, pyroxene). Relevant occurrences of talc are<br />
found in the area of Bosansko Petrovo Selo.<br />
1. Occurrences of talc in the Mid-Bosnian schist mountains<br />
A significant occurrence of talc was discovered in cracks and fractures<br />
within Palaeozoic phyllites outcropping near the village of Kupres (Busovača). The<br />
talc-serpentine-chlorite vein and the constituent minerals were studied by Šćavničar<br />
and Trubelja (1969). A block-diagram of this vein is shown in Figure 12.<br />
Figure 12. 3-D Block-diagram of the talc-serpentine-chlorite bearing vein from Kupres<br />
village, near Busovača (Šćavničar and Trebulja 1969)<br />
Talc occurs here in the form of a foliated aggregate with a pearly lustre. It<br />
is white in colour with greenish overtones. Occasional limonite encrustation gives<br />
the talc a brown colour. The talc foils (sheets) are elongated and look like bands up<br />
to 30 cm in length. The bands are mostly oriented perpendicular to the walls of the<br />
cracks (Figure 18).<br />
The coarse-grained and monomineralic talc variety was appropriate<br />
for mineralogical and other investigations, in order to determine the chemical<br />
composition and the formula of the mineral. Results of these investigations are<br />
presented in the paper by Šćavničar and Trubelja (1969).<br />
The chemical composition of talc is as follows:<br />
SiO 2<br />
= 62.04; TiO 2<br />
= ---; Al 2<br />
O 3<br />
= 1.30; Fe 2<br />
O 3<br />
= 0.15; FeO = 1.56; MnO = ---;<br />
MgO = 30.24; CaO = 0.41; Na2O = ---; H 2<br />
O + = 4.55; H2O - = 0.04;<br />
Total = 100.29<br />
167
SILICATES<br />
The mineral formula was calculated on the basis of 24 (O,OH)<br />
Ca 0.056<br />
(Mg 5.736<br />
Fe 2+ 0.166 Fe3+ Al )(Si Al ) O (OH) 0.014 0.096 7.901 0.099 20.137 3.836<br />
There is only minor substitution of Si and Mg with Al and Fe. The talc sheets<br />
are very thin and deformed, and could not be used for single-crystal XRD. Powder<br />
XRD was done, but sample preparation was a problem (not unexpected) because of<br />
the mechanical and structural properties of talc. The talc was ground for 2 hours in<br />
a vibrating mill and the crystals were finely ground but retained their plumose habit.<br />
The problem of preferred orientation of crystals could be obviated only to some<br />
extent by filling a capillary, but not in preparing the sample for the diffractometer.<br />
XRD data is given in Table 29 (powder method/film technique).<br />
Unit cell parameters, calculated from XRD data, are as follows:<br />
a o<br />
= 5.29 ± 0.007, b o<br />
= 9.170 ± 0.005, c o<br />
= 19.08 ± 0.02<br />
β = 101.4° ± 0.2°<br />
Based on the XRD data and calculation of cell parameters, Šćavničar and<br />
Trubelja were able to determine the indices for six Debye lines, previously unknown<br />
for talc (denoted with a star * in Table 29).<br />
Table 29. XRD data for talc, Kupres<br />
No. hkl d (Å) I relative<br />
No. hkl d (Å) I relative<br />
1 002 9.351 200 22 0.0.12 1.558 4 sh<br />
2 004 4.699 23 23 060, 3-32 1.528 70<br />
3 020, 1-11 4.567 111 24 330, 062, 3-34 1.511 21<br />
4 111* 4.318 17 b 25 1.3.10 1.461 3 a<br />
5 022* 4.130 14 b 26 2.0.10, 1.3.-12 1.391 19 a<br />
6 3.900 2 27 0.0.14 1.336 4<br />
7 3.485 3 28 260* 1.3204 18<br />
8 3.242 2 29 400* 1.2972 16<br />
9 006 3.177 124 30 1.2716 6<br />
10 2.720 2 b 31 1.248 3 b<br />
11 130* 2.636 32 32 1.191 2 b<br />
12 200 2.594 47 33 1.1686 1<br />
13 132, 2-04 2.480 111 34 1.1189 2<br />
14 2.331 1 35 1.050 1<br />
15 2.271 1 36 1.042 4<br />
16 134, 2-06 2.222 28 a 37 0.9948 12<br />
17 222, 204, 1-36 2.009 15 a 38 0.9789 1<br />
18 136 1.941 4 b 39 0.9371 2<br />
19 0.0.10 1.870 4 sh 40 0.9181 4b<br />
20 300* 1.729 17 41 0.8850 15 b<br />
21 138 1.683 19 a<br />
168
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The IR spectrum of the Kupres talc shows three bands in the region of<br />
O-H vibrations, at 3666, 3652 and 3640 cm -1 (or splitting of one maximum). The<br />
appearance of only one maximum for the O-H vibration would expected in an ideal<br />
talc structure, since every oxygen atom in the hydroxyl ion should have an identical<br />
bond strength towards the three Mg ions symetrically arranged around the OH dipole<br />
(i.e. a threefold symmetry).<br />
The 2V angle measured on a rotating stage = -7°.<br />
The origin of talc and associated chlorite and serpentine can be explained in<br />
terms of general paragenetic relationships in this part of the schist mountains. The<br />
vein carrying talc and the other minerals is located within the phyllite host rock, while<br />
there are several hydrothermal quartz, Fe-dolomite and ankerite mineralizations. The<br />
hydrothermal solutions from which talc formed were rich in silicic acid and had<br />
a sufficient concentration of magnesium. Such conditions were favourable for the<br />
crystallization of coarse plumose talc. The zonar vein structure indicates that the<br />
crystallization process went through several steps, and that in each of these steps an<br />
almost monomineralic phase formed, depending on the composition and temperature<br />
of the hydrothermal solution. Chlorite was formed first, then serpentine with a small<br />
amount of talc and finally the plumose talc, being also the most abundant phase.<br />
Jurković (1956) reports an occurence of talc with dolomite and baryte at the locality<br />
of Trnjač near Kreševo.<br />
Majer and Jurković (1957, 1958) report a secondary mineralization of talc in<br />
the diorites of the Zasenjak creek at Bijela Gromila, south of Travnik. Jakšić (1938)<br />
also mentioned an occurrence of talc in the Mid-Bosnian schist mountains, without<br />
providing details of localities.<br />
2. Talc in the area of the Bosnian serpentine zone<br />
Most of the cited authors have also reported on talc occurences in the<br />
ultramafic rocks of the Bosnian serpentine zone. The largest deposit, which is also<br />
commercially mines, is at Bosansko Petrovo Selo on the eastern slopes of Mt. Ozren.<br />
Đorđević (1969a) writes that the most important occurrences of talc in this area are<br />
at the localities of Mušići, Žarkovac and Tešanovići (Figure 13).<br />
169
SILICATES<br />
Figure 13. Talc occurences at Mušići – Bosansko Petrovo Selo<br />
Talc, or more precisely – the schistose talc rock, occurs in the Mušići creek<br />
near the village of Porečine ca. 5 km southeast of Bosansko Petrovo Selo. They are<br />
found at the contact between an altered granitoid rock and serpentinized peridotite.<br />
In addition to the schistose talc rock, talc also occurs in other host matrices such<br />
as talc- or carbonate-impregnated serpentinite, talc-bearing carbonates and pyritebearing<br />
schistose talc rock. The schistose talc rock has a schistose texture and a<br />
lepidoblastic structure. The talc flakes (0.05-0.5 mm in size) form compact masses.<br />
In thin section the talc shows vivid interference colours and a low relief. The rock<br />
contains also small amounts of chlorite, pyrite, chalcopyrite and pyrrhotite. The talc<br />
material was also subjected to DTA analysis.<br />
The origin of talc in this area is related to the activity of hydrothermal<br />
solutions which affected and altered the peridotites along tectonic fracture zones.<br />
These solutions were also the source of SiO 2<br />
which is of importance since such an<br />
environment is normally deficient in silica.<br />
170
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Pamić and Olujić (1974) and Pamić-Sunarić (Čičić 1975a) have recently<br />
reported on the talc-bearing hydrothermal-metasomatic listvenites from the northern<br />
part of Mt. Ozren, at the localities of Kloč and Tekućica. These occurrences have not<br />
been investigated in detail.<br />
Trubelja and Pamić (1965) noted the presence of small talc flakes in<br />
harcburgites from the Jadrina river valley near Bosansko Petrovo Selo, where it was<br />
formed by alteration of olivine and orthorhombic pyroxene. A similar occurrence of<br />
talc in chloritized peridotites at Duboštica was described by Pamić (1970). Ignjatović<br />
(1973) identified schistose talc rocks and talc-serpentinites in the chrysotile asbestos<br />
deposit of ‘Delić-Brdo – Brđani’ near Bosansko Petrovo Selo. Ilić (1954) and Podubsky<br />
(1955) report on the occurrence of steatite talc at Žepče, noting that talc is incorporated<br />
into kaolinite-montmorillonite clays, at Ljeskovica between Zavidovići and Žepče.<br />
Golub (1961) determined talc microscopically in the serpentinites of the<br />
Lubina creek, as well as in the lherzolites from the Jovača and Vrela creeks on Mt.<br />
Kozara. In thin sections prepared from these rocks, talc is optically biaxial and<br />
negative. In some cases the talc appears to be optically uniaxial, but this is probably<br />
caused by an oriented superposition of talc flakes. In samples from the Jovača creek,<br />
talc is found on the rims of enstatite grains and seems to be its alteration product.<br />
It needs to be said that the first report on the occurrence of talc in rocks from<br />
the Bosnian serpentine zone was written by Kišpatić (1897, 1900). He determined<br />
talc in thin section, in the lherzolite from Mimići at Mt. Kozara. The talc is colourless<br />
and plumose in habit, and appears to have formed by the alteration of diopside.<br />
Maksimović and Antić (1962) identified talc in the weathering zone of<br />
serpentinites and peridotites at Vardište in eastern Bosnia.<br />
3. Talc in rocks of Mt. Motajica<br />
Koch (1908) identified talc occurring together with beryl, orthoclase, kvarc<br />
and other minerals in the granite-pegmatite of Veliki Kamen near Vlaknica. The<br />
same information can be found the Katzer’s Geology of Bosnia and Hercegovina<br />
(1924, 1926).<br />
Use: talc is an important industrial mineral. It is used either as a raw<br />
material (as talcum powder) or as roasted talc, as a filling material in paper, rubber<br />
and paint production. For cosmetic purposes talc is used in body powders and soap<br />
manufacture. Further uses are as lubricant and polishing powder. Due to its inertness<br />
towards acids and bases, it also finds use in the production of insulating materials,<br />
porcelain and glass.<br />
171
SILICATES<br />
172<br />
MUSCOVITE<br />
KAl 2<br />
[AlSi 3<br />
O 10<br />
] (OH) 2<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.574 : 1 : 2.21; β = 95° 30’<br />
Cell parameters: a o<br />
= 5.19, b o<br />
= 9.04, c o<br />
= 20.08 Z = 4<br />
Properties: good cleavage on {001}. The lamellar crystals are flexible and elastic.<br />
Occasional parting on {010} and {110}. Hardness is 2.5 (on the cleavage plane) and<br />
4 ^ to the cleavage plane. Specific gravity = 2.8-2.9. Colour is white to silvery white.<br />
Streak is white, lustre vitreous to pearly. Resistant to acids. Refractive indices are<br />
higher than those of Canada balm. Maximum birefringence is very large.<br />
X-ray data: d 10.014 (100) 3.351 (100) 2.562 (75)<br />
IR-spectrum: 415 435 480 535 692 750 800 828 930 1030 1060 1635<br />
3430 3620 cm -1<br />
A u t h o r s: Arsenijević (1967), Barić (1969, 1970a), Barić and Tajder (1955,<br />
1956), Cissarz (1956), Čelebić (1963, 1967), Čutura (1918), Džepina (1970), Đorđević<br />
(1969a), Đorđević and Mijatović (1966), Đurić (1963a), Foullon (1893), Gaković and<br />
Gaković (1973), Ilić (1953), Jeremić (1960, 1963, 1963a), Č. Jovanović (1972), R.<br />
Jovanović (1957), Jurković (1954, 1956, 1958, 1958a, 1959, 1961, 1961a, 1962),<br />
Jurković and Majer (1954), Karamata (1953/54, 1957), Katzer (1924, 1926), Kišpatić<br />
(1897, 1900, 1904b), Koch (1908), Majer (1963), Majer and Jurković (1957, 1958),<br />
Majer and Pamić (1974), Magdalenić and Šćavničar (1973), Marić (1965), Marić and<br />
Crnković (1961), Mojsisovics, Tietze and Bittner (1880), Nöth (1956), Pamić (1957,<br />
1960, 1961, 1961a, 1961b, 1962, 1970), Pamić and Buzaljko (1966), Pamić and Olujić<br />
(1974), Pamić and Papeš (1969), Pamić and Tojerkauf (1970), Pavlović and Ristić<br />
(1971), Petković (1962/62), Pilar (1882), Podubsky (1968, 1970), Podubsky and Pamić<br />
(1969), Popović (1930), Ramović (1957, 1961, 1963), Ramović and Kulenović (1964),<br />
Ristić, Pamić, Mudrinić and Likić (1967), Sijerčić (1972), Simić (1972), Stangačilović<br />
(1956), Šćavničar and Jović (1962), Šćavničar and Trubelja (1969), Šibenik-Studen<br />
and Trubelja (1967), Tajder (1953), Tajder and Raffaelli (1967), Trubelja (1962, 1962a,<br />
1963, 1963a, 1963b, 1966a, 1967, 1969, 1970, 1970a, 1971, 1972, 1972a), Trubelja<br />
and Pamić (1957, 1965), Trubelja and Miladinović (1969), Trubelja and Sijarić (1970),<br />
Trubelja and Slišković (1967), Trubelja and Šibenik-Studen (1965), Tućan (1912),<br />
Varićak (1955, 1956, 1957, 1966), Vasiljević (1969), Vujanović (1962).<br />
Muscovite is a typical representative of the mica group of minerals. It is<br />
usually pale in colour or colourless. It occurs as a primary mineral in granites,<br />
granite-pegmatites and similar rocks, as well as in metamorphites (gneisses, schists<br />
etc.). It is often incorporated in clastic sediments, due to its resistance and stability. It<br />
can also form through hydrothermal alteration of feldspars (orthoclase, microcline).<br />
Sericite is a hydrated microcrystalline variety of muscovite, depleted in potassium.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Muscovite (and sericite) belong to the abundant rock-forming minerals in<br />
Bosnia and Hercegovina, occurring in igneous, metamophic and sedimentary rocks –<br />
especially in the Palaeozoic formations of north-west Bosnia, the Mid-Bosnian schist<br />
mountains and in the metamorphic rocks of eastern/south-eastern Bosnia. Muscovite<br />
is an essential constituent of igneous and metamorphic rocks at Mt. Motajica and<br />
Mt. Prosara (granites, gneisses, schists etc.). Muscovite and sericite are found in the<br />
products of Triassic magmatism and in Tertiary effusive rocks, as well as in some<br />
polymetallic ore bodies.<br />
In spite of their extensive regional distribution and abundance, not much<br />
has been published about muscovite and sericite, which have been microscopically<br />
investigated mainly by the authors referenced earlier in this chapter.<br />
1. Muscovite in rocks of Mt. Motajica and Mt. Prosara<br />
Among the first determinations of muscovite were certainly those of C. John<br />
(according to Mojsisovics et al. 1880), in the muscovite granite of Kobaš at Mt.<br />
Motajica. A more detailed account of muscovite occurrences in the above rocks was<br />
written by Koch (1908). Muscovite is an essential constituent of the granites from<br />
Veliki Kamen at Mt. Motajica, and occurs in the form of larger greyish-green leaves.<br />
Parallel overgrowths with biotite are common. Quartz grains with muscovite leaves<br />
bent around them are frequently seen. A similar form of occurrence is in the case of<br />
the granites from Brusnik, while there is very little muscovite in the granite-gneiss<br />
from Židovski potok.<br />
Arsenijević (1967) determined the following trace elements in the muscovite<br />
from Mt. Motajica: Be = 5 g/t, Sn = 62 g/t, Nb = 50 g/t.<br />
The muscovite gneiss from Studena Voda contains muscovite as the<br />
predominant mineral in the rock. The muscovite leaves are arranged in parallel<br />
layers so that the rock has a schistose texture. On the other hand, muscovite occurs<br />
much less frequently in the garnet-gneiss from the Kamen creek near Kobaš.<br />
Micaschists normally contain more biotite than muscovite, but the opposite<br />
case is also possible.<br />
A substantial amount of data on muscovite in various rocks in Bosnia and<br />
Hercegovina can be found in the Geology of Bosnia and Hercegovina by Katzer<br />
(1924, 1926). Katzer mentions Koch’s data, but provides his own microscopic<br />
measurements of muscovite from various localities. In many instances Katzer<br />
speaks of microcrystalline sericite. He found muscovite to be an abundant mineral<br />
in muscovite granites, granitic pegmatites, quartz veins, aplitic veins, phyllites and<br />
173
SILICATES<br />
orthogneisses. Tabular muscovite crystals up to 2 cm in size are common in veins.<br />
For muscovite occurrences in paragneisses and micaschists, Katzer mainly uses<br />
Koch’s data (1908).<br />
Varićak (1966) made detailed investigations of muscovite from te Mt.<br />
Motajica area (granit-type rocks, igneous and sedimentary rocks altered by<br />
contact metamorphism. Muscovite is also found in granitic dyke rocks, leucocratic<br />
granites, rhyolites, graniteporphyres and lamprophyres. Sedimentary rocks altered<br />
by contact metamorphism – migmatites, gneisses, micaschists, gneissphyllites –<br />
contain muscovite and sericite either as essential or accessory constituents. Those<br />
of igneous origin – hornblendites, amphibolites, amphibole schists, glaucophanites,<br />
albite-actinolite-epidote schists – contain only minor amounts of sericite. Muscovite<br />
and sericite are common minerals in almost all rock types outcropping at Mt.<br />
Motajica. Varićak (1966) established that in the greisen-granites muscovite occurs<br />
in very twisted aggregates. The optical axis angle 2V (measured in conoscopy)<br />
is in the range of -35° to -37°. The sericite usually pseudomorphically replaces<br />
primary feldspars.<br />
Muscovite from pegmatite veins is often deformed. The negative 2V angle<br />
= 39-40°; in albite gneisses the 2V angle is -40°. The Mt. Motajica muscovite was<br />
mentioned also by Pilar (1882 – reporting John’s data for the Kobaš muscovite) and<br />
Stangačilović (1956).<br />
Katzer (1924, 1926) and Varićak (1956, 1957) report on muscovite<br />
occurrences in igneous and metamorphic rocks of Mt. Prosara. Varićak (1957)<br />
investigated in some detail the products of regional metamorphism and found<br />
muscovite (and sericite) to be a constituent mineral of gneisses, micaschists, gneissmicaschists,<br />
quartzschists, phyllites, sericite- and chlorite-schists, quartz.schists<br />
of low crystallinity, marble, marble schists and green rocks. The author does not<br />
mention optical properties. Varićak’s 1956 paper describes the quartz porpyhres<br />
at Mt. Prosara, where muscovite is a primary mineral (ca. 0.5-2%) and sericite is<br />
secondary product of alteration.<br />
174<br />
2. Muscovite occurences in the Mid-Bosnian schist mountains (MBSM) and<br />
adjacent regions<br />
Katzer (1924, 1926) found muscovite (and sericite) to be an essential<br />
constituent of various igneous and metamorphic rocks in the Mid-Bosnian schist<br />
mountains (MBSM). It needs to be mentioned here that his findings are based<br />
primarily on macroscopic observations of the rocks, and not on microscopic<br />
determinations. Even today, the information we have on this vast area (but also for<br />
other Palaeozoic regions in Bosnia) is rather basic. According to Katzer, muscovite<br />
occurs primarily in metamorphic rocks of MBSM – gneisses, micaschists, quartzites
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
and quartzite sandstones, sericite-schists, phyllites and carbonate schists. The<br />
presence of muscovite leaves was also established in marbles, crystaline limestones<br />
and dolomites as well as sandstones. Sericite is present in sericitized quartz-porphyres,<br />
a very common rock in MBSM. This was also established earlier by Foullon (1893).<br />
Muscovite and sericite are abundant in the Palaeozoic metamorphites of<br />
Jezera and Sinjakovo – in phyllites and clayey schists, phyllites, sandstones and<br />
quartz-porphyres. Katzer reports occurrences of sericite in igneous rocks from the<br />
Trešanica cliff near Bradina. This sericite was recently investigated by Barić (1970a)<br />
who classified the host rock as a keratophyre. The sericite is an alteration product of<br />
hydrothermal and other metamorphic processes. Sericite occurs also in the mineral<br />
paragenesis of the sinjakovo albite rhyolites and at the contact of these rocks with<br />
Palaeozoic limestones from Alinovac near Jezera. Such rhyolites (quartz porphyres)<br />
with sericite – which may justifiably be referred to as sericite schists – are very<br />
common in the MBSM, particularly north-west of Busovača and in the Fojnica –<br />
Kreševo area (Jurković and Majer 1954).<br />
The muscovite and sericite in this area have been microscopically determined<br />
also by other authors (Tajder and Raffaelli, 1967; Šćavničar and Trubelja 1969;<br />
Trubelja and Sijarić 1970). The pyrophyllite schists from Parsovići, Hercegovina,<br />
contain 14.9% sericite (Barić and Tajder 1955, 1956). Kišpatić (1904b) found that<br />
muscovite is the predominant mineral in the chloritoide phyllite from Fojnica and<br />
Čemernica. The muscovite contained in this rock is microcrystalline and can be<br />
observed under the microscope – as minute colourless leaves with basal cleavage –<br />
only using large magnifications.<br />
Muscovite is common in the ore mineralizations within MBSM (Barić<br />
1969; Jeremić 1963, 1963a; Jurković 1956, 1958, 1958a, 1961, 1972; Popović 1930;<br />
Trubelja 1967; Vasiljević 1969). Jurković found sericite to be abundant around<br />
Busovača (localities Rog, Obla, Ravan, Jekanjska, Očenići, Kaćuni, Krnjača, Jela,<br />
Peska I, Rudno I and II, Slamina Kuća, Dolovi, Grude, Pridolci, Luke, Kozica,<br />
Rizvići, Šuplje Bukve and Oštra), Travnik and Ščitovo, and less abundant in other<br />
areas. Muscovite occurs only at a few localities (Busovača, Ščitovo, Brestovsko,<br />
Berberuša). Jurković (1956) reports also about a lithium mica associated with some<br />
katathermal quartz formations near Gruda. In the area of Ščitovo, sericite was found<br />
at following localities: Brezova Kosa, Dubrave, Crkvice, Gromiljak, Ivankovići,<br />
Pločari and Lopari. Some muscovite was found at Vrtlasce. In the area of Brestovsko,<br />
sericite occurs at the localities of Cigani and Gaj, while muscovite can be found at<br />
Hrastovo, Pobrđe and Datići. In the area of the Travnik ore mineralizations, sericite<br />
was found at following localities: Srednje Brdo, Kruščica Potok, Lupnica Potok,<br />
Gornje Grčice, Široki Do, Triljački Potok, Zaselje, Cakići, Zubići, Pečuj, Večeriska<br />
Gornja, Čehanovac, Bilkanov Potok, Kezik Potok, Varošluk, Ibrin Do, Vrelo potok,<br />
Njiva Potok, Zmajevački Potok, Podradola, Dubrave, Kremenje, Osoje, Katuništa,<br />
175
SILICATES<br />
Vilenice, Heldovi and Slimena. In the area of Berberuša, sericite occurs at three<br />
localities: Močenik, Komari and Bukva, while muscovite can be found at Banjak,<br />
Bukva I and II and Podljetovik. In the area of Kreševo, sericite is not common but can<br />
be found at Sotnica, Vidici, Dubrave, Dugi Dol and Duge Njive. Jurković believes<br />
that both muscovite and sericite are of hydrothermal origin (meso-epithermal stage).<br />
At Busovača, sericite is mainly associated with katathermal quartz deposits. Together<br />
with the lithium mica, they form aggregates of microscopically small flakes, which<br />
are deposited as encrustations along the walls of the cracks within quartz grains.<br />
The pneumatolytic and hydrothermal deposits of pyrrhotite at Vrtlasce<br />
contain abundant muscovite. Muscovite forms radiating aggregates of minute crystals<br />
(5 x 35 to 24 x 240 µm in size) with distinct cleavage. Some crstals are idiomorphic,<br />
others have irregular edges, and are incoporated in all sulphide minerals (less often<br />
in albite) – indicating a broad range for the crystallization temperature.<br />
The sericite from Dubrave (on the Kreševo – Tarčin road) forms large block<br />
and aggregates weighing several tens of kilograms. This sericite is related to the<br />
nearby baryte deposits. The sericite aggregate is of a pale green to yellow-green<br />
colour and quite compact. It has an irregular fracture and a greasy feel. In thin section,<br />
the sericite flakes are colourless and transparent. The aggregate is monomineralic<br />
and apparently pure. The refractive index is higher than that of Canada balm. The<br />
second-order interference colours are vivid. A detailed chemical analysis and XRD<br />
investigation of the Dubrave sericite (on the Kreševo – Tarčin road) was done<br />
(Trubelja 1967).<br />
Results of the chemical analysis (analyst F.Trubelja): SiO 2<br />
= 47.05; TiO 2<br />
= ---;<br />
Al 2<br />
O 3<br />
= 36.43; Fe 2<br />
O 3<br />
= 0.53; FeO = 0.17; MnO = ---; MgO = 1.61; Na 2<br />
O = 1.51;<br />
K 2<br />
O = 7.92; H 2<br />
O + = 4.98; H 2<br />
O - = 0.24; Total = 100.44<br />
The structural formula based on the chemical analysis data and 24 (O,OH)<br />
atoms is: (K 1.30<br />
Na 0.37<br />
) (Al 3.61<br />
Fe 2+ 0.01 Fe3+ 0.05 Mg 0.31 ) 3.98 (Al 1.93 Si 6.07 ) 8.00 (OH) 4.27<br />
Powder XRD data are given in Table 30.<br />
Table 30. Powder XRD of sericite from Dubrave<br />
d (Å) I d (Å) I<br />
9.91 vs 3.32 vs<br />
4.98 m 3.19 m<br />
4.46 vs 2.98 m<br />
3.72 m 2.56 vs<br />
3.48 m 1.51 s<br />
The specific gravity of sericite was determined by the pycnometric methods<br />
and is 2.790 (at 20°C). The sericite is of hydrothermal origin, like the baryte.<br />
176
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Jeremić (1938) also noted the relationship between baryte and sericite in<br />
MBSM. Barić (1969) observed that the thin and tabular muscovite crystals occurs<br />
on the substratum on which hyalophane crystals developed (at Zagrlski potok near<br />
Busovača). Barić was able to measure the optic axial angle on one crystal: 2V = -37.5°.<br />
Cissarz (1956), Nöth (1956) and Čelebić (1957) observed a sericitemagnetite<br />
paragenesis at Tovarnica, near Jablanica in Hercegovina.<br />
3. Muscovite in Palaeozoic rocks of the Sana – Una and Ključ regions<br />
Katzer (1924, 1926) observed the occurence of muscovite and sericite in<br />
various Palaeozoic metamorphic rocks of the Una – Sana region, rocks which are<br />
apparently similar to those in eastern Bosnia.<br />
Jurković (1959) described the magnetite deposit at Muhamedbegov<br />
Prisjek near Ključ and surroundig rocks, observing that quartz-sericite schists are<br />
transformed into finegrained quartz-sericite sandstones. Sericite and muscovite have<br />
been found at several localities within the iron ore complex of Ljubija (Jurković<br />
1961a; Marić and Crnković 1961; Jeremić 1960; Podubsky 1968; Podubsky and<br />
Pamić 1969). Jurković (1961a) believes the sericite to be a hypogenous mineral in<br />
the Ljubija paragenesis. Muscovite and sericite also occur at the Brdo and Nova<br />
Litica localities in the Ljubija complex (Marić and Crnković 1961). Podubsky (1968)<br />
provides a substantial amount of data on the occurrence and abundance of sericite<br />
and muscovite in Palaeozoic metamorphites of north-west Bosnia. He observed<br />
that the two minerals occur in rocks from lower Palaeozoic age to Permotriassic<br />
ones. In the older series, sericite is an essential constituent of clayey schists and<br />
metasandstones (subgraywacke and graywacke type sericite-chlorite-feldspar-quartz<br />
metasandstones). The Carbonian-age clayey schists are of the chlorite-sericite-quartz<br />
type. The abundance of mica minerals is variable (0.03-22.23%). The sericite is the<br />
product of the alteration of volcanic rocks of the Una – Sana Palaeozoic (Podubsky<br />
and Pamić 1969). Jeremić (1960) mentions a muscovite occurence in the ‘Žune’<br />
baryte-fluorite deposit near Ljubija.<br />
4. Muscovite in rocks of eastern and south-east Bosnia<br />
Katzer (1924, 1926) and Podubsky (1970) made the observation that the<br />
low-metamorphic schists and some Palaeozoic sediments of eastern and southeast<br />
Bosnia contain variable amounts of muscovite and sericite. These minerals<br />
are essential constituents of phyllites, sandstones, limestones and sericitized<br />
quartz-porphyres in the areas of Pale, Prača, Trnova, Goražde, Foča, Srebrenica,<br />
Vlasenica and Zvornik. According to Podubsky (1970) the phyllites, phyllite schists<br />
and metasandstones of lower Palaezoic age contain small to substantial amounts<br />
of muscovite and sericite. Rocks of Carbonian and Permian age contain these two<br />
minerals mainly in metasandstones, sandstones, alevrolite and clayey schists.<br />
177
SILICATES<br />
Information provided by Podubsky shows that the abundances of muscovite<br />
and sericite show large variations – between 0.7 and 9.57%. Samples used in this<br />
study were collected on several characteristic profiles of eastern Bosnia (Šutorina<br />
Rijeka, Vranječevići, Tegare, Zapolje – Zapoljska Rijeka, Nova Kasaba, Biljaša –<br />
Milić Brod, Mlječvanska Rijeka – Pašino Brdo and Brezovačka Rijeka. Kišpatić<br />
(1904b) observed that muscovite is not abundant in the quartz-phyllites from Polom<br />
on the Drina river, but that the flakes are easily observed in thin section (muscovite<br />
is pale green or colourless).<br />
5. Muscovite and sericite in igneous rocks of Bosnia and Hercegovina<br />
The various igneous rocks of Bosnia and Hercegovina contain sericite as a<br />
product of metamorphism (alteration) of feldspars (sericitization process). Sericite<br />
occurs in Triassic-age igneous rocks from the Vrbas river valley, from Kupres,<br />
Bugojno, Jajce, Komar, Kreševo, Jablanica, Prozor, Tjentište, Čajniče, Vareš,<br />
Čevljanovići, Ilidža – Kalinovik, Zvornik and other areas (Čutura 1918; Đurić<br />
1963a; Jovanović1957; Karamata 1957; Majer and Jurković 1957, 1958; Pamić<br />
1957, 1960, 1961, 1961a, 1961b, 1962; Pamić and Buzaljko 1966; Pamić and Papeš<br />
1969; Petković 1961/62; Ramović and Kulenović 1964; Šibenik-Studen and Trubelja<br />
1967; Trubelja 1962a, 1963, 1963a, 1969, 1972a; Trubelja and Pamić1957; Trubelja<br />
and Miladinović 1969; Trubelja and Slišković 1967; Vujanović 1962.<br />
Some igneous rocks of the Bosnian serpentine zone (BSZ) and products of<br />
Tertiary volcanism contain muscovite and sericite. Such rocks are found at Mt. Borja<br />
near Teslić, at Mt. Ozren, in the Bosna river valley, near Srebrenica, Bosanski Novi,<br />
Mt. Kozara, Mt. Ljubić. Many authors have made observation on the occurrence of<br />
muscovite and sericite in rocks of the BSZ (predominantly grantoids and rhyolites),<br />
and in Tertiary dacite-andesites. However, very little data on optical properties or<br />
microscopic measurements pertaining to these two minerals are given (Đorđević<br />
1969a; Karamata 1953/54; Majer 1963; Pamić 1970; Pamić and Olujić 1974; Pamić<br />
and Tojerkauf 1970; Ramović 1957, 1961, 1963; Tajder 1953; Trubelja 1962, 1963b,<br />
1966a, 1971a, 1972; Trubelja and Pamić 1965; Varićak 1955).<br />
6. Occurrence of muscovite and sericite in other rocks<br />
Up to now we have not taken into consideration the occurrences of muscovite<br />
and sericite in some sedimentary rocks and matmorphic rocks from the Bosnian<br />
serpentine zone BSZ. The following authors have made observations on muscovite<br />
and sericite in these areas: Džepina (1970), Gaković and Gaković (1973), Jovanović<br />
(1972), Kišpatić (1897, 1900), Majer and Pamić (1974), Magdalenić and Šćavničar<br />
(1973), Pavlović and Ristić (1971), Ristić, Pamić, Mudrinić and Likić (1967),<br />
Sijerčić (1972), Simić (1972), Šćavničar and Jović (1962), Trubelja (1970).<br />
178
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Papers by Džepina, Kišpatić, Majer and Pamić provide data on muscovite<br />
and sericite contained in amphibolites and similar rocks in the BSZ (Mt. Borja etc.).<br />
Gaković and Gaković investigated the abundance of muscovite in the insoluble residue<br />
of some carbonate sediments in the outer Dinarides. Jovanović (1972) mentions<br />
Pliocene sands of the Prijedor basin where the abundance of muscovite can be up to<br />
15% (determined by Sijerčić 1972, p. 15). Magdalenić and Šćavničar determined that<br />
sericite occurs together with chlorite in the matrix of Permian red clastites from Kulen<br />
Vakuf. Pavlović and Ristić (1971) found muscovite occurring together with sericite<br />
(and some other minerals) in the gravels and sands of the ‘Bijela Stijena’ deposit near<br />
Zvornik. Ristić et al. (1967) found sericite to be an essential constituent of sericite<br />
schists from Miljevica at Mt. Konjuh, where talc schists also occur. Sijerčić (1972)<br />
found sericite in the arenite of Eocene flysch on the western slopes of Mt. Majevica<br />
near Tuzla. Šćavničar and Jović (1962) identified muscovite in in the Pliocene sand of<br />
the Kreka coal basin, as well as in Eocene and Miocene clastic sediments.<br />
Simić (1972) established that muscovite is an abundant and essential<br />
constituent of lower Triassic clastic rocks in the Sarajevo area. The common<br />
paragenesis consists of muscovite, quartz and hydromica. Trubelja (1970) writes<br />
about the occurrence of sericite in clayey sediments related to diaspore bauxites from<br />
the village of Ljuša, near Donji Vakuf.<br />
Pamić and Olujić (1974) determined Cr-muscovite (fuchsite) as a constituent<br />
of listvenites (hydrothermal-metasomatic rocks) from the northern part of Mt.<br />
Ozren. Fuchsite is macroscopically green in colour. In thin section, pleochroism is Z<br />
= dark green, X = light green; the 2V angle = -68°. Fuchsite is the product of spinel<br />
alteration, and pseudomorphic growth of fuchsite is known to exist. The XRD data<br />
for the fuchsite were also collected.<br />
Tućan (1912) microscopically determined muscovite in the terra rossa from<br />
Eminovo Selo near Duvno. This observation was referenced by Marić (1965).<br />
GLAUCONITE<br />
K 0.8<br />
R 3+ 1.33 R2+ 0.67 [Al 0.13 Si 3.87 O 10 ] (OH) 2<br />
Crystal system and class: Monoclinic.<br />
Lattice ratio: a : b : c = 0.578 : 1 : 2.208; β = 95°<br />
Cell parameters: a o<br />
= 5.25, b o<br />
= 9.09, c o<br />
= 20.07 Z = 4<br />
Properties: occurs in the form of green, blue-green (to almost black) spheres and<br />
flakes. Hardness = 2. Specific gravity 2.5-2.8. Streak is green.<br />
X-ray data: d 2.592 (100) 1.519 (80) 10.05 (60)<br />
IR-spectrum: 440 470 500 575 610 680 810 1030 1110 1270 1630 3410 3540 3560 cm -1<br />
179
SILICATES<br />
Glauconite is a member of the phyllosilicate group of minerals. Its structure<br />
is similar to the structure of biotite. Chemically, it is a Fe-Al silicate with a highly<br />
variable chemical composition – especially in terms of potassium abundance.<br />
Celadonite has a similar composition and properties as glauconite.<br />
A u t h o r s : Pamić (1972d), Šibenik-Studen and Trubelja (1967), Trubelja<br />
(1966a, 1969, 1972a), Trubelja and Barić (1970), Varićak (1966).<br />
In Bosnia and Hercegovina, glauconite mostly occurs in the Hrčavka creek<br />
valley near Tjentište. This occurence has been investigated in some detail by Trubelja<br />
and Barić (1970).<br />
1. Glauconite in the Hrčavka valley near Tjentište<br />
In the Hrčavka valley near Tjentište, glauconite is a characteristic mineral<br />
of the lower Triassic series of rocks. The glauconite bearing veinlets are up to 10 cm<br />
thick and are mainly concentrated near the contact of the volcanic rock and sediment.<br />
It is also found in cavities and cracks within the rock itself. The tuffs and tuff-bearing<br />
sandstones have a greenish colour due to the presence of glauconite, which is finely<br />
dispersed in the rocks giving them the characteristic colour and names like ‘pietra<br />
verde’ or ‘green rock’.<br />
Glauconite was determined by thermal methods (DTA and TG), X-ray<br />
diffraction and chemical analysis. The pure, bluegreen glauconite material was used<br />
for these laboratory studies.<br />
The DTA curve is rather typical for glauconite, with two separate endothermic<br />
peaks: one at 150-200°C indicating a loss of adsorbed water, and the other one at<br />
550-600°C (loss of structural water). The TG curve indicated a 9% weight loss, and<br />
corresponds to similar curves for glauconite published in the literature. The curve<br />
shows two distinct steps indicating water loss as a consequence of heating.<br />
The X-ray diffraction data of glauconite are given in table 31.<br />
Table 31. XRD data for glauconite from Hrčavka (column 1) correlated to literature data<br />
(Torre de Assuncao and Garrido, 1953 – column 2)<br />
1 2<br />
No. d Å I Å I<br />
1 10.01 2 10.01 2<br />
2 4.52 10 4.50 10<br />
3 3.66 2 3.64 2<br />
4 3.33 10 3.29 10<br />
5 3.07 1 3.07 1<br />
180
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
6 2.59 10 2.57 10<br />
7 2.40 7 2.38 7<br />
8 2.13 1 2.13 1<br />
9 2.05 1 --- ---<br />
10 1.66 2 1.64 2<br />
11 1.51 8 1.49 8<br />
12 1.30 5 --- ---<br />
13 1.25 1 --- --<br />
A quantitative chemical analysis (analyst F. Trubelja) gave the following results:<br />
SiO 2<br />
= 46.60; TiO 2<br />
= 0.07; Al 2<br />
O 3<br />
= 17.69; Fe 2<br />
O 3<br />
= 14.45; FeO = 0.36; MnO = 0.03;<br />
MgO = 5.45; CaO = 0.84; Na 2<br />
O = 0.06; K 2<br />
O = 5.92; H 2<br />
O + = 5.74; H 2<br />
O - = 3.54;<br />
P 2<br />
O 5<br />
= 0.03; Total = 100.78%<br />
These results were used to calculate the number of ions in the crystalchemical<br />
formula, based on 20 (O) and 4 (OH), assuming that 4% H 2<br />
O are equivalent<br />
to 4 (OH). The rest of the water is given as nH 2<br />
O, as usually done in the literature.<br />
The formula of glauconite this is:<br />
(K 1.068<br />
Na 0.017<br />
Ca 0.129<br />
) (Al 1.669<br />
Fe 3+ 1.550 Fe2+ 0.043 Mg 1.171 Ti 0.008 ) Si 6.990 Al 1.310 O 20 (OH) 3.840 x<br />
nH 2<br />
O<br />
It is clear from the formula that this glauconite contains a substantial amount<br />
of aluminium. The aluminium partly substitutes silicon, and partly ferric iron in<br />
octahedral coordination.<br />
The glauconite from the Hrčavka valley is of sedimentary origin, forming<br />
as a result of diagenetic processes occuring in finely bedded sediments within a<br />
mid-Triassic geosyncline. Mud and other clastic particles were being deposited in<br />
a shallow marine environment, at a slow rate of deposition. Submarine effusions<br />
of lava were the source of potassium and other elements neccessary for glauconite<br />
formation. Almost all of the iron is in the oxidized ferric state so that we may<br />
conclude that the depositional environment was not a reducing one.<br />
2. Other occurences of glauconite (celladonite)<br />
Glauconite (celladonite) occurs in sandstones in the valley of Crna Rijeka<br />
at Mt. Kozara at localities known as Bunik and Bukovi Vrh (Trubelja 1966a). Here<br />
glauconite occurs in the form of blue-greeen flakes evenly dispersed in the rock.<br />
Sometimes it forms veinlets or small amygdales. Glauconite was determined by XRD.<br />
Glauconite can also be found at Kiprovac near Borovica (Vareš) where it<br />
is associated with mid-Triassic greenish tuff-containg rocks, similar in appearance<br />
to those in the Hrčavka valley. The greenish colour is caused by the presence of<br />
glauconite, identified here also by XRD (Trubelja 1969 and 1972a).<br />
181
SILICATES<br />
Mid-triassic igneous rocks of the Vrbas river valley occasionally contain<br />
glauconite (Šibenik-Studen and Trubelja, 1967). Pamić (1972d) mentions glauconite<br />
occurrences in amygdales within albite-containing volcanic rocks of the same age.<br />
Glauconite was identified, together with other minerals, in the arkosegraywacke<br />
type sandstones at Mt. Motajica (Varićak 1966). One large glauconite<br />
grain had the following characteristics when observed by microscope in transmitted<br />
light: cleavage along (001), high relief, strong pleochroism in lightgreen and<br />
olivegreen. The 2V angle is -23°; X : [001] = -2.5°. Interefrence colours are largely<br />
masked by glauconites own colour.<br />
Use<br />
Because of its high potassiom content, glauconite can be used as a fertlizer,<br />
either in its natural state or thermally processed. It has also been used as green<br />
pigment in paints, due to its chemical resistance. It is also used in water-softening<br />
technologies and for other industrial purposes as an ion-exchanger.<br />
PHLOGOPITE<br />
KMg 3<br />
[AlSi 3<br />
O 10<br />
] (OH) 2<br />
Crystallographically similar to biotite.<br />
Properties: chemically, phlogopite could be decribed like an iron-free biotite. It is<br />
light brown in colour.<br />
IR-spectrum: 466 615 675 695 815 980 1010 1630 3440 3650 cm -1<br />
A u t h o r s: Džepina (1970), Kišpatić (1915).<br />
Phlogopite occurs rarely in In Bosnia and Hercegovina, and literature data<br />
is very scarce. Kišpatić (1915) first mentions phlogopite in the bauxites from Široki<br />
Brijeg (Lištica) in Hercegovina. This author was also able to identify small amounts<br />
of other minerals – gibbsite, rutile, zircon, tourmaline, anatase, periclase, kyanite<br />
and calcite. Kišpatić mentions ‘sporogelite’ as an important constituent of bauxite,<br />
but this mineral name has been discredited.<br />
Džepina (1970) identified phlogopite in garnet-containing basic metamorphic<br />
rocks in the southern part of Mt. Borje. Garnet, hornblende, diopside and plagioclase<br />
are the dominant minerals in these rocks, while only minor amounts of phlogopite<br />
were found.<br />
182
BIOTITE<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
K(Mg,Fe 2+ ) 3<br />
[AlSi 3<br />
O 10<br />
] (OH) 2<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.575 : 1 : 1.103; β = 99° 18’<br />
Cell parameters: a o<br />
= 5.31, b o<br />
= 9.23, c o<br />
= 10.18 Z = 2<br />
Properties: distinct platelike habit with a predominant pinacoid, good cleavage<br />
on {001}. The lamellar crystals are flexible and elastic. Hardness is 2.5 (on the<br />
cleavage plane). Specific gravity = 2.8-3.4 depending on the iron content. Colour is<br />
darbrown to black. Streak is white or greyish, lustre vitreous to pearly, sometimes<br />
semi-metallic. Hot sulphuric acid dissolves biotite, but the SiO 2<br />
skeletal remains<br />
are resistant. Refractive indices are low to moderate. Usually Ny = Nz. Maximum<br />
birefringence is large.<br />
X-ray data: d 9.818 (100) 3.324 (71) 2.004 (14)<br />
d 10.01 (100) 3.346 (45) 2.631 (50)<br />
d 10.264 (100) 3.380 (80) 2.654 (70)<br />
IR-spectrum: 415 445 465 612 692 760 (975) 1000 1640 3440 3610 3650 cm -1<br />
A u t h o r s: Arsenijević (1967), Barić (1966a), Behlilović and Pamić (1963),<br />
Čelebić (1967), Dangić (1971), Đorđević and Stojanović (1964), Foullon (1893),<br />
Gaković and Gaković (1973), Hlawatsch (1903), Ilić (1953), John (1880, 1888),<br />
R. Jovanović (1957), Jovičić (1891), Jurković (1954a, 1956), Jurković and Majer<br />
(1954), Karamata (1953/54), Katzer (1903, 1910, 1924, 1926), Kišpatić (1897, 1900,<br />
1904, 1904a, 1910), Koch (1908), Luburić (1963), Luković (1957), Majer (1961,<br />
1963), Majer and Jurković (1957, 1958), Majer and Pamić (1974), Marić (1927),<br />
Mudrenović and Gaković (1964), Nikolić, Živanović and Zarić (1971), Nöth (1956),<br />
Pamić (1961, 1971, 1971a), Pamić, Dimitrov and Zec (1964), Pamić and Đorđević<br />
(1974), Pamić and Kapeler (1969), Pamić and Olujić (1969), Pamić and Papeš<br />
(1969), Pamić, Šćavničar and Međimorec (1973), Pamić and Tojerkauf (1970),<br />
Pavlović (1889), Pavlović and Ristić (1971), Pavlović, Ristić and Likić (1970), Paul<br />
(1879), Pilar (1882), Podubsky (1968, 1970), Podubsky and Pamić (1969), Primics<br />
(1881), Ramović (1957, 1961, 1962, 1963, 1966, 1968), Ristić, Likić and Stanišić<br />
(1968), Sijerčić (1972), Šćavničar and Jović (1961, 1962), Tajder (1951/53, 1953,<br />
1960), Trubelja (1962, 1963b, 1969, 1971a, 1972, 1972a), Trubelja and Paškvalin<br />
(1962), Trubelja and Sijarić (1970), Varićak (1955, 1957, 1966), Walter (1887).<br />
Biotite is a very common and ubiquitous mineral in Bosnia and Hercegovina.<br />
It occurs in igneous, sedimentary and metamorphic rocks. It is common in igneous<br />
rocks associated with Tertiary-age volcanism – such as dacites, andesites. The<br />
granites, gneisses and micaschists of Mt. Motajica contain biotite in addition to other<br />
minerals. Biotite occurs also in other areas i.e. the Bosnian Serpentine Zone (BSZ),<br />
in granitoids, rhyolites and basic vein rocks. The gabbro-diorites and Palaeozoic-age<br />
183
SILICATES<br />
rhyolites of the Mid-Bosnian schist mountains contain biotite either as a dominant or<br />
accessory mineral. Biotite was found also in the gabbros at Jablanica, as well as in<br />
various rocks in northwestern, eastern and central Bosnia. Biotite can occasionally<br />
be found in pyroclastic rocks of Triassic and Tertiary age. Clastic sediments and<br />
carbonate rocks in karst areas also contain some biotite.<br />
184<br />
1. Biotite in rocks associated with Tertiary-age volcanism<br />
Biotite is an important mineral constituent of dacites, andesites and pyroclastic<br />
rocks in the Srebrenica area and in the Bosna river valley. Biotite-containing tuffs<br />
can be found also around Livno and Duvno, and in the Tuzla basin. Information<br />
on biotite contained in these rocks was reported by Barić (1966a), Dangić (1971),<br />
John (1880), Jovičić (1891), Kišpatić (1904, 1904a), Luburić (1963), Luković<br />
(1957), Pamić, Dimitrov and Zec (1964), Pavlović (1889), Paul (1879), Primics<br />
(1881), Ramović (1957, 1961, 1962, 1963, 1966), Tajder (1951/53, 1953, 1960),<br />
Trubelja (1970a, 1971a, 1972), Trubelja and Pamić (1956, 1957, 1965), Trubelja and<br />
Paškvalin (1962), Walter (1887).<br />
John (1880) gives the first report on biotite and other minerals in Tertiary-age<br />
effusive rocks in the Srebrenica area. John identified biotite microscopically as black<br />
and darkgreen platelets in trachytes at Šušnjar (Kišpatić believes that the locality is<br />
at the village of Potočari), quartz-propylites at Srebrenica, dacites at Ljubovija and<br />
andesites at Zvornik (Veljava Glava). Walter (1887) noticed red-brown and green<br />
mica in the mentioned quartz-propilites. These rocks were later investigated by our<br />
petrographer Kišpatić (1904a). Almost all andesites and dacites investigated by<br />
Kišpatić contained biotite, fresh or altered.<br />
In the period after the II World War, the Srebrenica effusive rock formations<br />
were investigated by Tajder who published his results in two short papers and one<br />
monograph (Tajder 1951/53, 1953 and 1960). He found that biotite is an important<br />
mineral constituent of most of the investigated dacite rocks, except those which have<br />
been altered by hydrothermal propilitization processes.<br />
Biotite is found in the bytownite-containing dacite at Diminići, the biotitedacites<br />
of Jamno creek, around the villages of Ažlice, Sase, Divljak, at Diminić creek<br />
and at the foot of Mt. Drmnik. All of these rocks contain substantial amounts of<br />
biotite, so that it forms the name of the rocks. Furthermore, biotite is found also in<br />
dacite rocks from the Kiselica and Majdan creeks, and in the amphibole-containing<br />
dacites around Srebrenica. These rocks contain lesser amounts of biotite<br />
Biotite is the most common ferromagnesian mineral of the bytownitecontaing<br />
dacites from Diminići. It occurs as idiomorphic crystals displaying light<br />
yellow to dark brown pleochroism. Some crystals are rounded due to magmatic<br />
corrosion and these are often surrended with an omphacite layer. Crystals of
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
plagioclase and apatite are often embedded in the biotite crystals. At Jamno creek,<br />
the biotite occurs as idiomorphic crystals which are sometimes up to 1.5 mm in<br />
length. These are mostly fresh and show distinct pleochroism.<br />
Some dacites around Srebrenica contain chloritized and kaolinized biotite,<br />
so that some grains are pure chlorite. All investigated rocks show clear signs of<br />
opacitization.<br />
Propilitization processes are common in biotite. The dacites of Drenovac<br />
creek contain completely chloritized biotite but also epidote, magnetite and<br />
carbonates. Only some biotite crystals still show characteristic pleochroism.<br />
Biotite is the most common constituent of the lamprophyre dikes around<br />
the village of Sase near Srebrenica (Trubelja and Paškvalin 1962). It can be easily<br />
observed macroscopically in the form of brownish crystals with good cleavage<br />
along the base. Hexagonal crystals are comparatively rare. In thin section this biotite<br />
shows distinct pleochroism: Z = Y = dark brown, X = yellowish brown. It has a<br />
visible zonar texture so that the central sections of the biotite grains are much lighter<br />
in colour than other sections. It is optically negative with a small axial angle. It is<br />
altered to chlorite.<br />
Around the village of Bratunac in the srebrenica area, small amounts of<br />
biotite are found in kaolinized dacites at the Smoljave and Borići localities (Trubelja<br />
1970a, 1971a and 1972; Dangić 1971).<br />
The products of Tertiary-age volcanism in the Bosna river valley contain<br />
biotite as a common constituent. It was first determined by John (1880) who noted<br />
the biotites distinct pleochroitic colours (light yellow to black), especially in the<br />
trachytes from the Maglaj fortress. Similar rocks in the area were also investigated<br />
by Primics (1881). He identified biotite in the trachytes and green biotite-quartztrachytes<br />
between Žepče and Maglaj.<br />
Kišpatić (1904) provides more data on the biotite and other minerals in the<br />
andesites from the Bosna river valley. The andesites around Maglaj contain yellow<br />
and brownish phenocrystals of biotite with some embedded apatite. It is altered into<br />
chlorite and epidote, although it is mostly fresh in the investigated rocks. After the II<br />
World War, these rocks were extensively studied by F. Trubelja and J. Pamić (1956<br />
and 1965). Biotite-containing dacites were found at Jelovac village in the Bosna<br />
river valley. Sanidine-containg dacites occur at Brusnička Rijeka near the village<br />
of Parnice. The biotite in the Jelovac dacites is largely fresh and idiomorphic, with<br />
some grain elongation along cleavage directions. The pleochroitic colours are very<br />
distinct – X = light yellow, Y = dark brown. Biotite from the sanidine-containing<br />
dacites has somewhat different properties: X = light yellow, Y = greenish brown.<br />
Extinction is parallel. It is frequently opacitized due to exsolved magnetite.<br />
185
SILICATES<br />
Majer (1961) investigated the biotite in dacite-type rocks from the Blatnica<br />
creek near Teslić. Here the biotite forms phenocrystals together with plagioclase, and<br />
can be seen macroscopically. It is mostly fresh, with only occasional chloritization.<br />
Biotite also occurs in pyroclastic rocks – in volcanic tuffs of the Neogeneage<br />
sediments around Tuzla (Luković 1957). It displays distinct pleochroism in<br />
golden yellow and dark brown colours.<br />
Biotite is found also in tuffs of the Duvno and Livno area (Barić 1966a,<br />
Luburić 1963). Barić notes that biotite is common in the Tertiary-age rhyolite tuffs<br />
around Livno. Biotite occurs in the form of black hexagonal platelets, up to 2 mm in<br />
size. Investigations in thin sections have shown that the optical axes angle = 15° and<br />
negative. The biotite contained in tuffs from Vojvodinac is optically nearly uniaxial,<br />
or the optic axial angle is very small.<br />
186<br />
2. Biotite in rocks of the Bosnian Serpentine Zone<br />
Rocks of the Bosnian serpentine zone (BSZ) do not contain substantial<br />
amounts of biotite. It occurs in acidic to neutral intrusive rocks and vein-type effusive<br />
rocks such as albite-containing rhyolite. It can also be found in basic igneous and<br />
metamorphic rocks. A limited amount of data on biotite can be found in the papers<br />
by Đorđević and Stojanović (1964), John (1880), Karamata (1953/54), Kišpatić<br />
(1897, 1900), Majer (1963), Majer and Pamić (1974), Pamić (1971, 1971a), Pamić<br />
and Kapeler (1969), Pamić and Olujić (1969), Pamić, Šćavničar and Međimorec<br />
(1973), Pamić and Tojerkauf (1970), Trubelja (1962, 1963b), Varićak (1955).<br />
John (1880) was again the first author to identify biotite in the BSZ. Biotite<br />
occurs in the biotite-containg diabase around Žepče, close to Mt. Lupoglav. The<br />
biotite is of a red-brownish colour and strongly pleochroic. Kišpatić (1897 and<br />
1900) identified a moderate amount of biotite in diabase rocks near Čelinac. He<br />
also identified a large biotite grain in the olivine gabbro from Miljkovačka Rijeka,<br />
near Buletići.<br />
Biotite is an important mineral constituent of spilites near Bosanski Novi<br />
(locality Torić creek), according to Trubelja (1962). It occurs in the form of platelets<br />
or crystals elongated along cleavage directions. Larger crystal are frequently bent.<br />
Cleavage is perfect, with a parallel extinction in thin section. Pleochroism: X = light<br />
brown, Y = dark brown.<br />
Karamata (1953/54) found biotite in albite rhyolites near Bosansko Petrovo<br />
Selo. It also occurs in keratophyres of Mt. Ljubić (Trubelja 1963b).<br />
Several authors identified biotite in acidic granitoids and similar intermediary<br />
rocks of the BSZ. The albitic granite, found along the road Žepče – Maglaj close
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
to Selište, contains smaller amounts of biotite with respect to leucocratic minerals<br />
(Đorđević and Stojanović 1964). Grains are 2.43 x 2.70 mm in size and display<br />
distinct cleavage and pleochroism (yellowish to dark brown). The optic axial<br />
angle, measured in thin section, is in the range of 0-6°, negative. Chloritization is<br />
occasionally present.<br />
Pamić and Olujić (1969) identified biotite in albitic granite from Gostilje<br />
(Bosansko Petrovo Selo), where it is fresh and distinctly pleochroic (light yellow,<br />
yellow brown). Majer and Pamić (1974) found moderate amounts of biotite in<br />
altered shales in the northeastern part of ultramafic complex of Mt. Borje. The<br />
granitoid rocks of this area also contain some biotite (Pamić and Tojerkauf 1970).<br />
Some additional data on the occurence of biotite can be found in the publications by<br />
Pamić (1971, 1971a) and Pamić and Kapeler (1969).<br />
Varićak (1955) identified biotite in thin sections of pebbles contained in the<br />
so-called red granite from Maglaj. This rock was described previously by Kišpatić<br />
(1897). Here, biotite occurs as platelike crystals which show signs of corrosion and<br />
mechanical deformation. Transformation into chlorite is frequent. Pleochroism is<br />
distinct – X = light yellow to greenish, Z = Y = green.<br />
3. Biotite in rocks of Mt. Motajica and Mt. Prosara<br />
Information on the occurences of biotite in various rocks of the Mt. Motajica<br />
and Mt. Prosara complexes can be found in publications by Arsenijević (1967), Ilić<br />
(1953), John (1880), Katzer (1924 and 1926), Koch (1908), Pilar (1882) and Varićak<br />
(1957 and 1966).<br />
First extensive information on biotite in rocks from Mt. Motajica was<br />
published by Koch (1908) – moderate amounts of biotite occur in the granite of Veliki<br />
Kamen near Vlaknica as well as in the muscovite granite from Brusnik. Biotite is an<br />
important constituent mineral of the granite-gneiss rock from Židovski creek. This<br />
biotite is of a light brown colour, showing good cleavage and distinct pleochroism.<br />
It contains some embedded quartz and apatite.<br />
The muscovite gneisses of Studena Voda contain only minor amounts of<br />
biotite, which is – however – a major mineral constituent of biotite gneisses from the<br />
same locality. It also occurs in garnet-bearing biotite gneisses at Kobaš and Hercegov<br />
Dol near Bosanski Svinjar. The properties (cleavage, pleochroism) of these biotites<br />
are almost identical in thin section. Biotite also frequently occurs in micaschists,<br />
andalusite-bearing micaschists and amphibolites.<br />
Katzer’s treatise on the Geology of Bosnia and Hercegovina contains a<br />
substantial amount of data on biotite in rocks of the Mt. Motajica and Mt. Prosara<br />
complexes, as well as in other areas of the Paleozoic-age rocks in Bosnia (Katzer<br />
187
SILICATES<br />
1924, 1926). Most of his data is based on microscopic investigations done by F.Koch.<br />
Katzer (1926, p. 68) described the biotite in the granites from Mt. Motajica as follows:<br />
„among the mica minerals is biotite (lepidomelane), dark brown to black in colour<br />
and mostly fresh. It is dispersed within the rock, in the form of irregular grains or<br />
hexagonal platelets. Coarser granite varieties, especially pegmatite granites, contain<br />
biotite as hexagonal platelike crystals 1-2 cm in size, of a brown colour and strong,<br />
almost metallic lustre“. Biotite occurs also in other rocks found at Mt. Motajica<br />
(biotite-containg aplites, pegmatites, gneisses, micaschists and phyllites).<br />
More recent petrographic investigations by Varićak (1966) provide a<br />
substantial amount of data on biotite in various rock of the Mt. Motajica complex.<br />
Biotite is an important constituent of regular granites, granite porphyres (2V = -5°),<br />
lamprophyres, contactolites of sedimentary origin, gneisses, biotite cornites and<br />
amphibolites. The granites from Mt. Motajica contain up to 25 g/t tin and up to 40<br />
g/t beryllium (data by Arsenijević).<br />
Katzer (1924, 1926) and Varićak (1956 and 1957) provide a treatment of<br />
biotite in the Mt. Prosara complex. Katzer only described the occurence of biotite in<br />
acidic igneous rocks, where biotite occasionally occurs in copious amounts. Varićak<br />
(1956) identified biotite as an essential constituent mineral in quartzporphyres of Mt.<br />
Prosara. It seldom occurs in the form of fresh grains, and is usually depleted in iron.<br />
This process is visible due to the pale colour of biotite and the iron hydroxide layers<br />
along cleavage fissures. Transformation into chlorite or epidote is of less importance.<br />
The size of individual grains lies in the range between 0.02 x 0.3 and 0.2 x 2 mm. The<br />
overall amount of biotite is 0.5-2%. Varićak (1957) mentions biotite occurences also<br />
in various metamorphic rocks of the Mt. Prosara complex – in gneisses, micaschists,<br />
quartzite schists, marbles and green rocks. Transformation into chlorite is common.<br />
This author provides no further details.<br />
188<br />
4. Biotite in rocks of the mid-Bosnian schist mountains<br />
John (1880) was the first author to mention the occurence of biotite in the<br />
liparites (quartzporphyres or rhyolites) from Mt. Vranica. Jurković and Majer (1954),<br />
Katzer (1924, 1926) and Foullon (1893) identified biotite in similar rock types<br />
also in other regions of the mid-Bosnian schist mountains. According to Foullon,<br />
biotite occurs together with some potassium micas in certain quartzporphyres and<br />
metamorphic rocks of the Suhodol complex. Some information on biotite in gneisstype<br />
rocks of Voljevac and Prosje are provided by Katzer (1926, p. 106).<br />
Biotite is an essential mineral constituent of the biotite-chlorite-ankerite<br />
schists from the Ivanovica creek near Busovača, while moderate amounts can also<br />
be found in the albite-chlorite schists (Trubelja and Sijarić, 1970). The schist rocks in<br />
this area belong to the facies of green rocks. Biotite grains were extracted from these
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
rocks and investigated in thin section. Chemical and x-ray diffraction analysis was<br />
also done. In thin section biotite displays its characteristic cleavage along the base,<br />
strong pleochroism and parallel extinction.<br />
X-ray diffraction data for the biotite from Ivanovica creek are given in table 32.<br />
Table 32. X-ray diffraction data for biotite from Ivanovica creek (Trubelja and Sijarić 1970)<br />
Nr. d Å I Nr. d Å I<br />
1 14.343 just visible 13 2.534 medium<br />
2 10.100 very very strong 14 2.454 very strong<br />
3 7.115 medium 15 2.392 just visible<br />
4 4.493 medium 16 2.322 just visible<br />
5 4.051 medium 17 2.291 medium<br />
6 3.689 medium 18 2.190 strong<br />
7 3.545 medium 19 2.009 strong<br />
8 3.363 very strong 20 1.682 strong<br />
9 3.139 medium 21 1.546 very strong<br />
10 3.056 just visible 22 1.372 medium<br />
11 2.947 medium wide 23 1.333 medium<br />
12 2.639 very strong<br />
Chemical analysis of the same biotite yielded following results:<br />
SiO 2<br />
= 33.66; TiO 2<br />
= 2.28; Al 2<br />
O 3<br />
= 17.40; Fe 2<br />
O 3<br />
= 9.51;<br />
FeO = 9.63; MnO = 0.19; MgO = 11.61; CaO = 0.93;<br />
Na 2<br />
O = 2.10; K 2<br />
O = 6.60; H 2<br />
O + = 5.06; H 2<br />
O - = 0.69; P 2<br />
O 5<br />
= 0.18; Total = 99.84<br />
The structural formula based on the chemical analysis data and 24 (O,OH)<br />
atoms is:<br />
(Ca 0.14<br />
K 1.24<br />
Na 0.60<br />
)(Ti 0.25<br />
Fe 3+ 1.14 Fe2+ 1.19 Mn 0.02 Mg 2.55 )(Si 4.97 Al 3.03 ) O 19.01 (OH) 4.99<br />
In the area of mid-Bosnian schist mountains biotite also occurs in products<br />
of Triassic-age magmatism. This will be treated in a subsequent chapter.<br />
5. Biotite in rocks of northwestern, eastern and southeastern Bosnia<br />
In northwest Bosnia biotite occurs in schists of Paleozoic age as well as<br />
in some transformed basic volcanics. Data is very scarce, derived from only 2<br />
publications (Podubsky 1968, Podubsky and Pamić 1969). According to Podubsky<br />
(1968), in NW Bosnia biotite occurs primarily in metasediments of Paleozoic age,<br />
where the degree of its preservation is rather low. Transformation into chlorite and<br />
hydromica is common. The schists from eastern and southeastern Bosnia contain<br />
minor amounts of biotite, usually as an accessory mineral species. Greater quantities<br />
of biotite are contained in orthometamorphic rocks of Mlječvanska Rijeka where<br />
it is an essential mineral in chlorite-biotite-feldspar-epidote-amphibole schists and<br />
biotite-tourmaline-epidote-quartz-amphibole schists (Podubsky 1970).<br />
189
SILICATES<br />
6. Biotite in products of Triassic-age magmatic events<br />
Biotite occurs frequently in various rocks associated with Triassic-age<br />
magmatic events. However, again the data is scarce. These biotites are mentioned<br />
in publications by Behlilović and Pamić (1963), Čelebić (1967), Hlawatsch (1903),<br />
John (1888), Jovanović (1957), Jurković (1954a), Katzer (1903, 1910, 1924, 1926),<br />
Kišpatić (1910), Majer and Jurković (1957, 1958), Marić (1927), Nöth (1956), Pamić<br />
(1961), Pamić and Papeš (1969) and Trubelja (1969, 1972a).<br />
Most of the available data pertains to biotite occuring in basic and<br />
other intrusive rocks. Certain differentiates of the gabbro complex at Jablanica<br />
contains varying amounts of biotite (Marić 1927). Magnetite is frequently<br />
embedded in biotite grains. The gabbro rocks near the locality of Zlato often<br />
contain hexagonal biotite sheets. The biotite occuring in the gabbro from the<br />
central sections of the complex has distinct pleochroism: X = pale yellow, Z =<br />
red brown. Maximum birefringence is Nz – Nx = 0.047. In northern sections of<br />
the complex the biotite is of a pale brown colour due to surface weathering. One<br />
fissure within the gabbro series (near Bukov Pod) contain almost idiomorphic<br />
biotite crystals, elongated and green to black in colour, but with weathered<br />
surfaces. Some gabbro veins, high above the Neretva river bed, contain biotite<br />
sheets 2.5 x 3 cm in size. Some crystal are up to 7 cm in length, and 0.5-1 cm<br />
thick. They are chloritized on the surface.<br />
Information on biotite in the Jablanica gabbro complex can be found in<br />
publications of Čelebić (1967), Hlawatsch (1903), John (1888), Katzer (1903, 1910),<br />
Kišpatić (1910), Nöth (1956), Ramović (1968).<br />
Majer and Jurković (1957, 1958), Katzer (1910, 1924, 1926) and Kišpatić<br />
(1910) investigted the biotite contained in gabbrodiorite from the Bijela Gromila<br />
complex south of Travnik, where it occurs both as an essential or accessory mineral.<br />
Biotite is an essential mineral in diroites from Kopile and the Zasenjak creek<br />
(Majer and Jurković 1957, 1958). The biotite sheets are highly irregular in shape,<br />
as if subject to tearing. In thin section they display good basal cleavage and strong<br />
pleochroism (brown to red). Biotite also occurs in the olivine gabbros from Stajište<br />
(Novi Travnik).<br />
Jurković (1954a) identified biotite in the augite-labradorite andesites from<br />
Orašin near Bakovići.<br />
Jovanović (1957) and Pamić (1961) found biotite to be an essential mineral<br />
constituent – together with quartz and albite- of granites from the southern flanks of<br />
Mt. Prenj.<br />
190
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
According to available literature data, biotite was not found in effusive and<br />
vein-type rocks belonging to the series of Triassic-age magmatic differentiates in<br />
Bosnia and Hercegovina. However, biotite is contained in pyroclastic rocks (tuffs)<br />
which are spatially associated with the mentioned differentiates.<br />
Behlilović and Pamić (1963) identified biotite in tuffs and volcanic breccias<br />
of Ladinian-age volcanogenic-sedimentary rocks from the Drežanka river valley in<br />
Hercegovina, as well as in the area of Kupreško Polje (Pamić and Papeš 1969).<br />
The biotite is usually transformed into bauerite and chlorite, accompanied by the<br />
exsolution of magnetite.<br />
Trubelja (1969, 1972a) identified black biotite crystals in tuffs of mid-Triassic<br />
age at Borovica and Vareš. Biotite was also identified in volcanogenic-sedimentary<br />
rocks from the Smreka – south ore body at Vareš (Trubelja, unpublished results).<br />
7. Biotite in sedimentary rocks<br />
Very little data is available on biotite in sedimentary rocks, although some<br />
recent investigation have confirmed it occurence in these rocks – Gaković and<br />
Gaković (1973), Mudrenović and Gaković (1964), Nikolić, Živanović and Zarić<br />
(1971), Pavlović and Ristić (1971), Pavlović, Ristić and Likić (1970), Ristić, Likić<br />
and Stanišić (1968), Sijerčić (1972), Šćavničar and Jović (1961, 1962).<br />
Gaković and Gaković (1964) identified biotite, together with other minerals,<br />
in the insoluble residue of Triassic-age carbonate rocks from some karstic areas in<br />
Bosnia and Hercegovina. Mudrenović and Gaković (1964) mention biotite in clays<br />
from Zalomska Rijeka in eastern Hercegovina.<br />
Biotite is commonly found in the quartz-containing clastic sediments of the<br />
Tuzla basin – Pavlović, Ristić and Likić (1970), Ristić, Likić and Stanišić (1968),<br />
Sijerčić (1972), Šćavničar and Jović (1961, 1962).<br />
Pavlović and Ristić (1971) found only minor amounts of biotite in the quartz<br />
sands from the „Bijela Stijena“ deposit near Zvornik. Nikolić et al. (1971) also found<br />
minor amounts of biotite in bentonite clays from Šipovo in the Pliva river valley.<br />
191
SILICATES<br />
ILLITE<br />
K 0.65<br />
Al 2.00<br />
Al 0.65<br />
Si 3.35<br />
O 10<br />
(OH) 2<br />
Crystal system and class: Monoclinic.<br />
Properties: perfect cleavage along {001}. The colour is white, specific gravity 2.6-2.9;<br />
hardness = 1-2.<br />
Illite occurs as colourless pseudohexagonal platelets of very small<br />
dimensions. It is a typical representative of the illite group of minerals (illite clays).<br />
It was named after the state of Illinois in USA. Illite is structurally similar with<br />
the mica minerals. Some authors refer to illite as hydromuscovite (hydromica).<br />
The chemical composition is rather variable. Apart from aluminium, silica and the<br />
hydroxyl group, potassium is its main chemical component.<br />
Illite can form in several different ways – by atmospheric weathering of<br />
potassium feldspars, alteration of muscovite, metasomatic exchange of magnesium<br />
and calcium in montmorillonite or by recrystallization of potassium-containing<br />
clayey sediments.<br />
X-ray data:<br />
Hydromuscovite d 10.0 (VS) 3.34 (VS) 5.0 (S) 4.46 (S) 2.544 (S)<br />
Illite<br />
d 9.98 (VS) 4.47 (S) 2.56 (S) 3.31 (M) 2.38 (M)<br />
A u t h o r s: Ćatović, Trubelja and Sijarić (1976), Čelebić (1963), Jurković<br />
(1961a), Marić and Crnković (1961), Pavlović (1975), Pavlović, Ristić and Likić<br />
(1970), Podubsky (1955, 1968, 1970), Ristić, Likić and Stanišić (1968), Sakač (1969),<br />
Sijarić (1975), Sijarić and Trubelja (1974), Stangačilović (1956, 1956a, 1969, 1970),<br />
Šćavničar and Jović (1962), Tasić (1975), Trubelja (1970), Vasiljević (1969).<br />
Illite-type clays have a wide distribution in Bosnia and Hercegovina but<br />
literature data is scarce. Illite is a significant constituent of clays found in Prijedor<br />
and Sarajevo-Zenica basins. It occurs in Palaeozoic-age sediments of western,<br />
eastern and south-eastern Bosnia. Recent investigations dealing with bauxites have<br />
shown that illite is present in this matrix also. Illite is also commonly found in some<br />
clastic sediments (sands etc.).<br />
192<br />
1. Illite in Palaeozoic-age rocks<br />
Illite-containing sediments are very common rocks in the Sana river and Una<br />
river area in western Bosnia (Marić and Crnković 1961, Jurković 1961a, Podubsky<br />
1968). Illite occurs both as an important or accessory mineral in argillaceous and<br />
clay-schists and phyllites, together with quartz, muscovite, plagioclase relicts, and<br />
accesssory iron minerals.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
According to investigations by Marić and Crnković in the area of the Ljubija<br />
iron mine, illite is commonly found in the clay-schists of the Brdo and Nova Litica<br />
mineralizations. X-ray diffraction data of illite from these two mentioned localities<br />
is given in Table 33 and 34. This study has shown that illite is the dominant mineral<br />
in the rock, next to quartz, muscovite and feldspar. Microscopic determinations<br />
revealed that illite is the main component of the finegrained matrix. The dense illite<br />
mass sometimes contains rutile crystals which display characteristic twinning.<br />
Jurković (1961a) found illite to be a common mineral in the iron parageneses<br />
of the Ljubija iron ore body. Here it is found at the following localities: Nova Litica –<br />
Trešnjica, Redak, Bregovi, Jakarina Kosa, Jerkovača, Baščine and Paljevine. Točak,<br />
Stojančići, Kliment and Gradina are localities in the Tomašica area.<br />
Table 33. XRD data for the illite-containing rock from the Brdo mine (Marić and Crnković 1961)<br />
d Å Line intensity Mineral<br />
4.45 Medium Illite<br />
4.22 Medium Quartz<br />
3.86 Weak Muscovite<br />
3.71 Weak Muscovite<br />
3.35 Strong Quartz (Illite 3.33)<br />
3.20 Very weak Illite, muscovite<br />
2.99 Weak Illite, muscovite<br />
2.56 Medium strong Illite, muscovite<br />
2.46 Medium strong Quartz, illite<br />
2.38 Weak Illite<br />
2.24 Weak Illite<br />
1.50 Medium strong Illite<br />
1.38 Weak Illite<br />
1.37 Medium Quartz<br />
1.29 Weak – diffuse Quartz, illite<br />
1.25 Weak Quartz, illite<br />
Table 34. XRD data for the illite-containing rock from the Nova Litica mine (Marić and<br />
Crnković 1961)<br />
d Å Line intensity Mineral<br />
5.00 Weak Muscovite, illite<br />
4.47 Medium Muscovite (illite 4.46)<br />
4.29 Medium strong Quartz, illite<br />
4.15 Weak Feldspars<br />
3.49 Weak Muscovite<br />
3.35 Strong Quartz<br />
2.57 Medium Illite, muscovite<br />
2.46 Medium Quartz, illite<br />
2.30 Medium Quartz<br />
2.23 Medium Illite (2.24), quartz (2.22)<br />
2.14 Medium Illite (2.12)<br />
1.82 Medium Quartz<br />
1.67 Medium Quartz, illite<br />
1.55 Medium Quartz<br />
193
SILICATES<br />
1.51 Medium – diffuse Illite<br />
1.37 Strong Quartz, illite<br />
1.26 Medium Quartz<br />
1.24 Weak Illite<br />
Note: the feldspar lines are located within following ranges: 4.09-4.20 Å, 3.81-3.94<br />
Å, 3.73-3.77 Å, 2.97-3.01 Å, 2.61-2.67 Å, 2.40-2.41 Å.<br />
Some illite was extracted in the form of insoluble residue from the limonitic<br />
ore from the Stojančići locality. Illite occurs as flakes 10-30 μm in size. This illite<br />
was studied by thermal methods.<br />
Podubsky (1970) found illite in similar rocks in eastern and southeastern<br />
Bosnia, after this author made first findings of illite clays in Bosnia and Hercegovina in<br />
1955 (Podubsky 1955). He found illite to be a constituent mineral of the pyrophyllite<br />
schist at Parsovići in Hercegovina and in halloysite schists in SE Bosnia, near the<br />
village of Bakije. Illite was determined by XRD and thermoanalytical methods.<br />
2. Illite in the basins of Prijedor and Sarajevo – Zenica<br />
Illite contained in Palaeozoic age argillaceous and clay-schists can migrate<br />
into surrounding basins where it can form thick layers of allochtonous clays of<br />
Tertiary age, as is the case in the basins of Prijedor and Sarajevo – Zenica. The<br />
mineralogical characteristics of these clays were investigted by several authors<br />
(Stangačilović 1956a, 1969 and 1970; Pavlović 1975; Tasić (1975).<br />
In the Prijedor basin illite can be found at the following localities: Bišćani,<br />
Halilovci, Rizvanovići, Hambarine, Rakovčani, Carevina and Puharska. The<br />
parageneses commonly contain also kaolinite, montomorillonite and substantial<br />
amounts of quartz. The quantitative distribution of illite in argillaceous sediments of<br />
the Prijedor basin is given in Tables 35 and 36 (Pavlović 1975, Tasić 1975).<br />
Table 35. Mineral composition (%) of clays from the Prijedor basin (Pavlović 1975)<br />
Sample Illite Montmorillonite Kaolinite Quartz<br />
PC – 1 25.55 --- 23.80 49.51<br />
PC – 2 48.41 --- 23.80 24.93<br />
PC – 3 39.84 16.63 29.06 10.90<br />
PCM – 1 46.82 --- 24.38 23.65<br />
PCM – 2 45.71 --- 24.24 22.94<br />
PRC – 2/3 50.31 5.08 26.39 15.99<br />
PR – 1 51.58 3.21 22.01 21.92<br />
PR – 2 50.79 6.11 25.10 15.48<br />
PR – 3 47.61 5.24 20.52 23.75<br />
Note: PC and PCM = locality Puharska (Crna dolina); PRC = Carevina locality; PR = Rakelić<br />
(Kurteš) locality.<br />
194
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Table 36. Mineral composition (%) of clays from the Prijedor basin and Sarajevo – Zenica<br />
basin (Tasić 1975)<br />
Sample Illite Montmorillonite Kaolinite Quartz<br />
PZ – 3 36.34 16.93 42.04 1.18<br />
PZ – 4 45.07 7.60 34.80 7.34<br />
PZ – 4a 45.71 8.46 40.02 2.08<br />
PZ – 5 43.65 4.80 23.88 23.61<br />
KL 61.98 --- 7.18 20.34<br />
Note: PZ = locality Rizvanovići (left bank of the Sana river)<br />
KL = locality Klokoti (Sarajevo – Zenica basin)<br />
The qualitative and quantitative composition of the clays is based on X-ray<br />
diffraction, thermoanalytical methods and chemical analysis. The clays from the<br />
Prijedor basin contain some montmorillonite and quartz and are important raw<br />
materials for the manufacture of tiles and other ceramics.<br />
Stangačilović (1956a) investigated the illite clays in the Sarajevo –<br />
Zenica basin (Kobiljača nd Rakovica localities). These clays are of upper Tertiary<br />
age (Pontian). Other localities must also be mentioned – Busovača, Klokoti and<br />
Bilalovac. All these sediments have a compartively even clay mineral composition<br />
– illite, kaolinite, meta-halloysite and montmorillonite. The Kobiljača clays are of<br />
Tertiary age and occur at the west side of the Sarajevo – Zenica basin, some 18 km<br />
west of Sarajevo on the Sarajevo – Kiseljak road. These clays have been studied in<br />
detail by XRD, thermoanalytical and microscopic methods.<br />
XRD analysis and microscopic determinations showed that the Kobiljača<br />
and Rakovica clays contain also quartz. The quartz grains are mostly tiny, but some<br />
idiomorphic crystals were identified. The clays also contain sericitized and kaolinized<br />
orthoclase, calcite, biotite, muscovite, zircon, tourmaline (nice crystals displaying<br />
pleochroism). Ilmenite, garnet and apatite are rare. These accessory minerals can<br />
provide an indication of the source rocks from which the clays formed. The source<br />
rocks are mostly quartzporphyres, but also other rocks similar to the ones within<br />
the Una and Sana river Palaeozoic complex could have provided material for the<br />
formation of clays.<br />
The allochtonous clay deposits in the basins of Prijedor and Sarajevo – Zenica<br />
formed in peripheral region of the Pannonian basin, by deposition of clay minerals and<br />
subsequent formation of thin or thicker clay deposits of Miocene age. The deposits<br />
in the Prijedor area are characteristic for shallow-water, littoral environments. The<br />
material is mostly derived from rocks of Palaeozoic, possibly also Triassic age.<br />
According to Stangačilović, the clays in the Sarajevo – Zenica basin contain<br />
some coal and formed under lacustrine conditions. This author also investigated the<br />
195
SILICATES<br />
kaolinite clays of Mt. Motajica in which he found illite. More information can be<br />
found in the section dealing with kaolinite.<br />
3. Illite in bauxites and other sediments<br />
Detailed XRD investigations of bauxites from NW Bosnia (Grmeč, Srnetica)<br />
provide data on the qualitative and quantitative compositon and illite distribution in<br />
these matrices (Ćatović, Trubelja and Sijarić 1976, Sakač 1969, Sijarić 1975, Sijarić<br />
and Trubelja 1974).<br />
Illite commonly occurs in Triassic-age bauxites from the Bjelaj locality at<br />
Mt. Grmeč. The illite content is in the range between 3.3-19.9%. Other bauxites<br />
contain less illite. Trubelja (1970) identified illite in clays associated with the<br />
diaspore bauxites of Ljuša near Jajce.<br />
Pavlović et al. (1970) and Ristić et al. (1968) identified illite in sediments<br />
of the Tuzla basin. This finding is based on powder diffraction, DTA and TG<br />
measurements. Šćavničar and Jović (1962) made an x-ray diffraction determination<br />
of illite in the rocks associated with the coal series of the Kreka basin.<br />
Ćelebić (1963) identified illite in some iron-ore deposits around Konjic.<br />
The sedimentary quartzites of Podrašnica near Mrkonjić Grad contain some sericite<br />
and illite, based on microscopic determinations by S. Pavlović and D. Nikolić<br />
(Vasiljević 1969).<br />
Use: Illite is an important industrial mineral used in ceramics production<br />
and brick manufacture. It can also be used as a fertilizer, due to its high potassium<br />
content (ca. 6%).<br />
196<br />
HYDROMUSCOVITE<br />
(K,H 2<br />
O)Al 2<br />
[(H 2<br />
O,OH) 2<br />
│AlSi 3<br />
O 10<br />
]<br />
A u t h o r s: Barić and Trubelja (1971, 1975), Sijerčić (1972)<br />
Hydromuscovite is a rare mineral in rocks of Bosnia and Hercegovina.<br />
According to scarce literature, the mineral has been identified near the village of<br />
Repovci close to Bradina (Barić and Trubelja 1971, 1975) and on the western flanks<br />
of Mt. Majevica (Sijerčić 1972).<br />
1. The occurence at Repovci<br />
Hydromuscovite seems to be an essential mineral constituent of a<br />
hydromuscovite schist found near the village of Repovci, close to Bradina in
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Hercegovina. Some veins within this rock appear to contain a monomineralic<br />
hydromuscovite phase. The mineral has been identified using microscopic methods,<br />
powder diffraction, thermal and chemical analysis and IR spectroscopy.<br />
The optical properties of hydromuscovite are almost the same as for sericite,<br />
but detailed investigations have shown that it is not sericite. The optic axial angle<br />
2V = -20.75°, -19° and -24°. The Ny refractive index = 1.581 ± 0.002 was measured<br />
by the immersion method using monochromatic sodium light.<br />
The cited paper does not contains data on hydromuscovite shales and not<br />
on monomineralic hydromuscovite, so that the results of the other analyses are not<br />
presented here. The reader is referred to the publications by Barić and Trubelja<br />
(1971, 1975).<br />
2. The occurence at Mt. Majevica<br />
Sijerčić (1972, p. 106) identified hydromuscovite in arenite sands belonging to<br />
Eocene-age flysch deposits on the western flanks of Mt. Majevica. No further data is<br />
provided by the author.<br />
HYDROBIOTITE<br />
(K,H 2<br />
O)(Mg,Fe 2+ ) 3<br />
[(H 2<br />
O,OH) 2<br />
│AlSi 3<br />
O 10<br />
]<br />
X-ray data:<br />
d 12.3 (100) 3.5 (7.8) 23 (70) 3.02 (21) 2.73 (16)<br />
d 11.4 (100) 3.41 (80) 2.62 (80) 4.56 (20) 3.34 (20) 1.533 (60)<br />
A u t h o r s: Pamić and Đorđević (1974), Sijerčić (1972)<br />
Hydrobiotite is a rare mineral in Bosnia and Hercegovina and data is very<br />
scarce. Only Pamić and Đorđević (1974) mention this mineral entity found in rocks<br />
of the Bosnian serpentine zone. The hydrobiotite occurs in albitic rocks associated<br />
with the gabbro-dolerite complex of Bakinci. The authors maintain that hydrobiotite<br />
is an alteration product of biotite (p. 133).<br />
Sijerčić (1972, p. 106) also mentions hydrobiotite in arenite sands belonging<br />
to Eocene-age flysch deposits on the western flanks of Mt. Majevica. No further data<br />
on this mineral is available.<br />
197
SILICATES<br />
STILPNOMELANE<br />
(K,H 2<br />
O)(Fe 2+ Fe 3+ Mg, Al)
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
A u t h o r s: Barić (1966), Čičić and Pudar (1973), Đorđević (1969a), Đurić<br />
(1963), Filipovski and Ćirić (1963), Ilić (1954), Jakšić, Vuletić and Vrlec (1971),<br />
Jurković (1961a), Luburić (1963), Maksimović and Crnković (1968), Nikolić,<br />
Živanović and Zarić (1971), Pavlović (1975), Pavlović, Ristić and Likić (1970),<br />
Podubsky (1955), Ristić, Likić and Stanišić (1968), Soklić (1957), Stangačilović<br />
(1969, 1970), Tasić (1975), Trubelja (1966).<br />
Montmorillonite belongs to the group of clay minerals. In Bosnia and<br />
Hercegovina montmorillonite clays are widely distributed, but have not been<br />
sufficiently investigated. According to available literature data, montmorillonite clays<br />
occur in the Tertiary-age Prijedor basin, around the Ljubija ore deposits, around the<br />
city of Livno and elsewhere. It is a common constituent of soils, particularly those<br />
associated with underlying basic rocks (in the Bosnian serpentine zone).<br />
1. Montmorillonite in argillaceous sediments of the Prijedor basin<br />
Stangačilović (1969, 1970) provided first data on the occurence of<br />
montomorillonite in illite clays of the Prijedor basin. Montmorillonite is less abundant<br />
than other clay minerals. Pavlović (1975) and Tasić (1975) have done x-ray diffraction<br />
studies and thermal analysis of the argillaceous sediments of Prijedor basin. Pavlović<br />
investigated sediments from the localities of Crna Dolina, Carevina and Rakelić where<br />
the montmorillonite content is 3-16%. Tasić studied the clays of the Rizvanovići<br />
deposit on the left bank of the Sana river finding that the content of montmorillonite<br />
is approximately the same i.e. 4.8-16.9%. More data on the clays of Prijedor basin are<br />
given in the section on illite.<br />
2. Montmorillonite in the Brdo deposit at Ljubija<br />
Montmorillonite was identified in the iron mineral parageneses of the Ljubija<br />
deposit. Jurković (1961a) maintains that montmorillonite is a hypergene mineral in<br />
this deposit, since it is a ubiquitous associate, together with quartz, of goethite in the<br />
Brdo ore body. The variable content of these two minerals results in varying silica<br />
and alumina contents of the iron ore. Jurković performed thermal analysis on this<br />
montmorillonite.<br />
3. Montmorillonite from Livno<br />
Trubelja (1966) and Barić (1966) report on the occurence of montmorillonite<br />
at Podhum village, south of Livno, even though Luburić (1963) was the first to<br />
mention the tuffs and bentonites in this area. This authors wrote „in the Livno basin<br />
there are substantial outcrops of the newly discovered tuff layers. These outcrops can<br />
be seen from the village of Guber (SW of Livno) and further on towards Površje,<br />
Potok, Mandak (Podhum), Vojvodinac and Mt. Mala tušnica, for about 10 km. In the<br />
Duvno basin the tuff layers can be seen south of Duvno. Thin bentonite layers were<br />
observed at Podhum, Potok and Mandak – close to Vojvodinac – where the layer<br />
has a thickness of 30 cm“. Trubelja (1966) provides more laboratory data on this<br />
montmorillonite. He finds that this montmorillonite is associated with the rhyolite<br />
199
SILICATES<br />
tuffs, close to their contact with marls and limestones. The tuffs are primarily made<br />
up of volcanic glass, and the montmorillonite has formed as an alteration product of<br />
these tuffs. The tuffs are probably eolian in origin and of mid- to late-Miocene age,<br />
deposited in the lacustrine environment of the basin together with other sediments.<br />
The montmorillonite is usually mixed with calcite.<br />
Chemical analysis of almost pure montmorillonite gave following results:<br />
SiO 2<br />
= 49.95; TiO 2<br />
= 0.30; Al 2<br />
O 3<br />
= 18.43; Fe 2<br />
O 3<br />
= 2.16;<br />
FeO = 0.06; MnO = ---; MgO = 3.33; CaO = 2.07;<br />
Na 2<br />
O = traces; K 2<br />
O = traces; H 2<br />
O + = 6.65; H 2<br />
O - = 16.87; P 2<br />
O 5<br />
= 0.18;<br />
Total = 100.00<br />
The DTA curve is given in Figure 14.<br />
Figure 14. DTA curve of montmorillonite from Podhum near Livno (Trubelja 1966)<br />
4. Beidellite – montmorillonite clays of Šipovo near Jajce<br />
Nikolić et al. (1971) identified montmorillonite in the Tertiary-age Šipovo basin<br />
near Jajce. The bentonite clays of this area contain mostly beidellite, but also some<br />
montmorillonite (in the Grabež deposit, borehole BŠ-4, at a depth of 38.60-41.10 m).<br />
Results of chemical analysis of this montmorillonite, based on 24 (O,OH) cations<br />
are given in Table 37.<br />
Table 37. Chemical analysis of montmorillonite from the Grabež deposit<br />
% Number of ions<br />
SiO 2<br />
51.13 Si 7.67<br />
TiO 2<br />
0.15 Al 0.33<br />
Al 2<br />
O 3<br />
17.39<br />
Fe 2<br />
O 3<br />
3.46 Al 2.73<br />
MnO 0.02 Ti 0.02<br />
MgO 4.28 Fe 3+ 0.58<br />
CaO 2.00 Mg 0.95<br />
Na 2<br />
O 0.07<br />
K 2<br />
O 0.29 Ca 0.31<br />
H 2<br />
O - 12.72 Na 0.02<br />
H 2<br />
O + 8.66 K 0.05<br />
Total 100.17 OH 4.33<br />
8.00<br />
4.28<br />
0.38<br />
200
XRD data are given in Table 38.<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Table 38. X-ray diffraction data for the montmorillonite from Šipovo<br />
d Å I d Å I<br />
15.30 10 3.03 5<br />
5.08 1 2.57 6<br />
4.50 9 1.69 2<br />
3.33 7 1.50 5<br />
3.21 1<br />
5. Other occurences of montmorillonite<br />
Podubsky (1955) provided first data on the occurence of montmorillonite<br />
clays in Bosnia and Hercegovina, on the right bank of the Bosna river between<br />
Zavidovići and Žepče (Ljeskovica locality). The village of Ljeskovica is located<br />
2.5 km from the train station of Vinište, on the Doboj – Sarajevo railroad. Kaolinite<br />
occurs together with montmorillonite, so that these formations may be classified as<br />
kaolinite-montmorillonite clays. Thermal and XRD analysis showed that this material<br />
contained also a moderate quantity of carbonate and talc. The clays from Ljeskovica<br />
was previously studied by Ilić (1954) who regarded them as a talc formation.<br />
According to Stangačilović (1969, 1970), moderate amounts of<br />
montmorillonite occur also in the illite-kaolinite-metahalloysite clays of the Sarajevo<br />
– Zenica basin (deposits at Busovača, Klokoti, Bilalovac, Kobiljača). It is interesting<br />
to note that Tasić (1955) did not identify montmorillonite in the clays at Klokoti and<br />
Kobiljača.<br />
Pavlović et al. (1970) identified small amounts of montmorillonite in the<br />
clay fraction in the quartz sand of the Tuzla basin. Soklić (1957) mentions the<br />
montmorillonite deposits at Mt. Majevica, as alteration products of Tertiary-age<br />
(Helvetian) tuffs.<br />
Đorđević (1969a) found montmorillonite occuring together with talc near<br />
the village of Mušići at Mt. Ozren.<br />
Maksimović and Crnković (1968) identified Cr-montmorillonite and Crkaolinite<br />
as hydrothermal alteration products of ultrabasic rocks at Slatina near Teslić.<br />
Jakšić et al. identified montmorillonite within the clay fraction of the soils<br />
associated with serpentine rocks at Svatovac on Mt. Ozren. Montmorillonite was<br />
identified by XRD in the 0.2-2 μm fraction.<br />
Čičić and Pudar (1973) note the occurence of montmorillonite in bentonite<br />
clays of Bosnia and hercegovina, but provide no further data on the mineral.<br />
201
SILICATES<br />
BEIDELLITE<br />
Al 2<br />
[(OH) 2<br />
│Al 0.5<br />
Si 3.5<br />
O 10<br />
] -0.5 (CaNa) 0.3<br />
x nH 2<br />
O<br />
A u t h o r s: Caillere and Šibenik-Studen (1969), Đurić (1963), Jakšić,<br />
Vuletić and Vrlec (1971), Nikolić, Živanović and Zarić (1971).<br />
Beidellite is a member of the montmorillonite-type clays. In Bosnia and<br />
Hercegovina it has been investigated in some detail in the Šipovo area.<br />
202<br />
1. Beidellite at Šipovo in the Pliva river valley<br />
Caillere and Šibenik-Studen (1969) first mentioned the occurence of<br />
beidellite, a prominent mineral in bentonite clays found in the area of Šipovo near<br />
Jajce. These clays occur together with other sediments (sandstones, sandy clays and<br />
coal) in the lacustrine Tertiary-age basin of Šipovo. The sample in which beidellite<br />
was identified is from a borehole (depth 22.30-23.00 m).<br />
Laboratory analyses of the beidellite sample included thermal and chemical<br />
analysis, as well as x-ray diffraction. The DTA curve shows three endothermic peaks<br />
(at 100°, 500° and 900°C) and one exothermic effect between 940° and 1000°. A<br />
reverse run was done in view of a possible identification of quartz, but no effect<br />
was noted indicating that the amount of quartz present in the clay is negligible (less<br />
than 1%). The TG curve indicates a total weight loss of beidellite of 16%, within the<br />
following intervals – 10% between 0-270°, 5% between 275-600° and 1% between<br />
600-900°. The TG curve, published in the mentioned publication, also indicates that<br />
montmorillonite is stable up to 500°C. XRD data are given in Table 39.<br />
Table 39. X-ray diffraction data for the iron-containing beidellite from Šipovo<br />
d Å<br />
I<br />
15.10 10<br />
4.50 8<br />
2.59 8<br />
1.50 8<br />
The XRD pattern contains the most intensive line at around 15 Å, but after<br />
sample impregnation (and subsequent swelling) with ethylene-glycol the line moves<br />
to the 17.44 Å position. After heating for 2 hours at 300°C this interlattice distance<br />
diminishes to 10.2 Å, characteristic for beidellite. The XRD pattern shows also some<br />
weak lines belonging to quartz.<br />
Results of chemical analysis are as follows:<br />
SiO 2<br />
= 51.20; Al 2<br />
O 3<br />
= 19.00; Fe 2<br />
O 3<br />
= 5.80; FeO = traces; MgO = 3.70; CaO = 1.35;<br />
Na 2<br />
O =0.15; K 2<br />
O = 0.80; TiO 2<br />
= 1.00; H 2<br />
O + = 6.15; H 2<br />
O - = 11.30; Total = 100.45
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The small amount of quartz was not taken into account for the structural<br />
formula calculation of the iron-containing dehydrated beidellite<br />
(Si 3.71<br />
Al 0.29<br />
)(Al 1.34<br />
Fe 3+ 0.31 Mg 0.30 Ti 0.05 )O 11 Mg 0.10 Ca 0.10 Na 0.02 K 0.08<br />
It follows that the mineral is dioctahedral and that the Si 4+ vs. Al 3+ substitution<br />
in the tetrahedral layer is too large for montmorillonite. On the other hand, the amount<br />
of iron is too small for the mineral to be identified as nontronite.<br />
Two years after the first paper on the Šipovo beidellite was published,<br />
Nikolić et al. (1971) investigated with substantially more detail the beidellitemontmorillonite<br />
clays of the Šipovo basin. Four clay samples were analyzed in detail<br />
– three of those were beidellite while the fourth one was montmorillonite. Results of<br />
chemical analyses and XRD are presented in tables 40-42. Nikolić et al. (1971) came<br />
to the conclusion that the amount of clays in the upper Miocene-age argillaceous<br />
sediments is between 70 and 90%. Other minerals present are quartz, calcite,<br />
feldspar, muscovite, biotite, chlorite, staurolite, tourmaline, zircon, rutile, kyanite,<br />
garnet, pyrite and magnetite. The authors maintain that the clays formed from some<br />
pyroclastic material of unknown origin (perhaps of Miocene age or older).<br />
Table 40. X-ray diffraction data for beidellite from Šipovo (Nikolić et al. 1971)<br />
BŠ – 1 BŠ – 5 BŠ – 11<br />
d Å I d Å I d Å I<br />
15.50 8 14.50 10 14.50 10<br />
7.20 1 4.50 8 4.50 8<br />
4.45 10 4.22 1 4.22 1<br />
3.57 3 3.34 9 3.34 9<br />
3.34 7 2.58 6 2.58 6<br />
2.57 6 1.81 1 1.81 1<br />
2.35 2 1.68 3 1.68 3<br />
1.68 3 1.50 7 1.50 7<br />
1.50 4 1.37 2 1.37 2<br />
1.29 2 1.29 2<br />
BŠ – 1<br />
BŠ – 5<br />
BŠ – 11<br />
Grabež deposit, borehole, depth 27.5 m<br />
Grabež deposit, borehole, depth 41.5 m<br />
Sarići deposit, borehole, depth 5.20-6.30 m<br />
Table 41. Chemical analysis of the beidellite from Šipovo (Nikolić et al. 1971)<br />
BŠ – 1 BŠ – 5 BŠ – 11<br />
SiO 2<br />
46.30 46.53 47.31<br />
Al 2<br />
O 3<br />
25.06 21.00 18.76<br />
Fe 2<br />
O 3<br />
5.64 6.73 5.89<br />
MnO 0.03 0.02 0.03<br />
203
SILICATES<br />
MgO 2.16 2.66 2.19<br />
CaO 1.36 1.92 3.47<br />
Na 2<br />
O 0.07 0.07 0.07<br />
K 2<br />
O 0.33 0.75 0.34<br />
H 2<br />
O 100° 8.46 9.36 11.36<br />
H 2<br />
O 1000° 10.71 10.37 9.76<br />
Total 100.47 99.80 99.56<br />
Table 42. Calculation of the number of cations based on 24 (O, OH) for the Šipovo beidellite<br />
(Nikolić et al. 1971)<br />
BŠ – 1 BŠ – 5 BŠ – 11<br />
Si 6.68<br />
6.89<br />
7.17<br />
8.00<br />
8.00<br />
Al 1.32 1.11 0.83<br />
8.00<br />
Al 2.92<br />
2.55<br />
2.55<br />
Ti 0.03 0.04 0.04<br />
4.02<br />
3.93<br />
Fe 3+ 0.61 0.75 0.67<br />
3.75<br />
Mg 0.46 0.59 0.49<br />
Ca 0.21<br />
0.30<br />
0.56<br />
Na 0.01 0.25<br />
0.02 0.46<br />
0.02 0.63<br />
K 0.03 0.14 0.05<br />
OH 5.15 5.11 4.94<br />
2. Beidellite from the Višegrad area<br />
Đurić (1963) idenfied beidellite in clastic oolite sediments of the Zlatibor<br />
zone, in the area of the town of Višegrad. This author mentions the structural formula<br />
of beidellite as follows (Si 3.21<br />
Al 0.79<br />
)(Al 1.56<br />
Ni 0.36<br />
Cr 0.16<br />
Mn 0.09<br />
Ti 0.09<br />
)O 9.89<br />
Ca 0.15<br />
(OH) 2.11<br />
3. Beidellite from Mt. Ozren<br />
Jakšić et al. (1971) identified beidellite in the clay fraction from the soil<br />
overlying the serpentine-peridotite rocks at Mt. Ozren, Svatovac locality. XRD showed<br />
also the presence of montmorillonite and nontronite in the 0.2-2.0 μm fraction.<br />
NONTRONITE<br />
Fe 3+ [(OH) 2<br />
│Al 0.33<br />
Si 3.67<br />
O 10<br />
] -0.33 Na 0.33<br />
x nH 2<br />
O<br />
X-ray data: d 15.4 (100) 4.56 (90) 1.52 (90)<br />
IR-spectrum: 435 455 497 600 685 824 850 1035 1110 1640 3425 3568 cm -1<br />
A u t h o r s: Filipovski and Ćirić (1963), Đurić (1963), Jakšić, Vuletić and<br />
Vrlec (1971), Maksimović and Antić (1962), Trubelja (1971a, 1972).<br />
204
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Nontronite is a member of the montmorillonite clays. It may be fregarded as<br />
beidellite which contains Fe(III) instead of Al in the octahedral layer.<br />
Literature data on the distribution of nonotronite in Bosnia and Hercegovina<br />
is very scarce and makes any such evaluation very tenuous. It occurs mainly within<br />
the Bosnian serpentine zone (BSZ) and in the dacites of Bratunac near Srebrenica.<br />
1. Nontronite in the Bosnian serpentine zone<br />
Maksimović and Antić (1962) identified nontronite in relicts of the<br />
weathering cap of ultrabasic rocks in the Vardište and Višegrad areas (localities<br />
Prijevorac and Bijelo Brdo) in eastern Bosnia. Laboratory analyses including<br />
x-ray diffraction, chemical and thermal analyses showed that the mineral is<br />
an aluminum-bearing nontronite. Two samples were analyzed, one from the<br />
weathering crust and the other one from iron-bearing clay material. Their<br />
structural formulas are as follows:<br />
Nontronite 1 (from the weathering crust)<br />
(Si 3.68<br />
Al 0.32<br />
)(Fe 3+ 1.63 Al 0.17 Cr 0.05 Ni 0.06 Mg 0.05 Mn 0.01 Ti 0.02 )O 9.97 (OH) 2.03 Ca 0.20 Na 0.02 K 0.03<br />
Nontronite 2 (from the iron-bearing clay)<br />
(Si 3.1<br />
Al 0.9<br />
)(Fe 3+ 1.51 Al 0.26 Cr 0.13 Ni 0.15 Mg 0.23 Mn 0.02 Ti 0.01 )O 9.87 (OH) 2.13 Ca 0.10 Na 0.03 K 0.03<br />
X-ray diffraction data of the two nontronite samples are given in table 43.<br />
Table 43. X-ray diffraction data of nontronite (Maksimović and Antić 1962)<br />
Nontronite 1 Nontronite 2<br />
d Å I d Å I<br />
14.4 10 14.7 10<br />
*7.30 4 4.55 7<br />
4.55 7 2.524 9<br />
*3.65 6 2.45 2<br />
2.54 8 1.72 4<br />
1.526 9 1.305 2<br />
1.31 5<br />
The sample nontronite-1 contains also serpentine (*), while nontronite-2<br />
contains goethetite and magnite in addition to serpentine.<br />
Đurić (1963) mentions nontronite in oolitic clastic sediments from this<br />
same area. Jakšić et al. (1971) identified nontronite in the clay fraction from the<br />
soil overlying the serpentine-peridotite rocks at Mt. Ozren, Svatovac locality.<br />
XRD showed also the presence of montmorillonite and beidellite in the 0.2-2.0 μm<br />
fraction.<br />
205
SILICATES<br />
2. Nontronite in kaolinized dacites of Bratunac<br />
Trubelja (1971a, 1972) was able to identify small amounts of nonotronite in the<br />
dacites from Bratunac (Srebrenica area). The nontronite is almost completely altered<br />
into kaolinite.<br />
SAPONITE<br />
(Mg 3-2.25<br />
Fe 0-0.75<br />
) Σ3<br />
[(OH) 2<br />
│Al 0.33<br />
Si 3.67<br />
O 10<br />
] -0.33 (Ca,Na) 0.33<br />
x nH 2<br />
O<br />
Saponite also belongs to the montmorillonite group of clay minerals. In<br />
Bosnia and Hercegovina saponite was found on one location only – in the troctolite<br />
from Jovača creek on Mt. Kozara (Golub 1961). Here it occurs as a product of the<br />
alteration of olivine, occasionally replacing complete olivine grains as observed in<br />
thin section. It is present in the form of yellowish-brown to greenish-brown fibrous<br />
aggregates, optically uniaxial and negative.<br />
VERMICULITE<br />
Mg 2.36<br />
Fe 3+ 0.48 Al 0.16 [(OH) 2 │Al 1.28 Si 2.72 O 10 ]-0.64 Mg 0.32<br />
x nH 2<br />
O<br />
X-ray data: d 13.6 (100) 2.82 (40) 1.52 (40)<br />
A u t h o r s: Barić (1966a), Jakšić, Vuletić and Vrlec (1971)<br />
Jakšić et al. (1971) identified vermiculite in the clay from the soil overlying<br />
the serpentine-peridotite rocks at Mt. Ozren, Svatovac locality. Vermiculite was<br />
identified by X-ray diffraction.<br />
Barić (1966a) determined by microscopic methods vermiculite in tuffs from<br />
the Livno area. The mineral is colourless and a product of biotite alteration.<br />
CHLORITE GROUP<br />
SUDOITE Al 2<br />
[AlSi 3<br />
O 10<br />
] (OH) 2<br />
x Mg 2<br />
Al(OH) 6<br />
PENNINE (Mg,Al) 3<br />
[Al 0.5-0.9<br />
Si 3.1-3.5<br />
O 10<br />
] (OH) 2<br />
x Mg 3<br />
(OH) 6<br />
CLINOCHLORE (Mg,Al) 3<br />
[AlSi 3<br />
O 10<br />
] (OH) 2<br />
x Mg 3<br />
(OH) 6<br />
SHERIDANITE (Mg,Al) 3<br />
[Al 1.2-1.5<br />
Si 2.5-2.8<br />
O 10<br />
] (OH) 2<br />
x Mg 3<br />
(OH) 6<br />
RHIPIDOLITE (Mg,Fe,Al) 3<br />
[Al 1.2-1.5<br />
Si 2.5-2.8<br />
O 10<br />
] (OH) 2<br />
x Mg 3<br />
(OH) 6<br />
CORUNDOPHYLLITE (Mg,Fe,Al) 3<br />
[Al 1.5-2.0<br />
Si 2.0-2.5<br />
O 10<br />
] (OH) 2<br />
x Mg 3<br />
(OH) 6<br />
DAPHNITE (Fe 2+ ,Al) 3<br />
[Al 1.2-1.5<br />
Si 2.5-2.8<br />
O 10<br />
] (OH) 2<br />
x Fe 3<br />
(OH) 6<br />
KAEMMERERITE (Fe 2+ ,Fe 3+ ) 3<br />
[AlSi 3<br />
O 10<br />
] (OH) 2<br />
x (Fe,Mg) 3<br />
(O,OH) 6<br />
206
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The term chlorite encompasses a group of minerals with many types of Mg-<br />
Al-Fe phyllosilicates. The chemistry of chlorites is very complex. The abovenamed<br />
chlorites are all mentioned in the text which follows, and the formulae have been<br />
written according to Strunz (1966). According to this author, sheridanite is almost<br />
identical to grohauite, rhipidolite to prochlorite, and daphnite to bawalite. The<br />
layered structure of chlorites closeley resembles that of the mica group of minerals.<br />
Properties: chlorites are monoclinic (prismatic class). The platelike crystals have<br />
a pseudohexagonal habit. Cleavage is excellent along the base{001}. The plates<br />
can be bent but are not elastic. The most common type of occurence is as flaky<br />
aggregates. Rocks carrying chlorite minerals have a pearly lustre on their surface.<br />
The chlorites are green in colour, with different hues. The hardness is low. They<br />
are mostly products of hydrothermal alteration of Mg-Fe minerals in igneous rocks.<br />
They occur also as chloritic schists and in sedimentary rocks, in association with<br />
clay minerals.<br />
X-ray data of some chlorites:<br />
Sudoite d 14.2 (100) 4.40 (70) 4.78 (60) 2.32 (50) 2.55 (4) 1.493 (10)<br />
Pennine d 7.18 (100) 4.79 (100) 3.59 (100) 14.3 (60) 2.87 (60) 1.539 (20)<br />
Clinochlore d 7.12 (100) 3.548 (80) 3.56 (80) 14.3 (70) 4.63 (70) 1.535 (80)<br />
Rhipidolite d 7.07 (89) 3.535 (89) 14.4 (54) 4.714 (43) 2.828 (22) 1.5447 (6)<br />
IR-spectrum:<br />
Pennine 417 445 460 525 660 755 820 960 990 1050 1080 3430 3590 cm -1<br />
Clinochlore 415 445 460 525 655 820 960 1002 1058 1085 1635 3460<br />
3620 cm -1<br />
Rhipidolite 425 460 550 655 760 820 990 1640 3425 3560 cm -1<br />
Chamosite 430 462 540 618 670 990 1080 3410 3550 cm -1<br />
Minerals of the chlorite group are very common in rocks in Bosnia and<br />
Hercegovina. Although the number of available literature references is substantial,<br />
the minerals have not been investigated in detail. Most authors deal with the chlorites<br />
as a group, and investigations of specific chlorites are lacking.<br />
A u t h o r s: Atanacković, Mudrenović and Gaković (1968), Barić (1970a),<br />
Behlilović and Pamić (1973), Burić and Vujnović (1970), Buzaljko (1971), Cissarz<br />
(1956), Ćatović, Trubelja and Sijarić (1976), Čelebić (1963, 1967), Čutura (1918),<br />
Džepina (1970), Đorđević (1969a), Đorđević and Mojičević (1972), Đorđević and<br />
D.Stojanović (1972), Đorđević and V. Stojanović (1964), Đorđević, Buzaljko and<br />
Mijatović (1968), Đurić (1958, 1963a, 1968), Foullon (1893), Gaković and Gaković<br />
(1973), Golub (1961), Grafenauer (1975), Hauer (1879), Ilić (1953), Jakšić, Vuletić<br />
and Vrlec (1971), Jeremić (1961), John (1879), R. Jovanović (1957), Jurković (1954,<br />
1954a, 1957, 1959, 1962), Karamata (1953, 1957), Karamata and Pamić (1960,<br />
207
SILICATES<br />
1964), Katzer (1910, 1924, 1926), Kišpatić (1897, 1900, 1904, 1904a, 1904b,<br />
1917), Koch (1908), Kubat (1964, 1969), Magdalenić and Šćavničar (1973), Majer<br />
(1961, 1962, 1963), Majer and Jurković (1957, 1958), Majer and Pamić (1974),<br />
Marić (1927), Marić and Crnković (1961), Milenković (1966), Mojsisovics, Tietze<br />
and Bittner (1880), Nöth (1956), Olujić, Vuletić and Pamić (1971), Pamić (1957,<br />
1960, 1960a, 1961a, 1961b, 1962, 1963, 1969, 1969a, 1970, 1970a, 1971, 1972a,<br />
1972c, 1972d, 1974), Pamić and Buzaljko (1966), Pamić and Kapeler (1969, 1970),<br />
Pamić and Maksimović (1968), Pamić and Olujić (1974), Pamić and Papeš (1969),<br />
Pamić and Trubelja (1962), Petković (1962/62), Podubsky (1968, 1970), Podubsky<br />
and Pamić (1969), Popović (1930), Ramović (1957, 1962, 1963), Ristić, Likić and<br />
Stanišić (1968), Ristić, Pamić, Mudrinić and Likić (1967), Sijarić (1975), Sijarić and<br />
Šćavničar (1972), Sijarić and Trubelja (1974, 1974a), Sijarić,Trubelja and Šćavničar<br />
(1976), Sijerčić (1972, 1972a), V. Simić (1956), M. Simić (1966, 1968), Šćavničar<br />
and Jović (1962), Šćavničar and Trubelja (1969), Šibenik-Studen (1972/73), Šibenik-<br />
Studen and Trubelja (1967, 1971), Šinkovec and Babić (1973), Tajder (1953), Tajder<br />
and Raffaelli (1967), Trubelja (1957, 1960, 1961, 1962a, 1963, 1963b, 1963c, 1966a,<br />
1969, 1970, 1971a, 1972, 1972a, 1972/73), Trubelja and Miladinović (1969), Trubelja<br />
and Pamić (1956, 1957, 1965), Trubelja and Paškvalin (1962), Trubelja and Sijarić<br />
(1970), Trubelja and Slišković (1967), Trubelja and Šibenik-Studen (1965), Tućan<br />
(1928), Varićak (1955, 1956, 1957, 1966, 1971), Vasiljević (1969), Veljković (1971).<br />
Chlorites occur in Bosnia and Hercegovina in a variety of rocks in the<br />
serpentine zone and products of mid-Triassic and Tertiary-age magmatic events. In<br />
the case of igneous rocks, the chlorite is formed by alteration processes of pyroxenes<br />
and other ferromagnesian minerals. Basic igneous rocks (gabbros) of the Bosnian<br />
serpentine zone (BSZ), which have been subjected to hydrothermal alteration<br />
processes, contain chlorites in monomineralic veins. Chlorite forms foliated<br />
aggregates within veins in rocks associated with corundum-bearing amphibolites.<br />
Paleozoic-age rocks of northwestern, central and eastern Bosnia – sediments<br />
and schists of a low level of metamorphism, all contain chlorites as essential constituents.<br />
Chlorite bearing rocks are quite common at Mt. Prosara and Mt. Motajica.<br />
Chlorite platelets occur in various clastic sediments and in bauxites. Chlorite<br />
formed by hydrothermal processes occur also in association with ore formations in<br />
central Bosnia (schist mountains, Srebrenica area etc.).<br />
208<br />
1. Chlorite in rocks of the Bosnian serpentine zone (BSZ)<br />
The earliest investigations on chlorites in Bosnia and Hercegovina were<br />
done by Hauer, John and Kišpatić. Hauer (1879) and John (1879) mention chlorite<br />
in the diabase structure of the Doboj fortress, and in these rock outcropping between<br />
Maglaj and Žepče. The monograph by Mojsisovics et al. (1880) mentions John’s
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
microscopic determinations of chlorite in various rocks – diabase from Mt. Majevica,<br />
diorite from Kladanj, diabase from Žepče. The biotite-bearing diabases from Žepče<br />
(Mt. Lupoglav) contain chlorite in the form of flakes and leaves. It is a product of the<br />
alteration of biotite, elicts of which are still present in the rock.<br />
Kišpatić (1897, 1900) determined chlorite in different rocks – in the granite<br />
from Mt. Maglaj, in diabases, melaphyres, gabbros, amphibolites and garnetbearing<br />
phyllites from various locations. In all cases the chlorite is of secondary<br />
origin, formed by alteration processes of biotite, augite and garnet. Chlorite is most<br />
abundant in the garnet-bearing phyllites from Čamlija, next to quartz. In thin section<br />
this chlorite is green in colour, distinctly pleochroic.<br />
Chlorites in rocks of the BSZ is mentioned in more recent investigations.<br />
Pamić and Kapeler (1970) note the occurence of chlorite minerals in the serpoentinites<br />
of the Krivaja – Konjuh complex. At Donje Vijake, close to the contact zone between<br />
serpentinites and corundum-bearing amphibolites, veins carrying silvery-white<br />
chlorite aggregates are quite common. A preliminary chemical analysis indicated<br />
that the chlorite is a Al-Mg chlorite with ca. 5% iron oxide.<br />
Chlorites are accessory constituents of hydrothermally altered rocks (talc<br />
– listvenites) outcropping on the northern reaches of the Mt. Ozren serpentiniteperidotite<br />
complex. Prochlorite and corundophyllite were identified by Pamić and<br />
Olujić (1974).<br />
Golub (1961) identified micaceous aggregates of chlorite within plagioclase<br />
crystals hosted in the andesitic basalts from Brnjačin Jarak at Mt. Kozara. The<br />
chlorite also occurs in the matrix of the rock and within amygdales filled with calcite.<br />
The chlorite is optically uniaxial and negative. Pleochroic colours are green and blue<br />
green. Interference colours are grayish to lavender. The author maintains that the<br />
chlorite in this rock is of primary origin.<br />
Trubelja (1957, 1960, 1963c) found chlorite to be a fairly common constituent<br />
of igneous rocks in the Višegrad area. The paper published in 1960 provides the most<br />
data on chlorite. Occurences in feldspar-bearing peridotites from Bosanska Jagodina,<br />
uralite gabbros from the village of Smrijeća, gabbros from Pijavica, diabases from<br />
Banja Potok and dolerites from the Rzav river valley are described. These rocks<br />
carry only minor amounts of chlorite. Interference colours are bluish.<br />
More chlorite is found in the gabbro-pegmatites and hydrothermally altered<br />
veins within basic igneous rocks. In the gabbro-pegmatites chlorite has formed as a<br />
product of diallage alteration during the hydrothermal phase. At Višegradska Banja,<br />
whole grains of diallage have been transformed into a fibrous aggregate of chlorite,<br />
209
SILICATES<br />
which is isotropic in thin section. Lavender interference colours are indicative for<br />
chlorite. Close to the village of Lahci above Višegradska Banja, chlorite occurs in<br />
veins within the gabbro host rock. The chlorite sheets are up to 0.5 x 1.0 cm in<br />
size with good cleavage along (001). The colour is grayish to silvery white. In thin<br />
section, irregular extinction is commonly observed. The 2V angles were measured in<br />
convergent light: +2V = 73.3° to 65.3°. There is a low r
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The spilites from Jablanica and Prozor carry chlorite sometimes as an<br />
essential constituent. In thin section it is of a grass green colour, without pleochroism,<br />
and apparantly isotropic. In some sections chlorite has a yellowish colour and<br />
weak pleochroism. Interference colours are yellowish, and the 2V angle lies in the<br />
range +28° to +34° (prochlorite). In spilite-type rocks, chlorite is often embedded<br />
in phenocrystals of low-temperature albite, together with other secondary minerals<br />
like prehnite, calcite and sericite. This asociation indicates that chlorite cannot be<br />
regarded as a primary mineral of a late magmatic phase. The keratophyres in the<br />
valleys of the Rama and Doljanka rivers contain prominent amounts of chlorite, in<br />
the form of irregular flakes (Pamić 1961b). The chlorite sometimes has an elongated<br />
habit, inferring possible formation through alteration of primary amphibole. Here it<br />
has a green colour, pleochroic colours are yellow green to green. The 2V angle is in<br />
the range +64° to 74°, indicating clinochlore composition. Some of these chlorites<br />
show no pleochroic colours and are seemingly isotropic under crossed nicols. It<br />
should be noted that the presence of more than one variety of chlorite has bot been<br />
observed in keratophyres.<br />
The clinochlore in keratophyres from Lušac creek near Gračac probably<br />
formed from pyroxene, whose relicts are still present in the rock matrix. Pamić<br />
(1961b) investigated the quartz-bearing keratophyres from Mt. Lovin near Gračac<br />
where the chlorite (pennine) has a -2V angle in the range 26° to 36°, and a weak<br />
pleochroism (X = greenish, Y = Z = yellow green). Similar rocks from Mt. Krstac<br />
(village of Lug) contain chlorite as an essential constituent. The flakes are rather<br />
elongated and indicate formation through amphibole alteration.<br />
Marić (1927) investigated microscopically the chlorite from the veins in<br />
the gabbro rocks at Jablanica (Bukov Pod). The association comprises chlorite,<br />
green hornblende, feldspar and quartz. It occurs as fragile aggregates consisting of<br />
subhedral platelets which disintegrate easily. In thin section no pleochroic colurs<br />
were observed, the birefringence being weak. Pyroxene alteration into chlorite has<br />
been observed in some instances (in the central part of the gabbro complex). This<br />
chlorite has a higher birefringence and occurs in the form of fibrous aggregates, with<br />
green-blue pleochroism. The interference colours (blueish) seem to be characteristic<br />
for pennine.<br />
Cissarz (1956), Čelebić (1963, 1967) and Nöth (1956) investigated the<br />
magnetite deposit at Tovarnica where chlorite is prominent in the paragenesis of the<br />
contact zone. Here it is a product of garnet and biotite alteration.<br />
The albitic diabases near the village of Lug, south of Prozor, are altered by<br />
contact metamorphism and contain substantial amounts of chlorite in the form of<br />
coarser aggregates. In thin section the green-yellow chlorite shows no pleochroism,<br />
and has a -2V angle of 14-34°. It is probably pennine.<br />
211
SILICATES<br />
Occurences of chlorite in various rocks associated with mid-Triassic-age<br />
magmatic events have been described also by the following authors: Behlilović<br />
and Pamić (1963) – in the tuffs of Drežanka; Čuture (1918) – in igneous rocks of<br />
SW Bosnia; Jeremić (1961) – Triassic-age deposits of barite; Jurković (1954a) –<br />
the andesites from Orašin; Karamata (1953) – in melaphyres from Vareš; Karamata<br />
(1957) – in keratophyres from Zvornik; Katzer (1910) – in siderites from Vareš;<br />
Majer and Jurković (1957, 1958) – in gabbrodiorites from Bijela Gromila near<br />
Travnik; Mojsisovics et al. (1880) – in igneous rocks from Jajce and Donji Vakuf,<br />
according to determinations by John (1879); Pamić (1957, 1960, 1960a) - in spiliteand<br />
keratophyre-type rocks from Ilidža and Kalinovik; Pamić (1963) – in igneous<br />
rocks from Čevljanovići; Pamić and Buzaljko (1966) – keratophyres and similar<br />
rocks from Čajniče; Pamić and Maksimović (1968) – in quartz-albite diabases<br />
from Bijela-Konjic; Petković (1961/62) – in igneous rocks from Borovica-Vareš;<br />
M. Simić (1966) – basic effusive rocks from Mt. Bjelašnica; Šibenik-Studen and<br />
Trubelja (1967) – igneous rocks in the Vrbas river valley; Trubelja (1962a, 1963)<br />
– keratophyres and quartz-keratophyres from Čajniče; Trubelja (1969, 1972a) –<br />
in spilites from Borovica-Vareš; Trubelja and Miladinović (1967), Trubelja and<br />
Slišković (1967) – in igneous rocks from Tjentište and Sutjeska river; Trubelja and<br />
Šibenik-Studen (1965) – in granites and similar rocks from Komar and the Vrbas<br />
valley); Veljković (1971) – in the barite deposit at Veovača –Vareš.<br />
Very limited data on chlorite in products of Tertiary-age magmatic events<br />
is provided by following authors: Kišpatić (1904, 1904a), Ramović (1957, 1962,<br />
1963), Tajder (1953), Trubelja (1971a, 1972), Trubelja and Pamić (1956) and<br />
Trubelja and Paškvalin (1962). These authors mention occurences of chlorite in<br />
dacites, andesite dacites and kaolinized dacites outcropping in the Bosna river<br />
valley and around Srebrenica.<br />
212<br />
3. Chlorite in Paleozoic-age rocks<br />
Chlorite is a prominent mineral in various rocks of Paleozoic age, throughout<br />
Bosnia and Hercegovina. However, litearture data is very limited. Chlorite is often<br />
mentioned by Katzer (1924, 1926) and Varićak (1956, 1957 and 1966). Contributions<br />
to the knowledge about chlorite were provided by the following: Barić (1970a), Ilić<br />
(1953), Kišpatić (1904b), Koch (1908), Marić and Crnković (1961), Podubsky (1968,<br />
1970), Podubsky and Pamić (1969), Simić (1956), Šćavničar and Trubelja (1969),<br />
Tajder and Raffaelli (1967), Trubelja and Sijarić (1970). Some investigations by the<br />
above named authors included chemical and thermal analysis and determinations by<br />
x-ray diffraction.<br />
Koch (1908) investigated the rocks at Mt. Motajica where chlorite occurs in<br />
biotite-bearing granites and gneisses from Židovski Potok, the garnet-biotite gneiss<br />
from Studena Voda and Kobaš, biotite gneiss from Hercegov Dol near Bosanski
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Svinjar, biotite schists from Puljana Kosa and Studena Voda, micaschists from<br />
Kamen Potok near Kobaš and Šeferovac, andalusite schists from Resavac creek near<br />
Svinjar. All these rock contain minor amounts of chlorite which is a product of biotite<br />
and garnet alteration. Koch’s data on chlorite from Mt. Motajica can also be found<br />
in Katzer’s monograph on the Geology of Bosnia and Hercegovina (1924, 1926).<br />
Varićak (1966) made detailed microscopic investigations of various<br />
sedimentary, igneous and metamorphic rocks from Mt. Motajica, but provides little<br />
information about chlorite. Substantial amounts of chlorite (up to one third of the<br />
rock mass) are contained in the chlorite-epidote schists of the Osovica river. At Mt.<br />
Prosara Varićak (1956, 1957) determined chlorite in quartz-porphyres and various<br />
schists (gneiss, micaschists, green rocks). In quartz-porphyres chlorite is a product<br />
of biotite alteration.<br />
Katzer (1924, 1926) mentions occurences of chlorite in various rocks from the<br />
schists mountins of central Bosnia – in phyllites, argillaceous shales, carbonaceous<br />
phyllites, conglomerates (with chloriteschist pebbles), sandstones, quartzporphyres,<br />
diabases. According to Katzer, chlorite causes the green colour of some of these<br />
rocks. No further details are provided.<br />
Barić (1970a) determined chlorite in the keratophyres from Trešanica, near<br />
Bradina in Hercegovina. The chlorite is a product of alteration of hornblende or<br />
pyroxene. In thin section, this chlorite shows weak pleochroism (yellow and green),<br />
weak birefringence and brownish-violet interference colours (in section 0.03-0.04 mm<br />
thick). It is optically uniaxial and positive.<br />
Tajder and Raffaelli (1967) determined chlorite in altered porphyres and<br />
keratophyres in central Bosnia. In some cases, chlorite is an essential constituent of<br />
these rocks. Metamorphic rocks with chlorite belong to the low-temperature sector<br />
of the greenschist facies. The orthoschists from the Neretvica creek have chlorite<br />
aggregating in veins within the rock. It is green in colour, shows distinct pleochroism<br />
and anomalous interference colours (indigo). It is probably pennine. The schist from<br />
Željeznica creek, Neretvica creek and river Vrbas contains a substantial amount of<br />
chlorite formed from hornblende or biotite. It is green in colour (also pleochroic<br />
colours). Interference colours are anomalous (brown). It is probably prochlorite.<br />
Chlorite also occurs in paraschists, which are common in the area of central<br />
Bosnian schist mountains. In most cases it is prochlorite. Trubelja and Sijarić (1970)<br />
investigated in some detail the chlorite from biotite-chlorite-ankerite schists and<br />
albite-chlorite schists from Ivanovica creek near Busovača. Chemical and thermal<br />
analyses, as well as x-ray diffraction were done. In thin section the chlorite shows<br />
distinct pleochroic colours in various hues of green. Powder diffraction data indicate<br />
that the chlorite is prochlorite.<br />
213
SILICATES<br />
The talc-serpentine-chlorite vein in the phyllites from Kupres contains<br />
chlorite deposited directly on the surface of the rock. Chlorite was determined by<br />
microscopy, powder diffraction and chemical and thermal analysis. Diffraction<br />
data were compared with literature (Brown 1961) and indicated that the material<br />
investigated had an ordered structure but the three diffraction signals could not be<br />
assigned to chlorite (table 45, lines 7, 8 and 14). However, the relative intensities of<br />
the postivie and negative index would indicate a chlorite with orthochlorite structure<br />
(Schoen 1962; Petruk 1964).<br />
The powder diffraction pattern of the chlorite from Kupres had very sharp<br />
diffraction lines so that the dimension of the unit cell could be calculated:<br />
a 0<br />
= 5.327±0.005 Å; b 0<br />
= 9.236 ± 0.005 Å; c 0<br />
= 14.39 ± 0.01 Å; β = 97.2° ± 0.2°<br />
Table 44. X-ray diffraction data for chlorite (Ivanovica creek, Busovača)<br />
214<br />
d Å I d Å I<br />
14.329 Medium 2.403 Medium<br />
7.140 Very very strong 2.337 Just visible<br />
4.750 Medium 2.284 Medium<br />
4.040 Medium 2.206 Just visible<br />
3.910 Just visible 2.127 Just visible<br />
3.785 Just visible 2.086 Just visible<br />
3.677 Medium 2.016 Medium<br />
3.558 Very very strong 1.909 Medium<br />
3.386 Just visible 1.837 Medium<br />
3.215 Very strong 1.763 Just visible<br />
2.966 Very weak 1.733 weak<br />
2.803 Weak 1.680 Just visible<br />
2.761 Weak 1.627 Medium<br />
2.648 Just visible 1.565 Medium<br />
2.615 Medium 1.518 Medium<br />
2.565 Medium 1.474 Just visible<br />
2.472 Medium 1.422 Just visible<br />
1.400 Medium<br />
The chemical analysis of chlorite yielded following results:<br />
SiO 2<br />
= 31.19; TiO 2<br />
= 0.86; Al 2<br />
O 3<br />
= 12.36; Fe 2<br />
O 3<br />
= 4.30; FeO = 3.37;<br />
MnO = 0.07; MgO = 32.63; CaO = 1.94; Na 2<br />
O =0.48; K 2<br />
O = 0.38; H 2<br />
O + = 11.92;<br />
H 2<br />
O - = 0.41; P 2<br />
O 5<br />
= 0.03; Total = 99.94<br />
The structural formula of this chlorite is:<br />
(Ca 0.204<br />
Na 0.091<br />
K 0.048<br />
)(Mg 4.775<br />
Fe 2+ 0.277 Fe3+ 0.244 Al 0.495 Mn 0.006 Ti 0.063 )(Si 3.064 Al 0.936 )<br />
O 10.195<br />
(OH) 7.805<br />
The analyzed chlorite sample is a clinochlore. The zonar and concentric<br />
texture of the mineral association within the vein in the phyllite rock indicates that
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
the deposition of material occured in several phases of hydrothermal activity. Each<br />
of these phases resulted in the crystallization of a mostly monomineralic product,<br />
depending on the composition and temperature of hydrothermal solutions – chlorite<br />
was the first mineral to crystallize, before a finegrained and finally a coarsegrained<br />
variety of talc.<br />
Table 45. Powder diffraction data for chlorite from Kupres<br />
No. hkl d Å I No. hkl d Å I<br />
1 001 14.301 6 28 1.3034 1.5<br />
2 002 7.138 10 29 1.2923 3<br />
3 003 4.763 7.5 30 1.2777 0.5<br />
4 020 4.585 4.5 31 1.2265 2<br />
5 004 3.567 8.5 32 0, 0, 12 1.1935 1.5<br />
6 005 2.856 3 33 1.1807 0.5<br />
7 2.722 0.5 34 1.0969 1.5<br />
8 2.647 0.5 35 1.0468 1.5<br />
9 131 202 2.585 5 36 1.0369 1.5<br />
10 132 201 2.540 9 37 1.0025 1.5<br />
11 132 203 2.440 8 38 0.9921 2<br />
12 133 202 2.382 4 39 0.9811 1<br />
13 133 204 2.262 4 40 0.9569 1.5<br />
14 2.200 0.5 41 0.8952 2<br />
15 134 205 2.070 1 42 0.8884 2<br />
16 135 204 2.0085 7 43 0.8602 2b<br />
17 135 206 1.8886 3 44 0.8526 1<br />
18 136 205 1.8282 3<br />
19 136 207 1.725 1d<br />
20 137 206 1.6684 1.5<br />
21 137 208 1.5718 4<br />
22 060 331 1.5390 8<br />
23 062 331 333 1.5024 3.5<br />
24 063 332 334 1.4642 1.5<br />
25 139 208 1.4017 4b<br />
26 065 1.3531 1<br />
27 400 139 401 1.3214 3<br />
b = broad line<br />
d = diffuse line<br />
visual intensity estimate<br />
Kišpatić (1904b) described several schist-type rocks which contained<br />
chlorite as essential or accessory components. The green schists from Polom and<br />
Lonjina on the Drina river contain substantial amounts of chlorite. In the schist from<br />
Polom, chlorite completely displaces its precursor mineral – amphibole. The schist<br />
from Lonjina contains only a minor amount of chlorite which has green and pale<br />
yellow pleochroic colours. The chlorite schists from Vilenica near Travnik contain<br />
susbtantial amounts of feldspar and chlorite. Chlorite has a pale green colour,<br />
pleochroism and birefringence are weak. It was formed probably by alteration of<br />
amphibole. Kišpatić determined chlorite microscopically in chlorite-bearing phyllites<br />
215
SILICATES<br />
and schists from Fojnica, Čemernica, Kiseljak and Kreševo, and in the porphyrric<br />
diabases from Sinjakovo.<br />
In a more recent investigation of the lithostratigraphy of Paleozoic-age rocks<br />
in NW Bosnia, Podubsky (1968) determined several lithologic horizons containing<br />
chlorite minerals as essential constituents. Such is the case of the early Paleozoicage<br />
argillaceous schists which are green in colour from the chlorite. Chlorite is also<br />
a prominent mineral in metasandstones, and similar rocks outcropping in the Sana<br />
river valley (Marić and Crnković 1961).<br />
Likewise, chlorite is usually present in altered basic and neutral igneous<br />
rocks from the Ljubija area (Podubsky 1968, Podubsky and Pamić 1969), also in the<br />
Paleozoic-age rocks of eastern Bosnia (Podubsky 1970). In cases when the amount<br />
of chlorite is substantial, then this id reflected in the name of the rock i.e. chlorite<br />
schists, sericite-chlorite schists etc.).<br />
Paleozoic-age rocks, and the chlorites in them have not been up to now<br />
investigated in any great detail. In the schist mountains of central Bosnia, chlorite<br />
is often associated with various ore parageneses (Jurković 1954, 1956, 1962; Simić<br />
1956). Most of the information on these chlorites is in the PhD thesis of I. Jurković,<br />
published in 1956. Accoriding to Jurković, chlorite is a meso-epithermal mineral in<br />
the ore bodies at Busovača, Šćitovo, Brestovsko, Travnik, Berberuša, Travnik etc.<br />
Chlorite commonly occurs in the quartz veins and metamorphic magnetite<br />
deposits at Zagrlski potok near Busovača. The chlorite occuring in quartz veins is<br />
green in colour, like the one from the magnetite deposit. Simić (1956) identified also<br />
a chrome-bearing variety of chlorite.<br />
216<br />
4. Chlorite in other rocks<br />
Chlorite has also been identified in carbonates and clastic sediments and<br />
bauxite. Gaković and Gaković (1973) identified chlorite in the insoluble residue of some<br />
carbonate rocks from the outer Dinarides belt. Ilić (1953) found chlorite in weathered<br />
and altered granites from Mt. Motajica. The following authors have also determined<br />
chlorites in various rocks: Magdalenić and Šćavničar (1973) – in sandstones from<br />
Kulen Vakuf; Ristić et al. (1968) – in sands from the Tuzla basin; Sijerčić (1972) – in<br />
the Eocene-age flysch deposits of Mt. Majevica; Simić (1968) – in sediments from<br />
the Sarajevo area; Šćavničar and Jović (1962) – in clastic sediments of the Kreka coal<br />
basin; Varićak (1955) – in the red granite from Mt. Maglaj; Vasiljević (1969) – in<br />
sedimentary quartzites from Podrašnica – Mrkonjić Grad.<br />
Some recent investigations and determinations by powder diffraction showed<br />
that chlorites are fairly common constituents of bauxites – Ćatović et al. (1976),
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Sijarić (1975), Sijarić and Trubelja (1974, 1974a), Sijarić et al. (1976), Šćavničar et<br />
al. (1968), Šinkovec and Babić (1973), Trubelja (1970). Sijarić (1975) and Sijarić et<br />
al. (1976) determined chlorite in bauxite from Mt. Grmeč in NW Bosnia and found<br />
the chlorite to be the Al-bearing sudoite. Material from the following localities was<br />
determined – Borik, Vranjsko, Mijačica, Oštrelj, Grič, Kravljak and Karanovići. The<br />
sudoite content in the sample from Grič is 15.5% and 17.4%, while the Kravljak<br />
sample contains 12.0% of sudoite. Samples from Drljače, Guskarica and Leovača<br />
also contain some Fe-chlorite.<br />
Šinkovec and Babić (1973) also determined chlorite in the bauxite from<br />
the Oštrelj deposit. The three analyzed samples contained 5.59, 3.79 and 6.53%<br />
chlorite which is largely cryptocrystalline. Some chlorite flakes up to 10 μm in<br />
length were identified.<br />
Ćatović et al. (1976), Sijarić and Trubelja (1974, 1974a) identified chlorite<br />
in the bauxite from Mt. Srnetica near Ključ – the chlorite is daphnite (bawalite)<br />
and sudoite. The bauxite samples from Studnac contained between 6.0 and 13.3%<br />
sudoite. Samples from Jezerine, Pijetlov Vrh, Kladovača, Ravni Lom and Studenac<br />
also contain ca. 1-3% of the Fe-bearing chlorite daphnite (bawalite). The bauxite<br />
from Ravni Lom contains up to 7.6% daphnite.<br />
Trubelja (1970) determined chlorite in the disapore-type bauxite and bauxite<br />
clays from Ljuša near donji Vakuf. The boehmite-gibbsite bauxite from Korenduša –<br />
Vinjani (near Posušje) contains small amounts of chlorite (chamosite).<br />
Grafenauer (1975) identified kaemmererite in the chromium ore (chromite) at<br />
Krivaja near Duboštica. It occurs in small veins or associated with the ore. It probably<br />
formed as a result of the interaction of hydrothermal fluids and the chromite ore.<br />
KAOLINITE<br />
Al 4<br />
[Si 4<br />
O 10<br />
] (OH) 8<br />
Crystal system and class: Triclinic, pinacoidal class.<br />
Lattice ratio: a : b : c = 0.576 : 1 : 0.830<br />
α = 91° 48’ β = 95° 30’ γ = 90°<br />
Cell parameters: a o<br />
= 5.14, b o<br />
= 8.93, c o<br />
= 7.37 Z = 1<br />
Properties: kaolinite usually occurs in the form of earthy aggregates, less often<br />
as pseudohexagonal crystals visible with the aid of a microscope. Cleavage along<br />
{001} is good, but usually not macroscopically visible due to the small size of the<br />
crystals. Hardness is 2, the specific gravity = 2.6. Colour and streak are white. Lustre<br />
can be pearly but is usually earthy.<br />
217
SILICATES<br />
X-ray data: d 7.13 (100) 3.566 (66) 4.36 (50) 4.158 (46) 3.839 (33) 1.487 (11)<br />
IR-spectrum: 435 475 542 700 760 800 918 940 101 1038 1108 1640<br />
3460 3620 3660 3672 3702 cm -1<br />
A u t h o r s: Bišćević-Muštović, Trubelja and Sijarić (1976, 1976a), Burić and<br />
Vujnović (1970), Ćatović and Trubelja (1976), Ćatović, Trubelja and Sijarić (1976),<br />
Čičić (1975), Dangić (1971), Đorđević and Mijatović (1966), Ilić (1953), Jakšić,<br />
Glavaš and Trubelja (1967), Jeremić (1960, 1963, 1963a), Jurković and Sakač (1964),<br />
Karšulin, Tomić and Lahodny (1949), Katzer (1924, 1926), Maksimović and Crnković<br />
(1968), Mudrinić and Janjić (1969), Mudrinić and Tadić (1969), Pavlović (1889),<br />
Pavlović, Ristić and Likić (1970), Podubsky (1955, 1970), Ramović (1957a), Ristić,<br />
Likić and Stanišić (1968), Sakač (1969), Sijarić (1975), Sijarić and Trubelja (1974,<br />
1974a), Sijarić,Trubelja and Šćavničar (1976), Stangačilović (1956, 1969, 1970),<br />
Šćavničar, Trubelja and Sijarić (1968), Šibenik-Studen and Trubelja (1967), Šinkovec<br />
and Babić (1973), Tajder (1953), Trubelja (1962a, 1963, 1970, 1971, 1971a, 1972,<br />
1973, 1973a), Trubelja and Pamić (1956, 1965), Trubelja and Sijarić (1976), Trubelja<br />
and Vasiljević (1968, 1971b), Varićak (1956, 1966), Walter (1887), Weisse (1948).<br />
Kaolinite is the most common and best known clay mineral, and a typical<br />
representative of te group. In Bosnia and Hercegovina kaolinite has not been<br />
investigated in great detail and literature data is scarce.<br />
There are two types of kalinite deposits in Bosnia and Hercegovina. The<br />
first are the ‘in situ’ kaolinite deposits, where the mineral is in its primary location<br />
of origin. Some authors refer in this case to ‘primary kaolinite’ and autochtonous<br />
deposits. The other group of deposits are the reworked or allochtonous deposits.<br />
The kaolinite deposits at Mt. Motajica belong to the first group. Here<br />
kaolinite formed as an alteration product of various granitic and other rocks. The<br />
kaolinite from Srebrenica (Bratunac) formed on dacites.<br />
Allochtonous kaolinite deposits comprise argillaceous sediments where<br />
kaolinite occurs either alone or with other clay minerals (illite, montmorillonite).<br />
Such deposits are found in the basins of Prijedor and Sarajevo – Zenica.<br />
Kaolinite is a typical secondary mineral, formed as an alteration product<br />
of potassium feldspars and plagioclase. Under surface conditions, the process of<br />
kaolinization can take place only under the influence of atmospheric water (rain)<br />
and/or hydrothermal solutions. Therefore, kaolinite can be expected to occur in<br />
association with rocks containing feldspars. Many occurences of this mineral have<br />
been described in rather general terms, i.e. as ‘kaolinite minerals’. It needs to be<br />
mentioned that kaolinite is ubiquitous in various types of soil.<br />
218
1. Kaolinite at Mt. Motajica<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
In his Geology of Bosnia and Hercegovina, Katzer (1924, 1926) mentioned<br />
the alteration process of the granites at the Mt. Motajica complex. The process has<br />
advanced to subsurface parts of the granite body resulting in the formation of a<br />
sandy material. The surface of the granite body has been transformed into a thick<br />
layer of clayey soil.<br />
After Katzer, very little information was available abou the Mt. Motajica<br />
kaolinite until the paper by Ilić (1953) dealing with kaolinization of the granite<br />
complex in the watershed of the Grebski and Kameni creeks in the area of Bosanski<br />
Kobaš. The samples were analyzed microscopically and by powder diffraction. The<br />
paper contains two powder diffractograms and the results of chemical analysis of<br />
several samples of altered granite. Other minerals present in the rock are albite,<br />
muscovite, quartz and chlorite.<br />
Ilić believes that the alteration processes leading to kaolinite formation are<br />
the result of hydrothermal activity. An additional argument for this conclusion lies<br />
in the fact that the alteration process has advanced to a high degree particularly in<br />
the vicinity of quartz veins (which formed in the course of postmagmatic processes).<br />
Another publication dealing with alteration processes of the granite complex<br />
of Mt. Motajica was published at the same time by by Stangačilović (1956). This<br />
author determined kaolinite in samples from the locality Đidovi, using thermal<br />
analysis and the Debye-Scherrer powder diffraction method. The coarser fraction<br />
of kaolinite (0-15 μm) contained kaolinite, illite and quartz while the finer fraction<br />
(0-5 μm) consisted of almost pure kaolinite. Stangačilović however advanced a<br />
different view concerning the formation of kaolinite at Mt. Motajica, believing that<br />
hydrothermal processes have not caused the alteration of the granite. He maintains<br />
that the alteration of the granite, particularly in the area of Kobaš and Brusnik, took<br />
place during the Tertiary-age transgressions of the sea, since there is evidence for<br />
such a scenario in the area. After the sea-level subsided, further alteration took place<br />
in marshes and lacustrine environments, in areas with appropriate orography. The<br />
activity and infiltration of surface waters was particularly extensive along fissures<br />
which formed around the contact of the quartz veins and the granite host rock. This<br />
is why the alteration process is stronger along the quartz veins.<br />
In addition to kaolinite, illite and quartz, the granite contains also orthoclase,<br />
plagioclase, sericite, biotite, magnetite and zircon.<br />
Varićak (1966) frequently referrs to kaolinization processes of feldspars and<br />
‘clay minerals’ in his petrologic study of the granites and other rocks of Mt. Motajica.<br />
219
SILICATES<br />
2. The kaolinite deposit of Bratunac (Srebrenica)<br />
Tajder (1953) gave the first detailed account of the alteration processes<br />
(kaolinization) of the dacites and andesite-dacites in the area of Srebrenica. However,<br />
his treatment of the mineral kaolinite is only brief.<br />
Most of the igneous rocks around Srebrenica is comparatively fresh, and<br />
alteration processes are present to a limited extent. However, the dacites around<br />
Bratunac are almost completely altered (Trubelja 1970a, 1971a, 1972; Dangić<br />
1971). Occurences of kaolinite and altered dacite are located some 2.5 km SW<br />
from the village of Bratunac, i.e. some 8 km from Srebrenica. Best outcrops are<br />
located at Smoljave and Borići, where exploitation of kaolinite is taking place. Other<br />
occurences around Srebrenica are small-scale occurences.<br />
Trubelja identified the kaolinite and other associate minerals by optical<br />
microscopy, x-ray diffraction and thermal analysis. The DTA curve of the material<br />
consisting of altered dacite shows an endothermic peak at temperatures between 500°<br />
and 600°C characteristic for a complete loss of constitutional water. This effect was<br />
observed also on the TG curve. The kaolinite content of the material was estimated<br />
from the peak area. The kaolinite content is in the range between 28 and 60%, the<br />
average being around 35%.<br />
In addition to kaolinite, sanidine, quartz, biotite, marcasite, pyrite, goethite,<br />
chlorite, sericite and epidote were identified in the altered dacites. Dickite, sepiolite<br />
and nontronite were found in a few samples only.<br />
The altered dacite rocks at Bratunci are significant economically as they are a<br />
source of valuable kaolinite. Data from the field and from the laboratory indicate that<br />
the alteration process of rocks at Smoljve is more intensive than at Borići and elsewhere.<br />
The same is true for the quality of kaolinite as a natural resource. At Borići, the alteration<br />
process also led to the formation of sulfide and silicate mineralizations associated with<br />
hydrothermal waters. Surface weathering leads to the formation of secondary iron<br />
oxides and hydroxides – the cause of the occasional off-colour of kaolinite.<br />
The formation of kaolinite in the case of the Bratunac deposit can be<br />
explained in a comparatively simple way. The platelike magmatic (volcanic)<br />
body was in extensive contact with hydrothermal solutions during post-magmatic<br />
processes (hydrothermal stage). The feldspars contained in the dacite matrix<br />
were almost completely altered into kaolinite. However, alteration led also to the<br />
formation of chlorite, sericite, marcasite, pyrite and epidote. The original texture of<br />
the dacite is maintained to some extent, likewise the presence of sanidine feldspar.<br />
It is interesting to note that no plagioclase feldspars were found in the rock, which<br />
ma be due to their lower stability with respect to sanidine. Consequently, there is no<br />
evidence of plagioclase feldspars in the altered dacite.<br />
220
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The presence of marcasite which is in intimate contact with kaolinite<br />
would imply that the hydrothermal solutions had a low pH and comparatively low<br />
temperature. Marcasite is known to crystallize from acidic hydrothermal solutions at<br />
temperatures below 400°C, while pyrite forms at higher temperatures.<br />
The hydrothermally altered dacite at Bratunac may be classified as a primary<br />
(residual) deposit of kaolinite. Such deposits are rather rare in the world.<br />
3. Kaolinite in bauxite<br />
Kaolinite seems to be regularly associated with bauxites throughout Bosnia<br />
and Hercegovina. The kaolinite content is sometimes so high that the rock is classified<br />
as kaolinite-bearing bauxitic sediment.<br />
Using modern physical and chemical determinative methods, it was<br />
possible to identify kaolinite in several bauxites in Bosnia and Hercegovina – from<br />
Hercegovina, from eastern Bosnia (Vlasenica), from the area of Jajce and Mrkonjić<br />
Grad (Baraći), from Mt. Srnetica and Mt. Grmeč.<br />
Bišćević-Muštović et al. (1976, 1976a) determined kaolinite as an essential<br />
constituent of bauxitic clays from Prozor and Rama lake. In the available literature,<br />
kaolinite is usually described in sections dealing with bauxite, so that more information<br />
can be found in sections describing the minerals hematite, gibbsite, diaspore etc.<br />
Jurković and Sakač (1964), Sakač (1969), Sijarić (1975), Sijarić et al. (1976),<br />
Šinkovec and Babić (1973) and Trubelja note the presence of kaolinite in bauxites<br />
of NW Bosnia. First quantitative data on the kaolinite in bauxite from Oštrelj at<br />
Mt. Grmeč are given in the paper by Šinkovec and Babić (1973). The bauxites they<br />
studied had a kaolinite content between 26.48 and 57.26%. The material from Mt.<br />
Grmeč was also investigated by Sijarić (1975). According to this author, kaolinite was<br />
found in bauxite from the localities Bjelaj, Zec, Grbića Brdo, Karanovići, Leskovac,<br />
Borik, Gradina, Vranjsko, Trovrh, Mašine Doline, Guskarica, Vranovina, Brezove<br />
Poljane, Krnja Jela, Crni Vrh, Oštrelj and Leovača. The Triassic-age bauxite from<br />
Bjelaj has a particularly high kaolinite content. More data on the kaolinite content<br />
of these bauxite are given in the section on boehmite. Generally, a high content of<br />
kaolinite in bauxite makes them less appropriate for alumina production.<br />
Ćatović et al. (1976), Sijarić and Trubelja (1974, 1974a) studied the bauxites<br />
from Mt. Srnetica south of the town of Ključ. The bauxites have been classified<br />
as high-silica bauxite, due to their kaolinite content. The kaolinite contents are as<br />
follows: 21.3-35.6% at Studenac, 28.9% at Jezerine, between 21.3 and 24.8% at<br />
Pijetlov Vrh, Krčevine, Kladovača, Ravni Lom.<br />
221
SILICATES<br />
Trubelja (1971, 1973) found elevated contents of kaolinite also in the<br />
gibbsite-type bauxites from Mrkonjić Grad.<br />
Jakšić et al. (1967), Karšulin et al. (1949), Maksimović (1968), Šćavničar<br />
at al. (1968), Trubelja (1973, 1973a), De Weisse (1948) provide data on kaolinite<br />
in bauxites from Hercegovina. J.G. de Weisse was the first to estimate kaolinite<br />
concentrations in hercegovinian bauxites from Čitluk, Stolac, Domanovići, Zagorje<br />
etc). Maksimović (1968) found that theses bauxites contained between 15 and 32%<br />
kaolinite. Kaolinite is normally found in the lower parts of the deposit. Ćatović<br />
et al. (1976) investigated the kaolinite contents in pyrite-bearing bauxites from<br />
Hercegovina. Jeremić (1960a), Mudrinić and Janjić (1969), Mudrinić and Tadić<br />
(1969) all identified kaolinite in bauxites from Vlasenica in eastern Bosnia, but<br />
information on the content is lacking.<br />
Trubelja and Sijarić (1976) found kaolinite to be an essential constituent of<br />
the recently discovered bauxite at Miljevine (eastern Bosnia).<br />
4. Other occurences of kaolinite<br />
Stangačilović (1969, 1970) found kaolinite to be an essential constituent of<br />
allochtonous illite-type clays in the basins of Prijedor and Sarajevo – Zenica. Kaolinite<br />
contents in these sediments are lower than thos of illite (Pavlović 1975; Tasić 1975).<br />
Jeremić (1963, 1963a) investigated the alteration processes of quartzporphyric<br />
rocks from Mračaj in central Bosnia, associated with hydrothermal occurences of<br />
barite. Quartztrachyte alterations were mentioned by Walther (1887).<br />
Maksimović and Crnković (1968) determined Cr-bearing kaolinite at Slatina<br />
(near Teslić in the BSZ). Results of the quantitative chemical analysis are given in<br />
table 46. The analysis was done by B. Crnković.<br />
Table 46. Quantitative chemical analysis of Cr-kaolinite from Slatina (Teslić)<br />
SiO 2<br />
46.10 Si 4.02<br />
TiO 2<br />
0.56 Al 3.78<br />
Al 2<br />
O 3<br />
36.85 Cr 0.12<br />
Cr 2<br />
O 3<br />
1.72 Ti 0.04<br />
Fe 2<br />
O 3<br />
0.28 Fe 3+ 0-02<br />
MgO 0.48 Mg 0.06<br />
CaO 0.32 Ca 0.02<br />
Na 2<br />
O 0.03 Na --<br />
H 2<br />
O + 13.42 OH 7.80<br />
H 2<br />
O - 0.42<br />
Total 100.18<br />
222
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
According to Maksimović and Crnković (1968), the chromium-bearing<br />
kaolinite formed as a result of hydrothermal alteration of ultrabasic rocks.<br />
A limited amount of information on kaolinite and feldspar alterations can be<br />
found in the following publications: Đorđević and Mijatović (1966) – in oligoclase<br />
veins near Zavidovići; Podubsky (1955) – from Ljeskovica, between Zavidovići<br />
and Žepče; Ristić et al. (1968) – in sediments of the Tuzla basin; Šibenik-Studen<br />
and Trubelja (1967) – in igneous rock from the Vrbas river valley; Trubelja and<br />
Pamić (1956, 1965) – in dacites from Maglaj; Varićak (1956) – in quartzporhyric<br />
rocks from Mt. Prosara. Pavlović et al. (1970) identified kaolinite in the small<br />
fraction of the quartz sand in the Tuzla basin. Kaolinite was determined using<br />
thermal analysis and XRD.<br />
Use: Kaolinite is one of the most common and ubiquitous clay minerals.<br />
It has important industrial applications. The technical term ‘kaoline’ refers to an<br />
impure clay material which contains kaolinite as the dominant mineral. Depending<br />
on the content of impurities, kaoline is used in its natural form or purified by washing<br />
or some other separation and enrichment process. The most important and at the<br />
same time the earliest use of kaoline is in the production of ceramics and porcelain.<br />
Important in this respect are the plastic properties of kaolinite, and its transformation<br />
into a solid and firm material upon heating (ceramics). It is interesting to note the<br />
specific properties of kaolinite at different temperatures:<br />
100-150°C<br />
200-300°C<br />
400-600°C<br />
600-950°C<br />
950-1200°C<br />
1650-1775°C<br />
loss of pore water, including adsorbed water<br />
oxidation of organic impurities<br />
loss of structural OH groups<br />
loss of CO 2<br />
from carbonate-type impurities (carbonate minerals)<br />
formation of cristobalite<br />
melting commences – lower melting temperatures may be attained<br />
due to impurities (iron, alkalies, alkaline earths)<br />
Kaolinite is frequently used as a ‘filling’ material in the manufacture of<br />
paper. Some typers of paper contain as much as 40% kaolinite.<br />
Kaolinite is mined in Bosnia and Hercegovina at Bratunac and at Mt. Motajica<br />
near Bosanski Kobaš. Čičić (1975, p. 41) maintains that the available reserves of<br />
kaolinite at both of these localities are around 16 million tons. The kaolinite from<br />
Bratunac is mainly used in the production of ceramic tiles.<br />
223
SILICATES<br />
DICKITE<br />
Al 2<br />
[Si 2<br />
O 5<br />
] (OH) 4<br />
There is very little information on the occurences of dickite in Bosnia<br />
and Hercegovina. It has been determined by powder x-ray diffraction in altered<br />
(kaolinzed) sanidine dacites near Bratunac and Srebrenica (Trubelja 1971a and<br />
1972). This dickite is of hydrothermal origin.<br />
Pavlović et al. (1976) have identified dickite in the bluish-white matrix of<br />
oolitic bauxites of Vlasenica (localities Palež and Krunići).<br />
224<br />
NACRITE<br />
Al 2<br />
[Si 2<br />
O 5<br />
] (OH) 4<br />
As for dickite, data on the occurence of nacrite in Bosnia and Hercegovina<br />
are very scarce. Mudrinić and Janjić (1969) are the only authors to mention nacrite<br />
in the Vlasenica bauxites in eastern Bosnia, but no further details about this mineral<br />
are given.<br />
CHRYSOCOLLA<br />
(Cu,Al) 2<br />
H 2<br />
[Si 2<br />
O 5<br />
] (OH) 4<br />
x nH 2<br />
O<br />
Chrysocolla is monoclinic with a poorly ordered structure (metacolloidal).<br />
Aluminium and iron (III) can substite copper in the lattice, so different formulae can<br />
be associated with chrysocolla<br />
(Cu 2-x<br />
Al x<br />
) H 2-x [Si 2 O 5 ] (OH) 4 x nH 2 O<br />
Complete Al substitution results in the formation of halloysite or kaolinite.<br />
The name of this mineral dates back to antiquity. It has been used by Teophrastus (ca.<br />
370-285 BC) in his volume Peri Lithon (On stones). The name contains the words<br />
chrysos (gold) and colla (glue) since it was used as a soldering material. It is possible<br />
that malachite was also known under the name of chrysocolla.<br />
Jurković (1958, p. 230 and 236) idenitifed the mineral in the Trošnik ore<br />
body near Fojnica, in associateion with malachite, azurite and limonite. In pure form,<br />
chrysocolla is of a darkbrown colour and has a Mohs hardness of 3-4. Associated<br />
with limonite it attains a dark-greenish colour. Chemical analysis of this chrysocolla<br />
yielded following results: SiO 2<br />
= 32.65; Al 2<br />
O 3<br />
= 0.20; Fe 2<br />
O 3<br />
= 3.81; CuO = 42.91;<br />
loss-on-ignition = 20.31; MnO – traces; CaO – traces, amounting to a total of 99.98.<br />
The calculated molar ratios of SiO 2<br />
: CuO : H 2<br />
O = 0.54360 : 0.53929 : 1.12834<br />
indicates an iron-containing chrysocolla with traces of manganese impurities. These
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
impurities seem to give the characteristic darkbrown and darkgreen colouration to<br />
the chrysocolla from Trošnik, this being a secondary mineral within the mentioned<br />
ore-body.<br />
According to Đurić and Kubat (1962) chrysocolla occurs in association with<br />
copper mineralizations at Mt. Čavka (in the creeks Velika Borovica and Bijelina, and<br />
on the flanks of Klis and Otpočivaljka. Chrysocolla occurs here mainly associated<br />
with malachite. Kubat (1964) refers to chrysocolla as a typical secondary weathering<br />
mineral in the oxidation zone of the ‘Borovica’ mineralization in the central part of<br />
the Velika Borovica creek, some 2 km upstream from its confluence with the Velika<br />
Ukrina river. Kubat (1964) maintains that the chrysocolla is a product of chalcopyrite<br />
weathering in the presence of silica. It has a gel-like texture witha greasy lustre. One<br />
other publication by Kubat (1969) mentions chrysocolla in mineralizations around<br />
the village of Krnjići, some 15 km south-east of Srebrenica.<br />
When chrysocolla occurs in substantial amounts, it can be used as a copper<br />
ore. Such deposits are not known to exist in Bosnia and Hercegovina.<br />
SERPENTINE GROUP<br />
Mg 3<br />
[Si 2<br />
O 5<br />
] (OH) 4<br />
The serpentine group of minerals comprises several minerals with the same<br />
formula Mg 3<br />
[Si 2<br />
O 5<br />
] (OH) 4.<br />
The minerals antigorite (clino-antigorite and orho-antigorite),<br />
lizardite, chrysotile all belong to this group of minerals. A detialed classification of this<br />
group hase been made possible by the application of modern methods of x-ray diffraction<br />
analysis, thermal methods and IR-spectroscopy. The minerals antigorite, lizardite,<br />
chrysotile, clinochrysotile and garnierite are mentioned in this text.<br />
X-ray data:<br />
Antigorite d 3.60 (100) 7.19 (95) 2.527 (30) 2.42 (15) 4.59 (10)<br />
Lizardite d 3.63 (100) 7.19 (95) 2.49 (70) 2.45 (60) 4.53 (45)<br />
Clinochrysotile d 3.66 (100) 7.25 (85) 2.44 (65) 2.48 (40) 4.57 (25)<br />
IR-spectrum:<br />
Antigorite 410 442 585 615 850 1640 cm -1<br />
Chrysotile 411 435 480 545 607 1045 1078 1635 3440 3640 3682 cm -1<br />
A u t h o r s: Čičić (1975a), Džepina (1970), Đorđević (1958), Đorđević<br />
(1969a), Đorđević, Buzaljko and Mijatović (1968), Đurić (1968), Golub (1961), Hauer<br />
(1884), Ilić (1954), Ilić Miloje (1971), John (1879), Karamata and Petković (1957),<br />
Katzer (1924, 1926), Kišpatić (1897, 1900, 1904, 1910), Koch (1908), Majer (1962),<br />
Majer and Jurković (1957, 1958), Maksimović and Antić (1962), Marković and Takač<br />
225
SILICATES<br />
(1958), Marić (1927, 1969), Mitrović (1955), Mojsisovics, Tietze and Bittner (1880),<br />
Pamić (1960a, 1963a, 1969a, 1970, 1972, 1973, 1974), Pamić and Antić (1968), 1974),<br />
Pamić and Kapeler (1970), Pamić and Olujić (1974), Pilar (1882), Primics (1881),<br />
Radimsky (1889), Ristić, Pamić, Mudrinić and Likić (1967), Schiller (1905), Sijarić<br />
and Šćavničar (1972), Stevanović (1903), Sunarić and Olujić (1968), Šćavničar (1965),<br />
Šćavničar and Trubelja (1969), Šibenik-Studen (1972/73), Trubelja (1957, 1960, 1961,<br />
1962), Trubelja and Pamić (1965), Tscherne (1892), Tućan (1930, 1957), Vakanjac<br />
(1964, 1965, 1967 and 1968/69), Varićak (1966), Walter (1887).<br />
The minerals of the serpentine group belong to the most ubiquitous and widespread<br />
minerals in Bosnia and Hercegovina. Together with olivine and pyroxenes,<br />
the serpentine minerals are the building blocks of serpentinized peridotites – rocks<br />
which occur widely within the inner Dinarides in Bosnia. These peridotites and other<br />
basic volcanic rocks are spread over an area of more than 2000 sq. km, forming the<br />
‘Bosnian serpentine zone’ (BSZ). This name was given to this formation by Kišpatić<br />
(1897, 1900). Many mountain-massifs or parts thereof in Bosnia and Hercegovina<br />
are built by these rocks (Mts. Pastirevo, Kozara, Borja, Ljubić, Ozren, Konjuh and<br />
the western flanks of Mt. Zlatibor close to Višegrad).<br />
Several older publications dealing mostly with the geology of Bosnia<br />
and Hercegovina use the term ‘serpentine’ for these rocks, in fact referring to<br />
ultrabasic rocks.<br />
In terms of origin, the serpentine minerals are mostly secondary minerals,<br />
formed by weathering processes and alteration of olivine and pyroxenes. The amount<br />
of serpentine minerals in these rocks clearly reflects the degree of alteration of the<br />
original rocks. Unaltered pyroxenites contain only minor amounts of serpentine<br />
minerals. On the other end, serpentinites are largely monomineralic rocks built<br />
almost entirely of serpentine minerals.<br />
In ultrabasic rocks the serpentine minerals are contained in veins of various<br />
thicknesses, resulting often in fibrous aggregates (serpentine asbestos).<br />
Information on serpentine minerals in rock of the BSZ can be found in<br />
numerous publications, both old and recent ones.<br />
1. The Bosnian serpentine zone (BSZ)<br />
Data on serpentine minerals derived from microscopic determinations of<br />
these minerals can be retrieved from numerous literature sources (Hauer 1884; John<br />
1879; Mojsisovics et al. 1880; Pilar 1882; Primics 1881; Schiller 1905; Tscherne<br />
1892; Walter 1887). Among these early authors, John was the most prominent author<br />
with respect to microscopic investigations.<br />
226
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
In his classic publication under the title „The crystalline rocks of the Bosnian<br />
serpentine zone“ Kišpatić (1897, 1900) provides data on numerous microscopic<br />
determinations of serpentine minerals in lherzolite rocks, from Bosanski Novi in<br />
the north-west to Višegrad in the south-east. This author found that most of the<br />
serpentine minerals are alteration products of olivine and rhombic pyroxenes, less<br />
often of monoclinic pyroxenes.<br />
The gabbroid rocks of Mt. Kozara carry serpentine minerals in outcrops<br />
found around the Bistrica river and Benkovačko jezero (Benkovac lake). The<br />
peridoitets from this are contains serpetine which formed by alteration of olivine<br />
(Ljučica creek) or olivine and rhombic pyroxene (Kozarac, Benkovačka kosa).<br />
Serpentine mienrals can also be found in ultrabasic and basic rocks of Mts. Prisjeka,<br />
Skatovica, Uzlomac and Borja.<br />
In a south-east direction, the BSZ rocks (gabbros and peridotites) carry<br />
serpentine minerals (i.e. Mts. Ljubić, Ozren, Mahnača and Krivaja). Serpentine<br />
containing rocks are also found in the very south-east part of the BSZ, in the area of<br />
the township of Višegrad.<br />
Substantial information on serpentine minerals and serpentinization process<br />
of rocks around Višegrad can be found in publications by Trubelja (1957, 1960).<br />
Serpentine minerals are secondary minerals in harzburgites (Dobrun, Bosanska<br />
Jagodina), feldspar-peridotites (Bosanska Jagodina), troctolites (Gornji Dubovik),<br />
olivine gabbros (Mirilovići, Velika Gostilja, Banja creek). All mentioned rocks<br />
contain serpentine minerals in the form of veinlets forming fine networks. Relicts<br />
of olivine crystals can sometimes be observed in thin section. Sometimes the<br />
alteration of olivine to serpentine is accompanied with prehnitization of alkaline<br />
feldspars in troctolites. In troctolites therefore, a more advanced serpentinization<br />
means a more advanced prehnitization. This implies that the alteration of olivine to<br />
serpentine is a postmagmatic process. All rocks around Višegrad contain a fibrous<br />
variety of serpentine.<br />
A coarse, fibrous variety of serpentine (with almost acicular texture) occurs<br />
at the contact of gabbro and peridotite rock in the quarry on the left bank of the Rzav<br />
river, close to Bosanska Jagodina. The occurence is a vein with serpentine ‘crystals’<br />
positioned perpendicularly to the rims of the vein. This occurence is considered to<br />
be of hydrothermal origin, and we would like to point out that such coarse fibrous<br />
aggregates of serpentine minerals seem to be rather common in rocks of the BSZ.<br />
Results of chemical analysis of the serpentine from Bosanska Jagodina (Trubelja<br />
1960) are given in table 47 (sample 1).<br />
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SILICATES<br />
Table 47. Chemical composition of serpentine (analysis by F. Trubelja)<br />
Sample 1<br />
Bosanska Jagodina<br />
Sample 2<br />
Mt.Ozren<br />
SiO 2<br />
41.81 40.46<br />
TiO 2<br />
--- traces<br />
Al 2<br />
O 3<br />
1.38 2.36<br />
Fe 2<br />
O 3<br />
1.66 3.10<br />
FeO 1.38 1.17<br />
MnO 0.06 0.05<br />
MgO 40.08 38.74<br />
CaO --- races<br />
H 2<br />
O + 12.73 12.80<br />
H 2<br />
O - 0.90 1.35<br />
Total 100.00 100.03<br />
Some coarse fibrous serpentine (forming veins) was found on the northern<br />
flanks of Mt. Ozren, close to the village of Kakmuž (Trubelja and Pamić 1965). This<br />
serpentine is macroscopically and microscopically very similar to the one found at<br />
Bosanska Jagodina. The chemical composition (sample 2, table 47) is also very similar.<br />
The magnesite bearing complex of Miljevica, located near Kladanj and Mt.<br />
Konjuh, is closely associated with peridotite-serpentine rocks. Here we will present<br />
the results of our detailed investigations of serpentine rocks. The investigations mainly<br />
focused on the identification and determination of discrete serpentine minerals with<br />
different crystal structures. Mineralogical determinations on serpentine rock samples<br />
from the Miljevica area were done by Sijarić and Šćavničar (1972). These data are<br />
an important contribution to the understanding of polimineral aggregates found in<br />
the investigated rocks, as opposed to the largely monomineralic serpentine asbestos<br />
found at Bosansko Petrovo Selo.<br />
The determinations were done by powder x-ray diffraction analysis and<br />
thermal methods. Chemical analyses of macroscopically pure serpentine samples were<br />
also done. Based on the mentioned determinative methods, the following serpentine<br />
minerals were identified in the rocks from the Miljevica area: clinochrysotile, lizardite<br />
and antigorite. These minerals were found to have a zonal distribution on both sides<br />
of the magnesite veins. Samples taken 6-7 meters away from the vein contain all<br />
three mentioned minerals, while more distant samples contain clinochrysotile and<br />
lizardite only. Lizardite is the dominant serpentine mineral in samples taken close to<br />
the magnesite vein. This zonar arrangement of the serpentine minerls around the vein<br />
is certainly the results of hydrothermal activity which caused the inituial deposition<br />
of the serpentine minerals in veins within ultrabasic rocks. Hence, the origin of the<br />
serpentine minerals in the miljevica area is probably hydrothermal also.<br />
Unit cell dimensions of discrete serpentine minerals were determined from<br />
powder XRD data. The data obtained is in good agreement with literature data on<br />
clinochrysotile (Brown 1961) and lizardite (Rucklidge and Zussman 1965).<br />
228
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Clinochrysotile<br />
sample P 4.5z sample K 8.0z Reference<br />
a 0<br />
5.33 Å 5.31 Å 5.32 Å<br />
b 0<br />
9.22 Å 9.22 Å 9.20 Å<br />
c 0<br />
14.70 Å 14.62 Å 14.64 Å<br />
β 92° 18’ 93° 21’ 93° 20’<br />
Lizardite<br />
sample K 0.5p<br />
Reference<br />
a 0<br />
5.31 Å 5.31 Å<br />
b 0<br />
9.22 Å 9.20 Å<br />
c 0<br />
7.30 Å 7.31 Å<br />
Data obtained by thermal analysis is given in table 48. Powder XRD data<br />
indicated that the samples are different with respect to clinozoisite and lizardite<br />
content, this information could not be obtained by thermal analysis.<br />
Table 48. Thermal analysis data<br />
Sample Endothermic peak (min.) °C Exothermic peak (max.) °C<br />
K 15.0 c 668 805<br />
K 15.0 z 688 820<br />
K 8.0 c 672 820<br />
K 8.0 z 700 820<br />
K 6.0 c 680 (750) 810<br />
K 6.0 z 675 (770) 810<br />
K 2.6 u 665 (625) 810<br />
K 0.5 u 670 785<br />
P 6.5 c 680 812<br />
P 6.5 z 700 812<br />
P 9.5 690 805<br />
P 17.0 c 690 812<br />
P 17.0 z 670 812<br />
All samples showed almost identical behaviour upon heating, and small<br />
variations in the peak positions do not neccesarily reflect variations in composition,<br />
since they can be associated with experimental conditions. Also, dehydroxylation<br />
and recrystallization reactions of clinochrysotile and lizardite occur within similar<br />
temperature ranges. The endothermic temperatures in the brackets (table 48) refer to<br />
carbonate dissociation (750 and 770°C) and dehydroxylation of chlorite (625°C).<br />
In addition to serpentine minerals, the investigated rock samples also<br />
contain olivine, enstatite, diopside, amphibole, dolomite, magnesite, chromite,<br />
goethite and chlorite.<br />
229
SILICATES<br />
The occurences of serpentine asebestos around Bosansko Petrovo Selo have<br />
been imvestigated in detail (Ilić 1954; Mitrović 1955; Karamata and Petković 1957;<br />
Vakanjac 1964, 1965, 1967 and 1969; Šćavničar 1965; Đorđević et al. 1968). The<br />
investigations by S. Šćavničar are important as they provide the first characterization<br />
of discrete serpentine minerals.<br />
Ilić (1954) provides a short description of the occurence of serpentine<br />
asbestos around Bosansko Petrovo Selo, and considers briefly their origin. The<br />
occurences can mainly be found in the watershed area of the Jadrina river, at Delić<br />
Brdo, Senikovište, Krajnje Njive, Studen Potok etc. The asbestos occurs here within<br />
peridotites and serpentinized peridotites.<br />
The acidic effusive rocks (rhyolite) in the area of Bosansko Petrovo Selo<br />
are genetically associated with the serpentine rock formations. The hydrothermal<br />
processes linked with the rhyolite complex have influenced the formation of<br />
serpentine minerals and asbestos in this area (Ilić 1954, Vakanjac 1964).<br />
Šćavničar (1965) made a detailed investigation of four samples from the<br />
Bosansko Petrovo Selo occurence, using microscopy, powder XRD, thermal<br />
methods and chemical analysis. Two of the analysed samples are dense, massive,<br />
green aggregates of clinochrysotile and lizardite (in different proportions).<br />
Table 49. Powder x-ray diffraction data for serpentine from Bosansko Petrovo Selo<br />
(Šćavničar 1965)<br />
Sample # 1 Sample # 2 Sample # 3<br />
hkl d(Å) I d(Å) I d(Å) I<br />
002 7.30 100 7.27 100 7.28 100<br />
4.56 4.56<br />
020 22 18<br />
4.52 4.52 4.47 8b<br />
4.40 5 4.41 3<br />
4.24 7 4.23 4<br />
4.08 5 4.08 4<br />
3.89 5 3.89 3<br />
004 3.64 77 3.64 70 3.64 85<br />
024 2.87 3 2.87 3<br />
130 2.66 5 2.6 5<br />
201* 2.58 11b 2.58 5<br />
202 2.54 11 2.54 7<br />
202* 2.500 38 2.495 6<br />
202** 2.450 29 2.449 32 2.449 29<br />
006 2.420 11<br />
203** 2.333 6<br />
203* 2.273 3 2.271 5b 2.272 5<br />
204* 2.214 3<br />
204** 2.146 8b<br />
204 2.087 9 2.087 11 2.094 7<br />
230
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
205 1.964 9<br />
008 1.823 4b<br />
206* 1.737 6 1.738 9 1.740 6<br />
060 1.537 22 1.536 20 1.534 25<br />
208** 1.502 8 1.505 5<br />
0, 0, 10 1.465 5<br />
064 1.414 3 1.416 4<br />
Sample 1 – lizardite and clinochrysotile<br />
Sample 2 – clinochrysotile with lizardite<br />
Sample 3 – clinochrysotile asbestos<br />
* refers to β = 90°<br />
** refers to β = 93° 16’<br />
The third sample has a typical asbestos texture, of tough fibres between 0.2<br />
and 0.8 mm in length. This sample is almost pure chrysotile. The refraction indices<br />
were measured by the immersion method (1.542-1.552). The fourth sample is a white<br />
aggregate with a fibrous texture, containing rather thick, pliable fibres more than 5<br />
cm long. This sample is a mixture of antigorite and dolomite. Refractive indices are<br />
1.563-1.570.<br />
Table 50. Unit cell parameters for serpentine from Bosansko Petrovo Selo<br />
Sample # a 0<br />
Å b 0<br />
Å c 0<br />
Å β<br />
1 5.31 9.22 14.58 93° 16’<br />
2 5.31 9.22 14.58 93° 16’<br />
3 5.31 9.02 14.58 93° 16’<br />
Clinochrysotile<br />
Whittaker and Zussman<br />
1956<br />
5.34 9.2 14.65 93° 16’<br />
Sample 1 – lizardite and clinochrysotile<br />
Sample 2 – clinochrysotile with lizardite<br />
Sample 3 – clinochrysotile asbestos<br />
Data on x-ray structural analysis are given in tables 49 and 50. Table 51<br />
contains data on the thermal analysis of the four samples.<br />
Table 51. Thermal analysis of serpentine from Bosansko Petrovo Selo (Šćavničar 1965)<br />
Sample Endothermic peak °C Exothermic peak °C<br />
Characteristic temp. Peak temperature Characteristic Peak temperature B<br />
temp.<br />
1 608 708 766 780<br />
2 607 714 770 786<br />
3 622 700 771 787<br />
4 613 810 760 776<br />
Sample 1 – lizardite and clinochrysotile<br />
Sample 2 – clinochrysotile with lizardite<br />
231
SILICATES<br />
Sample 3 – clinochrysotile asbestos<br />
Sample 4 – fibrous antigorite<br />
Chemical analyses of two serpentine samples are given in table 52. The<br />
analyes were done by Ms. Dragica Sarvan.<br />
Table 52. Chemical analysis of serpentine from Bosansko Petrovo Selo (Šćavničar 1965)<br />
Sample 1 Sample 2<br />
SiO 2<br />
41.15 38.91<br />
Al 2<br />
O 3<br />
1.44 2.34<br />
Fe 2<br />
O 3<br />
3.14 4.27<br />
FeO 0.36 0.50<br />
NiO 0.07 0.10<br />
MnO --- 0.04<br />
MgO 40.41 39.93<br />
H 2<br />
O + 13.16 13.39<br />
H 2<br />
O - 0.59 0.41<br />
Total 100.32 99.89<br />
The structural formulae of the two serpentine sample, based on results of<br />
chemical analysis are as follows (based on 18 (O, OH) ions:<br />
Sample 1.<br />
O 6.072<br />
Si 3.839<br />
Al 0.081<br />
Fe 3+ 0.109 (H 4 ) 0.067 O 2.024+1.981 (OH) 1.981 (Mg 5.624 Fe2+ 0.029 Ni 0.005 Fe3+ 0.109 Al 0.081 )<br />
- (OH) 5.942<br />
Sample 2.<br />
O 5.924<br />
Si 3.695<br />
Al 0.132<br />
Fe 3+ 0.151 (H 4 ) 0.078 O 1.975+2.020 (OH) 2.020<br />
- (Mg 5.594<br />
Fe 2+ 0.039 Ni 0.007 Mn 0.003 Fe3+ 0.151 Al 0.132 )(OH) 6.061<br />
In these structural formulae the iron (III) and aluminium contents have been<br />
distributed between their tetrahedral and octahedral coordination sites.<br />
DTA curves of the serpentine samples are shown in Figure 15. The curves are<br />
obviously quite similar, implying that identification of discrete serpentine minerals,<br />
based solely on thermal analysis, is not possible.<br />
232
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Figure 15. DTA curves of serpentine from Bosansko Petrovo Selo<br />
(Šćavničar 1965)<br />
Đorđević et al. (1968) also provide data on the determination of serpentine<br />
asbestos from Bosansko Petrovo Selo, with special emphasis on the Jovanovići –<br />
Stepanovići locality. Based on powder XRD, the authors conclude that this serpentine<br />
probably belongs to the clinochrysotile variety. Their paper contains 2 chemical<br />
analyses: a pure chrysotile asbestos, and a serpentinite. At Jovanovići – Stepanovići<br />
the asbestos fibres are usually 1-4 mm long. Rarely their length is up to 12 cm.<br />
These authors also provide an account on other serpentine occurences in<br />
Bosnia and Hercegovina. The occurence at Grudići (Olovo) is in the immediate<br />
vicinity of the Petrovići train station, located on the narrow-gauge railway line<br />
Zavidovići – Han Pijesak. Further occurences have been identified near Zavidovići<br />
(at Turčinovići), near Žepče – at the well-known Ruda – Vis locality, some 10 km<br />
northwest of Žepče.<br />
Occurences of serpentine asbestos can further be observed in the Banja Luka<br />
area (at Čelinac and Bregovi).<br />
233
SILICATES<br />
The nickel-bearing serpentine from Duboštica has been described in older<br />
literature under the name nickel-gimnite (Hauer 1884). It forms thin green crusts<br />
over chromite. According to Hauer, nickel was determined in this mineral by C. John<br />
(1879). The name gimnite has been discredited as a mineral name, and is occasionally<br />
used to describe a nickel-enriched variety of antigorite.<br />
Đurić (1968) provides data on the cinnabarite mineralization at Mt. Ljubić,<br />
and mentions garnierite as a constituent of the green serpentine altered to listvenite.<br />
The author gives no further information on this mineral.<br />
Some general information on serpentine minerals in Bosnia and Hercegovina<br />
can be found in more recent literature, but none of these publications provide details<br />
about individual minerals of the serpentine group.<br />
2. Schist mountains of central Bosnia<br />
The occurence of serpentine within the Palaeozoic-age phyllites near the<br />
village of Kupres at Busovača presents somewhat of a geological curiosity. The<br />
serpentine occurs in close association with a flaky aggregate of talc (Šćavničar<br />
and Trubelja 1969). The talc-chlorite-serpentine vein is shown in Figure 15. The<br />
authors have shown that the core of the vein consists of talc surrounded by a layer<br />
of cryptocrystalline antigorite. Antigorite was determined by powder XRD, thermal<br />
analysis and quantitative chemical analysis. The powder x-ray diffraction data are<br />
given in table 53. The three strong diffraction peaks at 7.184, 3.599 and 2.522 Å, as<br />
well as the less intense 1.5645 Å signal probably indicate the presence of antigorite.<br />
However, we wish to point out that our x-ray diffraction pattern does not correspond<br />
exactly to literature data for antigorite (some of the weaker lines characteristic<br />
for antigorite did not appear on film even after long exposure times). Therefore,<br />
the calculation of the unit cell dimensions (using β = 91.6°) is based only on the<br />
strongest diffraction signals, and should be treated as moderately precise only. The<br />
thermal analysis data correspond to serpentine minerals.<br />
Chemical analysis of antigorite from Kupres yielded following results:<br />
SiO 2<br />
= 42.31; TiO 2<br />
= traces; Al 2<br />
O 3<br />
= 2.32; Fe 2<br />
O 3<br />
= 5.20; FeO = 2.67; MnO = 0.08;<br />
MgO = 35.34; CaO = 0.46; Na 2<br />
O = 0.36; H 2<br />
O + = 10.89; H 2<br />
O - = 0.43; P 2<br />
O 5<br />
= 0.01;<br />
Total = 100.31<br />
The structural formula, based on 9 (O,OH) ions is:<br />
(Ca 0.024<br />
Na 0.022<br />
K 0.022<br />
)(Mg 2.537<br />
Fe 2+ 0.108 Fe3+ 0.188 Al 0.132 Mn 0.003 )VI (Si 2.039<br />
) IV O 5.500<br />
(OH) 3.500<br />
The structural formula is based on the overall chemical analysis, including<br />
impurities which could not be excluded from the sample. Therefore, it corresponds<br />
234
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
only to some extent to serpentine. All these data corroborate our finding that the<br />
zonal buildup of the described serpentine vein at Kupres is the result of hydrothermal<br />
process which occured over several phases. A largely monomineralic species<br />
(depending on the composition and temperature of hydrothermal solutions) was<br />
deposited in each of these phases. Chlorite was deposited first, followed by antigorite<br />
and – finally – the flaky talc aggregate.<br />
Kišpatić (1910) and Majer and Jurković (1957 and 1958) determined<br />
serpentine in the olivine gabbros south of Travnik (the Bijela Gromila complex).<br />
Table 53. Powder x-ray diffraction data of serpentine from Kupres (Šćavničar and Trubelja 1969)<br />
Nr. hkl d (Å) I<br />
1 9.300 2.5<br />
2 001 7.188 30<br />
3 6.228 1<br />
4 5.191 1<br />
5 020 4.589 6<br />
6 4.183 3.5<br />
7 002 3.599 19<br />
8 3.448 0.5<br />
9 3.326 0.5<br />
10 3.100 2<br />
11 2.655 0.5<br />
12 2.585 1<br />
13 16, 0, 1 2.522 23<br />
14 2.50 – 2.39 2d<br />
15 2.214 1<br />
16 16, 0, 2 2.155 6<br />
17 2.101 1<br />
18 1.835 1<br />
19 1.804 1<br />
20 1.780 2<br />
21 1.725 1b<br />
22 1.588 0.5<br />
23 24, 3, 0 1.5645 7<br />
24 060 1.5395 7<br />
25 1.5225 2<br />
26 061 1.5050 3<br />
27 1.4754 0.5<br />
28 1.4407 1<br />
29 1.4162 1<br />
30 1.3804 0.5<br />
31 1.3403 0.5<br />
32 1.3159 5<br />
33 1.2981 1.5<br />
34 1.2660 1<br />
235
SILICATES<br />
35 1.2041 1<br />
36 1.0152 1<br />
37 1.0006 1<br />
38 0.9744 1<br />
39 0.9506 1<br />
40 0.8965 1<br />
b = broadening of line<br />
d = diffuse line<br />
3. Other occurences of serpentine<br />
Marić (1927) microscopically determined serpentine in some gabbro rock<br />
varieties around Jablanica. Pamić (1963a) mentions serpentine rocks in the river<br />
Rama region in Hercegovina. Katzer (1924, 1926) was the first author to mention<br />
serpentine at Mt. Motajica. Varićak (1966) microscopically identified serpentine<br />
(antigorite and chrysotile) in rocks in the Osovica river valley.<br />
4. Origin of serpentine<br />
We have already touched upon the origin of serpentine minerals in Bosnia<br />
and Hercegovina. In those case where serpentine minerals occur in the form of vein<br />
fills within tectonically fractured ultrabasic rocks, we believe that their origin is<br />
hydrothermal. This is particularly true for the area of Bosansko Petrovo Selo on<br />
the eastern flanks of Mt. Ozren where economically elevant asbestos deposits were<br />
formed. The same is true for the serpentines associated with Miljevica magnesite<br />
deposits at Mt. Konjuh where hydrothermal process caused both serpentinization<br />
and the deposition of magnesite. With respect to the origin of these hydrothermal<br />
solutions, we believe that they have been released in the late, mostly acid-toneutral<br />
magmatic events, since evidence of similar processes can also be observed<br />
elsewhere in Bosnia and Hercegovina, especially within the Bosnian serpentine<br />
zone (BSZ). However, also other processes leading to serpentinization have been<br />
observed or inferred, particularly in ultrabasic and basic rock types. One such case is<br />
autometamorphosis where the alteration of olivine and pyroxene is caused by water<br />
originating in magmatic processes which have caused a more or less contemporal<br />
crystallization of the ultrabasic rock itself. We agree with those authors which have<br />
investigated such processes in the BSZ that at least some of the serpentine may have<br />
originated through autometamorphism.<br />
Use: the numerous industrial and commercial applications of serpentine<br />
minerals involve mainly the chrysotile and chrysotile-asbestos variety. More than<br />
90% of asbestos products are based on serpentine minerals, while amphibole<br />
asbestos varietes (tremolite-actinolite, crocidolite) account for less than 10%. The<br />
236
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
asbestos cement industry is singled out as by far the largest current global user of<br />
chrysotile fibres. Main applications include the production of corrugated sheets, flat<br />
sheets and building boards, slates, moulded goods, including low-pressure pipes, and<br />
high-pressure water pipes. Chrysotile is also used, in much smaller quantities, in the<br />
manufacturing of friction products, gaskets, and asbestos paper. Serpentine rock is<br />
often used as dimension rock and for ornamental purposes. Gernierite deposits can<br />
be an important source of nickel.<br />
Čičić (1975a) estimates that the reserves of „asbestos ore“ at Delić Brdo near<br />
Bosansko Petrovo Selo amount to 116 milion tons.<br />
Recent research has indicated the hazards for the environment and human health<br />
associated with the use of asbestos and asbestos products, including exposure of<br />
humans to chrysotile asbestos. It is the recommendation of several international<br />
organizations to discontinue the use of crocidolite asbestos.<br />
HALLOYSITE – (METAHALLOYSITE)<br />
Al 2<br />
[Si 2<br />
O 5<br />
] (OH) 4<br />
Crystal system and class: Monolinic, domatic class.<br />
Cell parameters: a o<br />
= 5.15, b o<br />
= 8.9, c o<br />
= 7.9-7.5<br />
X-ray data: d 7.41 (60) 4.432 (100) 1.484 (50)<br />
Synonyms: (note added in translation) – according to newer classifications of the<br />
kaolinite-serpentine group of minerals, as adopted by the benchmark publication<br />
Fleischer’s Glossary of Mineral Species (Mandarino and Back, 2004), the use of the<br />
name metahalloysite has been discontinued. Metahalloysite is nowadays described<br />
as halloysite – (7Å), and may also be understood in terms of a dehydrated halloysite<br />
– (10Å). In this section of the book, the name metahalloysite has been changed to<br />
halloysite, and pertains to halloysite – (7Å).<br />
A u t h o r s: Dangić (1971), Podubsky (1955), Stangačilović (1956a),<br />
Šćavničar, Trubelja and Sijarić-Pleho (1968)<br />
There is not much information available on the occurences of halloysite in<br />
Bosnia and Hercegovina. It occurs in halloysite-schists at the locality of Bakija. It is<br />
also a constituent of Tertiary-age clays from Kobiljača in the Sarajevo basin. Some<br />
occurences associated with the bauxite deposits in Hercegovina have been observed.<br />
1. Halloysite-bearing schists in south-eastern Bosnia<br />
Podubsky (1955) determined halloysite-bearing schists near the village of<br />
Bakije, in Paleozoic-age formations near Goražde in south-eastern Bosnia. This is in<br />
fact the first information about this mineral in Bosnia and Hercegovina. The mineral<br />
237
SILICATES<br />
was identified by powder XRD. It is associated with quartz, sericite, muscovite and<br />
siderite. The paper by Podubsky also contains two DTA curves. Unfortunately, the<br />
material used for thermal analysis was previously dried at elevated temperatures, so<br />
the DTA curves cannot be used for halloysite determination.<br />
Dangić (1971) suspects the presence of halloysite in the kaolinite deposit at<br />
Bratunac near Srebrenica, but was unable to provide conclusive evidence.<br />
2. The Kobiljača occurence near Sarajevo<br />
Stangačilović (1956a) investigated the Tertiary-age clays at Kobiljača near<br />
Sarajevo and identified halloysite as a constituent mineral, second in importance only<br />
to illite. The determination is based on thermogravimetric measurements, differentialthermal<br />
analysis and powder x-ray diffraction. The DTA curves of two samples of<br />
illite-halloysite clays feature two prominent endothermic peaks in the 130-150°C<br />
temperature interval. These peaks are associated with the loss of interstitial water from<br />
the halloysite structure – an effect which has not been observed in the case of illite.<br />
The powder XRD pattern was important for the identification and<br />
characterization of halloysite, illite and quartz. The lines corresponding to d values<br />
of 7.22 Å and 7.41 Å are specific for hallyosite only (not for illite or quartz).<br />
3. Occurence of halloysite in bauxites from Hercegovina<br />
Šćavničar et al. (1968) used the powder x-ray diffraction method to determine<br />
hallyosite in some hercegovinian bauxites – i.e. the boehmite-gibbsite bauxites from<br />
Nevesinje; localities Zamršten – Zubača and Mukinja). A further occurence is in the<br />
bauxites from Mratnjača in western Hercegovina.<br />
SEPIOLITE<br />
Mg 4<br />
[Si 6<br />
O 15<br />
] (OH) 2<br />
x 6H 2<br />
O<br />
Crystal system and class: Orthorhombic, dipyramidal class.<br />
Cell parameters: a o<br />
= 5.28, b o<br />
= 26.8, c o<br />
= 13.4 Z = 2<br />
Properties: earthy to cryptocrystalline texture, white, yellowish or gray in colour.<br />
Hardness is 2.0-2.5, the specific gravity = 2. Sepiolite is usually very porous and<br />
normally floats on water.<br />
X-ray data: see text<br />
IR-spectrum: 443 475 500 535 600 640 782 850 890 985 1025 1972 1200<br />
1635 1660 3440 3570 3600 cm -1<br />
238
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
A u t h o r s: Golub (1961), Hantken (1867), Katzer (1909, 1912), Kišpatić<br />
(1893, 1895, 1897, 1900), Miladinović (1969), Mojsisovics, Tietze and Bittner<br />
(1880), Panić and Ristić (1972), Pavlović (1891), Pilar (1882), Potier (1879),<br />
Radimsky (1889), Ristić, Panić and Janjić (1965), Stevanović (1903), Trubelja<br />
(1971a), Tscherne (1892), Tućan (1930, 1947, 1957), Walter (1887).<br />
Sepiolite is a comparatively rare mineral in Bosnia and Hercegovina. Only<br />
two occurences have been described in the literature. One occurence, discovered<br />
more than a century ago, is in the vicinity of Prnjavor at Mt. Ljubić. The occurence,<br />
at Miljevica on Mt. Konjuh was discovered only recently. Some sepiolite was also<br />
found at Mt. Kozara and near Srebrenica (Bratunac).<br />
1. Sepiolite from Mt. Ljubić<br />
Hantken (1867) provides first data on the sepiolite occurence on the northern<br />
flanks of Mt. Ljubić, within serpentinized peridotites near the town of Prnjavor. This<br />
sepiolite has been mined for more than hundred years, at Kremna, Branešci and<br />
Reljevac. At Branešci, the sepiolite is associated with conglomerates containing<br />
serpentine. At Kremna, sepiolite is found together with magnesite veins (the<br />
magnesite is sometimes silified).<br />
Several papers dealing with sepiolite occurences near Prnjavor have been<br />
published at the beginning of this century, mainly by foreign investigators (Walter<br />
1887 and others). This is an indication that these authors had substantial interest<br />
in this comparatively rare mineral, possibly due to its use for the manufacture of<br />
smoking pipes. It is interesting to note that these authors considered the material<br />
to be magnesite, although they did use the term „bosnian sepiolite“. This situation<br />
motivated Kišpatić (1893, p. 99) to comment with some humor that „they were<br />
inclined to delete sepiolite from the list of bosnian ore materials“.<br />
Radimsky (1889) provides some data for the sepiolite from Mt. Ljubić, and<br />
notes several properties of this material. He thus notes that sepiolite produces a sticky<br />
sensation on the tongue, that it readily absorbs water and has a variable density<br />
between 0.47 and 0.95 and variable hardness (between 1 and 2.5). It dissolves in<br />
acid, releasing gelatinous silicic acid. When wet, sepiolite is easily cut with a knife.<br />
Tscherne (1892) provides some relevant data for the sepiolite from Mt.<br />
Ljubić. His paper contains some microscopic measurements and results of several<br />
chemical analyses (either of pure sepiolite or a mixture of sepiolite and magnesite,<br />
including some impurities). Table 54 contains results of 3 analyses of sepiolite<br />
material.<br />
239
SILICATES<br />
Table 54. Chemical composition od sepiolite from Mt. Ljubić<br />
Sample 1 Sample 2 Sample 3<br />
CO 2<br />
2.30 26.42 ---<br />
Loss on ignition 16.96 7.61 11.38<br />
Humidity --- --- 9.11<br />
Free SiO 2<br />
4.42 --- ---<br />
Bound SiO 2<br />
46.20 30.47 47.23<br />
MgO 23.90 34.53 24.55<br />
FeO (Fe 2<br />
O 3<br />
) 6.13 0.90 7.20<br />
Total 99.71 99.93 99.47<br />
Kišpatić (1893, 1895, 1897, 1900) provides. among other data, the results<br />
of chemical analysis of a pure sepiolite (table 55, sample 1). Before analysis, this<br />
sample was dried at 110°C which caused all hygroscopic water to be released.<br />
Katzer (1909) also gives results of the chemical analysis of one sepiolite sample<br />
from the Kremna locality (table 55, sample 2). His sample was also dried at 110°C.<br />
Table 55. Chemical composition of sepiolite from Mt. Ljubić<br />
Sample 1– Kišpatić<br />
Sample 2 – Katzer<br />
SiO 2<br />
61.09 57.80<br />
MgO 25.87 27.32<br />
Fe 2<br />
O 3<br />
and Al 2<br />
O 3<br />
2.59 3.12<br />
Loss on ignition and CO 2<br />
10.47 12.58<br />
Total 100.02 100.82<br />
240<br />
2. Sepiolite from Mt. Konjuh<br />
Ristić et al. (1965), Panić and Ristić (1972), Miladinović (1969) and<br />
Živanović (1968) provide data on the occurence of sepiolite in magnesite veins at<br />
Miljevica and Zeničica (Mt. Konjuh). Here, sepiolite and magnesite occur together<br />
in peridotite rocks. The sepiolite has a banded texture, the bands being 5-20 cm thick<br />
and several meters long. Sepiolite also forms lenses or crusts over magnesite.<br />
The sepiolite has a bluish-white or greyish-white colour, and displays<br />
a conchoidal fracture with a greasy to vitreous lustre. Sepiolite is normally very<br />
hygroscopic.<br />
In thin section, the sepiolite has the appearance of bent, fibrous aggregates.<br />
The immersion method was applied to measure refractive indices:<br />
Np = 1.517 ± 0.002 Ng = 1.527 ± 0.002 Ng – Np = 0.010<br />
The results of chemical analysis of two samples of sepiolite from the<br />
Miljevica locality are given in Table 56. The results indicate that sepiolite regularly
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
contains small amounts of carbon dioxide, caused by the presence of magnesite.<br />
DTA curves were characteristic for sepiolite. There is an endothermic peak in the<br />
50-150°C temperature range, indicating loss of adsorbed and zeolite-type water. The<br />
second endothermic peak between 350 and 450°C pertains to loss of intra-crystalline<br />
water (water of crystallization). The endothermic effect between 700 and 830°C is<br />
associated with the loss of structurally bound water and the collapse of the sepiolite<br />
crystal structure.<br />
Table 56. Chemical composition of sepiolite from Mt. Konjuh<br />
Sample Miljevica 11 Sample Miljevica 7<br />
SiO 2<br />
54.75 52.07<br />
Al 2<br />
O 3<br />
0.51 0.36<br />
Fe 2<br />
O 3<br />
0.26 0.18<br />
FeO --- ---<br />
MgO 24.28 26.86<br />
Na 2<br />
O 0.07 0.05<br />
K 2<br />
O 0.03 0.03<br />
CO 2<br />
0.33 0.85<br />
H 2<br />
O + 9.87 9.50<br />
H 2<br />
O - 9.93 10.02<br />
Total 100.01 99.81<br />
The cited authors believe that the genesis of sepiolite and magnesite in the<br />
Mt. Konjuh occurences are similar, both probably being of hydrothermal origin.<br />
Sepiolite was obviously deposited at low temperatures, during the epithermal or<br />
telethermal phases (possibly even at ambiental temperature).<br />
3. Sepiolite in rocks from Mt. Kozara<br />
Golub (1961) performed microscopic determinations of sepiolite in<br />
serpentines from the Lubina creek, and lherzolites of Vrelo creek. In the serpentine<br />
rock, the sepiolite very much resembles chrysotile, although it is optically uniaxial and<br />
negative. The refractive indices are lower than those of Canada balm. The sepiolite<br />
contained in the lherzolite rock has a fibrous texture or forms dense aggregates.<br />
4. Other occurences of sepiolite<br />
Trubelja (1971a) identified small amounts of sepiolite in kaolinized dacites<br />
from Bratunac, near Srebrenica. According to some early information provided by<br />
Potier (1879, p. 36), some sepiolite is apparently mined notheast of Banja Luka, also<br />
near Fojnica and Kreševo, but in minor quantities. The location of the Banja Luka<br />
occurence is not completely clear so we believe that this sepiolite is to be associated<br />
with the ones from Mt. Ljubić.<br />
241
SILICATES<br />
Sepiolite is used commercially in the production of fire-resistant materials<br />
and in the manufacture of (smoking) pipes.<br />
Table 57. Powder XRD data of sepiolite from Mt. Konjuh<br />
Miljevica 8 Miljevica 9 Zeničica 2 – north Zeničica 2 – south<br />
d (Å) I d (Å) I d (Å) I d (Å) I<br />
7.50 3 7.46 1 7.57 3 7.63 1-2<br />
12.28 10 12.03 9 12.20 10 12.12 7<br />
5.05 1 5.09 1<br />
4.58 5 4.53 1 4.53 4 4.55 1<br />
4.29 8 4.25 7 4.33 7 4.31 3<br />
3.75 5 3.74 1 3.77 4 3.74 2<br />
3.36 9 3.35 10 3.37 2 3.35 1-2<br />
3.15 3 3.17 1 3.16 1 3.19 1-2<br />
2.579 8 2.56 2 2.573 8 2.567 1-2<br />
2.456 6 2.456 4 2.456 3 2.411 1<br />
2.264 7 2.276 4 2.276 2 2.278 2<br />
2.075 3 2.066 1 2.073 2 2.072 1-2<br />
1.868 1-2 1.891 1-2 1.849 1-2<br />
1.701 4 1.728 5 1.709 2 1.701 9<br />
1.586 1 1.595 2<br />
1.543 5 1.543 6 1.563 2 1.566 1<br />
1.517 3 1.520 1 1.518 3 1.513 4<br />
1.416 1 1.419 1 1.422 1 1.417 1<br />
1.378 6 1.373 4 1.392 1<br />
1.299 4 1.292 2 1.303 3<br />
242<br />
PREHNITE<br />
Ca 2<br />
Al VI [Si 3<br />
O 10<br />
] (OH) 2<br />
Crystal system and class: Orthorhombic, pyramidal class.<br />
Lattice ratio: a : b : c = 0.8401 : 1 : 1.1536<br />
Cell parameters: a o<br />
= 4.61, b o<br />
= 5.47, c o<br />
= 18.48 Z = 2<br />
Synonyms: information in the treatise by B. G. Sage (Elements de mineralogie<br />
docimastique, 2eme edition, Paris 1777, p. 232) indicates that the author refers<br />
to prehnite. Some years later, Rome de l’Isle (Cristallographie ou description des<br />
formes propres a tous le corps du regne mineral etc., 2, Paris 1783, p. 275) describes<br />
prehnite smples brought by the monk Rochon from the Cape of Good Hope (Africa).<br />
Material brought to Germany (also from the Cape of Good Hope) in 1783 by the<br />
Dutch Colonel Prehn was investigated by the mineralogist A. G. Werner who gave<br />
the new mineral the name prehnite. The name koupholite was used earlier for a<br />
variety of prehnite occuring in the micaschists from Adelsfors in Sweden. Other<br />
discredited names include jacksonite and chlorastolite.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Properties: refractive indices are fairly high: Nz = 1.632-1.665, Ny = 1.615-1.642,<br />
Nx = 1.611-1.632. Birefringence Nz – Nx = 0.022-0.035. The optic axial angle<br />
+2V = 65-69°. Specific gravity is 2.90-2.95, hardness = 6-6.5. Good cleavage on<br />
{001}. Lustre is vitreous, sometimes pearly on (001). The colour varies from pale<br />
green to yellow, grey or white. Transparent in thin section. Optic anomalies are<br />
frequently observed – some samples show a wavy extinction and unusual interference<br />
colours. Prehnite has pyroelectric properties.<br />
X-ray data: see text<br />
IR-spectrum: 426 475 530 640 675 745 815 868 940 990 1075 1090 1630<br />
3475 3485 cm -1<br />
A u t h o r s: Atanacković, Mudrenović and Gaković (1968), Brajdić (1964),<br />
Džepina (1970), Đorđević (1958), Đorđević and Mojičević (1972), Đorđević and<br />
Stojanović (1972, 1974), Đurić and Kubat (1962), Golub (1961), Karamata and Pamić<br />
(1964), Kubat (1964), Majer (1962), Marić (1927), Pamić (1960, 1960a, 1961a, 1961b,<br />
1962, 1969, 1969a, 1971, 1972a, 1972d, 1973), Pamić and Kapeler (1970), Pamić and<br />
Papeš (1969), Pamić, Šćavničar and Medjimorec (1973), Pamić and Tojerkauf (1970),<br />
Petković (1962/62), Ristić, Panić, Mudrinić and Likić (1967), Šibenik-Studen and Trubelja<br />
(1971), Trubelja (1957, 1960, 1961, 1966a, 1971b, 1972, 1972/73, 1975), Trubelja and<br />
Miladinović (1969), Trubelja and Pamić (1957, 1965), Trubelja and Slišković (1967),<br />
Trubelja, Šibenik-Studen and Sijarić (1974, 1975, 1975a), Tućan (1957).<br />
Prehnite is among the more commonly occuring minerals in Bosnia and<br />
Hercegovina. It is mostly associated with basic rocks of the Bosnian serpentine zone<br />
(BSZ) and the surrounding diabase-chert complex (troctolite, olivine gabbro, diabase,<br />
spilite). Prehnite also occurs in amphibolites, and occasionally in granitoid rocks.<br />
Outside of the BSZ prehnite occurs within veins of the gabbros of Jablanica<br />
(Marić 1927), and on several other locations in Bosnia and Hercegovina. In the<br />
earlier days prehnite was mostly determined by microscopy. Today, modern methods<br />
of physico-chemical analysis, including infrared spectroscopy are used.<br />
Occurences of prehnite have also been observed in basic rocks belonging<br />
to the Triassic-age magmatic events, since such rocks are widely distributed in the<br />
Dinarides of Bosnia and Hercegovina (Trubelja et al. 1975).<br />
1. Prehnite in rocks of the Bosnian serpentine zone (BSZ)<br />
Most determinations of prehnite pertain to basic (but also other) rocks of the<br />
Bosnian serpentine zone (BSZ). It occurs around Višegrad, at Mt. Konjuh and Mt.<br />
Ozren, in the region between the rivers Bosna and Vrbas, and at Mt. Kozara. Within<br />
these rock types prehnite is usually associated with zeolite minerals, forming veintype<br />
parageneses.<br />
243
SILICATES<br />
a) Višegrad and surroundings<br />
Trubelja (1957, 1960, 1971b, 1972/73, 1975), Trubelja, Šibenik-Studen<br />
and Sijarić (1974, 1975, 1975a) provide more recent accounts on the occurence of<br />
prehnite in rocks of the Višegrad area, where prehnite is almost always present in<br />
basic magmatic rocks. It occurs in veinlets, either alone or associated with other<br />
postmagmatic vein-type minerals. Associations with zeolites are very common,<br />
and occasional pseudomorphoses of prehnite over alkaline palgioclase minerals<br />
have been determined.<br />
The association of prehnite with alkaline plagioclases is particularly<br />
evident in the case of troctolites from Gornji Dubovik. Prehnite is deposited within<br />
fractured plagioclase crystals or forms intergrowths. Prehnite grains are usually<br />
small but some columnar textures have been observed (the prehnite crystals are<br />
elongated parallel to [010]). In thin section the prehnite displays parallel extinction.<br />
Birefringence is high, the interference colours vivid. The optic axial angle is +2V =<br />
70°. Acicular and plumose prehnite growths have also been observed.<br />
The prehnitization process of alkaline plagioclase minerals is associated<br />
with the alteration of olivine (serpentinization). Based on numerous microscopic<br />
measurements, Trubelja (1960) maintains that progressive alteration of basic<br />
feldspars i.e. prehnitization usually also means advanced serpentinization.<br />
The troctolites from the village of Lahci (Banja creek valley) contain<br />
prehnite in association with zoisite, where both represent alteration prodcuts<br />
of plagioclase. Gabbro-pegmatites frequently contain hydrothermal prehnite,<br />
sometimes as pseudomorphoses over plagioclases. In such matrices the prehnite<br />
grains normally display distinct cleavage along (001). The optic axial angle +2V<br />
varies between 68.5° and 70°. In some rocks the 2V angle of prehnite grains can<br />
attain even larger values.<br />
At Pavitine (Suha Gora) prehnite forms vein-type associations with<br />
hornblende, clinozoisite and chlorite. Altered diabases, outcropping on the road<br />
from Višegrad to Dobrun, carry completely altered plagioclases, together with the<br />
rare mineral xonotlite (Trubelja 1971b, 1972/73, 1975).<br />
244<br />
b) Mt. Konjuh<br />
Trubelja (1961) made first determinations of prehnite in postmagmatic,<br />
hydrothermal vein-type associations within basic rocks of Mt. Konjuh. Prehnite<br />
occurences were found in the feldspar-carrying peridotites on the road between<br />
Olovo and Kladanj, in the olivine gabbros near the village of Bjeliš (Stupčanica
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
creek) and in porphyrric diabases of Blizanci. Brajdić (1964) made microscopic<br />
measurements of prehnite in the gabbro-pegmatites from Bjeliš. Here prehnite is an<br />
accessory constituent of 1-2 mm thick veins.<br />
Šibenik-Studen and Trubelja (1971) provide comparatively detailed<br />
determinations of prehnite occuring near Kovačići village on the eastern flanks of Mt.<br />
Konjuh. Prehnite is associated with thomsonite, in the form of white incrustations or<br />
veinlets within diabase-dolerites. These veinlets can be up to 1 cm thick.<br />
A quantitative chemical analysis of prehnite from Kovačići yielded following results:<br />
SiO 2<br />
= 40.41; Al 2<br />
O 3<br />
= 25.13; Fe 2<br />
O 3<br />
= 1.87; FeO = 0.19; MnO = 0.02;<br />
MgO = traces; CaO = 27.69; Na 2<br />
O = 0.28; H 2<br />
O = 5.06<br />
Total = 100.65<br />
The structural formula, based on 24 (O,OH) ions is:<br />
(Ca 4.100<br />
Na 0.083<br />
Al 3.678<br />
Fe 3+ 0.199 Fe2+ 0.025 ) (Al 0.406 Si 5.594 ) O 20 (OH) 4.665<br />
Trubelja et al. (1974, 1975, 1975a) determined several associations of veintype<br />
minerals in rocks outcropping on the eastern and southeastern flanks of Mt.<br />
Konjuh, using powder x-ray diffraction, IR-spectroscopy, thermal and chemical<br />
analysis. Their findings complement earlier determinations of prehnite as a very<br />
common hydrothermal vein mineral in these rock types (particularly in outcrops on<br />
the Olovo – Kladanj road). Associations with laumontite, low-temperature albite,<br />
epidote, calcite, tremolite, chlorite and clinozoisite have been observed. Prehnite in<br />
rocks of the Mt. Konjuh – Krivaja complex is also mentioned in other publications,<br />
but their authors provide no further data on this mineral (Ristić et al. 1967).<br />
Prehnite occurences were also identified in amphibolites of the Mt. Konjuh –<br />
Krivaja igneous-metamorphic complex (Pamić and Kapeler 1970; Pamić et al. 1973).<br />
c) Mt. Ozren<br />
Trubelja and Pamić (1965), Pamić (1973), Trubelja et al. (1974, 1975,<br />
1975a) determined prehnite to be a common constituent of veins in basic igneous<br />
rocks (mainly diabases and spilites) of Mt. Ozren. Monomineralic veins carrying<br />
prehnite were found at Brezici, Gornji Rakovac, Donji Rakovac, Omrklica creek and<br />
on the road between Gornji Rakovac and Gornja Bukovica. Associations of prehnite<br />
and calcite, albite and chlorite were found at Jadrina creek and on the road between<br />
Gornji Rakovac and Gornja Bukovica (here, the paragenesis consists of prehnite,<br />
rhipidolite and datolite). The IR-spectra of some of these mineral associations are<br />
shown in Figure 16.<br />
245
SILICATES<br />
246<br />
Figure 16. IR-spectra of prehnite from Mt. Ozren (Trubelja et al. 1975a)<br />
1. prehnite with a small amount of calcite (Brezici)<br />
2. prehnite (Gornji Rakovac)<br />
3. prehnite with albite (Jadrina creek)<br />
4. prehnite with chlorite (road G. Rakovac – G. Bukovica)<br />
5. prehnite (Brezici)<br />
Table 58. Powder XRD data for prehnite from Mt. Ozren (Gornji Rakovac) (Trubelja et al.<br />
1975a)<br />
No. d (Å) I No. d (Å) I<br />
1 5.2522 2 26 1.65564 3<br />
2 4.6082 3 27 1.63453 2<br />
3 4.1329 1 28 1.59562 1<br />
4 3.5256 4 29 1.56502 1<br />
5 3.4636 9 30 1.54225 4<br />
6 3.2950 6 31 1.53252 3<br />
7 3.2643 2 32 1.50069 2<br />
8 3.0623 10 33 1.47834 1<br />
9 2.8036 4 34 1.45517 1<br />
10 2.7401 1 35 1.44147 3<br />
11 2.6232 2 36 1.41389 1<br />
12 2.5509 10 37 1.40225 3<br />
13 2.3559 5 38 1.37822 2<br />
14 2.3060 2 39 1.36973 2<br />
15 2.2012 1 40 1.34133 1<br />
16 2.1146 1 41 1.31945 1
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
17 2.0668 4 42 1.30994 1<br />
18 2.04550 1.5 43 1.29022 2<br />
19 1.98602 1 44 1.23269 1<br />
20 1.93250 4.5 45 1.20231 1.5<br />
21 1.84272 3 46 1.17835 2<br />
22 1.76612 8 47 1.15923 1<br />
23 1.75226 1.5 48 1.14259 1<br />
24 1.71331 1 49 1.12238 1<br />
25 1.69571 2 50 1.08360 2.5<br />
d) The area between the rivers Vrbas and Bosna<br />
Several authors have determined prehnite in basic igneous and metmorphic<br />
rocks outcropping in the area between the rivers Vrbas and Bosna – Džepina (1970),<br />
Đorđević and Stojanović (1972, 1974), Đurić and Kubat (1962), Kubat (1964), Majer<br />
(1962), Pamić (1969a), Trubelja, Šibenik-Studen and Sijarić (1974, 1975, 1975a).<br />
Prehnite was likewise determined in granites and syenites (Đorđević and Mojičević<br />
1972; Pamić and Tojerkauf 1970).<br />
Monomineralic prehnite veins occur in diabases (at the edges of the serpentine<br />
complex) i.e. in the Usora river valley, on the Doboj – Teslić road. In samples taken<br />
from the Lelah – Teslić road prehnite is associated with analcime and calcite (XRD,<br />
DTA and IR-spectroscopic determinations). Similar prehnite veins in amphibolites<br />
are found in the Vrbanja river valley, near Čelinac (Trubelja et al., 1974, 1975a).<br />
Đorđević and Stojanović (1972) determined amygdaloidal prehnite and<br />
natrolite in diabases from Bojići near Banja Luka. Needlelike natrolite crystals<br />
often grow on a prehnite substrate. The prehnite is pale-green in colour, with a<br />
waxy lustre. The x-ray diffraction lines of this prehnite are: d (Å) 3.07 (100), 2.80<br />
(15), 2.55 (80), 2.47 (2), 2.37 (5) correspond well with published literature data<br />
(ASTM-card 7-333).<br />
Džepina (1970) determined prehnite in alkaline metamorphic rocks (some of<br />
which are garnet-bearing) on the southern flanks of Mt. Borja. This author believes<br />
that the prehnite is an alteration product of alkaline plagioclase, since they both<br />
occur in the same parageneses. He notes that veins carrying prehnite and plagioclase<br />
cut through all other mineral formations, implying their young age of formation.<br />
e) Mt. Kozara<br />
Golub (1961), Trubelja (1966a), Trubelja et al. (1974, 1975, 1975a)<br />
determined prehnite as a common mineral constituent in basic igneous rocks of<br />
Mt. Kozara (especially its northern and southern flanks). Prehnite is particularly<br />
prominent in altered gabbro-diabases, to be found on the Mrakovica – Kozarac road,<br />
247
SILICATES<br />
where it forms monomineralic veins or parageneses with other minerals (analcime<br />
and calcite). The IR-spectra of these prehnites are shown in Figure 17.<br />
Figure 17. IR-spectra of prehnites from Mt. Kozara (Mrakovica – Kozarac) road<br />
(Trubelja et al. 1975a)<br />
2. Prehnite in products of Triassic-age magmatic events<br />
Basic igneous rock of Triassic age are to be found in several areas in<br />
Bosnia and Hercegovina. These rocks often contain prehnite as a common or even<br />
important mineral constituent, both in intrusive and extrusive magmatics. Such rocks<br />
have important outcrops near Vareš – Atanacković et al. (1968), Đorđević (1958),<br />
Karamata and Pamić (1964), Petković (1961/62), Trubelja et al. (1974, 1975a).<br />
Marić (1927), Pamić (1960, 1960a, 1961a, 1961b, 1962, 1969), Pamić and<br />
Papeš (1969), Trubelja and Miladinović (1969), Trubelja and Slišković (1967),<br />
Trubelja, Šibenik-Studen and Sijarić (1974, 1975, 1975a) provide data on the<br />
occurence of prehnite in the areas of Konjic, Jablanica, Prozor, Kupres and within the<br />
Ilidža – Kalinovik – Tjentište zone. Marić (1927) made microscopic measurements of<br />
prehnite in the gabbro rocks from Jablanica. Here the prehnite is of secondary origin,<br />
occuring within veins in the gabbro. Prehnite is associated with calcite, hornblende,<br />
chlorite, titanite and quartz. Prehnite grains display complete cleavage along the<br />
base. Measured refractive indices are Nz = 1.6482, Ny = 1.62575, Nx = 1.61470<br />
(Na-lamp). Maximum birefringence Nz – Nx = 0.03181. The 2V angle is large.<br />
Pamić (1961a, 1961b) also made microscopic determinations of prehnite in<br />
rocks from the Jablanica and Prozor areas, including basalts and marbles from the<br />
contact zone. This author found prehnite to be associated with spilites i.e. with albite<br />
phenocrysts. Calcite and sericite often occur together with prehnite. The prehnite<br />
associated with spilites has a 2V angle of +64°.<br />
248
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Table 59. Powder x-ray diffraction data for prehnite from Vareš (Trubelja et al. 1975a)<br />
No. d (Å) I No. d (Å) I<br />
1 5.2522 3 27 1.59600 1<br />
2 4.6177 4 28 1.56405 1<br />
3 4.1291 1.5 29 1.54271 5<br />
4 3.5092 5 30 1.53023 4<br />
5 3.4530 10 31 1.50200 1<br />
6 3.2903 8 32 1.47707 1<br />
7 3.2456 3 33 1.45881 1<br />
8 3.0521 10 34 1.44107 3<br />
9 2.8002 4 35 1.40299 2.5<br />
10 2.6173 2.5 36 1.37573 2.5<br />
11 2.5509 10 37 1.34200 1.5<br />
12 2.3523 5 38 1.31626 1<br />
13 2.3094 2 39 1.30838 1<br />
14 2.1351 1.5 40 1.28872 2.5<br />
15 2.1118 1.5 41 1.26317 1<br />
16 2.0632 4 42 1.24025 1<br />
17 2.04200 1.5 43 1.23321 1<br />
18 1.98684 1 44 1.20154 1.5<br />
19 1.92940 5 45 1.17763 3<br />
20 1.84133 3 46 1.15747 1.5<br />
21 1.76549 9 47 1.14193 1.5<br />
22 1.75039 1 48 1.12280 1.5<br />
23 1.71212 1 49 1.09984 1<br />
24 1.69745 2 50 1.08286 1<br />
25 1.65509 3 51 1.06575 3.5<br />
26 1.63453 2<br />
Đorđević (1958) determined prehnite in gabbro from the Vareš area. Prehnite<br />
is associated with other minerals of secondary origin – uralite, chlorite, epidote,<br />
zoisite, albite, kaolinite, sericite and serpentine. Trubelja et al. (1974, 1975, 1975a)<br />
identified prehnite and pumpellyite in veins within altered melaphyres around Vareš.<br />
The prehnite crystals are up to several millimeters in size, and form amygdaloidal<br />
structures in the melaphyre. This finding is significant as it indicates the prehnitepumpellyite<br />
metamorhic stage.<br />
Powder XRD and IR-spectroscopy were used to determine prehnite in a basic<br />
igneous rock from Mt. Zvijezda. This mineral was also determined in a melaphyre<br />
sample obtained from the mineralogical collection of the Country Museum in<br />
Sarajevo. Here, prehnite is associated with albite and quartz.<br />
3. Origin of prehnite<br />
We have already described the occurences of prehnite and associated<br />
minerals in a variety of rocks belonging to the Bosnian serpentine zone (BSZ) or<br />
the Triassic-age igneous complex. Based on our own investigations, as well as data<br />
249
SILICATES<br />
obtained from the cited literature references, we may conclude that the prehnite is<br />
either associated with the hydrothermal phase, or is the alteration product of alkaline<br />
plagioclase minerals. The occurence of prehnite in amphibolites is an indication of<br />
its possible origin with regional metamorphic proceses.<br />
Hydrothermal prehnite usually occurs in the form of monomineralic (sometimes<br />
associated with other hydrothermal minerals) in veins, filling up older fractures in the<br />
host rocks (gabbro, diabase, spilite etc). The prehnite must have been deposited from<br />
hydrothermal solutions with high concentrations of Ca, Al and silicic acid.<br />
Formation of prehnite by alteration of alkaline plagioclases often results in<br />
prehnite pseudomorphoses of these feldspars. The alteration processes can also be<br />
understood in terms of hydrothermal metasomatic reactions.<br />
The occurence of prehnite in amphibolites (representing products of regional<br />
metamorphism) also implies its crystallization from Al, Ca, Si-enriched solutions at<br />
elevated temperatures.<br />
Generally, the origin of prehnites in Bosnia and Hercegovina is frequently<br />
associated with several processes leading to the formation of complex parageneses<br />
with secondary minerals like albite, serpentine, chlorite, epidote, clinozoisite, calcite<br />
and zeolite minerals.<br />
SEARLESITE<br />
NaB [Si 2<br />
O 5<br />
] (OH) 2<br />
Crystal system and class: Monoclinic, sphenoidal class.<br />
Lattice ratio: a : b : c = 1.1286 : 1 : 0.6957 β = 93° 56’<br />
Cell parameters: a o<br />
= 7.97, b o<br />
= 7.05, c o<br />
= 4.90 Z = 1<br />
The formula of searlesite is sometimes written as Na 2<br />
B 2<br />
[Si 4<br />
O 10<br />
│(OH) 4<br />
] or<br />
NaB[Si 2<br />
O 6<br />
] x H 2<br />
O (Ramdohr and Strunz 1967). The mineral was first determined<br />
in a core from Searles Lake, California, taken by John W. Searles, and named after<br />
this californian pioneer.<br />
Properties: see text concerning the Lopare deposit.<br />
A u t h o r s: Barić (1966, 1966b, 1966c), Barić and Jovanović (1966),<br />
Jovanović (1975), Č. Jovanović and O. Jovanović (1966).<br />
Deposits of searlesite occur very rarely. Barić and coauthors investigated<br />
the occurrence of this mineral in Bosnia and Hercegovina – Barić (1966, 1966b,<br />
1966c), Barić and Jovanović (1966). At Lopare, 15 km northeast of Tuzla, on the<br />
250
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
northern flanks of Mt. Majevica, searlesite occurs in two deposits. The deposits are<br />
not far from each other, but nevertheless separated. The first deposit is located in the<br />
creek Duboki Dol. This creek joins the Gnjica river which flows through Lopare.<br />
The searlesite occurs here as four 2-4 cm thick layers in a stratified marl. It needs<br />
to be said that this deposit was frequently referred to as the Trifunove vode deposit,<br />
which is incorrect.<br />
The second searlesite deposit is located south of the Duboki Dol creek.<br />
Near the crossing of the road Tuzla – Brčko with the road towards Veselinovci, the<br />
searlesite is locate within a complex of argillaceous schists in the Mijajlov Potok<br />
creek. The searlesite forms elliptical lenses about 4 x 10 cm in size. Both the marl<br />
and argillaceous schist host-rocks are intercalated with layers of tuff and tuff-bearing<br />
sandstone. Barić and Jovanović (1966) maintain that these sediments are of Miocene<br />
age (Burdigalian – Helvetian).<br />
Some veins and fissures within the host rocks contain small searlesite crystals<br />
which grow in a partially free space, with well developed crystal forms on the terminal<br />
side. The crystals are elongated along [001] with an overall platelike habit parallel to<br />
(100) – see Figure 18. The (100) form shows fine striations parallel to [001]. The<br />
crystals are mostly 2-3 mm long, the largest one found was 6 mm long.<br />
Goniometric measurements were done on 26 searlesite crystals (Barić<br />
1966). Even though the crystals were small, measurements on a Goldschmidt type<br />
2-circle reflection goniometer were easily performed. Barić determined the presence<br />
of following crystal forms on searlesite from Lopare: c {001}, b {010}, a {100}, i<br />
{210}, m {110}, z {120}, e {011}, s {101}, y {201}, q {-201}, p {-101}, f {111}, n<br />
{-111}, g {121}, h {331} and l {102} – a total of 16 crystal forms.<br />
Figure 18. Searlesite crystals from Lopare (Barić 1966)<br />
A number of the crystal forms determined on the material from Lopare.<br />
Earlier studies on searlesite crystal from USA determined the presence of these<br />
crystal forms only: b {010}, a {100}, m {110}, s {101}, y {201}, l {102}. This<br />
means that the forms<br />
251
SILICATES<br />
c {001}, i {210}, z {120}, e {011}, q {-201}, p {-101}, f {111}, n {-111}, g {121},<br />
h {331} have for the first time been identified on the searlesite from Lopare. The<br />
crystal form l {102} has been determined as a cleavage plane in both cases.<br />
The lattice ratio for searlesite was calculated from the polar coordinates of<br />
those crystal planes which had the best reflection signals (Barić 1966)<br />
a : b : c = 1.1286 : 1 : 0.6957 β = 93° 56’<br />
This ratio is in very good agreement with literature data for searlesite (Fahey<br />
and Axelrod 1950). Barić was also able to determine the relationships between<br />
geometrical and optical properties (Barić 1966, 1966b). The optic axial plane is in<br />
a normal symmetrical position. The principal vibrational direction Z corresponds to<br />
the [010] axis. The principal vibrational direction X is inclined with respect to the<br />
[001] axis – the inclination angle is 32° 23’. The refractive indices were determined<br />
on a thin section, carefully polished perpendicular to the vibrational direction Y. The<br />
measurement was done in sodium light (at 18°C) using a Klein-type refractometer<br />
Nz = 1.5351 Ny = 1.5306 Nx = 1.5226<br />
Furthermore, refractive indices were also measured on two cleavage planes parallel<br />
to (100)<br />
Nz = 1.5350 Nx’ = 1.5246<br />
Nz = 1.5349 Nx’ = 1.5224<br />
Maximum birefringence (and the partial Nz – Nx’ values) were determined<br />
on five cleavage planes parallel to (100), using a Berek-type compensator<br />
Nz – Nx = 0.0129 Nz – Nx’ = 0.0106<br />
The optic axial angle was measured on a rotating stage microscope.<br />
Somewhat thicker sections were used for this purpose, so that both axes could be<br />
measured. The mean value of ten measurements is -2V = 73° 53’. A weak r < v<br />
dispersion was determined in white light.<br />
Pure searlesite material was selected for quantitative chemical analysis<br />
which yielded following results (analyst Lj. Barić):<br />
SiO 2<br />
= 58.72; B 2<br />
O 3<br />
= 16.99; Fe 2<br />
O 3<br />
= 0.12; Na 2<br />
O = 15.16; K 2<br />
O = ---; CaO = ---;<br />
MgO = 0.02; H 2<br />
O +105 = 8.92; H 2<br />
O -105 = 0.08; Total = 100.01<br />
Searlesite is easily soluble in dilute hydrochloric acid. The qualitative test<br />
for the borate ion ws positive. The mineral melts under the blow pipe into a vitreous<br />
globule. The density of the minerals was determined using the pycnometric method<br />
(d = 2.462 g/cm 3 at 4°C).<br />
Powder x-ray diffraction was done using a Philips diffractometer, using<br />
CuKα radiation. The diffraction pattern of the Lopare searlesite, given in Table 60,<br />
252
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
corresponds well to the searlesite reference ASTM-card No. 6-0037 (which is for<br />
searlesite from Wyoming, USA).<br />
At Lopare, the searlesite occurs in association with kalcite, opal, pyrite and<br />
trona. Opal is occasionally present in substantial quantities, and can contain radial<br />
spherulites (up to 0.5 mm in size) of searlesite. The free terminal ends of individual<br />
searlesite crystals are sometimes covered with thin layers of hyalite opal.<br />
Table 60. Powder x-ray diffraction data for searlesite from Lopare<br />
Searlesite (Lopare) Searlesite ASTM 6-0037<br />
d (Å) I d (Å) I<br />
8.02 vvs 8.01 100<br />
5.32 w 5.32 10<br />
4.33 m 4.31 30<br />
4.05 s 4.06 50<br />
3.97 vs 3.98 20<br />
3.68 vw 3.70 10<br />
3.54 m 3.54 30<br />
3.48 vs 3.48 40<br />
3.24 s 3.24 40<br />
3.20 vs 3.21 30<br />
2.99 m 2.99 20<br />
2.92 ms 2.92 30<br />
2.75 m 2.76 20<br />
2.65 ms 2.66 30<br />
2.49 m 2.49 10<br />
2.46 mw 2.45 20<br />
2.40 m – broad 2.41 10<br />
2.39 10<br />
2.26 mw 2.28 10<br />
2.16 w 2.16 5<br />
2.13 w 2.12 10<br />
2.06 vw 2.06 10<br />
2.02 vw 2.02 5<br />
1.989 m – broad 1.992 10<br />
1.978 10<br />
1.949 vw 1.945 5<br />
1.914 m – broad 1.916 10<br />
1.896 10<br />
1.827 m 1.825 20<br />
1.765 mw 1.765 10<br />
1.746 mw 1.746 5<br />
1.686 vw 1.690 5<br />
1.669 vvw ---<br />
1.647 vvw 1.647 5<br />
1.631 vvw 1.632 5<br />
1.617 vvw 1.616 5<br />
1.605 vw 1.605 5<br />
1.592 vw 1.592 5<br />
1.555 m 1.554 20<br />
vvs = very very strong; vs = very strong; vvw = very very weak; w = weak; vw = very weak;<br />
m = medium; ms = medium strong; mw = medium weak<br />
253
SILICATES<br />
The dark colour of the host rocks (marls and argillaceous schists) is caused<br />
by the presence of organic matter. The organic matter can cause a yellow or brown<br />
surface colouration of searlesite. The same effect has been observed for the searlesite<br />
from the Green-River formation in Wyoming, USA.<br />
The origin of searlesite at Lopare can be explained by the action of boronenriched<br />
hydrothermal waters on silicic acid contained in the volcanic tuffs. A<br />
similar explanation was provided for the origin of searlesite from Esmeralda County,<br />
Nevada, USA (Foshag 1934). The present opal and hyalite is a strong indication that<br />
‘free’ silicic acid was available in the depositional environment.<br />
Jovanović (1975) mentions briefly an occurrence of searlesite in the halite<br />
deposit at Tuzla.<br />
Use: the searlesite deposit in the Green-River formation in USA has<br />
commercial significance. Searlesite crystals up to 15 cm long were found in this<br />
deposit. The material is used for production of borax and other perborate formulations<br />
for industrial and medicinal use.<br />
254<br />
NEPHELINE<br />
KNa 3<br />
[AlSiO 4<br />
] 4<br />
The only information on nepheline in Bosnia and Hercegovina was provided<br />
by Primics (1881). This author mentions two deposits – one at Duboštica near Vareš<br />
(where nepheline occurs in garnet-bearing amphibole schists), and the other one in<br />
the Žepče – Maglaj area, on the left bank of the Bosna river. Here, nepheline occurs<br />
as small crystals in biotite-quartz trachytes.<br />
ANALCIME<br />
Na [AlSi 2<br />
O 6<br />
] x H 2<br />
O<br />
Crystal system and class: Cubic, hexaoctahedral class.<br />
X-ray data: d 3.43 (100) 5.61 (80) 2.94 (70)<br />
IR-spectrum: 415 450 620 746 775 862 1040 1115 1635 3620 cm -1<br />
A u t h o r s: Đorđević and Stojanović (1972, 1974), Sijerčić, Pamić,<br />
Jovanović and Šljukić (1974), Trubelja (1962), Trubelja, Šibenik-Studen and Sijarić<br />
(1974, 1975, 1975a and 1976).<br />
There is not much information on the occurrence of analcime in Bosnia and<br />
Hercegovina. According to available literature data, analcime has been determined<br />
in basic igneous rocks of the Bosnian serpentine zone (BSZ) and in sediments of the<br />
salt deposit at Tuzla.
1. The Bosnian serpentine zone (BSZ)<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Trubelja (1962) made the first microscopic determination of analcime in<br />
biotite-spilites from Torić creek, near Bosanski Novi. Here, small amygdaloids<br />
are filled with analcime and calcite. In thin section the analcime displays a low<br />
birefringence and grey interference colours. The refractive index of analcime is<br />
lower than that of both calcite or Canada balsam (observation is based on the Becke<br />
line movements).<br />
The origin of analcime in these rocks is linked to postmagmatic hydrothermal<br />
processes which caused the albitization of plagioclases and the spilitization of basic<br />
rocks. Analcime is also found to form pseudomorphs over plagioclase.<br />
Đorđević and Stojanović (1972) mention analcime occurrences in rocks<br />
within the BSZ. Unfortunately, the authors do not give locations of these occurrences.<br />
In their paper published 2 years later, Đorđević and Stojanović (1974) determined<br />
analcime, in association with laumontite and datolite, in diabase rock at Bojići, near<br />
Hrvaćani, on the southern flanks of Crni Vrh. The diabases at Višegrad (close to the<br />
railway station) also contain some analcime, chlorite and anorthite (powder XRD<br />
determination). Analcime was also determined in dacites, andesites and tuffs around<br />
Srebrenica, Bratunac and Zvornik.<br />
Trubelja et al. (1974, 1976) investigated the mineralogy of veins in basic<br />
rocks of the BSZ finding that analcime frequently occurs within zeolite parageneses.<br />
An association of analcime with thomsonite, determined by powder XRD and IRspectroscopy,<br />
was identified in rock from the Karaula locality, on the southeastern<br />
flanks of Mt. Konjuh. The diabases at Gradina (Doboj) analcime occurs together with<br />
natrolite and calcite. The diabase-dolerites of Mt. Kozara (the Kozarac – Mrakovica<br />
sector) contain a paragenesis of analcime, prehnite, calcite and thomsonite.<br />
2. Analcime occurrences in the Tuzla salt deposit<br />
Sijerčić et al. (1974) reported on analcime-bearing aggregates (which they called<br />
analcimolites) within the sedimentary series of the Tuzla salt deposit. Analcime<br />
was determined by powder x-ray diffraction. In thin section, euhedral analcime<br />
crystals were identified. Analcime grains are completely isotropic. An outcrop of<br />
this ‘analcimolite’ rock was discovered near Mlič hill.<br />
255
SILICATES<br />
SANIDINE<br />
K [AlSi 3<br />
O 8<br />
]<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.657: 1 : 0.551 β = 115° 59’<br />
Cell parameters: a o<br />
= 8.56, b o<br />
= 13.03, c o<br />
= 7.175 Z = 4<br />
Properties: sanidine is a typical high-temperature alkaline feldspar with a partially<br />
ordered arrangement of Al and Si ions. It commonly occurs in young effusive<br />
rocks, sometimes as large, distinct phenocrysts. Due to rapid cooling of the host<br />
rock, sanidine normally retains high-temperature optical constants. Perfect cleavage<br />
parallel to {001}, good parallel to {010}. Hardness = 6. Specific gravity = 2.56.<br />
Sandine is normally colourless and transparent. Vitreous lustre. Resistant to acids,<br />
except hydrfluoric acid. Refractive indices are lower than those of Canada balsam.<br />
Birefringence is low.<br />
IR-spectrum: 415 430 546 585 638 728 778 1040 1060 1130 cm -1<br />
A u t h o r s: Barić (1966), Dangić (1971), John (1880), Majer (1961),<br />
Pamić (1962, 1969), Pamić, Dimitrov and Zec (1964), Pamić and Papeš (1969),<br />
Paul (1879), Ramović (1961, 1962), Simić (1968), Šibenik-Studen and Trubelja<br />
(1967), Tajder (1953), Trubelja (1970a, 1971a, 1972), Trubelja and Pamić (1956,<br />
1965), Varićak (1966)<br />
According to available literature references, sanidine has not a very wide<br />
distribution in rocks in Bosnia and Hercegovina. It has been determined in Tertiaryage<br />
igneous rocks at Srebrenica, as well as in the Bosna river valley and some other<br />
localities. Triassic rocks have also been mentioned to contain sanidine. We believe<br />
that some data on sanidine will have to be revised, since it has been obtained only by<br />
microscopic measurements.<br />
1. Sanidine in Tertiary-age igneous rocks<br />
C. M. Paul (1879) provides the earliest information on the occurrence of<br />
sanidine in trachytes of the Maglaj fortress. Sanidine is present as distinct crystals,<br />
some of which show twinning according to the Carlsbad law. The same sanidine was<br />
investigated also by other authors – John (1880), Pamić, Dimitrov and Zec (1964),<br />
Trubelja and Pamić (1956, 1965).<br />
The sanidine-bearing dacites from Brusnička Rijeka contains distinct,<br />
idiomorphic sanidine crystals (as phenocrysts), with clearly visible cleavage planes<br />
parallel to (010). The sanidine was measured on a rotating-stage microscope. The<br />
-2V angle varies in the range 27.5° to 30°. This is evidence for sanidine rather than<br />
256
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
anorthoclase, as could be deduced from the Nikitin diagram. The sanidine crystals<br />
have many inclusions, primarily andesine. Sanidine is also present in the matrix<br />
of the rock.<br />
Majer (1961) believes that sanidine in present the matrix of the dacitic rocks<br />
from the Blatnica creek near Teslić. The authors conclusion is based on chemical<br />
analysis of the rock.<br />
Barić (1966) made microscopic determinations of sanidine in tuffs from the<br />
Livno area. The grains are completely transparent, and their RI’s are lower than<br />
those of Canada balsam. Twinning is according to the Carlsbad law. Birefringence is<br />
low (Nz – Nx = 0.0061).<br />
Sanidine in dacites and similar rocks from Srebrenica has been investigated<br />
by several researchers – Dangić (1971), John (1880), Ramović (1961, 1962), Tajder<br />
(1953), Trubelja (1971a, 1972). The largest amount of information can be found in<br />
the publication by M. Tajder (1953). According to this author, sanidine occurs as<br />
phenocrysts in dacites from the Kiselica creek, in the biotite-dacite from the village<br />
of Ažlice and in the amphibole-dacites from Srebrenica. Based on chemical analyses<br />
of these rocks, the author maintains that some sanidine may also be present in the<br />
rock matrix. The sanidine from Kiselica creek (grain size 0.5 x 0.7 mm) has a low<br />
birefringence, uneven extinction and a very small optic axial angle (2V = -10°) so<br />
that it sometimes resembles a uniaxial mineral. Sanidine in other mentioned rocks<br />
has similar microphysiographic properties. The amphibole-dacites from Srebrenica<br />
contains larger sanidine crystals (5-12 mm), pink in colour and with clearly visible<br />
cleavage. It is present in the rock in the form of untwinned, single crystals. The<br />
-2V angle lies in the range 10-20°. Sanidine crystals contain numerous inclusions of<br />
amphibole, plagioclase, quartz, apatite and calcite.<br />
2. Sanidine in Triassic-age igneous rocks<br />
Pamić (1962, 1969), Pamić and Papeš (1969), Simić (1968), Šibenik-Studen<br />
and Trubelja (1967) made microscopic determinations of sanidine in Triassic-age<br />
volcanic rocks – in the Ilidža – Kalinovik zone, at Kupre, in the Vrbas river valley<br />
and in K-rich effusive rocks near Sarajevo. We wish to point out that microscopic<br />
determinations of sanidine in these rock were rather difficult to perform, so that the<br />
data should be treated with some caution. Further research, using complementary<br />
methods is obviously needed.<br />
3. Sanidine in rhyolite from Mt. Motajica<br />
Varićak (1966) believes that the K-feldspar, contained in the rhyolite from<br />
Mt. Motajica, is sanidine. This material is very weathered, and this result must also<br />
be regarded with caution.<br />
257
SILICATES<br />
ORTHOCLASE<br />
K [AlSi 3<br />
O 8<br />
]<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.659 : 1 : 0.553 β = 116° 01’<br />
Cell parameters: a o<br />
= 8.562, b o<br />
= 12.996, c o<br />
= 7.193 Z = 4<br />
Properties: orthoclase is a low-temperature feldspar, formed during the process of<br />
slow magma cooling. It is a ubiquitous constituent of acidic and neutral igneous<br />
rocks (granites, syenites). Other physical properties are similar to those of sanidine.<br />
Colour is usually white to pink.<br />
X-ray data: d 3.29 (10) 1.81 (9) 4.25 (7)<br />
IR-spectrum: 430 (460) 542 586 647 727 763 1040 1150 cm -1<br />
A u t h o r s: Foullon (1893), John (1880), Jovičić (1891), Katzer (1924,<br />
1926), Kišpatić (1897, 1900), Koch (1908), Majer and Jurković (1957, 1958), Marić<br />
(1927), Pamić (1957, 1960a), Pilar (1882), Primics (1881), Simić (1964, 1968),<br />
Simić, V. (1956), Šćavničar and Jović (1962), Trubelja (1963a), Trubelja and Pamić<br />
(1957), Tućan (1930, 1957), Varićak (1955, 1957, 1966), Vujanović (1962).<br />
Up to now, orthoclase has not been very well investigated in rocks from<br />
Bosnia and Hercegovina. The available data indicate that this mineral is most<br />
common in rocks from Mt. Motajica, where it was first determined by John (1880).<br />
Occurrences of orthoclase have also been identified in rocks from Mt. Prosara,<br />
as well as in gabbros, diorites and other products of Triassic-age volcanic events.<br />
Orthoclase is an important constituent of the ‘red granite’ which occurs in the Maglaj<br />
area in the form of pebbles. Some sedimentary rocks also contain orthoclase.<br />
258<br />
1. Orthoclase in rocks of Mt. Motajica and Mt. Prosara<br />
John (1880) made first microscopic determinations of orthoclase which is an<br />
essential mineral in muscovite granites from the Kobaš area at Mt. Motajica. Pilar<br />
(1882) provides a description of granites from the menitoned area, agreeing that<br />
orthoclase is their essential mineral constituent.<br />
Koch (1908) studied the Mt. Motajica rock-series in detail. According to this<br />
author, who made a very significant contribution to microscopic determinations of<br />
rock-forming minerals in this area, orthoclase is a prominent mineral in muscovite<br />
granites from Vlaknica, near Kobaš, as well as from Brusnik. The Vlaknica granitic<br />
pegmatites contain large orthoclase crystals, in association with quartz, mica,<br />
microcline and plagioclase. For the orthoclase in the granites from Veliki Kamen<br />
(Vlaknica), Koch determined several microphysiographic properties. This orthoclase<br />
displays good pinacoidal cleavage and a conspicuous zonar structure. Twins<br />
according to the carlsbad law can be frequently be observed. Polysynthetic twinning
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
with microcline and plagioclase is also present. Orthoclase decays into kaolinite,<br />
muscovite and other alteration products. Orthoclase often contains inclusions of<br />
hematite, apatite, biotite, tourmaline, zircon and epidote.<br />
Orthoclase can frequently be found in gneisses. It occurs in biotite-bearing<br />
granite-gneisses at Židovski potok, the muscovite gneisses and pegmatites of the<br />
Studena Voda creek, and biotite gneisses of Osovica creek near Šeferovac.<br />
Katzer (1924, 1926) notes the presence of orthoclase in rocks of Mt.<br />
Motajica, and makes reference to microscopic determinations done by Koch.<br />
Varićak (1966) published a treatise on the petrology of Mt. Motajica, with<br />
a substantial number of microscopic determintions of orthoclase. Varićak notes<br />
the apparent symmetry change of orthoclase from monoclinic to triclinic, and its<br />
transformation to microcline. According to this author, in normal granite orthoclase<br />
has a -2V angle = 62° (corresponding to ca. 32% albite). In the so called ‘frozenedge<br />
granite’ orthoclase shows signs of exsolution of albite, kaolinite and sericite.<br />
Orthoclase is also present in leucocratic granite, aplite and granite-porphyres<br />
(microperthite). In these rocks, the 2V angle of orthoclase shows large variations,<br />
within the -62° to -82° range of values (the average ab content is around 35%).<br />
Orthoclase in lamprophyres has a -2V angle = 64°. Twinning according to the<br />
Carlsbad and Manebach laws is frequent and such crystals have a -2V angle of 60-64°<br />
(32% ab). Contactolites of sedimentary origin contain orthoclase which often has an<br />
uneven, undulating extinction (2V = -83°).<br />
Igneous rocks from Mt. Prosara, which Katzer (1924, 1926) calles<br />
microgranite-porphyres, contain feldspars mainly as orthoclase. More recent<br />
investigations have not confirmed the occurrence of orthoclase in these rocks.<br />
2. Orthoclase in Triassic-age igneous rocks<br />
The presence of orthoclase in Triassic-age volcanic rocks has been noted<br />
by numerous researchers – Majer and Jurković (1957, 1958), Marić (1927),<br />
Pamić (1957, 1960a), Pilar (1882), Simić (1964, 1968), Trubelja (1963a) and<br />
Vujanović (1962).<br />
Majer and Jurković (1957, 1958) determined orthoclase to be an essential<br />
mineral constituent of diorites from Kopile, south of Travnik (the Bijela Gromila<br />
massif). Orthoclase is here usually associated with andesine and labradorite.<br />
Orthoclase crystals are usually fresh and single (not twinned), although some grains<br />
display relicts of zonar structure. The RI is lower than 1.54, and the -2V angle varies<br />
in the range 58-71°.<br />
259
SILICATES<br />
Marić (1927) determined orthoclase in some magmatic differentiates of the<br />
Jablanica rock series.<br />
Trubelja (1963) identified orthoclase and Na-orthoclase in amphibolegranites<br />
from Čajniče by microscopic measurements. The -2V angle varies in the<br />
range 63-81°. Some microperthite is present (intergrowths of orthoclase with albite).<br />
The orthoclase is generally weathered and altered to kaolinite and sericite.<br />
Pilar (1882) determined orthoclase as an essential constituent of the igneous<br />
rocks from the area of Jajce. The orthoclase is usually twinned according to the<br />
Carlsbad law, and shows signs of weathering and alteration.<br />
Pamić (1957, 1960a) and M. Simić (1964, 1968) determined orthoclase in<br />
rocks associated with the spilite-keratophyre series, near Sarajevo and Kalinovik.<br />
Vujanović (1962) mentions orthoclase associated with some manganese minerals<br />
(Čevljanovići).<br />
3. Other occurrences of orthoclase<br />
Kišpatić (1897, 1900) identified orthoclase in a pebble (red granite from<br />
Maglaj) he retrieved from the Mala Bukovica creek. Orthoclase is an essential<br />
constituent of this rock, and displays Carlsbad-law twinning. This rock was also<br />
studied by Varićak (1955), who notes the red colour of the orthoclase. In thin section,<br />
this orthoclase has a -2V angle between 67-73°. It forms microperthite intergrowths<br />
with albite. The crystals are single or twinned, usually strongly weathered and<br />
altered (to kaolinite). Orthoclase accounts for 25-30 vol. % of the granite pebble<br />
found in Jablanica creek.<br />
It is interesting to note early research of orthoclases, done by John (1880),<br />
Jovičić (1891) and Primics (1881). John described orthoclase in amphibolites from<br />
Rudo, in liparites from Mt. Vranica and in diorites from Kladanj. Jovičić noted the<br />
presence of orthoclase (or oligoclase) in microgranulites from Srebrenica. Primics<br />
made microscopic determinations of orthoclase contained in effusive rocks from the<br />
Maglaj – Žepče area, as well as in olivine gabbros from the Krivaja river valley and<br />
from the area of Duboštica.<br />
Šćavničar and Jović (1962) identified orthoclase and other feldspars in<br />
Eocene-age sandstones at Čorbin Han (Tuzla basin).<br />
Foullon (1893) and Katzer (1924, 1926) identified fresh and transparent<br />
feldspars (resembling adularia) in quartz-porphyres from the schist mountains of<br />
central Bosnia.<br />
260
MICROCLINE<br />
K [AlSi 3<br />
O 8<br />
]<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Crystal system and class: Triclinic, pinacoidal class.<br />
Lattice ratio: a : b : c = 0.660 : 1 : 0.556<br />
α = 90° 41’, β = 115° 59’, γ = 87° 30’<br />
Cell parameters: a o<br />
= 8.57, b o<br />
= 12.98, c o<br />
= 7.22 Z = 4<br />
Properties: microcline is a low-temperature feldspar, formed during the process of<br />
slow magma cooling. Like orthoclase, it is a ubiquitous constituent of acidic and<br />
neutral igneous rocks (granites, syenites). Other physical properties are similar to<br />
those of sanidine and orthoclase. Granitic pegmatites sometimes contain quite large<br />
microcline crystals.<br />
X-ray data: d 3.22 (10) 1.80 (8) 4.18 (6)<br />
IR-spectrum: 430 467 537 584 607 650 728 772 1018 1052 1085 1140 cm -1<br />
A u t h o r s: Jovanović (1957), Katzer (1924, 1926), Koch (1908), Pamić<br />
(1957), Šćavničar and Jović (1962), Trubelja and Pamić (1957), Tućan (1930, 1957),<br />
Varićak (1957, 1966).<br />
Microcline is not a very common mineral in rocks of Bosnia and Hercegovina,<br />
and not much has been written about this mineral. It occurs as an essential mineral<br />
constituent of various rocks from Mt. Motajica and Mt. Prosara. Some authors<br />
mention microcline in Triassic volcanic rocks, and in some sediments.<br />
1. Microcline in rocks from Mt. Motajica and Mt. Prosara<br />
F. Koch (1908) provides first data on the occurrence of microcline in granites<br />
from Mt. Motajica. In thin section the microcline has a texture characteristic for<br />
polysynthetic albite/pericline twinning. The muscovite granite from Brusnik also<br />
contains microcline.<br />
Katzer’s Geology of Bosnia and Hercegovina (1924, 1926) mentions only<br />
briefly microcline as a constituent of granites and aplites.<br />
Varićak (1966) determined microcline to be an essential mineral constituent<br />
of granite-type rocks (normal granite, leucocratic granite, aplite) from Mt. Motajica.<br />
Microcline is also contained in other igneous and metamorphic rocks (graniteporphyres,<br />
lamprophyres, pegmatites, gneisses) in which a ‘microclinization’<br />
orthoclase is present. Normal granite normally contains microcline with a gridiron<br />
(or quadrille) structure, although homogenous grains are also present. It displays<br />
good cleavage along (001) and (010), but also along (110) and (1-10). Carlsbad-type<br />
261
SILICATES<br />
twinning is frequently observed. The optic axial angle -2V varies in the range between<br />
75° and 84°. The 2V angle of microcline shows comparatively large variations also<br />
in other investigated rocks: -2V = 75-81° (aplites), 76-84° (granite-porphyres), 72-75°<br />
(lamprophyres), 69-85° (pegmatites), 78-86° (2-mica gneisses).<br />
Varićak (1957) determined microcline as an essential mineral constituent in<br />
gneisses and phyllites from Mt. Prosara.<br />
2. Microcline in Triassic volcanic rocks<br />
Little data is available on the occurrence of microcline in Triassic-age<br />
igneous rocks. Pamić (1957) determined microcline in rhyolites from the Ilidža –<br />
Kalinovik sector, near Ravne. The -2V angle varies in the range between 75° and<br />
88°. Using the Becke line method, it was determined that the RI of microcline are<br />
lower than the RI of Canada balsam. Larger microcline grains show the characteristic<br />
gridiron pattern. Microcline was also identified using the Nikitin diagram curves for<br />
angles between cleavage systems.<br />
Microcline is usually not a common mineral in acidic effusive igneous<br />
rocks. However, it has been identified in the rhyolites from Ravne, so it has probably<br />
formed by microclinization of some other feldspar. Jovanović (1957) determined<br />
microcline in granites from Mt. Prenj.<br />
3. Microcline in sedimentary rocks<br />
Šćavničar and Jović (1962) determined microcline in Eocene sandstones in<br />
the Kreka basin.<br />
ANORTHOCLASE<br />
(Na,K) [AlSi 3<br />
O 8<br />
]<br />
Anorthoclase is a Na-enriched high-temperature feldspar. It occurs almost<br />
exclusively in igneous rocks. According to Strunz (1966), anorthoclase is structurally<br />
not well defined. The symmetry is monoclinic or triclinic.<br />
A u t h o r s: Jurković and Majer (1954), Pamić (1957, 1960a), Simić (1968),<br />
Trubelja and Pamić (1956), Trubelja and Paškvalin (1962).<br />
Anorthoclase is a crystalline solid solution in the alkali feldspar series, in<br />
which the sodium-aluminium silicate member exists in larger proportion. It can also<br />
be understood in terms of an alkali feldspar intermediate between low sanidine and<br />
high albite. It occurs in sodium-rich effusive rocks.<br />
262
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
There exist very few literature references about anorthoclase in Bosnia<br />
and Hercegovina. It has been determined in rhyolites of the central Bosnian schist<br />
mountains and in some Tertiary and Triassic igneous rocks.<br />
1. Anorthoclase in rhyolites from the schist mountains of central Bosnia<br />
Jurković and Majer (1954) determined anorthoclase in Paleozoic rhyolites<br />
(quartz-porphyres) from Mt. Vranica (Krstac and Rosin localities). Anorthoclase<br />
phenocrysts are less abundant than quartz. The largest grains identified are up to<br />
3 x 5 mm in size, and have rounded or corroded rims. They occur as individual<br />
crystals or Carlsbad- or Baveno-type twins (sometimes the suture lines are wavy).<br />
The crystals display perfect cleavage, and often contain included quartz and biotite.<br />
Some grains are fractutred and display uneven extinction. The determination of<br />
anorthoclase is based on microscopic measurements (rotating-stage microscope) and<br />
the use of a Nikitin-type diagram. The measured -2V angle lies in the range between<br />
52° and 72°. The -2V angle of anorthoclase from the Rosin locality is also highly<br />
variable, probably reflecting a change in the chemical composition of anorthoclase<br />
phenocrysts. In these rocks, anorthoclase occurs together with albite, quartz and<br />
some accessory minerals.<br />
2. Anorthoclase in Tertiary-age effusive rocks<br />
Trubelja and Paškvalin (1962) determined anorthoclase in products of<br />
Tertiary-age volcanic events. Anorthoclase is an essential mineral (together with<br />
biotite) in the lamprophyre veins from Sasa. In thin section the anorthoclase has the<br />
form of elongated or platelike grains. Twinning was not observed. Cleavage along<br />
(010) is visible only on some grains. The grains are weathered and show signs of<br />
alteration. Inclusions of elongated apatite grains are present in anorthoclase crystals.<br />
Microscopic measurements, performed on a rotating-stage microscope, used with a<br />
Nikitin diagram confirmed that the feldspar is anorthoclase. The -2V angle lies in<br />
the range 41° to 51°. The RI’s of anorthosite are lower than those of Canada balsam<br />
(determined by the Becke line method).<br />
Trubelja and Pamić (1956) studied the dacites from the village of Parnice<br />
(Brusnička rijeka) and determined the present feldspar to be either anorthoclase or<br />
sanidine. The -2V angle lies in the range between 27.5° and 30°.<br />
3. Anorthoclase in Triassic igneous rocks<br />
Pamić (1957, 1960a) mentions anorthoclase in effusive rocks from the<br />
Sarajevo area. Within the scope of a study of igneous rocks at Mt. Igman and Mt.<br />
Bjelašnica, Pamić identified anorthoclase as an essential mineral constituent of<br />
alkaline dolerites (diabases) in the Mojčevići area. In thin section the anorthoclase is<br />
263
SILICATES<br />
present as idiomorphic crystals, usually elongated along the [100] axis. Twinning was<br />
not observed, and cleavage is parallel to (100). The RI’s of anorthoclase are lower<br />
than those of Canada balsam (determined by the Becke line method). Microscopic<br />
measurements confirmed the feldspar to be anorthoclase. The -2V angle varies in the<br />
range between 41° and 52°. The 2V angle measured on one of the grains was -64°, a<br />
value too high for anorthoclase.<br />
In addition to anorthoclase, Pamić (1957) was able to determine albite, chlorite,<br />
calcite and magnetite in the paragenesis. In a subsequent publication Pamić (1960a)<br />
found anorthoclase to be an important constituent of similar rocks from Kalinovik.<br />
Simić (1968) provides a description of basic potassium-enriched effusive<br />
rocks in the area delimited by the geological map – sheet Sarajevo. He does not<br />
refer specifically to anorthoclase, but discusses a sanidine-orthoclase feldspar with<br />
ca. 20% of albite displaying microintergrowths often seen in anorthoclase. It is<br />
interesting to note that this feldspar has a 2V angle similar to the one measured by<br />
Pamić on the anorthoclase from Mojčevići.<br />
HYALOPHANE<br />
(K, Ba, Na) [Al(Al, Si)Si 2<br />
O 8<br />
]<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 0.6557 : 1 : 0.5516 β = 115° 40’<br />
Cell parameters: a o<br />
= 8.557, b o<br />
= 13.037, c o<br />
= 14.441 Z = 8<br />
or a o<br />
= 8.557, b o<br />
= 13.040, c o<br />
= 14.400 Z = 8<br />
NB the cell parameters as given above are based on measurements of<br />
hyalophane crystals from Zagrlski (Zagradski) potok at Busovača – on a 2-circle<br />
Goldschmidt-type reflection goniometer (Barić 1969 and 1972). Cell parameters<br />
were calculated from x-ray diffraction data of two hyalophane crystals from the<br />
same locality. Both samples are kept in the British Museum in London (Gay and Roy<br />
1968). One sample is marked BM 1959, 359 and the other one as No. 195868. The<br />
derived lattice ratios are<br />
a : b : c = 0.6564 : 1 : 0.5534 β = 115° 41’<br />
a : b : c = 0.6562 : 1 : 0.5522 β = 115° 41’<br />
which is in good agreement with the ratio obtained by goniometric measurement.<br />
Properties: Hyalophane is an intermediary member of the orthoclase-celsian series,<br />
containing potassium and barium. The optical properties show considerable variation,<br />
depending on the potassium content. Here we will discuss only the data pertaining to<br />
hyalophane from the occurrence in Bosnia and Hercegovina.<br />
264
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The principal refractive indices show following variations: Nx = 1.5421-1.5463,<br />
Ny = 1.5447-1.5489, Nz = 1.5462-1.5503. The optic axial angle -2V varies between<br />
72° 27’ and 73° 51’ with a r
SILICATES<br />
Barić collected several samples of hyalophane, and investigated them in<br />
order to complement his earlier results published in 1957. This work reulted in two<br />
further papers (Barić 1969, 1972). The paper published in 1972 is a translation into<br />
german of his 1969 paper.<br />
In the Busovača occurrence, hyalophane forms beautiful crystals, usually<br />
yellowish in colour and semi-transparent (some terminal sections of the hyalophane<br />
crystals are quite transparent). Crystals found in this location were up to 10-15 cm in<br />
size, most of them twinned by the Baveno and Manebach laws. In addition to twins,<br />
multiple twins (i.e. interpenetration fourlings) are sometimes encountered. In such<br />
a case the [100] axes of all four individual crystals are synaxial with the fourfold<br />
symmetry axis.<br />
Numerous crystals (in the 0.5-3 mm size range) were measured on a<br />
Goldschmidt-type two circle reflection goniometer and the following crystal forms<br />
were determined: {001}, {010}, {100}, {310}, {110}, {130}, {-203}, {-506},<br />
{-101}, {-201}, {-111} and {-221}. Many of the measured crystal faces were ideally<br />
flat resulting in strong, high-quality reflections. Therefore, the lattice ratios could be<br />
derived from the measurements:<br />
polar elements: p 0<br />
= 0.8413 q 0<br />
= 0.4972 μ = 64° 20’<br />
linear elements a : b : c = 0.6557 : 1 0.5516 β = 115° 40’<br />
Gay and Roy (1968) provide following information about cell parmeters for two<br />
hyalophane samples<br />
Sample Cn wt% a 0<br />
b 0<br />
c 0<br />
β<br />
BM 1959, 359 43.3 8.557 13.037 14.441 115° 69’<br />
195867 45.3 8.557 13.040 14.400 115° 69’<br />
This data set can be used to calculate the lattice ratios for these two hyalophanes:<br />
Sample<br />
a : b : c<br />
BM 1959, 359 0.6564 : 1 : 0.5534 β = 115° 41’<br />
195867 0.6562 : 1 : 0.5522 β = 115° 41’<br />
There is very good correspondence of these data, obtained by x-ray diffraction, with<br />
those obtained by Barić (1969, 1972).<br />
266
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Figure 19. Hyalophane from Zagrlski (Zagradski) potok near Busovača (Barić 1969)<br />
1. Chemical analysis<br />
A total of five hyalophane samples were subject to chemical analysis. The<br />
results are given in Table 61.<br />
Table 61. Chemical analysis of hyalophane from Zagrlski (Zagradski) potok<br />
Analyst<br />
1.<br />
I. Janda<br />
2.<br />
V. Pavlović<br />
3.<br />
J.H. Scoon<br />
4.<br />
Lj. Barić<br />
5.<br />
Lj. Barić<br />
SiO 2<br />
49.64 49.42 49.54 49.39 51.04<br />
Al 2<br />
O 3<br />
23.54 23.57 24.14 23.43 22.80<br />
Fe 2<br />
O 3<br />
0.32 0.11 0.17 0.19<br />
BaO 18.97 18.43* 19.01 18.31 17.02<br />
CaO traces 0.19 0.30 0.21<br />
MgO traces 0.04<br />
K 2<br />
O 5.46 6.23 6.37 6.28 7.38<br />
Na 2<br />
O 1.97 1.67 1.65 1.63 1.42<br />
H 2<br />
O + 0.15** 0.17 0.11<br />
H 2<br />
O - 0.18 0.06 0.08 0.05<br />
Total 99.76 99.70 100.05 99.76 100.22<br />
* given as BaO + SrO in the original paper (Divljan 1954)<br />
** given as Loss-on-ignition (LOI) in the original paper (Divljan 1954)<br />
267
SILICATES<br />
The analysis of sample 1 was done by Ms. I. Janda in Vienna; results of<br />
chemical analysis of sample 2 was published by Divljan (1954); results for sample<br />
3 were published by Gay and Roy (1968); samples 4 and 5 were analyzed by Barić<br />
and published in 1969 and 1972.<br />
We conclude that the chemical composition of hyalophane from Busovača is<br />
not quite constant. A calculation of molecular percentages of celsian (Cn), anorthite<br />
(An), orthoclase (Or) and albite (Ab), based on the above chemical analyses give the<br />
following range of values:<br />
Cn 35.00-40.78%<br />
An 1.08-1.74%<br />
Or 38.25-49.39%<br />
Ab 14.44-20.97%<br />
Divljan and Simić (1956) maintain that the molecular ratio is 60% Or and<br />
40% Cn.<br />
This variation in chemical composition has an effect on the optical properties,<br />
so that a lower percentage of BaO corresponds to a smaller 2V angle, lower refractive<br />
indices and smaller [100] Λ X extinction angle in (010). The density also decreases.<br />
268<br />
Figure 20. Hyalophane from Zagrlski (Zagradski) potok near Busovača (Barić 1969)
2. Optical properties<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
First information on the optical properties of hyalophane from Busovača was<br />
published by Divljan and Simić (1956). They measured the -2V angle as 78.5°, the<br />
extinction angle [100] Λ X = 28.5°. Refractive indices were measured in daylight by<br />
the immersion method – Nz = 1.547, Nx = 1.542. According to Divljan (1954), the<br />
maximum variation of the optic axial angle -2V is in the range between 78° and 84°.<br />
He provides three more measurements of the extinction angle (20.5°, 23.5° and 28°).<br />
Two values for the specific gravity were obtained on two samples – 2.849 and 2.868.<br />
Roy (1965) gives further measurements for the samples in the British<br />
museum:<br />
Sample Cn % Or % Nz Ny Nx Nz-Nx 2V [100]ΛX D<br />
BM 1959, 43.3 --- 1.548 1.546 1.543 0.005 -76.3° 23.0° 2.837<br />
359<br />
195867 45.3 37.7 1.549 1.547 1.544 0.005 -68.9° 24.5° 2.875<br />
Figure 21. Hyalophane from Zagrlski (Zagradski) potok near Busovača (Barić 1969)<br />
Barić (1969, 1972) studied the optical properties of hyalophane from<br />
Busovača in considerable detail. He paid particular attention to the dispersion of<br />
optical elements, and this set of data is the first one obtained for hyalophane in<br />
general. For these investigations Barić used oriented thin sections – a) parallel to<br />
the (010) pinacoid, and b) parallel to the (-101) crystal form. The ease-of-vibration<br />
269
SILICATES<br />
direction (principal vibrational direction) Z coincides with the perpendicular on<br />
the second pinacoid (010) and the axis [010]. This direction is the obtuse bisectrix,<br />
meaning that hyalophane is optically negative. The X an Y vibrational directions<br />
are located in the plane of the pinacoid (010). The optic axial plane therefore has a<br />
normal symmetrical position. The deviation angle of the acute bisectrix X from the<br />
perpendicular on (-101) is only 16°.<br />
Figure 22. Hyalophane from Zagrlski (Zagradski) potok near Busovača (Barić 1969)<br />
It was possible to measure the optic axial angle in sections parallel to (010)<br />
or (-101), around both the acute and obtuse bisectrices. The sections used were ca.<br />
0.5 mm thick, in order to obtain better accuracy of the measurements. When a proper<br />
orientation of these two sections was attained, the r < v dispersion of optic axes was<br />
clearly visible around their acute bisectrix. In proper crystallographic orientation, the<br />
vibrational direction X has a posterior inclination i.e. within the acute angle β. The<br />
vobrational direction Y has an anterior inclination with respect to [001] i.e. towards<br />
the observer. These relationships can be visualised in Figure 23 39d which shows<br />
the (010) section. The [100]ΛX extinction angle was measured in this section, for<br />
different light wavelengths<br />
μm 643.86 578 ± 1 546.07 435.83<br />
[100]ΛX 27° 45’ 26° 42’ 26° 12’ 25° 28’<br />
The variation of the optic axial angle -2V (measured on several thin sections<br />
of the (010) or (-101) forms) is in the range between 70.3° and 81°.<br />
270
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Figure 23. The (010) section of hyalophane showing the r
SILICATES<br />
The measured specific gravity of this hyalophane sample is 2.883 gcm -3<br />
(pycnometric method at 4°C).<br />
The same set of measurements was done for sample no. 5 (see Table 61)<br />
which had a lower BaO content. Results are given in Table 63.<br />
Table 63. Optical constants of hyalophane from Zagrlski potok (BaO = 17.02%)<br />
Wavelength (μm) 690.75 623.44 589.3 ± 0.3 546.07 435.83<br />
Refractive indices<br />
Nx 1.5392 1.5408 1.5421 1.5443 1.5522<br />
Ny 1.5417 1.5433 1.5447 1.5469 1.5549<br />
Nz 1.5430 1.5447 1.5462 1.5484 1.5564<br />
Birefringence<br />
Nz – Nx 0.0038 0.0039 0.0041 0.0041 0.0042<br />
Nz – Ny 0.0013 0.0014 0.0015 0.0015 0.0015<br />
Ny – Nx 0.0025 0.0025 0.0026 0.0026 0.0027<br />
2V angle -71° 50’ -72° 27’ -72° 59’ -74° 36’<br />
The accuracy for the determination of refractive indices given in Tables 62<br />
and 63 is ± 0.0002.<br />
The measured specific gravity of this hyalophane sample is 2.842 gcm -3<br />
(pycnometric method at 4°C).<br />
The measurements presented in Tables 62 and 63 show that the dipersion of<br />
RI’s is small. This is consistent with the high Abbe number (also called V-number<br />
or constringence). For the hyalophane with higher Ba content, the Abbe number<br />
for Nz, Ny and Nx is 63, 65 and 66. The refractive indices for the lines C and<br />
F – required for the calculation of the Abbe number – were determined from the<br />
dispersion curves of these RI’s.<br />
Values of birefringence are also low. The birefringence was additionally<br />
measured using a Berek-type compensator. Four measurements on sections (thickness<br />
0.1-0.4 mm) of the high-Ba hyalophane were made: Ny – Nx = 0.0041; 0.0040;<br />
0.0041; 0.0040;<br />
while the partial birefringence values were Nz – Nx = 0.0015 and 0.0014;<br />
Ny – Nx = 0.0025 and 0.0025. For the low-Ba hyalophane these values are<br />
Nz – Nx = 0.0039, 0.0040 and 0.0040.<br />
These values are reasonably consistent with the values given by Divljan<br />
(1955, 1956) and Roy (1965), although they used the immersion method for RI<br />
determination – a procedure which is inherently less accurate than the precise optical<br />
measurements as done by Barić (1969).<br />
272
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
With respect to the extinction angle [100]ΛX, its value is 27° for the high-<br />
Ba hyalophane and 24° for the low-Ba variety. The range of values, measured on<br />
numerous hyalophane crystals from this occurrence, is between 23.8° and 31°.<br />
3. Microelement concentrations<br />
The concentration of microelements was done by spectrography, on several<br />
hyalophane samples. The analyses were done by Brandenstein and Schroll (Barić<br />
1969, 1972) on completely colourless and transparent hyalophane material. The<br />
results obtained (in ppm) are as follows: Rb 250, Sr 200, Pb 70, Ga 20, Tl 10, V 10,<br />
Ge 7, Mo 5, B 5, Cu 2, Zn 0.1. The following elements were below the detection<br />
limit of the technique: Ag, As, Be, Bi, Cd, Cs, Sb, Sn and Ti.<br />
A similar set of measurements was done by Arsenijević. He determined Al,<br />
Si, Ba, K, Na and Sr to be major constituents of the hyalophane. Traces of Ga, Mg,<br />
Ca, Ti, Ag, Pb, Mn, Cs, Fe and Ni were also determined (Divlajn 1954). A specific<br />
determination of rubidium, thallium and cesium (Arsenijević 1960) in six hylophane<br />
samples gave following results (concentrations given in ppm):<br />
Sample 1 2 3 4 5 6<br />
Rb 125 110 130 125 110 110<br />
Tl --- 4 4 --- 4 ---<br />
Cs 10 10 10<br />
In sample no. 3 Arsenijević (1960) also determined Pb = 10, Mn = 21, Sr =<br />
1600, V = 4, Cu = 9 (all values in ppm) as well as traces of Ti, Ca, Mg, Li, Ga, Cr,<br />
Ni and Co.<br />
The data provided by Arsenijević and Brandenstein and Schroll should be compared with<br />
some caution. While Brandenstein and Schroll used perfectly colourless and transparent<br />
hyalophane samples for analysis, Arsenijević used a grey variety of hyalophane.<br />
4. Origin and age of hyalophane (Busovača)<br />
At Busovača (Zagrlski or Zagradski potok), hyalophane occurs together<br />
with quartz, siderite, pyrite and muscovite. There are two generations of quartz. The<br />
first generation is represented by large, columnar, transparent crystals (up to 10 cm<br />
long), grey or darkgrey in colour. This quartz usually forms the base for hyalophane<br />
growth. As described earlier, the fissure in the Paleozoic schist, which carries<br />
the hyalophane, cuts across older structures, indicating that it is younger in age.<br />
Therefore, the K-Ar method was used to determine the absolute age of hyalophane.<br />
According to the results obtained by Čedžemov (published by Barić 1969, 1972)<br />
the age of hyalophane is 59.5 ± 6.4 million years. This indicated that this mineral<br />
association crystallized approximately during the Paleocene – Eocene transition.<br />
273
SILICATES<br />
The quartz veins at the Busovača locality were mentioned also by Ilić<br />
(1954) and Jurković (1956). Ilić believed that the quartz veins in the Paleozoic<br />
schists are remnants of older sulphide-ore deposits which have been washed away<br />
or eroded. The presence of specularite would indicate that such deposits belong to<br />
the oldest metallogenous period (Ilić 1954). However, the comparatively young age<br />
of hyalophane is not consistent with the opinion advnced by Ilić. Jurković (1954)<br />
described these veins as Alpine-type fissure veins formed during strong radial<br />
collisonal-tectonic events.<br />
274<br />
THE PLAGIOCLASE GROUP<br />
With regard to their chemical composition, the plagioclase group of minerals<br />
represents a continuous isomporphic series with albite Na [AlSi 3<br />
O 8<br />
] as the Na-rich endmember,<br />
and anorthite Ca [Al 2<br />
Si 2<br />
O 8<br />
] the Ca-rich end-member. Like potassium feldspars,<br />
plagioclase minerals also have their high-temperature and low-temperature modifications.<br />
The plagioclases can thus have high-temperature or low-temperature optical constants.<br />
Changes in chemical composition of the individual minerals of the plagioclase group are<br />
reflected in variations in optical constants and other physical properties.<br />
Plagioclases display perfect cleavage parallel to {001}. Cleavage is good<br />
along {010} and less pronounced along {110}. Hardness is 6 (anorthite) – 6.5<br />
(albite). the colour is usually white (transparent) but reddish, greenish and yellowish<br />
varieties are known. Streak is white, lustre vitreous (sometimes pearly on cleavage<br />
planes). Plagioclases with high An contents dissolve in hot hydrochloric acid, while<br />
hydrofluoric acid attacks all plagioclases.<br />
Plagioclase minerals are triclinic (pinacoidal class). The x-ray diffraction<br />
patterns of individual plagioclase minerals are quite similar to each other, and<br />
determination based solely on XRD is difficult.<br />
ALBITE<br />
Na [AlSi 3<br />
O 8<br />
]<br />
Lattice ratio: a : b : c = 0.637 : 1 : 0.560 (low albite)<br />
α = 94.26° β = 116.58° γ = 87.67°<br />
Cell parameters: a o<br />
= 8.144, b o<br />
= 12.787, c o<br />
= 7.160 Z = 4<br />
X-ray data: (low-albite) d 3.150 (30) 3.188 (100) 4.027 (67) 3.124 (55) 3.658 (37)<br />
IR-spectrum: 405 428 463 475 533 590 610 650 723 742 762 786 990 1010<br />
1045 1103 1165 cm -1 (from Moenke 1962). The vibrations at 645 and 529 cm -1 are<br />
characteristic for low-temperature albite (Zussman 1967).<br />
Synonyms: pericline, tetartine, clevelandite
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
A u t h o r s: Atanacković, Mudrenović and Gaković (1968), Barić (1959,<br />
1964, 1969a, 1970, 1970a, 1972b, 1975), Buzaljko (1971), Cissarz (1956), Čelebić<br />
(1967), Čutura (1918), Džepina (1970), Đorđević (1958), Đorđević and Mijatović<br />
(1966), Đorđević and Stojanović (1964), Golub (1961), Ilić (1953), Jovanović<br />
(1957), Jurković (1954, 1956, 1957, 1958, 1958a, 1961a), Jurković and Majer (1954),<br />
Karamata (1953/54, 1957), Karamata and Pamić (1960, 1964), Katzer (1924 and<br />
1926), Koch (1908), Majer (1963), Majer and Crnković (1961), Nöth (1956), Pamić<br />
(1957, 1960, 1960a, 1961, 1961a, 1961b, 1962, 1963, 1969, 1969b, 1970a, 1971,<br />
1972b, 1974a), Pamić and Buzaljko (1966), Pamić and Đorđević (1974), Pamić and<br />
Maksimović (1968), Pamić and Olujić (1969), Pamić and Papeš (1969), Pamić and<br />
Tojerkauf (1970), Pamić and Trubelja (1962), Petković (1961/62), Podubsky and<br />
Pamić (1969), Simić (1964, 1966, 1968, 1972), Stangačilović (1956), Šćavničar<br />
and Jović (1962), Šibenik-Studen and Trubelja (1967), Tajder and Raffaelli (1967),<br />
Trubelja (1957, 1960, 1962, 1962a, 1963, 1963a, 1963b, 1963c, 1966a, 1969, 1972a),<br />
Trubelja and Barić (1976), Trubelja and Miladinović (1969), Trubelja and Pamić<br />
(1957, 1965), Trubelja and Šibenik-Studen (1965), Trubelja, Šibenik-Studen and<br />
Sijarić (1974, 1975, 1975a), Varićak (1955, 1956, 1957, 1966), Vujanović (1962).<br />
Albite is one of the most abundant and ubiquitous rock-forming minerals.<br />
It is also one of the best researched minerals, as can be seen from the list of authors<br />
given above. Albite occurs in acidic, neutral and basic igneous rocks, both in the<br />
inner and outer Dinarides. It is very common in the Triassic igneous-sedimentary<br />
complex (the spilite-keratophyre series). Special mention deserves the omnipresence<br />
of albite in the rocks of the Bosnian serpentine zone (BSZ) and the associated<br />
diabase-chert series (albite-bearing granitoids, syenites, diorites, spilites, rhyolites,<br />
keratophyres etc.). The gneisses, granites and similar rocks from Mt. Motajica often<br />
contain albite. The same is true of the altered basic igneous rocks of Paleozoic age<br />
in the areal of the Una and Sana rivers and the schist mountains of central Bosnia.<br />
Albite is associated with the iron minerals at the Ljubija iron-ore deposit. Albite is<br />
sometimes an essential constituent of some schists.<br />
Apart from some early publications by Koch (1908), Čutura (1918) and<br />
Katzer (1924, 1926), all other information on albite in Bosnia and Hercegovina has<br />
been published in the period after the II World War.<br />
1. Albite in rock of the Midtriassic spilite-keratophyre series<br />
A variety of albite-containing igneous rocks are to be found in the area of<br />
Konjic, Jablanica and Prozor, in the area of Borovica, Vareš and Čevljanovići; in<br />
the Vrbas river valley; around the town of Bugojno, Sarajevo, Trnovo, Kalinovik,<br />
Čajniče and Tjentište.<br />
275
SILICATES<br />
a) The Konjic – Jablanica – Prozor area<br />
Pamić (1960, 1961, 1961a, 1961b), Pamić and Maksimović (1968) and<br />
Čelebić (1967) provide a substantial amount of data on the abundance of albite in<br />
spilites, keratophyres, quartz-keratophyres, albite diabases, albite granite-porphyres,<br />
quartz albitites and some pyroclastic rocks.<br />
According to Pamić, albite-carrying spilites are most abundant in the<br />
watershed of the Rama river, near the village of Lug and in the area of Marina Pećina<br />
– Gračanica. These rocks contains two generations of albite. The first generation<br />
albite crystals are often idiomorphic or hypidiomorphic, with a prominent (001)<br />
crystal form and good cleavage along (010). Twins according to the Carlsbad, albite,<br />
albite-Carlsbad laws are common. The second generation albite occurs in the form of<br />
microlites. In some spilites the albite is completely fresh, while alteration products of<br />
albite (prehnite, calcite and sericite) are common in other spilites. Prehnite appears<br />
to be the most common weathering product of albite. Some albite crystals contain<br />
inclusions of chlorite.<br />
The An content of albites in the Krstac igneous complex was determined<br />
by the Fedorov method using a rotating stage microscope. The An content is in the<br />
range 4-9.5%, the median being 4.7% An. The optic axial angle is rater large,<br />
2V = +79° to ±90°.<br />
Keratophyres are fairly abundant in the Krstac igneous complex, especially<br />
between the townships of Doljani and Vrata on the right bank of the Rama river.<br />
These rocks frequently contain albite (together with neutral plagioclases). Twinning<br />
according to the Carlsbad and albite laws is common. The phenocrysts are almost<br />
always twinned and included with calcite. Their An content is in the range 0-9%. The<br />
+2V angle lies in the range 79° to 87° (keratophyres from Gračanica).<br />
The andesine keratophyres from Bukove Ravni near Doljani contain albite<br />
within the matrix of the rock. The has been determined based on low RI’s (lower tha<br />
Canada balsam, observed by the Becke line method). The quartz-keratophyres also<br />
contain two generations of albite. Single crystal, twins and polysynthetic twins<br />
have been observed. Twins according to the Carlsbad and albite laws are most<br />
common. Most of the crystals are fresh, sometimes included with prehnite. The An<br />
content of albites in rocks from Gračac is between 1.5 and 8.5%. The +2V angle is<br />
in the range 77.5-87°.<br />
Albite phenocrysts in the quartz-keratophyres from Krstac (village of Lug)<br />
have a An content around 2%. The +2V angle is in the range 80-86°. Albite also<br />
occurs together with altered alkaline plagioclases in albite diabases. Their An content<br />
is 4.8%. The +2V angle is in the range +82° to ±90°.<br />
276
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Pamić and Maksimović (1968) determined albite in quartz-albite diabases<br />
from Bijela (near Konjic). Here the albite surrounds grains of altered plagioclases.<br />
The granite-porphyres from Ravnice (Gračac) contain albite whose An<br />
content is 1.3%. The +2V angle is in the range 80-86°. The quartz-albitites from<br />
Crima contain albite with 3.8% An.<br />
Albite has been determined in tuffs from the Gračanica river.<br />
b) the Borovica – Vareš – Čevljanovići area<br />
Albite is abundant in igneous rocks originating from Midtriassic magmatic<br />
events in Bosnia and Hercegovina, i.e. in the Borovica – Vareš – Čevljanovići area.<br />
Pamić (1963), Trubelja (1969, 1972) and Petković (1961/62) have published a<br />
substantial amount of data on albite in the rocks of this area. Albite occurs in, and<br />
is sometimes an essential constituent of keratophyres, spilites and albite diabases.<br />
Vujanović (1962) determined albite in the manganese mineral paragenesis at<br />
Čevljanovići. Albite is fresh in some of these rocks, the average An content is 4.8%.<br />
The +2V angle is in the range 70-80°. The keratophyre from Kiprovac (Borovica)<br />
contains albite with 0-10% An.<br />
c) Area of Kupres – Bugojno – Donji Vakuf – Jajce<br />
Pamić and Papeš (1969) and Trubelja and Šibenik-Studen (1965) have<br />
published relevant data on the occurrence of albite in spilites and similar rock types<br />
found in the Vrbas river valley, and in the area of Bugojno and Kupres.<br />
Pamić and Papeš (1969) note that albite is abundant in the sodium-rich<br />
effusive rocks (keratophyres), diabases (amphibole-albite diabases, ankerite-albite<br />
diabases). the authors believe that albite is a primary mineral in all these rocks, i.e.<br />
that it crystallized from a „spilite-keratophyre“ magma. No 2V angle measurements<br />
of these albites are available, but the authors have determined its positive optical<br />
character. Albite has also been determined in some tuffs from Kupres and the Vrbas<br />
river area.<br />
d) Area of Ilidža – Trnovo – Mt. Bjelašnica – Kalinovik<br />
Pamić (1957, 1960a, 1962), and Simić (1964, 1966, 1968) provide data on<br />
the occurrence of albite-bearing effusive rocks in the area of Sarajevo, Trnovo and<br />
Kalinovik. The igneous rock from Mt. Igman contain albite and other feldspars.<br />
There is not much information available on the optical properties of these albites,<br />
which seem to be somewhat different from albite occurring in other rocks. The<br />
optical character of these albites is positive, but the 2V angles are considerably<br />
277
SILICATES<br />
smaller. The albite in dolerites (diabase) from Donje Grkarice has a 2V angle = 68°,<br />
in the alkaline dolerite from Mojčevići this angle is in the range +64° to +74°.<br />
Albite occurs in spilites in the source area of the Željeznica river near the<br />
village of Godinje. The crystals are single or twinned by the Carlsbad law. The An<br />
content is 0-9%, the 2V angle is in the range 74° to 80°. The spilites from the Turovo<br />
area contain both albite and oligoclase. Simić (1964) determined optically negative<br />
albite in basic igneous rocks from the Sarajevo area. The 2V angle = -80°.<br />
278<br />
e) Eastern and south-eastern Bosnia<br />
Albite is the most abundant, and sometimes the only feldspar in Triassic<br />
igneous rocks of south-eastern Bosnia. Trubelja (1962a, 1963) and Pamić and<br />
Buzaljko (1966) made detailed microscopic determinations of albite in keratophyres<br />
from the Čajniče area. The keratophyres from Janjina Rijeka contain albite as<br />
irregular grains, although a transition from phenocrysts to small, matrix-embedded<br />
columnar crystals can be observed. Some grains show effects of alteration (into<br />
calcite and chlorite). Microscopic measurements on a rotating-stage microscope<br />
gave following results: the An content is rather stable in the 0-8% range. The albite<br />
is positive, the +2V angle = 82° to 86.5°, twinning is by the Carlsbad or albite law.<br />
Albite has similar properties in other rocks studied in the Čajniče area. In all<br />
cases, albite was optically positive and the 2V angle was large. The albite has lowtemperature<br />
optical properties.<br />
The origin of the albites in rocks from this area is linked to processes of<br />
alkaline (sodium) metasomatosis and the crystallization of andesine and labradorite.<br />
This metasomatosis process should be understood in terms of spilitization reaction<br />
mechanisms. Evidence for the secondary origin of the albite (deposited in the<br />
postmagmatic hydrothermal phase) include following:<br />
1. albite is an essential constituent of all investigated rocks, independent of the<br />
SiO 2<br />
content of the rock;<br />
2. all investigated rock contain albite with visible relicts of an initial zonar<br />
plagioclase structure. Pure albite does not have zonar structure;<br />
3. albite phenocrysts almost always contain calcite inclusions. The calcitization<br />
process is more pronounced in the center of the grains than towards the edges;<br />
4. the optical constants, measured on a rotating-stage microscope, correspond<br />
entirely to low-temperature albite of the ‘spilite’ type (2V = 79-88°);<br />
5. the acidic dacites from the Lim river area contain neutral plagioclases and<br />
have a lower sodium oxide content than the basic rocks from the Čajniče area;<br />
6. the rocks from the Čajniče area have been altered by albitization, but also by
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
other postmagmatic processes like chloritization, kaolinization, pyritization,<br />
sericitization and epidotization;<br />
7. IR-spectroscopic measurements have confirmed that the albites in rocks from<br />
the Čajniče area are typical low-temperature albites.<br />
Trubelja and Slišković (1967) and Trubelja and Miladinović (1969)<br />
determined albite as a fairly abundant mineral in some Triassic effusive rocks from<br />
Tjentište and Sutjeska.<br />
Karamata (1957) found albite to be a prominent constituent of keratophyres<br />
from the Zvornik area. The crystals (up to 1.5 x 1 mm in size) are usually altered<br />
(sericite, kaolinite). The RI’s are smaller than those of Canada balsam. The 2V angle<br />
is in the range +80° to ±90°.<br />
2. Albite in Triassic-age intrusive rocks<br />
Intrusive rocks (with albite) of Triassic age are not very abundant in Bosnia<br />
and Hercegovina. There are outcrops around Čajniče, Donji Vakuf, at Mt. Komar<br />
and Mt. Prenj. At the contact of the gabbros at Jablanica with surrounding sediments,<br />
some occurrences of albite have been observed. Data on albite in these rocks have<br />
been published by Cissarz (1956), Čutura (1918), Nöth (1956), Pamić (1961),<br />
Jovanović (1957), Trubelja (1963a) and Trubelja and Šibenik-Studen (1965).<br />
Albite is a prominent mineral in granites from the village of Luke, near<br />
Čajniče. The +2V angle is in the range 86° to 89°. Twinning of albite and orthoclase<br />
(microperthite) has been observed.<br />
Čutura (1918) provides first data about the abundance of albite in granitoid<br />
rocks from Mt. Komar (Gornji Vakuf). More recent research (Trubelja and Šibenik-<br />
Studen 1965) have confirmed this finding.<br />
Cissarz (1956) observed the occurrence of albite in the contact paragenesis<br />
within the gabbro complex at Jablanica (Tovarnica). This albite occurs in fresh and<br />
sometimes quite large crystals. The +2V angle is in the range 72° to 84°, the An<br />
content is 0-5%. Optical constants of this albite define its low-temperature origin,<br />
which is consistent with the formation conditions of the entire paragenesis. Albite<br />
crystallized after epidote.<br />
3. Albite in granitoids and other rocks of the Bosnian serpentine zone (BSZ)<br />
Albite is often found to be a prominent or even essential mineral constituent<br />
of granitoids and other rocks of the Bosnian serpentine zone (BSZ) and the lateral<br />
diabase-chert series. Relevant data on the abundance an optical properties of albite<br />
279
SILICATES<br />
has been published by a number of authors – Džepina (1970), Đorđević and Mijatović<br />
(1966), Đorđević and Stojanović (1964), Golub (1961), Karamata (1953/54),<br />
Karamata and Pamić (1960, 1964), Majer (1963), Pamić (1970a, 1971), Pamić and<br />
Buzaljko (1966), Pamić and Đorđević (1974), Pamić and Olujić (1969), Pamić and<br />
Tojerkauf (1970), Pamić and Trubelja (1962), Trubelja (1957, 1960, 1962, 1963b,<br />
1963c, 1966a), Trubelja and Barić (1976), Trubelja and Miladinović (1969), Trubelja<br />
and Pamić (1957, 1965), Trubelja, Šibenik-Studen and Sijarić (1974, 1975, 1975a).<br />
The basic metamorphic rocks (without garnets) from Mt. Borja contain albite in<br />
some albite-bearing actinolite schists (Džepina 1970). The garnet-bearing equivalents<br />
of the named rocks usually contain albite as an alteration product of andesine.<br />
Đorđević and Mijatovaić (1966) observed the presence of albite in serpentine<br />
rocks from the Zavidovići area, but provide no further information. Golub (1961)<br />
determined albite in rocks from Mt. Kozara. The albite has 8-10% An.<br />
Đorđević and Stojanović (1964) determined albite in granites at Selište,<br />
on the Žepče-Maglaj road. The albite is an essential constituent if this rock. The<br />
An content is 0-6%, the +2V angle variable, in the range between 78° and ±90°.<br />
Twinning by the Carlsbad and albite law is common.<br />
Karamata (1953/54) made numerous measurements of albite occurring<br />
in albite rhyolites around Bosansko Petrovo Selo (in the vicinity of the asbestos<br />
deposit). Albite phenocrysts (3.5 x 2 mm in size) contain 1-10% An (the average<br />
is 1-4%). The 2V angles are variable, but always large and positive. Albites with<br />
1-5.5% An have 2V angles between 78° and 82° (less frequetly between 72° and<br />
77°). Albite crystals are often twinned (Carlsbad, albite, Manebach law).<br />
Karamata and Pamić (1960, 1964) determined albite as a prominent mineral<br />
in spilites and granitoid rocks from Vareš (Tibija, Vijaka localities). The granite from<br />
Duboštica (Vita Kosa) contains albite with a 0-7% An content, and a variable +2V<br />
angle in the range 83° to 88°. This albite is a typical low-temperature variety.<br />
Majer (1963) identified zonar plagioclases in pebbles of a conglomerate<br />
belonging to the diabase-chert formation (from Prisoj). The central parts of the<br />
grains are composed of oligoclase (up to 12.5% An) while the albite rims contain<br />
ca. 7.5% An.<br />
Pamić (1970), Pamić and Olujić (1969) determined an abundance of albite<br />
in syenites and granites from Mt. Ozren. Albite-bearing granites form outcrops at Mt.<br />
Gostilj (774 m asl) near Bosansko Petrovo Selo. The albite grains are hypidiomorphic<br />
and are frequently intergrown by polysynthetic twinning. The An content varies<br />
between 0.5 and 7%. The +2V angle = 80-86°.<br />
280
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The spilites of Mt. Ozren sometimes contain significant amounts of albite<br />
(Pamić and Trubelja 1962; Trubelja and Pamić 1965). The spilite from Rakovac<br />
creek contains albite with 1-10% An, and the +2V angle is 88-90°. The granites at<br />
Mt. Borja (on the Doboj – Banja Luka road) contain albite and oligoclase (Pamić<br />
and Tojerkauf 1970). Veins within the diabase-spilite rocks often carry a prehnitealbite<br />
mineral association. This has also been observed at Mt. Kozara (Trubelja et<br />
al. 1974). Infra-red spectroscopy was used to confirm the finding that these albites<br />
are low-temperature forms of this mineral. The diabase rocks from Višegrad often<br />
contain albite associated with hydrothermal xonotlite, scolezite, stilbite and fassaite.<br />
The veins in rocks of Mt. Konjuh carry albite, prehnite and laumontite (locality<br />
Karaula, near the Olovo – Kladanj road).<br />
Trubelja (1960) determined albite in gabbro-pegmatites at Višegradska<br />
Banja, associated with labradorite, diallage, prehnite, chlorite, epidote and<br />
amphibole. Albite is present either as pseudomorphs after labradorite or as veinlets<br />
of very clear and transparent albite crystals. The An content is 0-2%, +2V = 84-88°<br />
(indicative of low-albite). Trubelja (1963c) determined albite in leucocratic diorites<br />
outcropping on the road Višegrad – Dobrun (in the immediate vicinity of Višegrad).<br />
The An content is 4-6%, the average +2V = 82.5°. Albite is an important constituent<br />
of spilites from Bosanski Novi (outcrops are north of the Blagaj railway station). It<br />
was formed by albitization of alkaline plagioclase (Trubelja 1962).<br />
Trubelja (1966a) determined albite in neutral and acidic igneous and<br />
pyroclastic rocks from the northern flanks of Mt. Kozara. The An content is 5-8%.<br />
Albite in tuffs contain less An. The keratophyres from Mt. Ljubić contain albite as<br />
phenocrysts and as small, columnar crystals within the rock matrix (Trubelja 1963b).<br />
4. Albite in rocks from Mt. Motajica<br />
Ilić (1953), Katzer (1924, 1926), Koch (1908), Stangačilović (1956),<br />
Varićak (1966) provide data on the abundance of albite in the various rocks from Mt.<br />
Motajica. Ilić discusses the optical measurements on albite (in kaolinized granites<br />
from Bosanski Kobaš) by Lj. Barić. The An content is 2-6%, the +2V angle 84°<br />
and 78.5° (2 measurements). Koch (1908) published first information on albite in<br />
gneisses and micaschists from Mt. Motajica. His qualitative microscpic observations<br />
were later used by Katzer (1924, 1926) in his description of igneous and other rocks<br />
of Mt. Motajica.<br />
Varićak (1966) published a substantial amount of data based on microscopic<br />
measurements on albite in various rocks from Mt. Motajica (a treatise on the petrology<br />
of Mt. Motajica). Albite in leptinolites had an average An content of 8.5%, and a +2v<br />
angle of 76-87°. Twinning by albite and pericline law is frequent. In chlorite-epidote<br />
schists albite is often twinned (Carlsbad and albite law). The An content is 0-9%<br />
(average value 4%), +2V = 75-87°. The leucocratic granite hosts albite with 5-8%<br />
281
SILICATES<br />
An. The measurements on this material included the maximum extinction method<br />
on the (010) plane. More information on microscopic measurements can be found in<br />
the mentioned treatise.<br />
5. Albite in Paleozoic-age rocks of western Bosnia and the schist mountains of<br />
central Bosnia<br />
Albite is an important mineral, and in many cases an essential constituent<br />
of numerous rocks of the Paleozoic complex of western Bosnia and the schist<br />
mountains of central Bosnia. Since these rocks cover a large area, it is not surprising<br />
that numerous authors were involved in research related to these complexes – Barić<br />
(1964, 1970a, 1975), Jurković (1951/53, 1956, 1957, 1958, 1958a, 1961a), Jurković<br />
and Majer (1954), Majer and Crnković (1961), Nöth (1956), Podubsky and Pamić<br />
(1969), Tajder and Raffaelli (1967), Trubelja and Sijarić (1970), Trubelja, Šibenik-<br />
Studen and Sijarić (1974, 1975, 1975a), Varićak (1956, 1957).<br />
282<br />
a) Albite in the Ljubija area<br />
Information on the occurrence of albite in rocks associated with the iron<br />
deposit at Ljubija has been published in papers by Barić, Jurković, Marić and<br />
Crnković, Nöth, Podubsky and Pamić.<br />
Nöth (1956) was the first to determine albite in the Kozin ore-body (as well<br />
as in sandstones in contact with the ore). The origin of albite in these environments<br />
is linked to the proximity of igneous rocks which contain significant amounts olf<br />
albite (Podubsky and Pamić 1969). Jurković (1961a) mentions albite only in the ore<br />
paragenesis of Bjeljevac – Kozin, where it occurs in a finegrained siderite aggregate.<br />
Fragments of albite were also observed in a breccia-type siderite mass.<br />
Marić and Crnković (1961) determined the 2V angle of albite as +85°,<br />
characteristic for low-temperature albite.<br />
Barić (1964) made a detailed investigation of the albite from Kozin,<br />
including numerous microscopic measurements. The albite grains are mostly fresh<br />
and completely transparent. An onset of sericitization was observed in some cases<br />
only. Measurements using a rotating stage microscope furnished a set of accurate<br />
data for the chemical composition of albite and 2V angles. The average value of<br />
+2V = 81.25°. The average An content is 1.6%. This albite has low-temperature<br />
optical constants.<br />
b) Area of the schist mountains of central Bosnia<br />
Jurković (1954, 1956, 1957, 1958, 1958a) identified albite as a prominent<br />
and occasionally essential constituent of ore-body related mineral parageneses in
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
the schist mountains of central Bosnia (SMCB). Albite occurs in metamorphic ore<br />
formations at Busovača (Zagradski potok) where it is associated with maghemite,<br />
chalcopyrite, tourmaline, biotite, chlorite and other minerals. Albite often shows<br />
distinct polysynthetic twinning. The crystals are usually fresh, with prominent<br />
twinning lamellae. It contains inclusions of rounded ankerite grains, indicating its<br />
younger age with respect to ankerite. The albite is obviously of hydrothermal origin<br />
(mesoepithermal stage).<br />
At Ščitovo – Vrtlasce, albite is associated with ore formations (pneumatolytic<br />
and hydrothermal stages), together with various sulfides and other minerals. Albite<br />
grains 0.2 x 1.5 mm i size) display an allotriomorphic shape in thin section. Freegrowing<br />
albite crystals (in cavities) can attain 3-4 mm in length. Albite contains<br />
inclusions of ankerite. Individual crystals, as well as twins and polysynthetic<br />
intergrowths can be observed. The lamellae and twinning sutures are of even and sharp<br />
outlines. Microscopic (rotating-stage) measurements gave results for +2V = 74-78.5°.<br />
The An content is 0-3%. RI = 1.54. Twinning according to the Carlsbad law.<br />
In the area of Brestovsko, albite is associated with barite mineralizations<br />
which carry numerous sulfides and silicate minerals (Hrastovo locality). Albite is<br />
of pneumatolytic origin (Jurković 1954). Some albite has been found also at the<br />
Trošnik locality.<br />
Albite is a common constituent mineral in rhyolites in the schist mountains<br />
of central Bosnia (SMCB). Jurković and Majer (1954) determined albite in the<br />
albite-bearing rhyolite from Sinjakovo. Albite phenocrysts (0.5-5 mm in size) are<br />
usually twinned (individual crystal are rarely found). The grains are usually cracked<br />
(fractured) and corroded (rims). Most grains show signs of alteration. Their An<br />
content is 0-10%, the +2V angle = 78-86°. These authors have also determined albite<br />
among the phenocrysts in rhyolites (quartz-porphyres) from Krstac and Rosin.<br />
Barić (1970a) determined albite as an important constituent of the kertophyres<br />
from the Trešanica gorge near Bradina in Hercegovina. Albite is present as phenocrysts<br />
but also in the rock matrix. The phenocrysts are usually ca. 1-3 mm long. Individual<br />
crystals and twins (including) multiple twins have been observed (twinning by<br />
Carlsbad, albite, pericline, Manebach laws). The average An content is 3.1%, the<br />
average +2V = 82.6°. This albite has low-temperature optical constants. Many of the<br />
albite fragments and phyenocrysts are fractured and bent, the fractures being filled with<br />
quartz or calcite. Some grains display uneven (wavy) extinction. The low-temperature<br />
variety of this albite has been confirmed by IR-spectroscopy (Barić 1975).<br />
Tajder and Raffaelli (1967) made numerous microscopic determinations of<br />
albite contained in metamorphosed porphyrite-keratophyres from the schist mountains<br />
of central Bosnia. Albite is frequently contained in several types of schist rocks.<br />
283
SILICATES<br />
The moderately altered schists from Neretvica creek, defined as an albitechlorite-muscovite<br />
schist (which belongs to the greenschist facies) contains albite<br />
mainly in the matrix of the rock. A similar schist from the Željeznica creek contains<br />
albite both in the matrix and as phenocrysts (actually porphyroblasts). Albite was<br />
probably formed by albitization of alkaline plagioclases. The An content is 0-5%<br />
with an average of 2%. Twinning is by Carlsbad and albite laws. Albite of similar<br />
features is contined in schists from the source area of the Vrbas river and some other<br />
localities. The authors provide no data on the 2V angle.<br />
Trubelja and Sijarić (1970) determined albite in schists from the upper<br />
reaches of the Ivanovica creek near Busovača. The albite is a prominent mineral<br />
in the albite-chlorite schists, but only of minor importance in the biotite-chloriteankerite<br />
schist. Some albite is contained in veinlets within these rocks (together<br />
with ankerite and quartz), indicating the significance of exsolution processes for the<br />
formation of the albite-ankerite paragenesis.<br />
284<br />
c) Albite in rocks from Mt. Prosara<br />
Varićak (1956, 1957) found albite to be a common and occasionally essential<br />
mineral constituent of both igneous and metamorphic rocks. The quartzporphyres<br />
from Mt. Prosara contain albite both as phenocrysts and in the rock matrix. The<br />
albite is usually twinned by the Carlsbad and albite laws (twinning by the periciline<br />
law is rarely encountered). Individual crystals are rare. Mechanical deformation of<br />
the albite grains is the cause of substantial optical inhomogenities. The An content<br />
of these rocks is 2-10%, the +2V angle = 74-88°. The grains are ca. 0.3 x 1.5 mm in<br />
size. Albite is also a constituent of phyllites and limeschists from Mt. Prosara, but no<br />
detailed information has yet been made available.<br />
6. Other occurrences of albite<br />
Varićak (1955) established that albite is an important constituent of the socalled<br />
‘Maglaj red granite’ whose primary location has not yet been identified (it has<br />
been found only in the form of pebbles in the river Jablanica and smaller creeks in<br />
the Maglaj area).<br />
In this red granite, albite is contained as idiomorphic crystal grains.<br />
Individual crystals are rare and twinning by the albite or pericline law is common<br />
(also polysynthetic twinning). Double twins, by both the Carlsbad and Manebach<br />
laws have been identified. The grains are normally up to 2 mm in size, and some<br />
display a two-zone structure (the inner zone is usually much more weathered than<br />
the outer zone). The measured +2V angle = 71-80°, the average An content is 9.6%.<br />
It is interesting to note that Varićak also mentions neoalbite, which seems to have<br />
crystallized in an environment of warm alkali-enriched solutions. Such neoalbite is<br />
usually fresh and grows next to the ‘old’ albite grains – making them larger.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Simić (1972) provides information on the occurrence of albite in some<br />
clastic rocks in the Sarajevo area. Albite is an important constituent of sandstones,<br />
arkoses and quartz-feldspar rocks (outcropping on Mt. Trebević, Mt. Ozren, near<br />
Kijevo, Tarčin, Osenik and Ostrožac, and in the Miljacka river valley). The sediments<br />
show evidence of alteration processes. The identified mineral associations consist<br />
of quartz, albite, muscovite, hydromuscovite, pyrophyllite, K-feldspar and chlorite.<br />
Simić gives no further data on albite.<br />
Šćavničar and Jović (1962) determined the presence of albite in sediments of<br />
the Kreka coal basin: in Eocene and Miocene clastic sediments and Pliocene sands.<br />
7. Final considerations<br />
All available literature data and results of other resarch indicate that the<br />
Triassic igneous rocks, including the spilite-keratophyre series, contain the lowtemperature<br />
variety of albite. This conclusion is based, among other indicators,<br />
on the large and positive 2V angle of albite as well as on IR-spectra. Moreover, in<br />
other parts of the world similar rocks always contain low-temperature albite. We<br />
wish to place some emphasis on this conclusion because J. Pamić (1969, 1969a,<br />
1972) tried to advance a theory that some of the mentioned rocks hosted albite<br />
which had optical properties of the high-temperature variety. A detailed discussion<br />
of this issue can be found in the cited publications by Pamić and those of Lj. Barić<br />
(1970, 1972b, 1975).<br />
We therefore wish to conclude that albite contained in the rocks and ore<br />
formations in Bosnia and Hercegovina is clearly of the low-temperature variety. The<br />
only exception to this conclusion could be the albites in basic igneous rocks from the<br />
Sarajevo area for which Simić (1964) determined a negative optical character. This<br />
is, however, not compatible with literature data.<br />
We have received certain comments implying that the transition from<br />
high-temperature albite to low-temperature albite would neccessarily be a very<br />
long process. But time does not seem to be a limiting factor in this case, since the<br />
discussed rocks belong to the Triassic (i.e. their age is about 200 million years).<br />
Moreover, some recent investigations have shown that the concentration of alkaline<br />
solutions and their temperature can have a pronounced effect on transitions of albite<br />
and K-feldspars (Senderova, Jaskima and Byčkova 1975). This and other research<br />
provides sufficient evidence for the fact that the transition from high-temperature to<br />
low-temperature albite proceeds at enhanced reaction rates at temperatures around<br />
700°C (Senderov and Ščekina 1976). Hence, the time required for this transition<br />
can be estimated to be 1000 years at temperatures of 400°C or 1 million years at<br />
temperatures of 300°C.<br />
285
SILICATES<br />
OLIGOCLASE<br />
(Na, Ca) [AlSi 3<br />
O 8<br />
]<br />
An 10<br />
– An 30<br />
(Ab 90<br />
– Ab 70<br />
)<br />
Lattice ratio: a : b : c = 0.636 : 1 : 0.556 α = 93° 49’ β = 116° 27’ γ = 88° 59’<br />
Cell parameters: a o<br />
= 8.169, b o<br />
= 12.836, c o<br />
= 7.134 Z = 4<br />
IR-spectrum: 405 430 470 538 590 643 729 748 760 788 1010 1040 1105 1160 cm -1 .<br />
A u t h o r s: Barić (1966), Đorđević and Mijatović (1966), Golub (1961),<br />
John (1880, 1888), Jovanović (1957), Katzer (1924 and 1926), Kišpatić (1897,<br />
1917), Koch (1908), Majer (1963), Marić (1927), Pamić (1961a, 1961b, 1962, 1969,<br />
1969a, 1971, 1971a, 1972d), Pamić and Kapeler (1969), Pamić and Papeš (1969),<br />
Pamić, Šćavničar and Međimorec (1973), Pamić and Tojerkauf (1970), Paul (1879),<br />
Simić (1964), Stangačilović (1956), Schafarzik (1879), Trubelja (1966a), Trubelja<br />
and Pamić (1956), Varićak (1957, 1966), Vujanović (1962).<br />
Oligoclase belongs to the plagioclase group of minerals (acid plagioclases),<br />
and is a typical rock-forming mineral. Literature data on the occurrence of oligoclase<br />
in Bosnia and Hercegovina is very scarce, particularly with respect to information<br />
available for the other members of the plagioclase group. Data on quantitative optical<br />
measurements are particularly lacking.<br />
Oligoclase occurs in Bosnia and Hercegovina in igneous and metamorphic<br />
rocks of the Bosnian serpentine zone and in Triassic igneous rock series. Very<br />
little data is available on the abundance of oligoclase in Tertiary effusive rocks and<br />
associated tuffs. Nevertheless, oligoclase has been determined in various rocks of<br />
Mt. Motajica and Mt. Prosara, and from other localities.<br />
286<br />
1. Oligoclase in rocks of the Bosnian serpentine zone (BSZ)<br />
C. von John (1880) published first data on the occurrence of oligoclase in<br />
rocks from the BSZ (area of Višegrad). Results of a chemical analysis of oligoclase<br />
is as follows: SiO 2<br />
= 64.12, Al 2<br />
O 3<br />
= 23.48, CaO = 3.82, MgO = traces, Na 2<br />
O = 8.49,<br />
K 2<br />
O = 0.90, Total = 100.81<br />
The oligoclase grains are, according to John, up to 3-4 cm long. Golub (1961)<br />
determined oligoclase as en essential constituent of the oligoclasites from Kotlovača<br />
creek (oligoclase forms an aggregate of a vein within an actinolite gabbro), and basalts<br />
from Brnjačin Jarak at Mt. Kozara. The available microscopic measurements (done on<br />
a rotating stage microscope) indicate an An content of 19.5% and a negative average<br />
-2V angle of 83°. Oligoclase occurs together with andesine in the basalt rock from Mt.<br />
Kozara. The An content is 19%, the -2V angle is in the range 84° to 87°.<br />
Pamić and Kapeler (1969) studied the gabbro-dolerites of Kozarački potok,<br />
where they determined oligoclase occuring together with other plagiolases.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Trubelja (1966a) determined oligoclas as an important mineral in the andesitedacites<br />
from the Bukovica creek, and delenites from the Trnova potok on Mt. Kozara.<br />
Oligoclase occurs in rocks on Mt. Borja (Pamić and Tojerkauf 1970), and – together<br />
with albite – in the granites outcropping in the Teslić – Kotor Varoš region.<br />
Majer (1963) identified zonar plagioclases in pebbles of a conglomerate<br />
belonging to the diabase-chert formation (from Prisoj). The central parts of the<br />
grains are composed of oligoclase (up to 12.5% An) while the albite rims contain<br />
ca. 7.5% An.<br />
Đorđević and Mijatović (1966) determined oligoclase and albite in veins<br />
within serpentine rocks in the Zavidovići area. The veins are ca. 3 m thick and about<br />
8 meters long. Oligoclase was determined by microscopic measurements and x-ray<br />
diffracton. The average An content is 13%.<br />
Paul (1879) and Schafarzik (1879) studied the diabases rock used in the<br />
construction of the Doboj fortress where they found oligoclase. Kišpatić (1897, 1900)<br />
also notes the presence of oligoclase and andesine in sandstones from Kostajnice<br />
(Doboj) and in pebbles of the ‘red Maglaj granite’.<br />
Pamić (1969a, 1971, 1971a), Pamić et al. (1973) determined the presence<br />
of plagioclases, including oligoclase, in the amphibolites from the Bosnian<br />
serpentine zone. For instance, oligoclase and andesine are essential constituent of<br />
the amphibolites (pyroxene schists) from Mt. Skatavica, and in the Mt. Krivaja – Mt.<br />
Konjuh ultrabasic/amphobolite series. The cited authors also found a relationship<br />
between the chemical composition of plagioclases and some physical properties of<br />
amphiboles. Acid plagioclases (oligoclase, andesine) normally occur together with<br />
optically negative amphiboles (green and brown hornblende). This relationship is<br />
illustrated in Figure 24.<br />
Figure 24. The relationship between plagioclase composition and optic axial angles of<br />
amphiboles in amphibolites of the Bosnian serpentine zone (Pamić et al. 1973).<br />
287
SILICATES<br />
2. Oligoclase in Triassic igneous rocks<br />
According to available literature data, oligoclase occurs in rocks of mid-<br />
Triassic age outcropping in the area of Konjic, Jablanica, Prozor and Čevljanovići,<br />
as well as in the Ilidža – Kalinovik zone – Marić (1927), Pamić (1961a, 1961b, 1962,<br />
1969), Jovanović (1957), Simić (1964), Vujanović (1962).<br />
Marić (1927) determined oligoclase as an essential constituent of some<br />
differentiates of the gabbro rocks at Jablanica. Here, the basic plagioclase labradorite<br />
is usually surrounded with a layer (rim) of oligoclase (i.e. the rocks from the village<br />
of Zlato). Microscopic measurement (the symmetrical extinction procedure) of the<br />
oligoclase layer of plagioclase grains, an average An content of 25% was determined.<br />
More acid oligoclases (surrounding andesine grains) have also been identified, and these<br />
contain ca. 15% An. John (1888) provides results of the chemical analysis of oligoclase<br />
from a vein within the gabbro: SiO 2<br />
= 62.90, Al 2<br />
O 3<br />
= 22.80, Fe 2<br />
O 3<br />
= 1.05, CaO = 3.55,<br />
MgO = 0.40, Na 2<br />
O = 8.49, K 2<br />
O = 0.53, Loss-on-ignition = 0.90, Total = 100.81<br />
Pamić (1961a, 1961b) determined oligoclase in spilites, andesinekeratophyres<br />
and quartz-keratophyres from the area of Konjic, Jablanica and Prozor.<br />
Oligoclase occurs usually in association with albite and contains ca. 13-15% An.<br />
Jovanović (1957) noted the presence of oligoclase in granites from Mt. Prenj.<br />
Pamić (1962) identified oligoclase as a prominent mineral in K-Na- spilites<br />
from the Turovo area of the Ilidža – Kalinovik zone, near the source of the Željeznica<br />
river. The An content of this oligoclase can be as high as 20%.<br />
Simić (1964) studied the basic volcanic rocks from the Rača creek (north<br />
of Sarajevo) and found oligoclase (27% An) and andesine plagioclases in them.<br />
Andesine is normally surrounded with a rim of oligoclase.<br />
Vujanović (1962) determined oligoclase in the manganese mineral<br />
paragenesis at Čevljanovići.<br />
3. Oligoclase in rocks from Mt. Motajica and Mt. Prosara<br />
Koch (1908) provides first data on the abundance of oligoclase in rock from<br />
Mt. Motajica. It occurs in the granite from Veliki Kamen (Vlaknica), and in the<br />
muscovite-bearing granite from Brusnik. Oligoclase is much less abundant than the<br />
other plagioclases.<br />
Stangačilović (1956) determined oligoclase as am accessory constituent of<br />
altered granites from Mt. Motajica.<br />
288
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Varićak (1966) published a substantial amount of data based on microscopic<br />
measurements of oligoclase in various rocks from Mt. Motajica (a treatise on the<br />
petrology of Mt. Motajica). Oligoclase thus occurs in normal granites, „frozenedge<br />
granites“, leucocratic granites, pegmatites and aplites, contactolites, gneisses,<br />
kornites, amphibolites and amphibolite-schists. In norml granite, oligoclase has an<br />
An content between 10% and 18%, while the 2V angle lies in the range +86° to -86°.<br />
The „frozen-edge“ granite contains normally oligoclase with a zonar structure (two<br />
zones). The An content is 18-20%. The -2V angle = 83-84°. Twinning according the<br />
albite law is common. The leucocratic granite contains oligoclase associated with<br />
albite. The An content of this oligoclase is 15%. Oligoclase in other mentioned rocks<br />
has similar properties.<br />
Varićak (1957) found that oligoclase and albite are essential constituent<br />
of the green metamorphic rocks of Mt. Prosara, but gives no further data on these<br />
plagioclases.<br />
4. Oligoclase in Tertiary igneous rocks<br />
John (1880) provides first information on the occurrence of oligoclase in<br />
Tertiary-age effusive rocks fro Srebrenica. Subsequent reserach could not confirm<br />
this finding.<br />
Trubelja and Pamić (1956) made microscopic determinations of oligoclase<br />
(and andesine) in biotite-bearing dacites from the left bank of the Bosna river.<br />
Barić (1966) determined oligoclase in Tertiary volcanic tuffs found in the<br />
Livno area. Although most microscopic determinations indicate the presence<br />
of andesine, some data correspond to high-temperture oligoclase (28-30% An,<br />
2V = -81.5°).<br />
ANDESINE<br />
(Na, Ca) [Al 1-2<br />
Si 2-3<br />
O 8<br />
]<br />
An 30<br />
– An 50<br />
(Ab 70<br />
– Ab 50<br />
)<br />
Lattice ratio: a : b : c = 0.635 : 1 : 0.552<br />
α = 93° 24’ β = 116° 10’ γ = 90° 24’<br />
Cell parameters: a o<br />
= 8.176, b o<br />
= 12.879, c o<br />
= 7.107<br />
IR-spectrum: 429 465 537 632 741 1005 1090 1143 cm -1 .<br />
(for andesine with 33% An, ref. Zussman 1967).<br />
428 471 538 625 678 744 1005 1090 1143 cm -1 .<br />
(for andesine with 43% An, ref Zussman 1967)<br />
289
SILICATES<br />
A u t h o r s: Barić (1966), Buzaljko (1971), Behlilović and Pamić (1963),<br />
Čelebić (1967), Džepina (1970), Đorđević (1958), Golub (1961), Jurković (1954a),<br />
Katzer (1924 and 1926), Kišpatić (1897, 1900, 1917), Koch (1908), Luković (1957),<br />
Majer (1961), Majer and Jurković (1957, 1958), Matić (1927), Pamić (1961a, 1961b,<br />
1969, 1969a, 1971, 1971a, 1972, 1972d), Pamić, Dimitrov and Zec (1964), Pamić<br />
and Kapeler (1969), Pamić and Papeš (1969), Pamić, Šćavničar and Medjimorec<br />
(1973), Paul (1879), Podubsky and Pamić (1969), Polić (1951), Ramović (1957,<br />
1962), Schafarzik (1879), Simić (1964), Stangačilović (1956), Šćavničar and Jović<br />
(1962), Tajder (1951/53, 1953), Trubelja (1960, 1961, 1962a, 1963, 1963b), Trubelja<br />
and Pamić (1956, 1957, 1965), Trubelja and Slišković (1967), Varićak (1966).<br />
Andesine occurs in Bosnia and Hercegovina in igneous, sedimentary and<br />
metamorphic rocks and is a typical rock-forming mineral. It is fairly abundant in<br />
igneous and metamorphic rocks of the Bosnian serpentine zone and the associated<br />
diabase-chert series. The Triassic igneous rocks in the Konjic – Jablanica – Prozor<br />
area also contain andesine as an essential constituent. The granites and some other<br />
rocks at Mt. Motajica contain andesine. The Tertiary-age effusive rocks and tuffs<br />
contain andesine together with other plagioclases.<br />
290<br />
1. Andesine in rocks of the Bosnian serpentine zone (BSZ)<br />
According to available literature reference, andesine occurs in various<br />
rocks belonging to the Bosnian serpentine zone. These rocks are found in the area<br />
of Višegrad, at Mt. Konjuh, in the watershed of the rivers Bosna and Vrbas (at Mt.<br />
Skatovica) as well as on Mt. Kozara.<br />
Trubelja (1960) determined andesine in the basalts from the village of<br />
Lahci, near Višegradska Banja. Labradorite is also present in this rock. The andesine<br />
grains are mostly idiomorphic and fresh. Occasional fractures are filled with more<br />
acidic third-generation plagioclase (albite ?). Their zonar structure is clearly visible<br />
under the microscope. The andesine and labradorite grains are frequently pitted<br />
and corroded, an effect of their partial resorption. The An content of these andesine<br />
grains is around 50%. The +2V angle = 77.5-84.5°. Microscopic measurements were<br />
done on twins and multiple andesine twins.<br />
Trubelja (1961) determined andesine and labradorite as essential constituents<br />
of the gabbro-diorite vein at the village of Podpaklenik, near Veliki Rastik on Mt.<br />
Konjuh. The An content of this andesine is more zhan 45%, while the +2V angle =<br />
78° to 82°. The plagioclases have a zonar structure.<br />
Đorđević (1958) identified extensively altered plagioclase in gabbroid rocks<br />
from the Vareš area. Microscopic measurements correspond to an An content of<br />
50%, so the plagioclase can be defined as basic andesine.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The amphibolites from the Krivaja – Mt. Konjuh area contain andesine, usually<br />
associated with optically negative amphiboles (Pamić 1971a, Pamić et al. 1973).<br />
Džepina (1970) determined andesine in the garnet-bearing metamorphic<br />
rocks from the southern flanks of Mt. Borja. This andesine has an An content of 42%,<br />
and usually occurs in the form of xenoblasts displaying some twinning lamellae.<br />
Alteration of plagioclase to prehnite, albite and sericite is more or less extensive. The<br />
metamorphic rocks (garnet-diopside schists) from Mt. Skatovica near Banja Luka<br />
contain andesine with 41% An (Pamić 1969, Pamić et al. 1973).<br />
Paul (1879) and Schafarzik (1879) studied the diabases rock upon which the<br />
Doboj fortress is erected, in which they determined andesine. Kišpatić (1897, 1900)<br />
also notes the presence of andesine in sandstones of this area and in pebbles of the<br />
‘red Maglaj granite’ (found at Mala Bukovica).<br />
Barić (unpublished results) made a detailed microscopic study of the diabases<br />
from Doboj (fortress). Measurements done using a rotating-stage microscope<br />
confirmed that the plagioclase contained in the diabase is a basic andesine (or acid<br />
labradorite) with high-temperature optical constants. The variations of anorthite<br />
content and 2V angles is as follows:<br />
% An 52-48 44-46 54-51 53-50.5 51-52 51 55<br />
2V +75-79° -80° +77.5° +75° +78° +73° +75°<br />
One twinned plagioclase crystal had 62-63% An, corresponding to labradorite.<br />
Golub (1961), Trubelja (1966a), Pamić and Kapeler (1969) investigated<br />
andesine-bearing rocks of Mt. Kozara. According to Golub, andesine is an essential<br />
constituent of diabases from the Kotlovače and Huremovac creeks. The diabase<br />
from Kotlovače creek contains columnar andesine grains with 39-46.8%<br />
An (+2V = 84-85°). The grains are 0.3-2 mm in size, and often zonar in structure.<br />
The material from Huremovac contains prismatic andesine grains. Larger grains are<br />
uncommon and display extensive alteration. Microscopic measurements (extinction<br />
angle measurements on 8 grains) correspond to 45% An.<br />
Trubelja (1966a) identified andesine of dolerites and diabases on the northern<br />
flanks of Mt. Kozara (Trnova creek). The content of An varies in the range 36.3-50%.<br />
The 2V angles can be positive or negative.<br />
2. Andesine in Triassic igneous rocks<br />
Andesine is often an essential constituent of intrusive, effusive and veintype<br />
rocks of Triassic age in various regions of Bosnia and Hercegovina (also in<br />
associated pyroclastic rocks).<br />
291
SILICATES<br />
Pamić (1961a, 1961b) determined andesine in andesites from Vrata near<br />
Sovići, in the area of Jablanica and Prozor in Hercegovina. Andesine occurs together<br />
with labradorite. The An content is 47-50%, the +2V angle = 83°. The andesine grains<br />
have zonar structure and are mostly fresh. Twinning according to the Carlsbad, albite<br />
and pericline laws have been observed.<br />
Marić (1927) was able to identify plagioclases in some differentiates of the<br />
gabbro series at Jablanica. The composition of these plagioclases corresponds to<br />
andesine – labradorite.<br />
Čelebić (1967) studied the andesine-containing keratophyres from Bukove<br />
Ravni near Doljani, where andesine is an essential constituent. The andesine occurs<br />
as idiomorphic or hipidiomorphic phenocrysts, twinned according to the albite law<br />
(less often by the Carlsbad law). Microscopic measurements correspond to 34-48%<br />
An, with an average value of 42%, +2V = 77-83°.<br />
Behlilović and Pamić (1963) determined neutral plagioclase (probably<br />
andesine) in tuffs from the Drežanka river watershed. Andesine was also determined<br />
in the tuffs from Stupari.<br />
The basic and neutral intrusive igneous rocks from Bijela Gromila (Travnik<br />
area) contain andesine and labradorite as essential constituents (Majer and Jurković<br />
1957, 1958). Andesine and labradorite also occur in andesites from the village of<br />
Orašine in the schist mountains of central Bosnia (Jurković 1954a).<br />
Polić (1951) maintains that andesine and labradorite are essential constituents<br />
of andesites from Ljubovički creek, close to the village of Gojevići, near Bakovići.<br />
Microscopic measurements were done by V. Nikitin.<br />
Simić (1964) determined the presence of andesine in the complex of<br />
basic rocks, located to the north of Sarajevo, near the source of Orački creek. The<br />
plagioclase grains are zonar. The central portions contain about 46% An, while the<br />
rims consist of oligoclase.<br />
Trubelja (1962a, 1963), Trubelja and Slišković (1967), Buzaljko (1971)<br />
studied the igneous rocks and their pyroclastic associates in south-eastern Bosnia.<br />
Andesine is often an essential constituent of these rocks. The dacites (quartzporphyres)<br />
from the Lim river valley contain zonar andesite with 45-47% An<br />
(+2V = 80°). The rock from the village of Omačine has more than 50% An and a<br />
corresponding +2V angle of 85°.<br />
The celadonite-bearing sandstones from Kiprovac and Borovica (near<br />
Vareš) contain andesine with 45-48% An. Andesine was determined by microscopic<br />
measurements and x-ray diffraction (Ramović 1957, Trubelja 1969).<br />
292
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Trubelja and Slišković (1967) measured the andesine in andesites from the<br />
Tjentište area. The andesine contains 35-44% An.<br />
3. Andesine in Tertiary igneous rocks<br />
The treatise on the petrology of dacites in the Srebrenica area (Tajder<br />
1951/53, 1953) contains numerous microscopic determinations of plagioclases<br />
(including andesine) in these rocks. Andesine is an essential constituent of biotitebearing<br />
dacites (Jamno creek, Sase, Divljak), dacites (Kiselica creek, Majdan creek),<br />
biotite-bearing dacites (village of Ažlice), amphibole-bearing dacites (Srebrenica)<br />
and propilitized dacites (Crvena Rijeka).<br />
The biotite-bearing dacites from Jamno creek contain andesine and<br />
labradorite as large, idiomorphic crystals (the largest ones are more than 1 mm long).<br />
Twinning on the albite, Carlsbad and combined CA law is common. Some grains<br />
are zonar. The An content is in the range 48-50% which correspond to very basic<br />
andesine. Alteration into kaolinite can be extensive. The +2V angle = 76-87.5°. The<br />
andesine from the dacites of Kiselica creek contain 42-50% An. The idiomorphic/<br />
hipidiomorphic crystals are large (the largest one was 1.8 x 2.2 mm in size) and<br />
sometimes zoned. Similar twinning as in the previous case.<br />
The biotite-bearing dacites from Ažlice contains andesine with 43-50% An<br />
(+2V = 80-89°). Some grains correspond to labradorite composition. The plagioclase<br />
grains are mostly idiomorphic, zonar and almost always twinned (albite, Carlsbad<br />
laws). Some grains are twinned on the pericline law and display a rhombic twinning<br />
plane. Most of the grains are fresh, although some show signs of moderate alteration<br />
(to calcite and kaolinite).<br />
The amphibole-bearing dacites from Srebrenica contain andesine of similar<br />
microphysiographic properties. The An content is 46-49%, the +2V angle = 80-85°.<br />
The biotite-bearing dacites from the village of Sase contain andesine<br />
phenocrysts with an averag An content of 44% (+2V = 80.5°). A similar rock from<br />
Divljak carries andesine with 46% An (+2V = 86°).<br />
The treatise on the petrology of the Srebrenica area (Tajder 1953) discusses<br />
also the temperature relationships of plagioclase, icluding andesine. Important are<br />
spherical coordinates and angles of specific geometric elements with the proncipal<br />
vibrational directions X, Y and Z. The cited publication by Tajder contains 37 such<br />
measurement (for the [010] axis) of which only 5 datasets correspond reasonably<br />
well to the migration curve in the Nikitin diagram (1936). The rest of the data is<br />
‘grouped’ to the ‘southwest’ of the existing curve, in an area where there is no<br />
curve in the Nikitin diagram. The first corresponding curves (for high-temperature<br />
293
SILICATES<br />
optics) were published in 1958 by Zavarickij et al. This is a strong indication that<br />
the andesine contained in the Tertiary effusive rocks of the Srebrenica complex is a<br />
high-temperature variety of this plagioclase (Barić 1959).<br />
Trubelja and Pamić (1956) and Pamić et al. (1964) determined andesine as<br />
an essential constituent of the andesite-dacite rocks from the Bosna river valley. The<br />
biotite-bearing dacite on the left bank of the Bosna river (around Maglaj) contain<br />
idiomorphic to hipidiomorphic andesine, which is sometimes extensively altered to<br />
kaolinite and calcite. A comparatively small number of microscopic measurement<br />
(on a rotating-stage microscope) indicate that the An content is in the range 34-37%.<br />
More data is available for the andesine occurring in amphibole-bearing<br />
dacites from the village of Parnice. Andesine phenocrysts are usually zoned and<br />
twinned on the Carlsbad, albite or complex Carlsbad-albite law (multiple twins were<br />
also observed). Alteration of the andesine grains can be extensive. Their An content<br />
is in the range 34-45.5%. The optical character is negative, 2V = -79° to -88°. Some<br />
grains only have a positive 2V angle of 80° to 82°.<br />
Majer (1961) determined that the dacitelike rocks from the Blatnica creek<br />
near Teslić contain andesine with a 40.5% An content (this is the average value of<br />
several measurements). Grains can be up to 3 mm in length, have a zonar structure and<br />
show polysynthetic twinning. Some grains show signs of extensive kaolinitization<br />
and calcitization. Many have rounded rims due to corrosion.<br />
294<br />
4. Andesine in sediments and pyroclastic rocks<br />
There is a quite limited amount of data on the presence of andesite in sediments<br />
and pyroclastic rocks – Barić (1966), Luković (1957), Šćavničar and Jović (1962).<br />
Barić (1966) made numerous microscopic determinations of plagioclases<br />
contained in tuffs from the Livno area, and found that most of the grains are andesine.<br />
Their An content is 30-39.5% and the 2V angles are negative, with a few exceptions.<br />
This andesine has high-temperature optical constants. Luković (1957) determined<br />
andesine as an essential constituent of Neogene tuffs from Tuzla. Šćavničar and<br />
Jović (1962) determined andesine in Pliocene-age sands from the Kreka coal basin.<br />
5. Andesine in rocks from Mt. Motajica<br />
Koch (1908), Katzer (1924, 1926), Stangačilović (1956) and Varićak (1966)<br />
provide data on the abundance of andesine in the various rocks from Mt. Motajica.<br />
According to Varićak (1966), andesine occurs in amphibole-bearing gneisses,<br />
hornblendites, amphibolites, amphibole schists and granite porphyres. Stangačilović<br />
notes the presence of andesine in kaolinized granites, but only as an accessory
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
constituent. Granite porphyres contain less andesine than albite and oligoclase. The<br />
amphibole-bearing gneisses contain andesine as a prominent mineral, together with<br />
oligoclase. Andesine crystals and grains are usually twinned on the pericline law so<br />
that it displays a lamellar texture. Manebach-type twins are rare. The An content is<br />
34-38.5% (+2V = 85-87°).<br />
LABRADORITE<br />
(Ca, Na) [Al 1-2<br />
Si 2-3<br />
O 8<br />
]<br />
An 50<br />
– An 70<br />
(Ab 50<br />
– Ab 30<br />
)<br />
Lattice ratio: a : b : c = 0.635 : 1 : 2 x 0.552<br />
α = 93° 34’ β = 116° 06’ γ = 89° 47’<br />
Cell parameters: a o<br />
= 8.16, b o<br />
= 12.86, c o<br />
= 2 x 7.10 Z = 8<br />
IR-spectrum: 427 465 538 622 674 744 992 1089 cm -1 .<br />
(for labradorite with 52% An, ref. Zussman 1967).<br />
427 465 538 619 679 747 992 1093 1139 cm -1 .<br />
(for labradorite with 67% An, ref Zussman 1967)<br />
The peaks at 538 and 622 cm -1 are diagnostic.<br />
A u t h o r s: Barić (unpublished results), Brajdić (1964), Džepina (1970), Golub<br />
(1961), John (1880, 1888), Jurković (1954a), Karamata (1953), Kišpatić (1897, 1900,<br />
1904, 1904a, 1904b, 1910), Majer and Jurković (1957, 1958), Marić (1927), Pamić<br />
(1960a, 1961a, 1961b, 1969a, 1971, 1971a, 1972, 1972d), Pamić and Antić (1964), Pamić<br />
and Kapeler (1969), Pamić, Šćavničar and Medjimorec (1973), Polić (1951), Ramović<br />
(1957, 1962), Ristić, Panić, Mudrinić and Likić (1967), Sijerčić (1972a), Šibenik-Studen<br />
and Trubelja (1971), Tajder (1953), Trubelja (1957, 1960, 1961, 1966a), Trubelja and<br />
Pamić (1957, 1965), Trubelja and Slišković (1967), Tućan (1928).<br />
Labradorite is a very common and abundant mineral in the rocks of Bosnia<br />
and Hercegovina. It occurs most frequently in basic igneous rocks (gabbro, diabase<br />
etc.) and amphibolites of the Bosnian serpentine zone (BSZ).<br />
Labradorite is also an essential constituent of Triassic-age igneous rocks of<br />
the volcanogenic-sedimentary series. It is abundant both in basic intrusive rocks as<br />
well as effusives, veins and tuffs.<br />
The Tertiary volcanic rocks rocks contain plagioclases, including labradorite,<br />
as essential mineral constituents.<br />
1. Labradorite in rocks of the Bosnian serpentine zone (BSZ)<br />
C. von John (1880) published first data on the occurrence of labradorite in<br />
rocks from the BSZ. He determined the mineral in the gabbro rocks from Barakovac<br />
and troctolites from the Višegrad area.<br />
295
SILICATES<br />
The wellknown treatise on the rock of the serpentine zone (Kišpatić 1897,<br />
1900) contains a substantial number of microscopic determinations of plagioclases<br />
in various rocks of the BSZ. However, not much information refers specifically to<br />
labradorite. Nevertheless, Kišpatić notes that labradorite is an essential constituent<br />
of the eclogite pyroxenite from Višegrad as well as basic igneous rocks from the<br />
Doboj area. A description of labradorite contained in amphibolite from Mt. Borja<br />
has been published in a separate paper (Kišpatić 1904b). This labradorite is usually<br />
fresh and transparent, with irregular, polysynthetically twinned grains (twinning on<br />
the albite and pericline laws is also common). It contains 66% An. Unpublished<br />
results of microscopic investigations of the Gradina diabases from Doboj showed the<br />
presence of high-temperature labradorite and andesine (Barić, unpublished results).<br />
Trubelja (1957, 1960) determined labradorite is abundant in gabbros,<br />
diabases, gabbro-pegmatites and gabbro-peridotites from Višegrad. The gabbroperidotites<br />
from Bosanska Jagodina contain the low-An variety of labradorite with<br />
an average An content of 56%. Based on the results of numerous microscopic<br />
measurements (on a rotating-stage microscope) the An content varies between<br />
50% and 63.5% (+2V = 74.5-85°). Grains are frequently twinned on the albite and<br />
Carlsbad law.<br />
The olivine-bearing gabbros from Rijeka, near Velika Gostilja, contain<br />
a high-An labradorite with an average An content of 69.3% (so that grains with<br />
bytownite chemistry may be encountered). The abundance of labradorite in this rock<br />
is more than 50%. Grains are mostly fresh, and only a few cases of fracturing and<br />
alteration have been observed. The An content is comparatively stable, in the range<br />
64.5% to 70% (+2V = 80° to 86°). Twinning according to the albite, Carlsbad and<br />
comples albite-Carlsbad law is common. The gabbro rock also hosts monomineral<br />
labradorite veins. This labradorite has more or less identical properties to the one in<br />
the rock matrix. The An content is 69%, so that some of the labradorite may in fact<br />
be bytownite.<br />
The gabbros from the village of Pijavice contain labradorite and some<br />
bytownite. The An content is 65-70%. The veins in the gabbro-pegmatite from<br />
Višegradska Banja are composed largely of labradorite (the grains are of variable<br />
size, in the millimeter to centimeter range). Twinning lamellae are often bent due to<br />
tectonic forcing. The An content is 57.5-62% (+2V = 84°).<br />
The diabases from Banja Potok contain labradorite with an An content of<br />
58.5% (+2V = 80-82°) and some of the plagioclase is probably andesine. The crystals<br />
are prismatic and often twinned. The dolerite outcrops on the Dobrun – Smrijeće<br />
road in the river Rzav valley contain some labradorite (68.5% An).<br />
296
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The basalts found in the Lahci area contain labradorite as an essential<br />
constituent, in addition to andesine. The phenocrysts have a zonar structure, are<br />
mostly idiomorphic and fresh with occasional evidence of resorptive corrosion.<br />
Twinning on the albite and Carlsbad law is common. The An content is variable<br />
(53-70%) and the optic axial angle +2V = 74-83°.<br />
Rocks of the Krivaja – Konjuh ultrabasic complex often contain labradorite<br />
as their essential constituent. This is true both for the igneous as well as for the<br />
metamorphic rocks. This complex has been investigated in detail, and numerous<br />
microscopic determinations, chemical and XRD analyses are given in publictions<br />
by Trubelja (1961), Brajdić (1964), Pamić (1971, 1971a), Pamić and Antić (1964),<br />
Pamić et al. (1973), Šibenik-Studen and Trubelja (1971), Ristić et al. (1967), Pamić<br />
and Kapeler (1970).<br />
The dolerites from Blizanci creek are largely composed of labradorite and<br />
some bytownite (Trubelja 1961). The crystals are prismatic (up to 1 cm in length)<br />
with a zonar and lamellar structure. The zonar structure is in some grains so expressed<br />
that the central portion of the grain is dark when observed in polarized light, while<br />
the sectors on the rim are not in extinction position. The polysynthetic twinning<br />
lamellae are very narrow so microscopic measurements (rotating stage) could be<br />
done only with some difficulty. Nevertheless, most of the grains were fresh and the<br />
An content was determined as 64.5-70% (+2V = 80-85°).<br />
Brajdić (1964) determined labradorite in the gabbro-pegmatite from<br />
Olovo (village of Bjeliš). The labradorite grains were quite dark (grey) due to<br />
inclusions of amphibole. Twinning according to the albite law is common, less<br />
frequently according to the Carlsbad or pericline law. Based on a number of<br />
microscopic rotating-stage measurments, the An content was determined as 50-58%<br />
(corresponding to +2V = 74-86°).<br />
Chemical analysis of this labradorite yielded following results (in %):<br />
SiO 2<br />
= 53.29; TiO 2<br />
= 0.13; Al 2<br />
O 3<br />
= 28.19; Fe 2<br />
O 3<br />
= 0.16; FeO = 0.80; MgO = 0.05;<br />
CaO = 10.98; Na 2<br />
O = 5.54; H 2<br />
O + = 1.11; H 2<br />
O - = 0.98; Total = 100.33%<br />
If the minor amounts of TiO 2<br />
, Fe 2<br />
O 3,<br />
FeO and MgO are disregarded (these<br />
probably reflect amphibole chemistry), and the remainder of the composition<br />
recalculated into albite and anorthite molecules (so that the entire amount of CaO<br />
and N 2<br />
O are bound to equivalent mount of Al 2<br />
O 3<br />
and SiO 2<br />
), a plagioclase with<br />
53.62% An content is obtained, corresponding to an acidic labradorite. This result is<br />
in accordance with microscopic measurements.<br />
The density of this labradorite, determined by the pycnometric method, is<br />
2.702 at 20°C. Ristić et al. (1967) determined labradorite as an essential constituent<br />
of the gabbro rocks from Mt. Konjuh. The average An content of gabbros from<br />
297
SILICATES<br />
Katranička Rijeka and Gnjilo Brdo is 55% (+2V varies in the range between 70°<br />
at Katranička Rijeka, to 85° at Gnjilo Brdo). These authors provide results of a<br />
chemical analysis of labradorite from the source area of the Bukovica river<br />
SiO 2<br />
= 51.11; Al 2<br />
O 3<br />
= 22.28; Fe 2<br />
O 3<br />
= 0.34; FeO = 0.88; MgO = 1.12; CaO = 12.06;<br />
Na 2<br />
O = 6.65; H 2<br />
O + = 4.20; H 2<br />
O - = 0.50;<br />
The results given above indicate that the labradorite is quite contaminated.<br />
Pamić and Antić (1964) determined labradorite to be the predominant and sometimes<br />
the only present plagioclase in the gabbro complex of Gostovička Rijeka near<br />
Zavidovići. The An content of this labradorite is 50-64% (+2V = 76-88°). The grains<br />
are mostly fresh, and twinning according to the albite law is common.<br />
Labradorite and other plagioclases are importanst and essential constituents<br />
of metamorphic rocks in the Krivaja – Konjuh area. They usually occur in<br />
amphibolites and corundum-bearing amphibolites (Pamić and Kapeler 1970;<br />
Pamić et al. 1973). Labradorite normally occurrs in association with pargasiteedenite<br />
and green hornblende.<br />
Trubelja and Pamić (1965) determined labradorite as an essential constituent of<br />
basic rocks at Mt. Ozren. The plagioclases contained in porphyrric amphiboledolerites<br />
of the Krivaja creek comprise two generations. The grains of the first generation<br />
are quite large and idiomorphic and rather weathered. Their An content is 64-79%<br />
corresponding to basic labradorite or acidic bytownite. Plagioclases of the second<br />
generation are more acidic than the porphyry labradorite phenocrysts.<br />
The metamorphic series of rocks at Mt. Skatovica frequently contain<br />
labradorite and other plagioclases (Pamić 1969, 1972; Pamić et al. 1973), mostly<br />
the oligoclase-bytownite members. Even some reaction effects between different<br />
plagioclases have been observed. For example, the sample which contains mainly<br />
oligoclase (21% An), contains also relicts of labradorite (58% An). This could mean<br />
that the rock originally contained basic plagioclases (labradorite through bytownite),<br />
but that alteration processes resulted in the formation of more acidic plagioclase<br />
(andesine and oligoclase).<br />
Golub (1961), Trubelja (1966a), Pamić and Kapeler (1969) identified<br />
labradorite as an important mineral in basic igneous rocks at Mt. Kozara, especially<br />
in the gabbro-type differentiates. Golub provides numerous and detailed microscopic<br />
measurements (rotating stage microscope) of labradorite in olivine gabbros, gabbros,<br />
uralite gabbros and gabbro-pegmatites from the southern flanks of Mt. Kozara.<br />
The gabbros from Jovača creek contain labradorite with an An content in the<br />
range 57.75-66% (average = 63% An). The average +2V angle = 84.5°. Twinning<br />
is according to the albite law. The optical constant of the labradorite contained in<br />
the olivine-bearing gabbros from Kozarački creek are almost identical to the ones<br />
298
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
cited above. On the other hand, the gabbros from Kozarački creek contain more<br />
acidic labradorite (average is 51% An, +2V angle = 80°). The composition of the<br />
labradorite in uralite gabbros is very similar (62.7% An, and 2V = +80°).<br />
The data on the abundance of labradorite in the above mentioned rocks is<br />
quite interesting. The olivine gabbro (Jovača creek) contains ca. 35% labradorite,<br />
while the olivine gabbro from Kozarački creek contains 70% labradorite. The<br />
abundance of labradorite in the gabbro from Kozarački creek is 57.5%, while the<br />
uralite gabbro contains 61% labradorite.<br />
The pegmatite veins from Kotlovača creek contains coarse grained<br />
labradorite. The crystals are 0.5-8 cm in length. The labradorite contains 55.5% An,<br />
the +2V angle is 76°.<br />
Trubelja (1966a) determined labradorite as an essential constituent of<br />
diabase-dolerites from the northern flanks of Mt. Kozara. The diabase from<br />
the Bukovica creek contains labradorite with 52-55% An and 2V = 84°, almost<br />
identical to the labradorite in dolerites form Trnava creek (54.5-56% An,<br />
+2V = 78-87°). The plagioclase in diabase porpyrites from Dobrlin are also<br />
labradorite (Kišpatić, 1904b).<br />
2. Labradorite in products of Triassic volcanism<br />
Labradorite is the most common and abundant mineral in rocks of the<br />
Triassic-age magmatism in various areas of Bosnia and Hercegovina (apart from<br />
rocks belonging to the Bosnian serpentine zone).<br />
The gabbro-diorites from Bijela Gromila (south of Travnik, schist mountains<br />
of central Bosnia) labradorite and other plagioclases (andesine, bytownite) as<br />
essential constituents (Majer and Jurković 1957, 1958). The diorite from Kopile<br />
contains plagioclase with 66% An, corresponding to labradorite – usually located in<br />
the central portions of the grains. The rims of the grains are normally composed of<br />
more acidic plagioclase (andesine). Such is the case with the olivine-bearing gabbros<br />
from Stajište (Margetići).<br />
Gabbros and its differentiates in the Jablanica complex contain labradorite<br />
as an essential constituent (John 1888, Kišpatić 1910, Marić 1927). In his account<br />
of gabbros in the Travnik – Bugojno area, Kišpatić (1910) notes the presence of<br />
labradorite and bytownite in the gabbros of the Jablanica complex. John isolated a<br />
rather clean labradorite from the ‘augite-diorite’ rock outcrops on the southern flanks<br />
of the complex and made a chemical analysis of this material:<br />
SiO 2<br />
= 53.50; Al 2<br />
O 3<br />
= 29.65; Fe 2<br />
O 3<br />
= 0.20; CaO = 11.55; MgO = 0.28; Na 2<br />
O =<br />
4.67; K 2<br />
O = 0.77; Loss-on-ignition = 0.75; Total = 101.37<br />
299
SILICATES<br />
Marić (1927) determined that the zonar plagioclase grains of the Jablanica<br />
gabbros are composed of labradorite in the core and oligoclase on the rim of such<br />
grains (the gabbro from the village of Zlata). In some cases labradorite forms the<br />
rim while bytownite the core of grains. The extensively altered gabbros contain<br />
labradorite with an An content of 53-58%, 2V = +75° (rim of grain); 61-69% An,<br />
2V = 83-83.5º (core of grain). The chemical composition of the labradorite was<br />
derived from the Fediuk curves and correspond to low-temperature plagioclase<br />
(Barić, unpublished results).<br />
Jurković (1954a) determined labradorite in the andesites near Orašine,<br />
close to Bakovići. Numerous microscopic measurements correspond to labradorite,<br />
although some grains were closer to andesine. The grains are quite different in size<br />
(0.03 x 0.03 mm to 2.0 x 1.3 mm. Jurković measured the grains using a standard<br />
micrometer-eyepiece. The labradorite crystals are mostly prismatic or columnar,<br />
only occasionally tabular parallel to (010). Most of the crystals are twinned<br />
(Carlsbad, albite and complex law) – polysynthetic twinning is also common. Zonar<br />
structure is more pronounced in the case of smaller grains. Crystal grains of the first<br />
generation are mostly fresh and display distinct cleavage planes along (001) and<br />
(010). Microscopic measurements (using arotating stage) on 3 grains gave following<br />
results: 57.5-59.25% An, +2V = 78-80°. The highest An content determined on some<br />
grains was 66%.<br />
Polić (1951) maintains that labradorite and andesine are essential constituents<br />
of andesites from Ljubovički creek, close to the village of Gojevići, near Bakovići.<br />
Microscopic measurements were done by V. Nikitin.<br />
Labradorite is also an important mineral of the spilite-keratophyre<br />
rocks found in the areas of Jablanica and Prozor, and elsewhere – Tućan (1928),<br />
Karamata (1953), Ramović (1957), Pamić (1960a, 1961a, 1961b). Tućan determined<br />
phenocrysts of zonar but completely fresh labradorite and bytownite in the andesites<br />
from Vrata in the river Doljanka watershed. Pamić (references as above) identified<br />
labradorite in the basalto-andesitic and pyroclastic rocks from Jablanica and Prozor.<br />
The An content of this labradorite is quite high (63-70%). The andesites from Vrata<br />
and Krstac contain labradorite with 52-54% An (+2V = 77-87°) associated with<br />
basic andesine. The labradorite in the tuffs from this are has an average of 62% An<br />
(+ 2V = 87°), while the tuff from Stupari contain a slightly more acidic plagioclase.<br />
Labradorite is an essential constituent of basalto-andesites from Kalinovik (Pamić<br />
1960a). Karamata (1953) and Ramović (1957) determined labradorite in basic<br />
igneous rocks and associated tuffs in the area of Vareš.<br />
Trubelja and Slišković (1967) determined labradorite in basic-to-neutral<br />
effusive and vein rocks of Mid-Triassic age. These rock are particularly abundant in<br />
the Hrčavka river valley. The labradorite has an An content of 64-67%.<br />
300
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
3. Labradorite in products of Tertiary volcanism<br />
Information on the abundance of labradorite in products of Tertiary volcanism<br />
can be found in the papers by Kišpatić (1904, 1904a), Ramović (1962) and Tajder (1953).<br />
Kišpatić determined labradorite – together with bytownite – in the<br />
hypersthene-bearing andesite from Potočari and Crveni Potok in the Srebrenica area.<br />
This labradorite contains 56% An (Kišpatić 1904a). It is also a constituent of dacites<br />
(from Kneževac near Srebrenica, and from Protin Han – on the road between Potočari<br />
and Srebrenica). Kišpatić (1904) found labradorite to be an essential constituent of<br />
the andesite-type rocks outcropping in the Bosna river valley. The same is the case<br />
for the andesitesfrom Maglaj.<br />
Tajder (1953) provides a substantial amount of data on the labradorite<br />
contained in the effusive rocks of the Srebrenica area. The dacites from the village of<br />
Diminići contain 50-56% An, the biotite-bearing dacite from Jamno creek (between<br />
50% and 52% An), from Ažlice (73% An). Based on the optical constants, the<br />
labradorite contained in the effusive rocks from Srebrnica is of the high-temperatures<br />
variety, like andesine.<br />
4. Labradorite in chlorite-bearing schists from Mt. Vilenica near Travnik<br />
Kišpatić (1904b) studied the labradorite contained in the chlorite-bearing<br />
schists found at Mt. Vilenica near Travnik. The labradorite grains have a vitreous<br />
texture and contain inclusions of epidote and chlorite.<br />
BYTOWNITE<br />
(Ca, Na) [Al 1-2<br />
Si 2-3<br />
O 8<br />
]<br />
An 70<br />
– An 90<br />
(Ab 30<br />
– Ab 10<br />
)<br />
Lattice ratio: a : b : c = 0.635 : 1 : 1.102<br />
α = 93° 22’ β = 115° 58’ γ = 90° 31’<br />
Cell parameters: a o<br />
= 8.171, b o<br />
= 12.869, c o<br />
= 14.181 Z = 8<br />
IR-spectrum: 425 431 480 538 620 680 751 938 987 1093 1134 cm -1 .<br />
(for bytownite with 85% An, ref. Zussman 1967).<br />
A u t h o r s: Đurić and Kubat (1962), Esih and Natević (1963), Golub (1961),<br />
John (1888), Karamata (1953), Katzer (1924, 1926), Kišpatić (1897, 1900, 1904,<br />
1904a, 1910, 1917), Kubat (1964), Majer (1962), Majer and Jurković (1957, 1958),<br />
Marić (1927), Marković and Takač (1958), Pamić (1960a, 1961b, 1969, 1969a,<br />
1971, 1971a, 1972, 1972d, 1974), Pamić and Kapeler (1969), Pamić, Šćavničar and<br />
301
SILICATES<br />
Medjimorec (1973), Pamić and Trubelja (1962), Ramović (1957), Schiller (1905),<br />
Tajder (1953), Trubelja (1957, 1960, 1961), Trubelja and Pamić (1965), Tućan<br />
(1928), Varićak (1966).<br />
Bytownite has quite a significant abundance as a rock-forming mineral<br />
in Bosnia and Hercegovina. It is a ubiquitous mineral and essential constituent of<br />
gabbro-type rocks and igneous rock series of Triassic and Tertiary age. It occurs<br />
frequently in metamorphic rocks, typically amphibolites.<br />
Basic igneous rocks (containing bytownite) are most common in the Bosnian<br />
serpentine zone. Triassic igneous rocks belong to the schist mountains of central<br />
Bosnia, in the Jablanica – Prozor area, in the Borovica – Vareš – Čevljanovići sector,<br />
and around Kalinovik. Bytownite is also a common constituent of the Tertiary-age<br />
effusive rocks of Mt. Motajica.<br />
302<br />
1. Bytownite in rocks of the Bosnian serpentine zone<br />
Kišpatić (1897, 1900, 1917) provided initial information on bytownite<br />
in rocks of the Bosnian serpentine zone (BSZ). This author made microscopic<br />
determinations of this plagioclase contained in the rocks of the Gostovići – Krivaja<br />
area, as well as around Višegrad. The diabases around Doboj contain bytownite<br />
associated with labradorite.<br />
In the Gostovići – Krivaja area bytownite occurs in troctolites from Ravni<br />
Potok, in lherzolites from Gostovići, in amphibolites on the Kopalište – Duboštica<br />
road and from Otežna, as well as in the pyroxene amphibolite from Borovnički<br />
creek. In the area of Višegrad, bytownite is an essential constituent of several basic<br />
igneous and metamorphic (and vein type) rocks. Bytownite is contained in diabases<br />
from the Lazački creek, in troctolites from the village of Lahci and the Rzav valley,<br />
in olivine gabbros from the Rijeka river valley near Dobrun and from Pijavice, in<br />
the actinolite schists and eclogite pyroxenites from Vidakovićev Potok, and in the<br />
pyroxene amphibolite from Kruševački Potok and Sokolovići.<br />
Kišpatić (1917) maintains that bytownite is quite abundant in the rocks of<br />
the Bosnian serpentine zone, and that almost all plagioclase in gabbros from Bosnia<br />
is bytownite (p. 37). The serpentinites and lherzolites also contain small amounts of<br />
bytownite. Schiller (1905) wrote about bytownite and anorthite contained in gabbroid<br />
rocks from the Višegrad area. These rock were also studied in more recent times by<br />
Trubelja (1957, 1960) and Marković and Takač (1958). These authors made numerous<br />
microscopic measurments of the plagioclases, using a rotating-stage microscope.<br />
The troctolites from Gornji Dubovik contain bytownite with an An content<br />
between 73% and 85% (average 79.5%). It can be optically positive or negative.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The optic axial angle lies in the range +2V = 85-87.5° or -2V = 86-89.5°. Bytownite<br />
grains are sometimes only fresh but commonly cracked. The fissures are often<br />
filled with secondary prehnite. More advanced serpentinization of olivine is usually<br />
accompanied with more extensive prehnitization of plagioclases. Bytownite grains<br />
are often twinned according to the Carlsbad or albite law. Another troctolite sample<br />
from the same location (Gornji Dubovik) contained bytownite with an An content<br />
above 80% (81% – 88% An). This bytownite is optically negative (-2V = 81-89°).<br />
Twinning is frequent (Carlsbad, albite or complex laws).<br />
The olivine gabbros from the village of Mirilovići contain bytownite with<br />
an average An content of 82.25% (range is between 79% and 85.5%) and a negative<br />
optical character (-2V = 83-89°). Twinning is common (albite and complex law). At<br />
Velika Gostilja, the olivine gabbro contains mostly labradorite and some bytownite<br />
(acidic bytownite with an average of 73.5% An, +2V = 82-84°).<br />
The troctolite from Lahci village in the Banja Potok valley contains bytownite<br />
with more than 80% An (the average is 84.5% An). The negative 2V angle varies<br />
between -81° and -89°. The uralite gabbros from the village of Smrijeće contain<br />
bytownite as an essential constituent. The grains are usually twinned and have a<br />
lamellar texture – many of the grains are fractured. Their An content is in the range<br />
76-88%, the average value is 81%. The -2V angle is in the range -78° to -89°.<br />
The bytownite contained in the almost monomineralic veins within the<br />
troctolite host rock near Čige has a very similar composition (average An content<br />
of 82%). The gabbros from the village of Pijavice contain both bytownite and<br />
labradorite.<br />
Trubelja (1960) provides further data on the abundance of bytownite<br />
in the basic effusive and vein rocks near Višegrad. The basic igneous and some<br />
metamorphic rocks of the Krivaja – Konjuh area contain variable amounts of<br />
bytownite and labradorite (Trubelja, 1961; Pamić 1971, 1971a, 1974; Pamić<br />
and Kapeler 1970, Pamić et al. 1973). The lherzolite from Grbovica creek at Mt.<br />
Konjuh contain a minor amount of bytwonite and anorthite. Their An content is<br />
84%, the -2V angle = 79° to 81°.<br />
The feldspar-peridotites at Karaula, on the Olovo – Kladanj road, contains a<br />
significant amount of bytownite so that it may be regarded as an essential constituent.<br />
Some anorthite is also present in the rock. The troctolite from the source area of the<br />
Blizanci creek contains bytownite with 71-82.5% An (-2V is between 85.5° and 89°).<br />
The dolerite rock from this creek contains more labradorite than bytownite.<br />
The olivine gabbros from Stupčanica creek (village of Bjeliš) contain<br />
bytownite with 77.5-89% An. This bytownite is extensively altered to prehnite.<br />
303
SILICATES<br />
The amphibolite rocks of the Krivaja – Konjuh complex contain bytownite<br />
which is almost always associated with pargasitic and edenitic hornblende. Similar<br />
parageneses occur also elsewhere in the Bosnian serpentine zone – i.e. at Mt. Skatavica<br />
near Banja Luka. Pamić et al. (1973) provide some more indepth information on the<br />
relationships between individual plagioclase minerals in these rocks.<br />
The basic igneous rocks of Mt. Ozren contain substantial amounts of<br />
bytownite (Pamić and Trubelja 1962; Trubelja and Pamić 1965). The olivine<br />
gabbros from Paklenica contain bytownite with 70-78% An (2V between +85°<br />
and -87°). Amphibolites from this area also contain bytownite – i.e. the pyroxene<br />
amphibolite from Gornja Bukovica contains quite fresh bytownite grains with<br />
72-82% An and -2V = 87-89°. Bytownite is also quite abundant in amphibolites<br />
and basic igneous rocks in the area between the rivers Vrbas and Bosna. The<br />
amphibole- and garnet-bearing gabbros and hornblendites contain both bytownite<br />
and anorthite (Majer 1962).<br />
The diabases at Mt. Čavka contain bytownite with 76% An (Đurić and Kubat<br />
1962; Kubat 1964). Bytownite is an essential constituent of the amphibolites at Mt.<br />
Skatovica near Banja Luka (Pamić 1969; Pamić et al. 1973).<br />
Bytownite is a rather common constituent of gabbros and associated basic<br />
igneous rocks from Mt. Kozara and Kozarački creek. Golub (1961) provides detailed<br />
microscopic measurements of plagioclases from these rocks. The troctolites from the<br />
Jovača creek contain ca. 54% bytownite by volume, as crystals 0.5-2 mm in size, of a<br />
columnar habit. Twinning and prehnitization are a common feature of this bytownite.<br />
The An content is in the range 74.5-79% (average is 76.7%). The 2V angle varies in<br />
the range -82° to -86°.<br />
The actinolite-bearing gabbros from Kotlovača creek contains an acidic<br />
bytownite with 72% An and a -2V angle of 85° to 88°.<br />
304<br />
2. Bytownite in products of Triassic volcanism<br />
Bytownite has been microscopically determined in several rock types<br />
belonging to the spilite-keratophyre series in Hercegovina, around Jablanica<br />
and Prozor (John 1888; Kišpatić 1910; Marić 1927; Tućan 1928; Pamić 1961a,<br />
1961b, 1969).<br />
The earliest reference on bytownite in the gabbro from the Jablanica massif<br />
is the paper by John (1888). In addition to microscopic measurements, John also<br />
provides a chemical analysis of a sample which he claims to be from the central<br />
portion of the massif.<br />
SiO 2<br />
= 46.80; Al 2<br />
O 3<br />
= 33.50; Fe 2<br />
O 3<br />
= 0.90; CaO = 15.85; MgO = 0.56; Na 2<br />
O =<br />
2.23; K 2<br />
O = 0.21; Loss-on-ignition = 0.67; Total = 100.72
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Kišpatić (1910) mentions labradorite and bytownite as essential constituents<br />
of the gabbro rock from Jablanica, failing to provide further information on bytownite.<br />
Marić (1927) determined that zonar grains frequently have bytownite in the center of<br />
the grains and labradorite on the rim. Marić reports that rocks containing labradorite<br />
can be found on right bank of the Neretva river, and near Bukov Pod.<br />
Bytownite is an essential constituent of many Triassic basic intrusive rocks<br />
(gabbros) from the schist mountains of central Bosnia – Bijela Gromila, south of<br />
Travnik (Kišpatić 1910; Katzer 1924, 1926; Majer and Jurković 1957, 1958).<br />
Microscopic determinations done by Pamić and Tućan provide evidence for<br />
the occurrence of bytownite (and labradorite) in some basalts and andesites in the<br />
area of the Rama and Doljanka rivers. The andesites from Vrata, near Sovići, contain<br />
fresh phenocrysts of zonar labradorite and bytownite (0.1-2.5 mm in size). Some<br />
alteration products (calcite, epidote) can be observed.<br />
Bytownite has been determined as an essential constituent of baslats<br />
and silimar rocks of the Triassic-age igneous-sedimentary series of Kalinovik,<br />
Rogatica, Draževići and Vareš (Pamić 1960a; Esih and Natević 1963; Ramović<br />
1957, Karamata 1953).<br />
3. Bytownite in products of Tertiary volcanism<br />
According to available literature references, bytownite occurs only in<br />
the effusive rocks of the Srebrenica area (Kišpatić 1904a; Tajder 1953). Kišpatić<br />
determined bytownite in the hypersthene-bearing andesite from Sikirić, and dacites<br />
from Ljubovija and Protin Han. Tajder (1953, based on microscopic measurments)<br />
determined bytownite only in the bytownite-dacites from the village of Diminići.<br />
The bytownite has 80% An.<br />
4. Bytownite in hornfelses from Mt. Motajica<br />
Varićak (1966) determined bytownite as an essential constituent of pyroxene<br />
hornfels at Mt. Motajica. The crystal grains display characteristic lamellar twinning<br />
(albite law). The average An content is 78.5%, the -2V angle is in the range 76-80º.<br />
305
SILICATES<br />
ANORTHITE<br />
Ca [Al 2<br />
Si 2<br />
O 8<br />
]<br />
Lattice ratio: a : b : c = 0.635 : 1 : 2 x 0.550<br />
α = 93° 10’ β = 115° 51’ γ = 91° 13’<br />
Cell parameters: a o<br />
= 8.177, b o<br />
= 12.877, c o<br />
= 14.169 Z = 8<br />
X-ray data: d 3.194 (100) 3.180 (100) 3.210 (58) 3.261 (53) 4.035 (52)<br />
IR-spectrum: 407 433 470 484 575 603 624 668 700 728 758 950 1020<br />
1085 1160 cm -1 .<br />
A u t h o r s: John (1888), Kišpatić (1897, 1900), Majer (1962), Pamić (1971,<br />
1971a, 1972d), Pamić and Kapeler (1970), Pamić, Šćavničar and Medjimorec (1973),<br />
Ristić, Panić, Mudrinić and Likić (1967), Schiller (1905), Trubelja (1960, 1961).<br />
The only occurrence of anorthite (as a rock-forming mineral) in Bosnia and<br />
Hercegovina are the rocks of the Bosnian serpentine zone, especially in its central<br />
and eastern parts. It occurs, sometimes as an essential constituent, in basic intrusive<br />
rocks and amphibolites. Some peridotites contain bytownite as an accessory mineral.<br />
306<br />
1. Anorthite in basic and ultrabasic rocks<br />
The occurrence of anorthite in basic instrusive rocks of the Bosnian<br />
serpentine zone was first determined by John (1880). He maintains that anorthite is<br />
an essential constituent of troctolites. In thin section, the anorthite grains are mostly<br />
fresh showing distinct polysynthetic twinning. The results of chemical analysis are<br />
quite close to that of anorthite:<br />
SiO 2<br />
= 44.7 3<br />
; Al2O3 = 34.50; CaO = 17.44;<br />
In his research concerning the basic plagioclases contained in gabbros from<br />
the Višegrad area, Schiller (1905) determined them as bytownite. However, as stated<br />
by this author, some measurements indicate that some present plagioclase could be<br />
anorthite (97-98% An).<br />
Kišpatić (1897, 1900) determined anorthite in the troctolite from Vukovac<br />
creek in western Bosnia, and near Rakovac (Doboj area). Anorthite is an essential<br />
constituent of olivine-bearing gabbros from Gostovići and Ravni Potok near<br />
Duboštica. This rock series belongs to the Krivaja – Konjuh ultrabasic complex.<br />
More recent microscopic investigations of the igneous rocks from the<br />
Višegrad area (Trubelja 1960) indicate that the gabbropegmatite from Karaula<br />
contains bytownite and anorthite. The An content is 90-100%, the -2V angle = 76° to<br />
83°. Microscopic and x-ray diffraction data also show that anorthite is an important
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
mineral of gabbros, gabbro-peridotites and peridotites of the Krivaja – Konjuh<br />
metamorphic complex (Trubelja 1961; Ristić et al. 1967; Pamić 1971).<br />
Lherzolites from Mt. Konjuh (Zečji Vrat, 1275 m asl) contain anorthite as an<br />
accessory constituent. Anorthite grains are fresh and have an isometric shape with a<br />
lamellar texture. Their An content is 90-100% (-2V = 75-86.5°). The lherzolite from<br />
the source area of the Grabovica creek also contains minor amounts of bytownite and<br />
anorthite. Twinning lamellae have a wedge-like shape (they are broader on one end).<br />
The An content is 96-97%.<br />
The gabbro-peridotite outcrops on the Olovo – Kladanj road, southwest<br />
from Karaula contain bytownite and anorthite (optically negative) which are more<br />
or less extensively altered by prehnitization processes. Anorthite is an essential<br />
constituent of this rock. Majer (1962) determined anorthite and bytownite as essential<br />
constituents of gabbros, garnet-bearing gabbros and hornblendites belonging to the<br />
serpentine zone in the area between the rivers Bosna and Vrbas.<br />
2. Anorthite in metamorphic rocks<br />
The amphibolites and other metamorphic rocks of the Bosnian serpentine<br />
zone (BSZ) contain some anorthite, in addition to the other plagioclase minerals<br />
(Kišpatić 1897, 1900; Pamić 1971a; Pamić and Kapeler 1970; Pamić et al. 1973).<br />
Kišpatić (1897) determined anorthite in the pyroxene amphibolite from<br />
the Rudine and Velika Bukovica creeks at Mt. Ozren. Similar rocks in the area of<br />
Višegrad – Kruševački Potok, Vidakovića Potok and Obrenska Rijeka – contain<br />
anorthite associated with bytownite.<br />
Pamić et al. (1973) determined the abundance and properties of anorthite<br />
and the other plagioclases contained in amphibolites from Vareš (Duboštica, Vijake),<br />
Banja Luka and Rudo. The relationship between the chemical composition of the<br />
plagioclases and their optical character is shown by Figure 24. For example, the<br />
basic anorthite and bytownite are normally associated with amphiboles enriched in<br />
the pargasitic and edenitic end-members which have a positive optical character.<br />
Pamić and Kapeler (1970) determined anorthite in the corundum-bearing<br />
amphibolites (pargasitic hornblende) from Donje Vijake, near Vareš. The level of<br />
prehnitization is low and anorthite grains are mostly fresh. Their An content is 90-96%.<br />
Use: feldspars and plagioclases are important industrial minerals. Pure<br />
feldspar material, derived from pegmatites, is used in the production of ceramics<br />
and glass. The alkali feldspars are of particular interest in terms of industrial use of<br />
feldspars. Basically, the two properties which make feldspars useful for downstream<br />
industries are their alkali and alumina content.<br />
307
SILICATES<br />
Plagioclase and feldspar in general is an important ingredient in the<br />
manufacture of glass and an important raw material as well, because it acts as a<br />
fluxing agent, reducing the melting temperature of quartz and helping to control the<br />
viscosity of glass. The alkali content in feldspar acts as flux, lowering the glass batch<br />
melting temperature and thus reducing production costs.<br />
In the manufacture of ceramics, feldspar is the second most important<br />
ingredient after clay. Feldspar does not have a strict melting point, since it melts<br />
gradually over a range of temperatures. This greatly facilitates the melting of quartz<br />
and clays and, through appropriate mixing, allows modulations of this important step<br />
of ceramic making. Feldspars are used as fluxing agents to form a glassy phase at<br />
low temperatures and as a source of alkalies and alumina in glazes. They improve the<br />
strength, toughness, and durability of the ceramic body, and cement the crystalline<br />
phase of other ingredients, softening, melting and wetting other batch constituents.<br />
Feldspars also are used as fillers and extenders in applications such as paints,<br />
plastics and rubber. Beneficial properties of feldspars include good dispersability,<br />
high chemical inertness, stable pH, high resistance to abrasion, low viscosity at high<br />
filler loading, interesting refractive index and resistance to frosting. The products<br />
used in such applications are generally fine-milled grades.<br />
LAZURITE<br />
(Na,Ca) 7-8<br />
(AlSi) 12<br />
(O,S) 24<br />
[(SO 4<br />
)(Cl,OH) 2<br />
]<br />
Evlija Čelebija writes about lazurite – or lapis lazuli – in Bosnia and<br />
Hercegovina. In his travel report (see translation by Hazim Šabanović – Evlija<br />
Čelebija: Travel reports, published 1954-1973 in Sarajevo) the following<br />
information can be found on pages 133 (1954), p. 120 (1967) and p. 120 (1973)<br />
– cit. in this area there is orpiment (a depilating agent). There is also lazurite (a<br />
blue stone) which, like the european variety, has a play of thousand of colours.<br />
No further information on lazurite in Bosnia and Hervegovina can be found in<br />
professional references. We therefore believe that this famous turkish traveller<br />
probably saw (in the environs of Sarajevo) the blue mineral azurite, which occurs<br />
in the schist mountains of central Bosnia.<br />
SCAPOLITE<br />
The term Scapolite actually refers to the series between the sodium chloride<br />
rich mineral called marialite Na [AlSi 3<br />
O 8<br />
] NaCl, and the calcium carbonate rich<br />
mineral meionite Ca 3<br />
[Al 2<br />
Si 2<br />
O 8<br />
] CaCO 3<br />
. It crystallizes in the tetragonal system.<br />
308
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Scapolites are rare minerals in Bosnia and Hercegovina. Kišpatić (1897,<br />
1900) microscopically determined scapolite contained in the eclogitic amphibolite<br />
from Ravanke, Gornje Vijake, near Vareš. This scapolite is associated with amphibole,<br />
omphacite, garnet, hypersthene and plagioclase. The scapolit is not dispersed, but<br />
forms agglomerations in some parts of the rock complex. The scapolite grains are<br />
colourless, with a high birefringence so interference colours in thin section are<br />
correspondingly high. Extinction is parallel, the optical character is negative. A dark<br />
cross can sometimes be seen in convergent light.<br />
NATROLITE<br />
Na 2<br />
[Al 2<br />
Si 3<br />
O 10<br />
] x 2H 2<br />
O<br />
IR-spectrum: 417 515 545 600 633 680 980 1067 1090 1640 3240 3330<br />
3550 cm -1 .<br />
A u t h o r s: Đorđević and Stojanović (1972, 1974), Trubelja, Šibenik-Studen<br />
and Sijarić (1974, 1975, 1976), Trubelja, Šibenik-Studen, Sijarić and Šljukić (1974).<br />
In Bosnia and Hercegovina, natrolite has been identified and investigated<br />
only recently (as can be deduced from the cited literature). Ocurrences of natrolite<br />
have been identified in the Bosnian serpentine zone and in fissures of the gabbro<br />
complex at Jablanica. Đorđević and Stojanović (1972, 1974) determined natrolite<br />
(beautiful needle-like crystals) at Bojići (Hrvaćani) near Banja Luka, as well as near<br />
the Višegrad railway station.<br />
1. The occurrence at Bojići near Banja Luka<br />
Đorđević and Stojanović (1974) identified the presence of natrolite in the<br />
diabases from Bojići-Hrvaćani, on the south-western flanks of Mt. Crni Vrh. Here,<br />
natrolite is associated with analcime, laumontite, prehnite, datolite and some other<br />
vein minerals forming a hydrothermal paragenesis. The natrolite needles (5-10<br />
mm long) usually grow on prehnite. In thin section natrolite appears as colourless,<br />
prismatic grains with almost square-shaped cross-sections. The refractive index of<br />
natrolite is lower than that of Canada balsam. Extinction is parallel, with respect<br />
to the elongation of the crystal grains. A pure natrolite specimen was analysed by<br />
powder x-ray diffraction. The diffraction pattern corresponds to literature data<br />
(ASTM-card 19-1185). The diffraction data are given in table 64.<br />
309
SILICATES<br />
Table 64. Powder x-ray diffraction data for natrolite, Bojići<br />
Natrolite (Bojići) Natrolite (ASTM 19-1185)<br />
d Å I d Å I<br />
6.51 100 6.49 100<br />
5.88 30 5.90 65<br />
4.64 80 4.65 40<br />
4.59 25 4.56 25<br />
4.37 25 4.37 25<br />
4.34 20 4.35 30<br />
4.14 80 4.15 50<br />
4.09 50 4.10 25<br />
3.62 3 3.63 4<br />
3.26 15 3.27 10<br />
3.19 18 3.20 20<br />
3.15 20 3.15 25<br />
3.10 10 3.10 14<br />
2.93 15 2.945 18<br />
2.860 70 2.860 45<br />
2.837 60 2.837 35<br />
2. The occurrences at Mt. Konjuh and Doboj<br />
Trubelja et al. (1976) determined the presence of natrolite in the diabase<br />
upon which the fortress of Doboj is erected, and on the Sarajevo – Tuzla road (near<br />
Karaula) on Mt. Konjuh. Natrolite was identified using powder x-ray diffraction and<br />
infrared spectroscopy.<br />
The diabase at Doboj (Gradina) contains natrolite in association with calcite<br />
and analcime. At Mt. Konjuh, natrolite occurs as fillings in veins, either alone or<br />
together with thomsonite. The XRD and IR-spectroscopy data can be retrieved from<br />
the cited paper.<br />
3. Occurence in the gabbro from Jablanica<br />
Trubelja et al. (1976) identified natrolite in the veins and fissures within the<br />
gabbro rock massif of Jablanica (in the quarry of Ploče). Natrolite occurs in the form<br />
of very thin, acicular crystals forming aggregates which appear like ‘hairy’ bundles.<br />
Based on the x-ray diffraction data, the authors maintain that this a calcium-enriched<br />
mixed crystal approaching the composition of mesolite. The slight differences in<br />
values of the inter-lattice distances (d) and intesnities (I) between the natrolite<br />
from Ploče and the literature refernce, probably reflect the minor differences in the<br />
chemical composition of the two natrolites. Some Crystal-structure parameters of<br />
the Ploče natrolite have been determined (by M. Šljukić). The parameters, related to<br />
literature data, are given in Table 65.<br />
310
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Table 65. Unit-cell parameters of natrolite from Ploče with respect to literature data<br />
(Meier 1960)<br />
Natrolite (Ploče) Natrolite (ref. Meier 1960)<br />
a 0<br />
= 18.368 Å a 0<br />
= 18.30 Å<br />
b 0<br />
= 18.685 Å b 0<br />
= 18.63 Å<br />
c 0<br />
= 6.618 Å c 0<br />
= 6.60 Å<br />
D m<br />
= 2.268 Å<br />
V 0<br />
= 2271.20 Å 3 V 0<br />
= 2250.10 Å 3<br />
Z = 8 Z = 8<br />
D x<br />
= 2.220 g/cm 3 D x<br />
= 2.245 g/cm 3<br />
Orthorhombic<br />
Fdd2<br />
Some issues of the origin of natrolite in the rocks of Bosnia and Hercegovina<br />
will be discussed in the section on chabasite.<br />
SCOLECITE<br />
Ca [Al 2<br />
Si 3<br />
O 10<br />
] x 3H 2<br />
O<br />
Crystal system and class: Monoclinic, domatic class.<br />
Lattice ratio: a : b : c = 0.976 : 1 : 0.345 β = 90° 45’<br />
Cell parameters: a o<br />
= 18.48, b o<br />
= 18.94, c o<br />
= 6.4 Z = 8<br />
A u t h o r s: Šibenik-Studen (1972/73), Trubelja, Šibenik-Studen and Sijarić<br />
(1974, 1976), Trubelja, Šibenik-Studen, Sijarić and Šljukić (1974).<br />
Up to now, scolecite has been identified at one location only in Bosnia and<br />
Hercegovina, in the Ribnica creek near Višegrad (Šibenik-Studen 1972/73). Scolecite<br />
occurs in the form of white, sometimes vein-like aggregates in basic gabbro-diabase<br />
host rocks. Scolecite is often associated with stilbite.<br />
Quantitative chemical analysis yielded following results:<br />
SiO 2<br />
= 44.67; TiO 2<br />
= traces; Al 2<br />
O 3<br />
= 24.98; Fe 2<br />
O 3<br />
= 0.38; CaO = 14.26;<br />
MgO = 0.31; Na 2<br />
O = 0.61; K 2<br />
O = --; H 2<br />
O + = 14.11; H 2<br />
O - = 0.72;<br />
Total = 100.04<br />
Atomic and molecular ratios were calculated from the chemical analysis<br />
results, based on 20 oxygen atoms, and are as follows:<br />
Si = 5.97 Al = 3.92 Fe 3+ = 0.04 Ca = 2.03<br />
Mg = 0.06 Na = 0.14 H 2<br />
O measured<br />
= 6.25 H 2<br />
O calculated<br />
= 6.41<br />
The difference between H 2<br />
O measured<br />
and H 2<br />
O calculated<br />
is – 0.16. Based on this<br />
calculation, the structural formula of scolecite is given as follows:<br />
Ca 2.03<br />
Na 0.14<br />
Mg 0.06<br />
Al 3.92<br />
Fe 3+ Si O • 6.25 H O<br />
0.04 5.97 20 2<br />
311
SILICATES<br />
Foster (1965) studied in detail the composition and water content of<br />
scolecites from various localities. The structural formulae for all investigated<br />
scolecites were calculated on the basis of 20 oxygen atoms. Our calculation (for the<br />
Ribnica scolecite) can therefore be directly compared with the cited reference, and it<br />
corresponds very well with Foster’s data.<br />
Table 66. Powder XRD data for scolecite from the Ribnica creek (Šibenik-Studen 1972/73)<br />
No. d Å I No. d Å I<br />
1 6.637 5 29 1.903 1<br />
2 5.817 8 30 1.876 1.5<br />
3 4.760 4 31 1.855 1.5<br />
4 4.598 4 32 1.834 1<br />
5 4.387 8 33 1.807 3<br />
6 4.183 3 34 1.766 2<br />
7 3.642 3 35 1.743 2<br />
8 3.227 4 36 1.720 1.5<br />
9 3.153 4 37 1.685 1<br />
10 2.068 5 38 1.674 1.5<br />
11 2.994 1 39 1.656 1.5<br />
12 2.936 8 40 1.634 5<br />
13 2.861 10 41 1.614 4<br />
14 2.679 1 42 1.597 0.5<br />
15 2.572 4 43 1.582 0.5<br />
16 2.474 3 44 1.542 1<br />
17 2.423 3 45 1.525 1<br />
18 2.312 3 46 1.491 0.5<br />
19 2.262 3 47 1.481 0.5<br />
20 2.246 2 48 1.469 4<br />
21 2.204 6 49 1.446 0.5<br />
22 2.168 2 50 1.433 3<br />
23 2.141 2 51 1.420 1<br />
24 2.106 1 52 1.383 3<br />
25 2.069 2 53 1.374 0.5<br />
26 2.034 5 54 1.357 0.5<br />
27 1.992 2 55 1.343 1<br />
28 1.955 4 56 1.327 3<br />
The scolecite from Ribnica was also subjected to powder x-ray diffraction,<br />
thermal analysis and infrared spectroscopy. Hand-picked scolecite crystals of ca.<br />
1 cm in length were used for these analyses. The powder diffraction data (Deby-<br />
Scherrer metod) is given in table 66.<br />
The IR-absorption spectrum of this scolecite contains absorptions with<br />
following wavenumbers: 632 664 707 926 986 1018 1068 1096 and 1389<br />
cm -1 . The literature reference for the IR spectrum of scolecite (Moenke 1962) has<br />
wavenumbers 410 455 497 536 650 677 695 810 910 933 980 1003 1055<br />
1405 and 3440 cm -1 .<br />
The origin of scolecite and other zeolite minerals is decribed in the section<br />
on chabasite.<br />
312
MESOLITE<br />
Na 2<br />
Ca 2<br />
[Al 2<br />
Si 3<br />
O 10<br />
] 3<br />
• 8H 2<br />
O<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
A u t h o r s: Trubelja, Šibenik-Studen and Sijarić (1974, 1976), Trubelja,<br />
Šibenik-Studen, Sijarić and Šljukić (1974).<br />
Up to now, mesolite has been identified at one location only in Bosnia and<br />
Hercegovina, in the veins within the gabbro host rock at Jablanica. Mesolite occurs<br />
in association with natrolite. The mineral, occurring as needle-like crystals, has been<br />
identified by powder x-ray diffraction. Unit cell parameters were determined by M.<br />
Šljukić as:<br />
a 0<br />
= 18.368 Å b 0<br />
= 18.685 Å c 0<br />
= 6.618 Å β = 90°<br />
V 0<br />
= 2271.20 Å 3 D m<br />
= 2.268 Å D x<br />
= 2.220 g/cm 3 Z = 8<br />
This mesolite is orthorhombic (Fdd2). The data given above is slightly<br />
different from the information provided by Taylor et al. (1933).<br />
No more information is available for mesolite from the gabbros at Jablanica.<br />
More material will have to be collected in future so that additional analyses can be<br />
made, especially chemical analysis.<br />
THOMSONITE<br />
NaCa 2<br />
[Al 5<br />
Si 5<br />
O 20<br />
] • 6H 2<br />
O<br />
Crystal system and class: Orthorhombic, dipyramidal class.<br />
Lattice ratio:a : b : c = 0.998 : 1 : 1.012<br />
Cell parameters: a o<br />
= 13.07, b o<br />
= 13.09, c o<br />
= 13.25 Z = 4<br />
IR-spectrum: 412 440 595 630 1008 (1100) 1640 3440 3550 cm -1 .<br />
A u t h o r s: Šćavničar, Trubelja and Sijarić-Pleho (1968), Šibenik-Studen<br />
and Trubelja (1971), Trubelja, Šibenik-Studen and Sijarić (1974, 1975, 1975a, 1976),<br />
Trubelja, Šibenik-Studen, Sijarić and Šljukić (1974).<br />
Thomsonite has been determined in Bosnia and Hercegovina only recently.<br />
According to available literature, thomsonite occurs in basic igneous rocks on<br />
the edges of the Bosnian serpentine zone – at Mt. Kozara, Mt. Ozren and Mt.<br />
Konjuh. However, it is interesting to note that thomsonite was first determined in<br />
the boehmite-gibbsite bauxites from Posušje, in the Galića Njive – Vinjani area<br />
(Šćavničar et al. 1968).<br />
313
SILICATES<br />
1. The thomsonite occurrence at Mt. Konjuh<br />
Thomsonite occurs in veins within diabase outcrops, mainly on the Olovo –<br />
Kladanj sector of the Sarajevo – Tuzla motorway. It is associated with prehnite (near<br />
the village of Kovačići) or analcime (the Karaule locality).<br />
Šibenik-Studen and Trubelja (1971) note that thomsonite occurs (at<br />
Kovačići) as radial aggregates of columnar crystals which are transparent and of<br />
a vitreous lustre. These aggregates can also occur as thin crusts. Thomsonite fills<br />
veins and fissures, either alone or associated with prehnite. In thin section these two<br />
minerals can be identified due to differences in grain shape, intereference colours<br />
and refractive indices. Thomsonite has a lower RI than Canada balsam and displays<br />
parallel extinction (interference colours are yellowish and grey). Quantitative<br />
chemical analysis of thomsonite (the material was carefully separated under a<br />
binocular loupe) yielded following results:<br />
SiO 2<br />
= 39.85; Al 2<br />
O 3<br />
= 28.64; CaO = 14.06; Na 2<br />
O = 4.84; K 2<br />
O = traces;<br />
H 2<br />
O = 12.58; Total = 99.97<br />
The structural formula of this thomsonite, based on 80 oxygen atoms is:<br />
Na 4.983<br />
Ca 8.017<br />
(Al 17.950<br />
Si 21.272<br />
O 80<br />
) • 24H 2<br />
O<br />
The chemical analysis and structural formula correspond well to literature<br />
data (Deer et al. 1963).<br />
Powder x-ray diffraction data for the thomsonite from Kovačići is given<br />
in table 67. The diffraction pattern corresponds well to literature data (ASTM-card<br />
9-490).<br />
Thomsonite occurs also in several places at the locality called Karaule,<br />
on the Olovo – Kladanj road. Powder XRD and infrared spectroscopy was used to<br />
identify the thomsonite association with natrolite or analcime. Detailed results of<br />
these analyses can be found in the paper by Trubelja et al. (1976).<br />
Table 67. X-ray diffraction data for thomsonite from Kovačići (Šibenik-Studen and<br />
Trubelja 1971)<br />
No. d Å I No. d Å I<br />
1 6.444 s 33 1.57 w<br />
2 5.917 s 34 1.56 vw<br />
3 5.498 w 35 1.54 m<br />
4 4.670 vs 36 1.51 vw<br />
5 4.395 s 37 1.47 vs<br />
6 4.152 ms 38 1.44 m<br />
314
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
7 3.829 w 39 1.42 vw<br />
8 3.504 s 40 1.39 m<br />
9 3.189 w 41 1.33 m<br />
10 3.114 s 42 1.31 m<br />
11 3.084 w 43 1.30 m<br />
12 2.967 vvs 44 1.29 m<br />
13 2.866 vvs 45 1.28 w<br />
14 2.792 vw 46 1.27 w<br />
15 2.668 s 47 1.26 w<br />
16 2.586 m 48 1.24 vw<br />
17 2.432 w 49 1.23 vw<br />
18 2.262 m 50 1.22 sm<br />
19 2.190 s 51 1.19 m<br />
20 2.14 vw 52 1.17 m<br />
21 2.08 vw 53 1.15 vw<br />
22 2.02 s 54 1.14 m<br />
23 1.95 w 55 1.07 w<br />
24 1.89 w 56 1.06 sm<br />
25 1.82 m 57 1.03 m<br />
26 1.76 vw 58 1.01 vw<br />
27 1.73 m 59 1.00 w<br />
28 1.71 w 60 0.98 w<br />
29 1.65 w 61 0.97 w<br />
30 1.63 mw 62 0.96 vw<br />
31 1.62 mw 63 m<br />
32 1.59 w<br />
2. The thomsonite occurrence at Mt. Ozren<br />
Trubelja et al. (1976) determined thomsonite in diabase-spilitic rocks in the<br />
Omrklica creek near Megare, and on the road between Gornji Rakovac and Gornja<br />
Bukovica (Mt. Ozren). Based on XRD and IR-spectrometry, the authors conlcude<br />
thaT homsonite occurs here alone.<br />
3. The thomsonite occurrence at Mt. Kozara<br />
Trubelja et al. (1976) determined thomsonite in association with analcime in<br />
numerous samples of vein fillings collected from basic igneous rocks in the Kozarac<br />
– Mrakovica area at Mt. Kozara. Analcime is more abundant than thomsonite.<br />
315
SILICATES<br />
LAUMONTITE<br />
Ca [AlSi 2<br />
O 6<br />
] 2<br />
• 4.5H 2<br />
O<br />
Crystal system and class: Monoclinic, prismatic class.<br />
Lattice ratio: a : b : c = 1.131 : 1 : 0.573 β = 111° 30’<br />
Cell parameters: a o<br />
= 14.90, b o<br />
= 13.17, c o<br />
= 7.55 Z = 4<br />
X-ray data: d 4.18 (100) 6.97 (60) 3.53 (60)<br />
IR-spectrum: 410 432 492 525 565 625 765 960 1000 1038<br />
1095 1134 1655 3470 and 3560 cm -1 .<br />
A u t h o r s: Đorđević and Stojanović (1972, 1974), Trubelja, Šibenik-<br />
Studen and Sijarić (1974, 1975, 1975a, 1976), Trubelja, Šibenik-Studen, Sijarić and<br />
Šljukić (1974).<br />
In Bosnia and Hercegovina laumontite has been identified only recently, and<br />
only within the Bosnian serpentine zone. It occurs as fillings in fissures in basic<br />
igneous rocks at Mt. Kozara and Mt. Konjuh. Đorđević and Stojanović (1974)<br />
identified a laumontite occurrence at Bojići, near Banja Luka.<br />
316<br />
1. The laumontite occurrence at Mt. Kozara<br />
Occurrences of laumontite are quite common on the southern flanks of Mt.<br />
Kozara, on the Kozarac-Mrakovica road. It is also found on the northern flanks of<br />
the mountain, in the Bukovica and Trnova creeks, where it occurs associated with<br />
prehnite or plagioclase.<br />
Laumontite and the associated minerals were all identified using powder x-ray<br />
diffraction and infrared spectroscopy. The results were published in several publications<br />
– Trubelja et al. (1974, 1975, 1975a, 1976), Trubelja, Šibenik-Studen, Sijarić and Šljukić<br />
(1974). We wish to point out that we had some difficulties with the identification of<br />
laumontite by IR-spectroscopy, especially when plagioclases were present in the<br />
samples. This is due to the fact that diagnostic absorption peaks of plagioclases are<br />
located in the low-wavenumber part of the IR spectrum (400-650 cm-1) and overlaps<br />
with the absorption which are caused by laumontite and other zeolites are inevitable.<br />
Complementary use of infrared spectroscopy and x-ray diffraction helped to eliminate<br />
possible biases in the identification procedures. The respective data-sets for the IRspectra<br />
and XRD patterns can be found in the paper by Trubelja et al. (1976).<br />
Đorđević and Stojanović (1974) identified laumontite in the diabase<br />
outcrops at Bojići, near Banja Luka. This laumontite is associated with natrolite,<br />
analcime and datolite. In thin section, the laumontite has a lower refractive index<br />
than Canada balsam, and a higher relief than natrolite. The x-ray diffraction diagram<br />
of this laumontite showed following peaks (d) 9.58; 6.98; 4.19; 3.66 and 3.52 Å.<br />
Another occurrence of laumontite, according to these authors, is close to the<br />
railway station in Višegrad.
2. The laumontite occurrence at Mt. Konjuh<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Laumontite occurs, together with other vein minerals (prehnite and<br />
plagioclases) in the outcrops along the Olovo – Kladanj road, in the area called<br />
Karaule. The respective data-sets for the IR-spectra and XRD patterns of this<br />
laumontite can be found in the paper by Trubelja et al. (1976).<br />
STILBITE<br />
(Ca 0.5<br />
,K,Na) 9<br />
[Al 9<br />
Si 27<br />
O 72<br />
] • 28H 2<br />
O<br />
A u t h o r s: Katzer (1920, 1924, 1926), Kišpatić (1902), Koch (1899),<br />
Marić (1927), Šibenik-Studen (1972/73), Trubelja, Šibenik-Studen and Sijarić<br />
(1974, 1976), Trubelja, Šibenik-Studen, Sijarić and Šljukić (1974).<br />
Literature references on stilbite in Bosnia and Hercegovina are very<br />
scarce. The first short account on the occurrence of stilbite in the pegmatite veins<br />
at Mt. Motajica were published by Koch (1899). He noted that crystals of stilbite<br />
were quite small and were attached to black quartz. Koch was able to identify four<br />
crystallographic forms on these crystals: M (clinopinacoid), T (base pinacoid), N<br />
(orthopinacoid) and P (orthodome). This stilbite is colourless or white. The lustre<br />
on the clinopinacoid plane is pearly. A sample of this stilbite is located in the<br />
Mineralogical-petrographical Museum in Zagreb.<br />
Kišpatić (1902) investigated the same mineral, but called it heulandite.<br />
The data provided by Kišpatić are not identical to the information published by<br />
Koch, and it will obviously be neccessary to make a critical revision of both datasets.<br />
Stilbite (heulandite) from the same locality was also briefly mentioned by<br />
Katzer (1924, 1926).<br />
According to Katzer (1920), desmine (stilbite) occurs associated with<br />
chabasite in amygdaloids within melaphyres from the Stavnja river valley near<br />
Vareš. Marić (1927) also mentions radial aggregates of stilbite in the gabbros from<br />
Jablanica.<br />
More recently, stilbites from Višegrad and Jablanica have been investigated<br />
by Šibenik-Studen (1972/73), Trubelja, Šibenik-Studen and Sijarić (1974, 1976),<br />
Trubelja, Šibenik-Studen, Sijarić and Šljukić (1974).<br />
317
SILICATES<br />
1. The stilbite occurrence at Ribnica near Višegrad<br />
Šibenik-Studen (1974) made a detailed investigation of stilbite from the<br />
Ribnica creek, near Višegrad. It occurs as fillings of veins within basic gabbro-type<br />
igneous rocks which have penetrated the diabase-dolerite complex. Stilbite usually<br />
forms radial aggregates but individual crystals have also been observed. Its colour<br />
is white and has pearly lustre. Stilbite aggregates occasionally form thin crusts over<br />
greenish-grey fassaite.<br />
Stilbite material was carefully selected for chemical, thermal and x-ray<br />
diffraction analyses. Quantitative chemical analysis yielded following results:<br />
SiO 2<br />
= 54.10; Al 2<br />
O 3<br />
= 16.55; Fe 2<br />
O 3<br />
= 0.61; TiO 2<br />
= 0.24; CaO = 9.25;<br />
Na 2<br />
O = 0.87; K 2<br />
O = 0.29; H 2<br />
O + = 14.88; H 2<br />
O - = 3.37; Total = 100.16<br />
The structural formula of this stilbite, based on 72 oxygen atoms is:<br />
(Ca 4.75<br />
Na 0.81<br />
K 0.17<br />
) (Al 9.38<br />
Fe 0.23<br />
Ti 0.09<br />
Si 26.08<br />
O 72<br />
) • 29.33H 2<br />
O<br />
Compared to five different stilbites reported by Deer et al. (1963), the stilbite<br />
from Višegrad can be classified as normal, somewhat Si-depleted stilbite. The powder<br />
diffraction pattern of stilbite is given in table 68.<br />
The stilbite from Ribnica was also analysed by thermogravimetry and<br />
differential thermal analysis. The TG and DTA curves can be found in the paper<br />
(Šibenik-Studen 1974). The results of thermal analysis correcpond very well to<br />
literature references (Pecsi-Donath 1962; Njirkov and Kobilev 1962).<br />
Table 68. X-ray diffraction data for stilbite from Ribnica (Šibenik-Studen 1974)<br />
No. d Å I No. d Å I<br />
1 9.156 vs 17 2.5996 wd<br />
2 6.748 jwd 18 2.3382 w<br />
3 5.3723 wd 19 2.2095 wd<br />
4 4.6707 s 20 2.05343 wd<br />
5 4.3744 jw 21 2.02296 wd<br />
6 4.2908 m 22 1.88644 wd<br />
7 4.0767 vvs 23 1.86466 wd<br />
8 3.7385 wd 24 1.82067 w<br />
9 3.4930 jw 25 1.76676 w<br />
10 3.4089 m 26 1.72046 w<br />
11 3.2098 m 27 1.69397 vw<br />
12 3.1274 jw 28 1.64748 vw<br />
13 3.0079 vs 29 1.63400 vw<br />
14 2.8630 vw 30 1.58411 w<br />
15 2.7883 w 31 1.54178 m<br />
16 2.7352 w 32 1.43279 vw<br />
318
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The IR spectrum of stilbite features following wavenumbers: 400 439<br />
550 590 720 785 870 1030 1145 1640 3250 and 3400 cm -1 . The IR spectrum<br />
of the Ribnica stilbite corresponds very well to the spectrum of stilbite from<br />
Teigarhorn, Iceland.<br />
2. The occurrence of stilbite in gabbro at Jablanica<br />
Stilbite, associated with other hydrothermal minerals, is often present as<br />
fillings of veins within the Jablanica gabbro complex. Such veins are particularly<br />
well exposed in the Ploče quarry. Here, stilbite is associated with small amounts<br />
of albite, prehnite and chabasite. In one case, stilbite and albite grew on substrate<br />
consisting of pumpellyite, chlorite and hornblende, presenting evidence of the<br />
succession of postmagmatic activity and the sequence of crystallization of the<br />
minerals in the paragenesis.<br />
Trubelja et al. (1976) performed a set of analyses on this stilbite. The<br />
chemical composition is as follows:<br />
SiO 2<br />
= 55.48; Al 2<br />
O 3<br />
= 15.80; CaO = 8.91; Na 2<br />
O = 1.14; K 2<br />
O = 0.40;<br />
H 2<br />
O + = 16.04; H 2<br />
O - = 2.91; Total = 100.37<br />
The structural formula of this stilbite, based on 72 oxygen atoms is:<br />
(Ca 4.61<br />
Na 1.04<br />
K 0.29<br />
) (Al 8.93<br />
Si 26.61<br />
O 72<br />
) • 30.5H 2<br />
O<br />
The chemical composition and structural formula of the Jablanica stilbite<br />
and the Ribnica stilbite are quite similar. The x-ray powder diffraction pattern and<br />
IR-spectrum of this stilbite is given in the cited paper (Trubelja et al. 1976).<br />
X-ray structural analysis on monocrystals of stilbite (done by M. Šljukić)<br />
gave following parameters:<br />
a 0<br />
= 13.669 Å b 0<br />
= 17.699 Å c 0<br />
= 11.189 Å β = 127°<br />
V 0<br />
= 2161.86 Å 3 D m<br />
= 2.173 g/cm 3 D x<br />
= 2.235 g/cm 3 Z = 4<br />
monoclinic system – C2/m<br />
CHABASITE<br />
(Ca 0.5<br />
Na,K) 4<br />
[Al 4<br />
Si 8<br />
O 24<br />
] 2<br />
• 12H 2<br />
O<br />
X-ray data: d 2.907 (100) 4.291 (90) 9.31 (80)<br />
d 2.95 (100) 4.35 (90) 9.5 (70)<br />
IR-spectrum 415 465 517 630 700 1025 1100 1645 and 3440 cm -1 .<br />
A u t h o r s: Katzer (1920), Majer (1953), Ramović (1968), Trubelja,<br />
Šibenik-Studen and Sijarić (1974, 1976), Trubelja, Šibenik-Studen, Sijarić and<br />
Šljukić (1974), Tućan (1957).<br />
319
SILICATES<br />
In Bosnia and Hercegovina, chabasite has been found and studied only at<br />
Jablanica, where it occurs in veins within the gabbro host rock. According to limited<br />
information provided by Katzer (1920), chabasite also occurs in amygdaloides<br />
within the melaphyres from the Stavnja river near Vareš.<br />
Tućan (the textbook on special mineralogy, published in 1957) provides first<br />
information on the chabasite from Jablanica. Chabasite occurs together with titanite,<br />
tourmaline, prehnite, a plagioclase, amphibole, chlorite and colourless quartz. The<br />
2V angle varies from +70.5° to +82° (average of six individual measurments is<br />
+78°). Maximum birefringence Nz – Nx = 0.0010 (optical constants determined by<br />
Lj. Barić). The chabasite seems to be pseudo-biaxial.<br />
Ramović (1968) also notes the chabasite occurrence at Jablanica. A large<br />
specimen of altered gabbro from Jablanica is deposited in the mineralogical collection<br />
of the National Museum in Sarajevo. A chabasite aggregate 0.5 cm in diameter is<br />
attached to this specimen. The crystals are transparent or white (vitreous lustre) and<br />
posess a rhomohedral habit. This material was used for chemical and other analyses.<br />
The results of chemical analysis is given in table 69.<br />
Table 69. Chemical analysis of chabasite from Jablanica (Trubelja et al. 1976) and Bor (Majer<br />
1953)<br />
Chabasite (Jablanica)<br />
Chabasite<br />
(Bor)<br />
SiO 2<br />
48.12 48.78<br />
TiO 2<br />
--- ---<br />
Al 2<br />
O 3<br />
18.36 18.04<br />
Fe 2<br />
O 3<br />
--- ---<br />
MgO --- ---<br />
CaO 8.96 9.77<br />
Na 2<br />
O 0.27 0.98<br />
K 2<br />
O 1.75 0.60<br />
H 2<br />
O +110 17.29 22.04<br />
H 2<br />
O -110 4.97 ---<br />
Fe, Mn --- traces<br />
Total 99.72 100.21<br />
The structural formula of this chabasite, based on 72 oxygen atoms is:<br />
(Ca 4.95<br />
K 1.11<br />
Na 0.25<br />
) (Al 11.20<br />
Si 24.78<br />
O 72<br />
) • 38.18 H 2<br />
O<br />
and corresponds well to literature data (Coombs et al. 1959). The chemical composition<br />
of the chabasite from Jablanica is similar to the compositon of a chabasite from the<br />
copper mine in Bor (Serbia), as given in table 69. The potassium and water content<br />
are slightly different.<br />
Trubelja et al. (1974) collected further chabasite material from the Jablanica<br />
gabbro complex and compared its powder diffraction pattern with that of the<br />
320
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
chabasite from the museum in Sarajevo (tables 70 and 71). Apart from the Debye-<br />
Scherrer film technique, instrumental diffraction analysis was also done in view of a<br />
better evaluation of the signal intesities.<br />
Table 70. Powder x-ray diffraction data for chabasite (sample from the National Museum in<br />
Sarajevo)<br />
No. d Å I No. d Å I<br />
1 9.718 8 16 2.6173 2<br />
2 6.992 2 17 2.5081 2<br />
3 5.5877 1 18 2.3037 1<br />
4 5.6229 7 19 2.0941 2<br />
5 5.0675 7 20 1.81390 2<br />
6 4.7051 1 21 1.72769 2<br />
7 4.3532 9 22 1.69513 1<br />
8 3.8900 3 23 1.68363 1<br />
9 3.6043 4 24 1.64474 1<br />
10 3.4662 2 25 1.56069 1<br />
11 3.2433 1 26 1.52204 1<br />
12 3.2022 1 27 1.41808 1<br />
13 2.9402 10 28 1.40861 1<br />
14 2.9122 1 29 1.34233 1<br />
15 2.6936 1<br />
Table 71. Powder x-ray diffraction data for chabasite (Ploče quarry, Jablanica)<br />
No. d Å I No. d Å I<br />
1 9.408 8 23 2.0969 2<br />
2 6.970 3 24 1.92018 1<br />
3 6.398 1 25 1.87548 1<br />
4 5.5737 6 26 1.86108 1<br />
5 5.0276 6 27 1.80987 4<br />
6 4.7199 1 28 1.77442 1<br />
7 4.3448 10 29 1.72769 2<br />
8 3.9971 1 30 1.69803 1<br />
9 3.8833 5 31 1.67512 1<br />
10 3.6129 6 32 1.64908 2<br />
11 3.4609 5 33 1.56309 2<br />
12 3.2433 2 34 1.52430 2<br />
13 3.1865 2 35 1.49114 1<br />
14 2.9459 10 36 1.45351 1<br />
15 2.8937 5 37 1.42115 1<br />
16 2.8488 1 38 1.40974 1<br />
17 2.7849 1 39 1.36518 1<br />
18 2.6952 3 40 1.34568 1<br />
19 2.6187 6 41 1.33077 1<br />
20 2.5081 5 42 1.28691 1<br />
21 2.3559 1 43 1.26777 1<br />
22 2.3094 1<br />
321
SILICATES<br />
A comparison of the powder diffraction patterns of the chabasite from<br />
Jablanica with literature references for this mineral results in some discrepancies.<br />
The diffraction patterns of our chabasite (Jablanica) contains some diffraction peaks<br />
(signals) which have not been observed by other authors (Mason and Greenberg<br />
1954; Mikheev 1957). At first we believed that the extra signals were caused by<br />
albite, but the IR-spectrum did not reveal the presence of this mineral. Moreover,<br />
the Na 2<br />
O = 0.27% content does not imply the presence of albite in the material used<br />
for powder diffraction analysis. Crystal-structure parameters were also measured on<br />
monocrystals of chabasite (table 72):<br />
Table 72. Structural parameters of the Jablanica chabasite compared with literature data<br />
(Dent and Smith 1958)<br />
1. Chabasite (Ploče quarry, Jablanica) M t<br />
= 530.9155<br />
a r<br />
= 9.453 Å<br />
a x<br />
= 13.801 Å<br />
α = 94° 24’<br />
c x<br />
= 15.028 Å<br />
V = 841.76 Å 3 V = 2478.88 Å 3<br />
D m<br />
= 2.078 g/cm 3 D m<br />
= 2.078 g/cm 3<br />
Z = 2 Z = 6<br />
D x<br />
= 2.094 g/cm 3 D x<br />
= 2.134 g/cm 3<br />
Rhombohedral (hexagonal) system – R-3m<br />
2. Chabasite (ref. Dent and Smith 1958) M t<br />
= 552.4514<br />
a r<br />
= 9.40 Å<br />
a h<br />
= 13.78 Å<br />
α = 94° 18’<br />
c h<br />
= 15.01 Å<br />
V = 828.1 Å 3 V = 2468.4 Å 3<br />
Z = 2 Z = 6<br />
D x<br />
= 2.22 g/cm 3 D x<br />
= 2.23 g/cm 3<br />
Rhombohedral (hexagonal) system – R-3m<br />
Based on the above crystallographic and structural data, the Jablanica<br />
chabasite belongs to the rhombohedral system, which corresponds to literature<br />
references, as above. However, the difference in optical constants remain. The<br />
chabasite from the Ploče quarry is optically biaxial with a large positive 2V angle.<br />
The reason for this optical anomaly is unknown. Deer et al. (1963) note that such<br />
anomalie have been observed in the case of chabasite, gmelinite and levinite. It is<br />
worth noting that the chabasite from Bor was also determined as biaxial.<br />
322<br />
The origin (genesis) of zeolites<br />
In our description of the occurrences of chabasite, laumontite, natrolite,<br />
scolecite, stilbite and thomsonite in Bosnia and Hercegovina, we have made it clear<br />
that these minerals occur as fillings of fissures and veins hosted by basic igneous or<br />
vein-type rocks in the Bosnian serpentine zone and within the gabbro complex at<br />
Jablanica. They form monomineral or polymineral veinlets, the thickness of which is<br />
in the range from several millimeters to several centimeters. Therefore, the zeolites<br />
in Bosnia and Hercegovina can be described as typical vein-type minerals.
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
The host rocks of the zeolite minerals are largely similar. They consist of<br />
gabbros, diabases, spilites (or their effusive equivalents which contain plagioclases<br />
as essential constituents). The zeolite parageneses are usually simple, but complex<br />
associations occur within the Jablanica complex. This implies the influence of late,<br />
low-temperature post-magmatic effects on the composition of these parageneses.<br />
The origin of the zeolites can therefore be discussed in terms of two<br />
different scenarios. The zeolites may have formed as primary minerals, crystallizing<br />
in the final deposition stages from hot solutions which were in contact with igneous<br />
bodies. The other possibility for zeolite formation would be their crystallization<br />
from hydrothermal solutions enriched in calcium, sodium, aluminum and silica (and<br />
other elements) as a consequence of the leaching of surrounding rocks (especially<br />
plagioclases contained in them). In such cases, pseudomorphic zeolite growth over<br />
plagioclases could be observed.<br />
The composition of some zeolite parageneses occurring within the Jablanica<br />
complex or the Bosnian serpentine zone confirms the notion that they may have<br />
been formed by either of the described processes (depending on their location). For<br />
example, at Mt. Konjuh (Karaula area) the paragenesis is rather complex (zeolites,<br />
thomsonite, laumontite, natrolite, prehnite, analcime etc), and it is obvious that<br />
natrolite was the last mineral species to crystallize (natrolite can be deposited even<br />
from completely cold solutions, percolating through the fissures of basic igneous<br />
rocks). At Mt. Kozara, laumontite is oftn associated with plagioclases, occasionally<br />
present as a secondary pseudomorphic growth.<br />
The crystallization sequence of zeolite minerals, as established by Kostov<br />
(cited in Deer et al. 1963) is based upon the Al:Si ratio and the energy index. A low<br />
energy index corresponds to high crystallization temperatures. This author maintains<br />
that scolecite is a high-temperature member of the calcium zeolites. This would be in<br />
accordance with our findings for the scolecite from Ribnica near Višegrad.<br />
The origin of chabasite and other zeolites in tha gabbro of the Jablanica<br />
complex can be related to hydrothermal processes. Both low-temperature and hightemperature<br />
zeolite parageneses have been identified in this area. We therefore believe<br />
that the solutions carrying Ca, Na, Al and Si (enriched by laterl secretion processes)<br />
are linked to surrounding gabbro rocks. Hydrothermal solutions originating at<br />
greater depths had considerably higher temperatures, but cooled off as they rose<br />
toward the surface. These solutions, therefore, did not have a profound effect on the<br />
chemistry of the gabbro rock. Evidence of this are the fresh plagioclases, which are<br />
quite abundant in the host rock.<br />
Uses: Zeolite minerals have specific structural properties which enables them<br />
to absorb substantial quantities of ‘zeolite water’. This, and some other properties<br />
make them important industrial minerals.<br />
323
SILICATES<br />
There are three main uses of zeolites in industry: catalysis, gas separation<br />
and ion exchange. Zeolites are extremely useful as catalysts for several important<br />
reactions involving organic molecules. The most important are cracking,<br />
isomerisation and hydrocarbon synthesis. Zeolites can promote a diverse range of<br />
catalytic reactions including acid-base and metal induced reactions. Zeolites can also<br />
be acid catalysts and can be used as supports for active metals or reagents. Zeolites<br />
can be shape-selective catalysts either by transition state selectivity or by exclusion<br />
of competing reactants on the basis of molecular diameter. They have also been used<br />
as oxidation catalysts. The reactions can take place within the pores of the zeolite,<br />
which allows a greater degree of product control. The main industrial application<br />
areas are: petroleum refining, synfuels production, and petrochemical production.<br />
Synthetic zeolites are the most important catalysts in petrochemical refineries.<br />
Zeolites are used to adsorb a variety of materials. This includes applications<br />
in drying, purification, and separation. They can remove water to very low partial<br />
pressures and are very effective desiccants, with a capacity of up to more than 25% of<br />
their weight in water. They can remove volatile organic chemicals from air streams,<br />
separate isomers and mixtures of gases. A widely used property of zeolites is that<br />
of gas separation. The porous structure of zeolites can be used to “sieve” molecules<br />
having certain dimensions and allow them to enter the pores. This property can be<br />
fine tuned by variating the structure by changing the size and number of cations<br />
around the pores. Other applications that can take place within the pore include<br />
polymerisation of semi conducting materials and conducting polymers to produce<br />
materials having unusual physical and electrical attributes.<br />
Hydrated cations within the zeolite pores are bound loosely to the zeolite<br />
framework, and can readily exchange with other cations when in aqueous media.<br />
Applications of this can be seen in water softening devices, and the use of zeolites in<br />
detergents and soaps. The largest volume use for zeolites is in detergent formulations<br />
where they have replaced phosphates as water-softening agents. They do this by<br />
exchanging the sodium in the zeolite for the calcium and magnesium present in the<br />
water. It is even possible to remove radioactive ions from contaminated water.<br />
324
References<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
I General references<br />
Anonymous: Corpus inscriptionen latinarum, III Commentariensis aurarium Delmatorum.<br />
Anonymous (1879): L’annacus Florus, Epitomae 1, Vol. III, Leipzig.<br />
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Deer, W.A., Howie, R.A. and Zussman. J (1962 and 1963): Rock-forming minerals. Volumes<br />
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Fahey, J.J. and Axelrod, J.V. (1950): Searlesite from Green River formation of Wyoming.<br />
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Mineralogy. Moscow (in Russian).<br />
Fiala, F. (1899): Das Flashgräberfeld und die prähistorische Ansiedlung in Sanski Most.<br />
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U.S. Geol. Survey Professional Paper 504-D.<br />
Görgey, R. (1915): Katzer, F. (Sarajevo): Poechit, ein Manganeisenerz von Vareš in Bosnien.<br />
Ref. in Zs. Kristallogr. 54, 408.<br />
Group of authors (1966): Cultural history of Bosnia and Hercegovina. Sarajevo (in Bosnian).<br />
Jireček, J. (1951): Commercial roads and mines of Medieval Serbia and Bosnia. Svjetlost,<br />
Sarajevo (in Bosnian, translate originally from German).<br />
Johnstone, S.J. and Johnstone M.G. (1961): Minerals for the chemical and allied industries.<br />
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325
SILICATES<br />
Kravčenko, V.B. (1964): The crystal structure of searlesite. Kristallografija, 9, 182, Moscow<br />
(in Russian).<br />
Majer, V. (1953): Chabasite and desmine from Bor in eastern Serbia. Memorial volume of<br />
Mišo Kišpatić, Yugoslav Academy of Sciences and Arts, 175, Zagreb (in Croatian).<br />
Mandić, M. (1931): The prehistoric settlement at Sanski Most. Journal of the National<br />
Museum of Bosnia and Hercegovina, vol. XLIII, 2, Sarajevo (in Bosnian).<br />
Mason, B. and Greenberg, S.S. (1960): Zeolites and associated minerals from southern<br />
Brasil. Ark. Mineral. Geol., 1, 519-526.<br />
Meier, V.M. (1960): The crystal structure of natrolite. Zeit. Kristallogr., 113, 430.<br />
Miheev, V.I. (1957): Determination of minerals by x-ray diffraction. Gosgeoltehizdat,<br />
Moscow (in Russian).<br />
Mikolji, V. (1969): The history of iron and iron manufacture in Bosnia, Zenica (in Bosnian).<br />
Moenke, H. (1962): Mineralspektren. Akademie Verlag, Berlin.<br />
Mohs, F. (1824): Grundriss der Mineralogie, 2 Bänder, Dresden.<br />
Nikitin, W.W. (1936): Die Fedorow-Methode, Bornträger, Berlin.<br />
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Petruk, W. (1964): Determination of the heavy-atom content in chlorite by means of the x-ray<br />
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Radimsky, V. (1891): On some prehistoric and Roman artefacts in the area of the Sana river<br />
in Bosnia. Journal of the National Museum of Bosnia and Hercegovina, vol. III,<br />
Sarajevo (in Bosnian).<br />
Ramdohr, P. and Strunz, H. (1967): Klockmann’s Lehrbuch der Mineralogie. 15th edition. F.<br />
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326
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Spaho, F. (1913): The Turkish mining laws. Journal of the National Museum of Bosnia and<br />
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Strunz, H. (1966): Mineralogische Tabellen. 4. völlig neubearbeitete und erweiterte Auflage<br />
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moyen des rayones X. Lisbonne.<br />
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Textband. Schweitzerbart’sche Verlagsbuchhandlung, Stuttgart.<br />
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Truhelka, Ć. (1936): Sultan Suleyman I law on the silver-mines and coin mints in Bosnia and<br />
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Mitteilungen aus Bosnien und Herzegovina, Wien.<br />
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Vojtkevič, G.V., Mirošnikov, A.E. and Prohorov, V.G. (1970): A short handbook of<br />
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Wallerius, J.G. (1778): Systema mineralogicum. Duo tomi.Vindobonae.<br />
Whittaker, E.J.W. and Zussman, J. (1956): The characterisation of serpentine minerals by<br />
x-ray diffraction. Min. Mag., 31, 107.<br />
Zavarickij, A.N., Sobolev, V.S., Kvaša, L.G., Kostyuk, V.P. and Bobrievič, A.P. (1958): New<br />
diagrams fro the determination of high-temperature plagioclases. Zap. Min. Ob. 87,<br />
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Zussman, J. (1967): Physical methods in determinative mineralogy. Academic Press, London<br />
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II References pertaining to the minerals of Bosnia and Hercegovina<br />
Arsenijević, M. (1960): Geochemical investigations of potassium feldspars from pegmatitepneumatolytic<br />
formations (Prilep area). Journal of the Natural History Museum of<br />
Serbia, A-13, 69-104, Belgrade (in Serbian).<br />
Arsenijević, M. (1967): Preliminary investigations on the distribution of beryllium, tin,<br />
niobium and molybdenum in granitoid minerals as indicators of geochemical areals<br />
in the Dinarides and the Carpatho-Balkan arc. Ann. Inst. Geol. Mining and Nucl.<br />
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Atanacković, M., Mudrenović, V. and Gaković, M. (1968): The stratigraphy and tectonics of<br />
the Borovica area near Vareš. Geol. gazette, 12, 5-36, Sarajevo (in Bosnian).<br />
Barić, Lj. (1942): Mineralogical and petrological investigations of the Bosnian schist<br />
mountains. Journal of the Croatian Geological Survey and Geological Museum, I,<br />
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327
SILICATES<br />
Barić, Lj. (1955): Bariumhaltiger Orthoklas von Busovača in Zentralbosnien. Bull. Sci.<br />
Cons. Acad. Yougosl., tome 2/2, 55, Zagreb.<br />
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Barić, Lj. (1959): On the neccessity and possibilities of precise microscopic determinations<br />
of plagioclases. Journal of the Geological and Geophysical Survey of NR Serbia, 11,<br />
99-113, Belgrade (in Croatian).<br />
Barić, Lj. (1960): Beryl from Mt. Motajica. Acta Geologica, II, 71-82, Yugosl. Acad. Sci.<br />
Arts, Zagreb (in Croatian).<br />
Barić, Lj. (1961): Über die Hyalophane von Busovača. Tschermaks Min. Petr. Mitteilungen,<br />
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Barić, Lj. (1966a): Über die Bestandteile einiger Tuffe der Umgebung von Livno in<br />
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Barić, Lj. (1966b): Searlesite from Lopare in north-eastern Bosnia. Journal of the Museum<br />
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Feldpäte mit Hochtemperatur-Optik in den Gesteinen der mitteltriassischen Spilit-<br />
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Universität in Zagreb. Mitteilung 1. Juni 1969, Zagreb.<br />
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Dianrides really contain albite with apparently high-temperature optics ? Proceedings<br />
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Barić, Lj. (1970a): Keratophyre from the Trešanica gorge near Bradina in Hercegovina.<br />
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5-12, Sarajevo (in Croatian).<br />
Barić, Lj. (1971): Hyalophan aus Zagrlski (Zagradski) potok bei Busovača (Zentralbosnien).<br />
2nd International symposium on the mineral deposits of the Alps, Bled, Slovenia,<br />
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Zentralbosnien. Mitt. des Bosnisch-Herzegowinischen Landesmuseums, Bd. II,<br />
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Symp. on the mineral deposits of the Alps, 281-285, Ljubljana.<br />
Barić, Lj. (1972b): Sind eigentlich in den Gesteinen der mitteltriassichen Spilit-Keratophyre-<br />
Assoziation in Dinariden, die Albite, deren Optik angeblich völlig klar auf die<br />
Hochtemperaturoptik hinweist, erhalten? Presentations at the VII Congress of<br />
Yugoslav Geological Societies, Mineralogy and Petrology Section, 29-41, Zagreb.<br />
328
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Barić, Lj. (1975): Albite in rocks of the Middle Triassic spilite-keratophyre association of the<br />
dinarides is low, well-ordered albite. Geol. gazette, 28, 173-194, Zagreb.<br />
Barić, Lj. and Jovanović, Č. (1966): A short lithostratigraphic description of the Šibošnica-<br />
Lopare basin and investigations on searlesite. Geol. gazette, 28, 173-194, Sarajevo<br />
(in Croatian).<br />
Barić, Lj. and Tajder, M. (1955): Pyrophyllitschiefer von Parsovići in der Herzegowina. Bull.<br />
Sci. Cons. Acad. Yougosl., tome 2, 3, 91, Zagreb.<br />
Barić, Lj. and Tajder, M. (1956): Pyrophyllite schists from Parsovići in Hercegovina. Geol.<br />
gazette, VIII-IX, 187-190, Zagreb (in Croatian).<br />
Barić, Lj. and Tajder, M. (1967): Microscopic determination (microphysiography) of rockforming<br />
minerals. Školska knjiga, Zagreb (in Croatian).<br />
Barić, Lj. and Trubelja, F. (1971): Hydromuscovite schists from the area of Repovac<br />
west of Bradina (Hercegovina). Journal of the National Museum of Bosnia and<br />
Hercegovina, new series vol. X, 5-12, Sarajevo (in Croatian).<br />
Barić, Lj. and Trubelja, F. (1975): Hydromuskovitschiefer aus der Umgebung des Dorfes<br />
Repovci westlich von Bradina in der Herzegowina. Wiss. Mitteilungen des Bosnisch-<br />
Herzegowinischen Landesmuseums, Bd. IV/V, Heft C, 33-40, Sarajevo.<br />
Barić, Lj. and Trubelja, F. (1975a): Friedrich Katzer – the mineralogist and crystallographer.<br />
Geol. gazette (memorial volume) 20, 165-176, Sarajevo (in Croatian).<br />
Barić, Lj. and Tućan, F. (1925): Notes about some minerals from our area. Geological Annals<br />
of the Balkan Peninsula, VIII/1, 129-135, Belgrade (in Croatian).<br />
Baumgärtel, B. (1904): Das Nebengestein der Chromeisen-Erzlagerstätten bei Duboštica<br />
in Bosnien und das Auftreten von sekundär gebildetem Chromit im demselben.<br />
Tschermaks Min. und Petr. Mitt., 23, 5, 393-400.<br />
Behlilović, S. and Pamić, J. (1963): Ladinian volcanogenic formations in the river Drežanka<br />
valley (Hercegovina). Geol. gazette, 7, 39-44, Sarajevo (in Bosnian).<br />
Biščević-Muštović, F., Trubelja, F. and Sijarić, G. (1976): Gibbsite-kaolinite bauxites<br />
from the shores of lake Rama. Presentation at the IV Yugoslav Symposium on the<br />
prospecting and exploitation of bauxite, 11-15.10.1976, Herceg Novi (in Bosnian).<br />
Boué, A. (1828): Zusammenstellung der bekannten geognostischen Tatsachen über die<br />
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Boué, A. (1840): Esquisse geologique de la Turquie d’Europe. Paris.<br />
Boué, A. (1840a): La Turquie d’Europe. Paris.<br />
Boué, A. (1870): Mineralogisch-geognostisches Detail über einige meiner Reiserouten in der<br />
europäischen Türkei. Sitzb. d.K. Akademie d. Wissenschaften, Band LXI, I Abt.,<br />
Februar Heft, 203-294, Wien.<br />
Brajdić, V. (1964): Gabbropegmatite from the area of Olovo in north-east Bosnia. Geol.<br />
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Burić, P. and Vujnović, L. (1970): Some data on the bauxite deposit at Ljuša village, between<br />
Jajce and Donji Vakuf (Bosnia). Geol. gazette, 14, 191-195, Sarajevo (in Bosnian).<br />
Buzaljko, R. (1971): Geological setting of the area between Goražde and Rudo (south-east<br />
Bosnia). Geol. gazette, 15, 69-90, Sarajevo (in Bosnian).<br />
Caillère, S. et Studen, M. (1969): Sur une beidellite ferrifere rencontree par une sondage<br />
pres de Šipovo – Jajce, Bosnie (Yougoslavie). Bull. du Museum National d’Historie<br />
Naturelle, serie 2, tome 41, 3, 767-769, Paris.<br />
Cissarz, A. (1956): Über ein ungewöhnliches Magnetitvorkommen am Kontakt des<br />
Gabbromassivs von Jablanica in der Herzegowina. Journal of the Geological and<br />
Geophysical Survey of NR Serbia, 12, 201-221, Belgrade.<br />
329
SILICATES<br />
Conrad, A. (1870): Die Mineralschätze in Bosnien (mit kleinen , stellenweisen Bemerkungen<br />
von O. Hingenau). Österreichische Zeitschrift für Berg- und Hüttenwesen, XVIII<br />
Jahrgang, 20, 137-141, Wien.<br />
Conrad, A. (1871): Bosnien mit Bezug auf seine Mineralschätze. Mitteilungen der K.K.<br />
Geographischen Gesellschaft, Bd. XIII (1870) 219-228, Wien.<br />
Čelebić, Đ. (1963): Sedimentary deposits of iron and manganese ores in the diabase-chert<br />
series of north-west Hercegovina. Geol. gazette, 7, 145-159, Sarajevo (in Bosnian).<br />
Čelebić, Đ. (1967): Geological and tectonic setting of the Paleozoic- and Mesozoic-age area<br />
between Konjic and Prozor – with special attention to Fe and Mn ores. Geol. gazette,<br />
X (special editions), 1-139, Sarajevo (in Bosnian).<br />
Čičić, S. (1975): Geological prospecting in Bosnia and Hercegovina, and enhancement of<br />
possibilities for the period 1976-1985. I Conference of miners and geologists of<br />
Bosnia and Hercegovina, Tuzla, December 1975, addendum to the Geol. gazette,<br />
17, 7-13, Sarajevo (in Bosnian).<br />
Čičić, S. (1975a): Non-metal resources in Bosnia and Hercegovina. I Conference of miners<br />
and geologists of Bosnia and Hercegovina, Tuzla, December 1975, addendum to the<br />
Geol. gazette, 17, 38-51, Sarajevo (in Bosnian).<br />
Čičić, S. and Pudar, N. (1973): Geological, explorational, technical and economic features of<br />
the clay deposits of Bosnia and Hercegovina. Geol. gazette, 17, 203-260, Sarajevo<br />
(in Bosnian).<br />
Čutura, O. (1918): Volcanic rocks in south-west Bosnia. Journal of the National Museum of<br />
Bosnia and Hercegovina,XXX, 11-20, Sarajevo (in Bosnian).<br />
Ćatović, F. and Trubelja, F. (1976): Occurrences of pyrite-bearing bauxites in some deposits<br />
in Hercegovina. Presentation at the IV Yugoslav Symposium on the prospecting and<br />
exploitation of bauxite, 11-15.10.1976, Herceg Novi (in Bosnian).<br />
Ćatović, F., Trubelja, F. and Sijarić, G. (1976): Bauxites of the Srnetica mountain (Bosnia).<br />
Travaux du Comite international pour l’etude des bauxites, de l’alumine et<br />
d’aluminium (ICSOBA), No. 13, 103-113, Academie Yougoslave des Sciences et<br />
des Arts, Zagreb.<br />
Dangić, A. (1971): The deposit of primary kaoline at Bratunac. Geol. Ann. Balkan Peninsula,<br />
36, 223-237, Belgrade (in Serbian).<br />
Divljan, S.B. (1954): Discovery of barium adulare (hyalophane) near Busovača in Bosnia.<br />
Proceedings of the ‘Jovan Žujović’ Institute, 7, 269-275, Belgrade (in Serbian).<br />
Divljan, S. and Simić, V. (1956): Statement on the discovery of barium adulare (hyalophane)<br />
at Busovača in central Bosnia. Memoirs of the Serbian Geological Society (for<br />
1954), 91 and 137, Belgrade (in Serbian).<br />
Džepina, D. (1970): Results of mineralogic and petrologic investigations of regionally<br />
metamorphosed basic rocks in the southern part of Mt. Borja in Bosnia. Journal of<br />
the Museum of Natural History in Belgrade, A 25, 129-144, Belgrade (in Serbian).<br />
Đorđević, D. (1969): Tourmaline- and quartz-bearing rocks from the Srebrenica mine area.<br />
Geol. gazette, 13, 217-223, Sarajevo (in Bosnian).<br />
Đorđević, D. (1969a): The mineralogy and origin of talcites from Mušići near Bosansko<br />
Petrovo Selo. Geol. gazette, 13, 301-310, Sarajevo (in Bosnian).<br />
Đorđević, D., Buzaljko, R. and Mijatović, V. (1968): New occurrences of asbestos in the<br />
Bosnian serpentine zone with special attention to the Jovanovići-Stepanovići deposit<br />
(Bosansko Petrovo Selo). Geol. gazette, 12, 309-322, Sarajevo (in Bosnian).<br />
Đorđević, D. and Mijatović, V. (1966): Oligoclase-bearing veins in serpentinites from the<br />
Zavidovići area. Geol. gazette, 11, 485-487, Sarajevo (in Bosnian).<br />
330
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Đorđević, D. and Mojičević, M. (1972): Albite syenite from the flanks of the Mt. Borja<br />
ultramafic complex. Geol. gazette, 16, 137-143, Sarajevo (in Bosnian).<br />
Đorđević, D. and Stojanović, D. (1972): Mineralogical investigations of natrolite in diabase<br />
rocks from Bojići near Banja Luka. Geol. gazette, 16, 157-164, Sarajevo (in<br />
Bosnian).<br />
Đorđević, D. and Stojanović, D. (1974): Analcime, laumontite, natrolite and the boron<br />
mineral datolite in diabase rocks from Banja Luka (Bosnia, Yugoslavia). Journal<br />
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Đorđević, D. and Stojanović, V. (1972): Discovery of albite-bearing granite in the ophiolitic<br />
zone Konjuh-Ozren-Uzlomac. Geol. gazette, 10, 230-240, Sarajevo (in Bosnian).<br />
Đorđević, P. (1958): Basic igneous rocks from Vareš (Bosnia). Annals of the Faculty of<br />
Mining and Geology in Belgrade, 5/1957, 39-44, Belgrade (in Serbian).<br />
Đorđević, P. (1960): Amphiboles and pyroxenes in the gabbro rock from Stavnja creek near<br />
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Đurić, S. (1958): Exploration of the Ni-Fe ore deposit in the Vardište area near Višegrad in<br />
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Đurić, S. (1960): Optimal oolitic-clastic sediments of the Zlatibor zone. Geol. gazette, 7,<br />
131-143, Sarajevo (in Bosnian).<br />
Đurić, S. (1963a): Occurrences of magnetite in the Čajniče area. Geol. gazette, 7, 167-174,<br />
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Đurić, S. (1968): Cinnabarite mineralisation of listvenitised serpentinites of Mt. Ljubić in<br />
northern Bosnia. Geol. gazette, 12, 159-163, Sarajevo (in Bosnian).<br />
Đurić, S. and Kubat, I. (1962): Occurrences of copper ore in the Mt. Čavka area (Bosnia).<br />
Geol. gazette, 6, 197-219, Sarajevo (in Bosnian).<br />
Đurić, S. and Nikolić, D. (1969): Xonotlite from some localities. Memoirs of the Serbian<br />
Geological Society (for 1964-1967, special edition), 811-813 and 855, Belgrade (in<br />
Serbian).<br />
Esih, O. and Natević, Lj. (1963): Contribution to the age determination of the diabase-chert<br />
series in the Rogatica area. Geol. gazette, 8, 123-125, Sarajevo (in Bosnian).<br />
Evlija Čelebija (1954, 1967 and 1973): Travel-logs. Translation, introduction and comments<br />
by Hazim Šabanović, Sarajevo (in Bosnian).<br />
Filipovski, Gj. and Ćirić, M. (1963): Soils of Yugoslavia, Belgrade (in Serbian).<br />
Foullon, H.B. (1893): Über Goldgewinnungsstätten der Alten in Bosnien. Jahrbuch der K.K.<br />
Reichsanstalt, XLII, Heft I, 1-52, Wien.<br />
Foullon, H.B. (1895): Über ein Asbestvorkommen in Bosnien. Verhandlungen der K.K.<br />
Geol. Reichsanstalt, 14, 365-367, Wien.<br />
Gaković, J. and Gaković, M. (1973): Insoluble residue in the Triassic carbonate rocks of the<br />
external Dinarides in Bosnia and Herzegovina. Bull. Sci. Cons. Acad. Yugosl., tome<br />
18, No. 7-9, 136-137, Zagreb.<br />
Gay, P. and Roy, N.N. (1968): The mineralogy of the potassium-barium feldspar series, III:<br />
subsolidus relationships. Min. Magazine, 36, No. 283, 914-932.<br />
Gojković, E.S. and Nikolić, R.D. (1967): Uranium and thorium in the beryls of Yugoslavia.<br />
Ann. Inst. Geol. Mining and Nucl. Mat. Min. Resources, 3, 219-222, Belgrade (in<br />
Serbian).<br />
Golub, Lj. (1961): The petrology and origin of the igneous rocks from the southern flanks<br />
of Mt. Kozara. Acta Geologica III, 253-312, Yugoslav Acad. Sci. Arts, Zagreb (in<br />
Croatian).<br />
331
SILICATES<br />
Götting, A. (1886): Über Manganerzlager bei Čevljanovići und über Bleierzgänge von<br />
Srebrenica in Bosnien. Berg-Hüttenmänn. Zeitung, 89 und 345, Leipzig.<br />
Grafenauer, S. (1975): Ore petrology of ultramafic rocks of Yugoslavia. Annals of the<br />
Slovenian Academy of Sciences and Arts, 1-152, Ljubljana (in Slovenian).<br />
Grimer, I. (1897): An occurrence of asbestos near Halilovac in the Sanski Most area. Journal<br />
of the National Museum of Bosnia and Hercegovina, IX, 501-503, Sarajevo (in<br />
Bosnian).<br />
Grimmer, J. (1889): Das Asbestvorkommen von Alilovci im Bezirke Sanskimost.<br />
Wissenschaft. Mitt., VI, 887-888, Wien.<br />
Hantken, M. (1867): Neues Meerschaumvorkommen in Bosnien. Verhandlungen der K.K.<br />
Geol. Reichsanstalt, 10, 227-228, Wien.<br />
Hauer, F. (1879): Miemit von Žepče in Bosnien. Verhandlungen der Geol. Reichsanstalt, 16,<br />
121-123, Wien.<br />
Hauer, F. (1884): Erze und Mineralien aus Bosnien. Jahrbuch der K.K. Geol. Reichsanstalt,<br />
XXXIV, 751-758, Wien.<br />
Hiessleitner, G. (1951/52): Serpentin- und Chromerz-Geologie der Balkanhalbinsel und eines<br />
Teiles von Kleinasien. Jahrb. Geol. Bundesanstalt, Sonderband 1, 1-683, Wien.<br />
Hlawatsch, C. (1903): Eine merkwürdige Hornblende aus dem Gabbro-Diorit von Jablanica.<br />
Tschermak’s Min.-Petr. Mitt., 22, 499-500.<br />
Ignjatović, P. (1973): The incomplete spatial zonarity of the chrysotile-asbestos deposit ‘Delić<br />
Brdo – Brdjani’ at Bosansko Petrovo Selo. Geol. gazette, 17, 305-308, Sarajevo (in<br />
Bosnian).<br />
Ilić, M. (1954): General characteristics of the asbestos deposits at Bosansko Petrovo Selo.<br />
Memoirs of the Serbian Geological Society (for 1950-1952), 121-126, Belgrade (in<br />
Serbian).<br />
Ilić, M. (1954a): On the occurrence of talc (steatite) at Žepče in Bosnia. Memoirs of the<br />
Serbian Geological Society (for 1950-1952), 52-55, Belgrade (in Serbian).<br />
Ilić, M. (1971): Contribution to the understanding of fundamental geological problems of<br />
Alpine-type ultrabasic rocks. Annals of the Faculty of Mining and Geology in<br />
Belgrade, 13/1970, 81-89, Belgrade (in Serbian).<br />
Ilić, S. (1953): Kaoline from Mt. Motajica. Journal of the Society of Chemists of Bosnia and<br />
Hercegovina, 2, 5-18, Sarajevo (in Bosnian).<br />
Ilić, S. (1954): Vein quartz – occurrences of vein quartz at Busovača near Sarajevo. Mining<br />
and Metallurgy, 5, 1414-1416, Belgrade (in Serbian).<br />
Jakšić, D., Glavaš, M. and Trubelja, F. (1967): Exploration of herzegovinian bauxites<br />
with the aid of thermogravimetry and differential thermal analysis. Journal of the<br />
National Museum of Bosnia and Hercegovina, new series vol. VI, 15-22, Sarajevo<br />
(in Bosnian).<br />
Jakšić, T. (1927): Bauxites in Herzegovina, particularly around Mostar. Gazette of the<br />
Geological Survey in Zagreb, II, 82-120, Zagreb (in Croatian).<br />
Jakšić, T. (1929): On the age and geological and mining characteristics of the salt deposit in<br />
the Tuzla area. Mining and Metallurgy gazette, I/3, 97-104, Belgrade (in Serbian).<br />
Jakšić, T. (1930): The arsenic-ore body at Hrmza (manuscript). Sarajevo (in Bosnian).<br />
Jakšić, T. (1934): Contribution to the knowledge on bauxites in Hercegovina. The stratified<br />
deposit at Stolac. Mining and Metallurgy gazette, VI/3-4, 45-48, Belgrade (in<br />
Serbian).<br />
Jakšić, T. (1937): Ores in the Sarajevo area. Gajret calendar for 1938, 137-140, Sarajevo (in<br />
Bosnian).<br />
332
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Jakšić, T. (1938): Occurrences and deposits of manganese ores at Mt. Kozara near Banja<br />
Luka. Mining gazette, II, 1-12, Ljubljana (in Serbian).<br />
Jakšić, T. (1938a): General overwiev of the geology of Bosnia and Hercegovina. In: Koen,<br />
Džikovski and Sunarić, editors – ‘The economic area of Bosnia and Hercegovina’,<br />
Sarajevo (in Bosnian).<br />
Jakšić, V., Vuletić, N. and Vrlec. Ž. (1971): Contribution to the understanding of brown<br />
soils on the serpentinites of Bosnia. Memorial volume of professor Gračanin’s 70th<br />
birthday, 123-127, Zagreb (in Croatian).<br />
Janković, S. and Vakanjac, B. (1969): Non-metal mineral deposits. Građevinska knjiga,<br />
Belgrade (in Serbian).<br />
Jeremić, M. (1959): Occurrences and deposits of manganese in Bosnia and Hercegovina.<br />
Journal of the Museum of Natural History in Belgrade, A 12, 167-188, Belgrade (in<br />
Serbian).<br />
Jeremić, M. (1960): Barite-bearing areas of the Una and Sana river watersheds in north-east<br />
Bosnia. Tehnika, 2, 241-255, Belgrade (in Serbian).<br />
Jeremić, M. (1960a): A new metallogenic province of bauxite and iron ores of eastern Bosnia,<br />
in the Peručac – Šekovići sector. Tehnika, 10, 1870-1877, Belgrade (in Serbian).<br />
Jeremić, M. (1961): Triassic-age barite deposits in Bosnia. Geol. gazette, 5, 107-161,<br />
Sarajevo (in Bosnian).<br />
Jeremić, M. (1963): Hydrothermal alterations of rocks around barite deposits in the schist<br />
mountains of central Bosnia. Technologica Acta, I/3, 89-98, Tuzla (in Bosnian).<br />
Jeremić, M. (1963a): The metalogenesis of Paleozoic barite deposits in Bosnia. Technologica<br />
Acta, I/1-2, 1-59, Tuzla (in Bosnian).<br />
John, C. (1879): Über einige Eruptivgesteine aus Bosnien. Verhandlungen der K.K. Geol.<br />
Reichsanstalt, 11, 239-241, Wien.<br />
John, C. (1880): Über krystallinische Gesteine Bosniens und der Hercegovina. Anhang zu<br />
den Grundlinien der Geologie von Bosnien-Hercegovina, 273-296, Wien.<br />
John, C. (1888): Über die Gesteine des Eruptivstockes von Jablanica an der Narenta. Jahrbuch<br />
der K.K. Geol. Reichsanstalt, XXXVIII, 343-354, Wien.<br />
Joksimović, Ž. (1903): Comments on the paper by Grimmer ‘ An occurrence of asbestos<br />
near Halilovac in the Sanski Most area’, published in the Journal of the National<br />
Museum of Bosnia and Hercegovina, IX, 501-503, 1897, Sarajevo. Geological<br />
Annals of the Balkan Peninsula, VI/1, 351, Belgrade (in Serbian).<br />
Jovanović, Č. (1972): Contribution to the geology of Tertiary sediments between the rivers<br />
Una and Vrbas. Geol. gazette, 16, 5-26, Sarajevo (in Bosnian).<br />
Jovanović, Č. and Jovanović, O. (1966): The Miocene of the Šibošnica-Lopare area. Geol.<br />
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Jovanović, R. (1957): An overview of Mesozoic series of rocks, and some new data on the<br />
stratigraphy and tectonics of NR Bosnia and Hercegovina. II Congress of Yugoslav<br />
Geologists, 38-63, Sarajevo (in Bosnian).<br />
Jović, P. (1965): On the sedimentology and petrology of sedimentary rocks on the sheet<br />
Drvar (Geological map of Yugoslavia – translators remark). Archive of professional<br />
documents of the Institute of Geology, 3994/4, Zagreb (in Croatian).<br />
Jovičić, M.Z. (1891): Microgranulites from Srebrenica and Ljubovija. Geological Annals of<br />
the Balkan Peninsula, III, 111-113, Belgrade (in Serbian).<br />
333
SILICATES<br />
Jurković, I. (1954): Ni-lineite (siegenite) and millerite in tourmalinized barite from Brestovsko<br />
in the schist mountains of central Bosnia. Geol. gazette, V/VII (1951-53), 273-291,<br />
Zagreb (in Croatian).<br />
Jurković, I. (1954a): Augite- and labradorite-bearing andesites from Orašin, south-east of<br />
Bakovići (Bosnia). Geol. gazette, V/VII (1951-53), 111-126, Zagreb (in Croatian).<br />
Jurković, I. (1956): The mineral parageneses of schist mountains of central Bosnia with<br />
special emphasis on tetrahedrites. Unpublished PhD thesis, Zagreb (in Croatian).<br />
Jurković, I. (1956a): Bournonite in the barite deposit at Rimska Jama near Kreševo. Geol.<br />
gazette, 2, 5-20, Sarajevo (in Bosnian).<br />
Jurković, I. (1957): The basic characteristics of the metallogenic region of the Mid-Bosnian<br />
ore mountains. II Congress of Yugoslav Geologists, 504-519, Sarajevo (in Bosnian).<br />
Jurković, I. (1958): Tetrahedrite from the Trošnik ore body near Fojnica in the schist<br />
mountains of central Bosnia. Geol. gazette, 4, 221-246, Sarajevo (in Bosnian).<br />
Jurković, I. (1958a): Cassiterite, stannine and molybdenite in the Vrtlasce ore body east of<br />
Fojnica. Geol. gazette, 4, 309-320, Sarajevo (in Bosnian).<br />
Jurković, I. (1959): Occurrences of barite in Croatia. Geol. gazette, 12/1958, 77-94, Zagreb<br />
(in Croatian).<br />
Jurković, I. (1961): Realgar and auripigmente (orpiment) in the ore bodies of the schist<br />
mountains of central Bosnia. Geol. gazette, 5, 199-240, Sarajevo (in Bosnian).<br />
Jurković, I. (1961a): Minerals of the iron deposits of Ljubija near Prijedor. Geol. gazette,<br />
14/1960, 161-212, Zagreb (in Croatian).<br />
Jurković, I. (1962): Parageneses of ore bodies in the Čemernica area near Fojnica. Geol.<br />
gazette, 6, 141-156, Sarajevo (in Bosnian).<br />
Jurković, I. and Majer, V. (1954): Rhyolites (quartz-porphyres) from Mt. Vranica and albitebearing<br />
rhyolite from Sinjakovo in the schist mountains of central Bosnia. Journal<br />
of the Geological and Geophysical Survey, XI, 207-233, Belgrade (in Croatian).<br />
Jurković, I. and Sakač, K. (1964): Stratigraphical, paragenetical and genetical characteristics<br />
of bauxites in Yugoslavia. Symposium sur les bauxites, oxydes et hydroxydes<br />
d’aluminium, 1, 253-263, Zagreb.<br />
Kacer, F. (1926): Geology of Bosnia and Hercegovina. Part 1. (translation from German by<br />
T. Jakšić and M. Milojković), Sarajevo (in Bosnian).<br />
Karamata, S. (1953): General characteristics of melaphyres from the Vareš area (Bosnia).<br />
Memorial volume of Mišo Kišpatić, Yugoslav Academy of Sciences and Arts, 237-<br />
246, Zagreb (in Serbian).<br />
Karamata, S. (1953/54): Albite-bearing rhyolites from the area of Bosansko Petrovo Selo.<br />
Annals of the Faculty of Mining and Geology in Belgrade, 249-255, Belgrade (in<br />
Serbian).<br />
Karamata, S. (1957): Keratophyres from the Zvornik area. Geol. gazette, 3, 181-183, Sarajevo<br />
(in Bosnian).<br />
Karamata, S. (1960): The melaphyres from Vareš. Symposium on the problems of Alpinetype<br />
initial magmatism. Ref 5, 1-17, Ilidža-Vareš (in Bosnian).<br />
Karamata, S. and Pamić, J. (1960): Gabbros, diabases and spilites from the Tribije area.<br />
Symposium on the problems of Alpine-type initial magmatism. Ref 5, 1-15, Ilidža-<br />
Vareš (in Bosnian).<br />
Karamata, S. and Pamić, J. (1964): Occurrences of granitoid rocks in central Bosnia. Geol.<br />
gazette, 10, 227-232, Sarajevo (in Bosnian).<br />
Karamata, S. and Petković, M. (1957): Comments on the paper ‘Chrysotile asbestos from<br />
Bosansko Petrovo Selo’. Geol. gazette, 3, 189-190, Sarajevo (in Bosnian).<br />
334
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Karšulin, M., Tomić, M. and Lahodny, A. (1949): Investigations on bauxite. Proceedings<br />
(Rad) Yugosl. Acad. Sciences and Arts, Vol. 276, 125-138, Zagreb (in Croatian).<br />
Katzer, F. (1900): Das Eisenerzgebiet von Vareš in Bosnien. Berg- und Hüttenmänn, Jahrbuch<br />
der Bergakademie zu Leoben und Pribram, 48. Jahrg., 99-190, Wien.<br />
Katzer, F. (1901): Über die Zusammensetzung der Goldseife (des Pavlovac Baches) in<br />
Bosnien. Österreichische Zeitschrift für Berg- und Hüttenwesen, XLIX, 277-280,<br />
Wien.<br />
Katzer, F. (1903): Geologischer Führer durch Bosnien und die Hercegovina. Sarajevo.<br />
Katzer, F. (1904): Über ein Glaubersaltzvorkommen in den Werfenser Schichten Bosniens.<br />
Zenetralbl. f. Mineralogie, Geologie etc. 13, 399-402, Stuttgart.<br />
Katzer, F. (1905): Die Schwefelkies und Kupferkieslagerstätten Bosniens und der Hercegovina<br />
(Mit einem einleitenden Überblick der wichtigsten Schwefelkiesvorkommen und<br />
der Bedeutung der Kiesproduktion Europas). Berg- und Hüttenmänn. Jahrb. der<br />
Montaninst. Hochschulen, 53, 251-338, Wien.<br />
Katzer, F. (1906): Die geologischen Verhältnisse des Manganerzgebietes von Čevljanović<br />
in Bosnien. Berg- und Hüttenmänn, Jahrbuch der Bergakademie zu Leoben und<br />
Pribram, 54/3, 203-244, Wien.<br />
Katzer, F. (1907): Die Fahlerz- und Quecksilberlagerstätten Bosniens und der Hercegovina.<br />
Berg- und Hüttenmänn, Jahrbuch der Bergakademie zu Leoben und Pribram, 55/2,<br />
145-265, Wien.<br />
Katzer, F. (1908): Die Minerale des Erzgebietes Sinjakovo und Jezero in Bosnien. Jahrbuch<br />
der Bergakademie zu Leoben und Pribram, 55/2, 285-330, Wien.<br />
Katzer, F. (1909): Über bosnischen Meerschaum. Jahrbuch der Bergakademie zu Leoben und<br />
Pribram, 57, 64-88, Wien.<br />
Katzer, F. (1909-1911): Die Eisenerzlagerstätten Bosniens und der Hercegovina. Jahrbuch<br />
der Bergakademie zu Leoben und Pribram, Bd. 57/1909, 173-330, Bd. 58/1910,<br />
202-230, Bd. 59/1911, 25-98 und 180-194, Wien.<br />
Katzer, F. (1910): ): Die Eisenerzlagerstätten Bosniens und der Hercegovina. Ergänzter<br />
Sonderabdruck aus dem Jahrbuch der Bergakademie zu Leoben und Pribram (mit<br />
einer Übersichtskarte und 52 Abbildungen im Text), 1-343, Wien.<br />
Katzer, F. (1911): Poechit – ein Manganeisenerz von Vareš in Bosnien. Österreichische<br />
Zeitschr. f. Berg- und Hüttenwesen, 59, No. 17, 229-232, Wien.<br />
Katzer, F. (1912): Zur Kentniss der Arsenlagerstätten Bosniens. Österreichische Zeitschr. f.<br />
Berg- und Hüttenwesen, 60, No. 20, 267-270 und 285-288, Wien.<br />
Katzer, F. (1912a): Über das Meerschaumvorkommen und die Meerschaumindustrie<br />
Bosniens. Steinbruch und Sandgrube, 1-6 (Sonderdruck), Halle and der Saale.<br />
Katzer, F. (1917): Das Bauxitvorkommen von Domanović in der Hercegovina. Zeitschr. f.<br />
praktische Geologie, 8, 133-138, Halle.<br />
Katzer, F. (1920): Minerals of Bosnia and Hercegovina. Elements. Extract from the book<br />
‘Topographic and practical mineralogy of Bosnia and Hercegovina’ by F. Katzer.<br />
Translation by D. Marinković. Journal of the National Museum of Bosnia and<br />
Hercegovina, vol. 32/3-4, 227-244, Sarajevo (in Bosnian).<br />
Katzer, F. (1921): Schwarzer Poechit aus der metasomatischen Eisenerz-zone von Vareš in<br />
Bosnien. Zentralbl. f. Mineralogie, Geologie etc., 24, 738-741, Stuttgart.<br />
Katzer, F. (1924): Geologie Bosniens und der Hercegovina. Erster Band, I Hälfte, 480 Seiten,<br />
Sarajevo.<br />
Katzer, F. (1925): Geologie Bosniens und der Hercegovina. Erster Band, II Hälfte, 480-560,<br />
Sarajevo.<br />
335
SILICATES<br />
Kišpatić, M. (1893): Sepiolite from Mt. Ljubić near Prnjavor. Journal of the National<br />
Museum of Bosnia and Hercegovina, vol. 5, 99-105, Sarajevo (in Bosnian).<br />
Kišpatić, M. (1895): Der Meerschaum aus der Ljubić planina bei Prnjavor. Wiss. Mitt. aus<br />
Bosnien und der Hercegovina, Bd. III, 590-595, Wien.<br />
Kišpatić, M. (1897): Crystalline rocks of the serpentine zone in Bosnia. Memoirs (Rad) of the<br />
Yugosl. Acad. Sci. and Arts, Vol. 133, 95-231, Zagreb (in Croatian).<br />
Kišpatić, M. (1900): Die krystallinischen Gesteine der bosnischen Serpentinzone. Wiss. Mitt.<br />
aus Bosnien und der Hercegovina, Bd. VII, 377-484, Wien.<br />
Kišpatić, M. (1902): Mineralogical notes from Bosnia. Memoirs (Rad) of the Yugosl. Acad.<br />
Sci. and Arts, Vol. 151 (32), 28-68, Zagreb (in Croatian).<br />
Kišpatić, M. (1904): Andesite and dacite from the banks of the Bosna river. Memoirs (Rad)<br />
of the Yugosl. Acad. Sci. and Arts, Vol. 159 (36), 28-38, Zagreb (in Croatian).<br />
Kišpatić, M. (1904a): Hypersthene-bearing andesite and dacite from the Srebrenica area in<br />
Bosnia. Memoirs (Rad) of the Yugosl. Acad. Sci. and Arts, Vol. 159 (36), 1-27,<br />
Zagreb (in Croatian).<br />
Kišpatić, M. (1904b): Petrographical notes from Bosnia. Memoirs (Rad) of the Yugosl. Acad.<br />
Sci. and Arts, Vol. 159 (36), 39-66, Zagreb (in Croatian).<br />
Kišpatić, M. (1909): Über einige Mineralien aus Bosnien. Tschermak’s Min. Petr. Mitt., Bd.<br />
XXVIII, Heft 3, 297-298, Wien.<br />
Kišpatić, M. (1910): Ein Gabbrovrokommen zwischen Travnik und Bugojno in Bosnien.<br />
Tschermak’s Min. Petr. Mitt., Bd. XXIX, 172-175, Wien.<br />
Kišpatić, M. (1912): Bauxite des kroatischen Karstes und ihre Entstehung. Neues Jahrbuch f.<br />
Mineralogie etc., Beilageband, Bd. XXXIV, 513-522, Stuttgart.<br />
Kišpatić, M. (1915): Neuer Beitrag zur Kentniss der Bauxite des kroatischen Karstes. Journal<br />
of the Croatian Society of Natural History, XXVII, 52-55, Zagreb.<br />
Kišpatić, M. (1917): Angeblicher Serpentin- und Gabbro-Durchbruch in der Nähe von<br />
Kostajnica bei Doboj in Bosnien. Journal of the Croatian Society of Natural History,<br />
XXIX, 33-37, Zagreb.<br />
Koch, F. (1897): Tetrahedrite from Mačkara near Gornji Vakuf in Bosnia. Journal of the<br />
National Museum of Bosnia and Hercegovina, IX, 505-509, Sarajevo (in Bosnian).<br />
Koch, F. (1899): Beryl from Mt. Motajica. Journal of the National Museum of Bosnia and<br />
Hercegovina, vol. XI, 1-12, Sarajevo (in Bosnian).<br />
Koch, F. (1899a): Fahlerz von Mačkara bei Gornji Vakuf. Wiss. Mitt. aus Bosnien und der<br />
Hercegovina, Bd. VI, 880-890, Wien.<br />
Koch, F. (1902): Ein Beryll aus dem Gebirge Motajica planina in Bosnien. Wiss. Mitt. aus<br />
Bosnien und der Hercegovina, Bd. VIII, 427-431, Wien.<br />
Koch, F. (1908): A contribution to the petrography of Mt. Motajica in Bosnia. Journal of the<br />
National Museum of Bosnia and Hercegovina, vol. XX, 1-22, Sarajevo (in Bosnian).<br />
Koechlin, R. (1922): Über einige Mineralien von Ljubija bei Prijedor in Bosnien. Tschermak’s<br />
Min. Petr. Mitt., Bd. 35, Heft 22, 1-12, Wien.<br />
Krenner, J.S. (1884): Auripigment und Realgar aus Bosnien. Földtany Közlöny, XIV, Heft<br />
1-3, 107-110, Budapest.<br />
Kubat, I. (1964): A contribution to the knowledge on copper ores in north-east Bosnia, with<br />
emphasis on structural and tectonic features. Geol. gazette, 10, 171-179, Sarajevo<br />
(in Bosnian).<br />
Kubat, I. (1969): Manganese and iron in the Drina metallogenic province of eastern Bosnia.<br />
Geol. gazette, 13, 243-270, Sarajevo (in Bosnian).<br />
336
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Kunštek, E. (1940): The iron ore deposit at Ljubija. Priroda (Nature), XXX, 133-140, Zagreb<br />
(in Croatian).<br />
Luburić, P. (1963): Occurrence of tuffs and bentonite in freshwater Neogene sediments in<br />
the Livno-Duvno basin in south-west Bosnia. Geol. gazette, 8, 203-211, Sarajevo<br />
(in Bosnian).<br />
Luković, S. (1957): On volcanic tuffs in Neogene-age sediments of the Tuzla area (with<br />
emphasis on similar occurrences in other countries). Annals of the Faculty of Mining<br />
and Geology in Belgrade, 5, 15-18, Belgrade (in Serbian).<br />
Magdalenić, Z. and Šćavničar, B. (1973): Authigenic tourmaline in sedimentary rocks of<br />
northern Dalmatia and south-eastern Bosnia. Geol. gazette, 26/1972, 113-122,<br />
Zagreb (in Croatian).<br />
Majer, V. (1961): Dacitoid rocks from the Blatnica creek near Teslić in Bosnia. Journal of the<br />
Geological and Geophysical Survey, A 29, 235-239, Belgrade (in Serbian).<br />
Majer, V. (1962): Results of investigations in the ‘serpentine zone’ in Bosnia, between the<br />
rivers Vrbas and Bosna. 5th Conference of Geologists of Yugoslavia, II, 109-116,<br />
Belgrade (in Serbian).<br />
Majer, V. (1963): Albite-bearing granite in conglomerates of the diabase-chert series near<br />
Prisoj in Bosnia. Geol. gazette, 15/2 for 1961, 365-368, Zagreb (in Croatian).<br />
Majer, V. and Barić, Lj. (1973): Xonotlite and pectolite from basic rocks of the gabbroperidotite<br />
complex at Mt. Zlatibor, Yugoslavia. Geol. gazette, 25/1971, 197-210,<br />
Zagreb (in Croatian).<br />
Majer, V. and Jurković, I. (1957): Petrological characteristics of the diorite of Bijela Gromila<br />
south of Travnik (Bosnia). II Congress of Yugoslav Geologists, 263-270, Sarajevo.<br />
Majer, V. and Jurković, I. (1958): The diorite of Bijela Gromila south of Travnik in the schist<br />
mountains of central Bosnia. Geol. gazette, 11, 129-142, Zagreb (in Croatian).<br />
Majer, V. and Pamić, J. (1974): Metamorphosed graywackes and shales on the NW border of<br />
the Borje ultramafic massif in Bosnia (Yugoslavia). Bull. Sci. Cons. Acad. Yugosl.,<br />
A 19, No. 11-12, 334-335, Zagreb.<br />
Maksimović, Z. (1968): Distribution of trace elements in bauxite deposits of Herzegowina,<br />
Yugoslavia. Travaux du Comite International etc., Academie Yougoslave, 5, 63-70,<br />
Zagreb.<br />
Maksimović, Z. and Antić, R. (1962): Mineralogical and chemical composition of of the<br />
weathering core relicts of the ultrabasic rocks in the Vardište area near Višegrad<br />
(eastern Bosnia). Geol. gazette, 6, 157-179, Sarajevo (in Bosnian).<br />
Maksimović, Z. and Crnković, B. (1968): Halloysite and kaolinite formed through alteration<br />
of ultramafic rocks. Proceedings of the XIII International Geological Congress, Vol.<br />
14, 95-105.<br />
Marić, L. (1927): The gabbro massif near Jablanica. Gazette of the Geological Survey in<br />
Zagreb, II, 1-65, Zagreb (in Croatian).<br />
Marić, L. (1953): Mišo Kišpatić in the light of modern petrography and petrology. Memorial<br />
volume of Mišo Kišpatić, Yugoslav Academy of Sciences and Arts, 9-33, Zagreb (in<br />
Croatian).<br />
Marić, L. (1954): Magmatismus und Alkalimetasomatose im jugoslawischen Raum. Neues<br />
Jahrbuch f. Mineralogie Abhandl., 87/1, 1-32, Stuttgart.<br />
Marić, L. (1965): Terra rossa in the karst of Yugoslavia. Acta Geologica IV, 19-72, Yugoslav<br />
Acad. Sci. Arts, Zagreb (in Croatian).<br />
Marić, L. (1969): The contribution of geological science to the post-war development of our<br />
country. Mining, geology and metallurgy, XX/1, 67-73, Belgrade (in Serbian).<br />
337
SILICATES<br />
Marić, L. (1974): Minerals, rocks and ore deposits of our country – from ancient history to<br />
contemporary time. Yugoslav Acad. Sci. Arts, Zagreb (in Croatian).<br />
Marić, L. and Crnković, B. (1961): Sedimentary rocks of Paleozoic age of the Sana area – the<br />
Ljubija ore province. Geol. gazette, 14, 143-158, Zagreb (in Croatian).<br />
Markov, C. and Mihailović-Vlajić, N. (1969): General observations on accessory minerals<br />
in the granitoid rocks of Yugoslavia. Ann. Inst. Geol. Mining and Nucl. Mat. Min.<br />
Resources, 6, 249-278, Belgrade (in Serbian).<br />
Marković, B. and Takač, L. (1958): The origin of amphibolites in the massif of Mt. Zlatibor<br />
and their importance for the tectonics of this area. Annals of the Geological Institute<br />
‘Jovan Žujović’, 10, 105-118, Belgrade (in Serbian).<br />
Mihailović-Vlajić, N. (1967): Accessory minerals in granites of Mt. Motajica. Ann. Inst.<br />
Geol. Mining and Nucl. Mat. Min. Resources, 3, 191-209, Belgrade (in Serbian).<br />
Mikinčić, V. (1955): Beryl. Yugoslav Encyclopedia, 1, 480, Zagreb (in Croatian).<br />
Miladinović, D. (1969): Fundamental economic and geological features of the magnesitebearing<br />
rocks in the central part of the Bosnian ophiolite zone. Geol. gazette, 13,<br />
293-300, Sarajevo (in Bosnian).<br />
Milenković, D. (1966): Detailed geomagnetic investigations of the magnetite occurrences at<br />
Tovarnica near Jablanica on the Neretva river. Geol. gazette, 11, 157-179, Sarajevo<br />
(in Bosnian).<br />
Milojković, M. (1929): The stratigraphy of geological formations in Bosnia and Hercegovina.<br />
Editions of the Geological Survey in Sarajevo, II, 1-231, Sarajevo (in Bosnian).<br />
Mitrović, M. (1955): Chrysotile asbestos at Bosansko Petrovo Selo. Geol. gazette, 1, 199-<br />
213, Sarajevo (in Bosnian).<br />
Mitrović, M. (1958): Response to the discussion ‘On the paper about chrysotile asbestos at<br />
Bosansko Petrovo Selo’ (by Karamata and Petković, 1957). Geol. gazette, 4, 321-<br />
323, Sarajevo (in Bosnian).<br />
Mojsisovics, E., Tietze, E. und Bittner, A. (1880): Grundlinien der Geologie von Bosnien-<br />
Hercegovina. Alfred Hölder K.u.K. Hof- und Universitätsbuchhändler, Wien.<br />
Mudrenović, V. and Gaković, J. (1964): Contribution to the knowledge on the stratigraphy<br />
of the lower and upper Triassic in the area of Zalomska river (eastern Hercegovina).<br />
Geol. gazette, 10, 139-157, Sarajevo (in Bosnian).<br />
Mudrinić, Č. and Janjić, S. (1969): The mineralogy of the Vlasenica bauxite deposit. Mining<br />
and Technology Archive, VII/1, 3-7, Tuzla (in Bosnian).<br />
Mudrinić, Č. and Tadić, J. (1969): Rare-element distribution in the Vlasenica bauxite deposit.<br />
Geol. gazette, 13, 235-242, Sarajevo (in Bosnian).<br />
Muftić, M. and Čičić, S. (1969): Results of geological explorations in Bosnia and Hercegovina<br />
1964-1968 and lines of research for the future. Geol. gazette, 13, 5-25, Sarajevo (in<br />
Bosnian).<br />
Nikolić, D. (1962): The beryls of Yugoslavia. 5th Conference of Geologists of Yugoslavia, II,<br />
11-12, Belgrade (in Serbian).<br />
Nikolić, R.D. (1963): The pegmatites of FNR Yugoslavia. Unpublished PhD thesis. Belgrade<br />
(in Serbian).<br />
Nikolić, D., Živanović, M. and Zarić, P. (1971): Bentonites from Šipovo near Jajce (Bosnia).<br />
Journal of the Museum of Natural History in Belgrade, A 26, 103-116, Belgrade (in<br />
Serbian).<br />
Nöth, L. (1956): Über den heutigen Stand unserer Kentnisse der Eisenerzlagerstätten<br />
Jugoslawiens. 1st Yugoslav Geological Congress, 219-230, Ljubljana.<br />
338
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Olujić, J., Vuletić, N. and Pamić, J. (1971): Preliminary data on titanium abundances in the<br />
ophiolitic zone in Bosnia. Geol. gazette., 15, 99-107, Sarajevo (in Bosnian).<br />
Pamić, J. (1957): The petrology of effusive rocks in the Ilidža-Kalinovik area (Bosnia). I. The<br />
area of Mt. Igman and the north-eastern flanks of Mt. Bjelašnica. Geol. gazette, 3,<br />
171-180, Sarajevo (in Bosnian).<br />
Pamić, J. (1960): Contact metamorphism in Triassic sediments south of Prozor (Bosnia and<br />
Hercegovina). Geol. gazette, 13/1959, 197-212, Zagreb (in Croatian).<br />
Pamić, J. (1960a): Basic characteristics of Triassic igneous rocks in the Kalinovik area.<br />
Symposium on the problems of Alpine-type initial magmatism. Ref 7b, 1-10, Ilidža-<br />
Vareš (in Bosnian).<br />
Pamić, J. (1961): Results of microscopic and chemical investigations of the granites from Mt.<br />
Prenj in Hercegovina. Geol. gazette, 5, 263-269, Sarajevo (in Bosnian).<br />
Pamić, J. (1961a): The characteristics of igneous rocks of the diabase-chert series at Jablanica<br />
and Prozor (Bosnia and Hercegovina). III Congress of Yugoslav Geologists, 363-<br />
382, Titograd (in Croatian).<br />
Pamić, J. (1961b): The spilite-keratophyre association at Jablanica and Prozor. Acta Geologica<br />
III, Yugosl. Acad. Sci. Arts, 5-94, Zagreb (in Croatian).<br />
Pamić, J. (1962): The petrology of effusive rocks in the Ilidža-Kalinovik area (Bosnia). II. The<br />
source area of the river Željeznica. Geol. gazette, 6, 45-60, Sarajevo (in Bosnian).<br />
Pamić, J. (1963): Triassic-age igneous rocks at Čevljanovići and a short account on the<br />
Triassic volcanic events of the Borovica-Vareš zone. Geol. gazette, 7, 9-20, Sarajevo<br />
(in Bosnian).<br />
Pamić, (1963a): On the problem of volcanogenic-sedimentary formations in the Dinarides<br />
and Bosnia-Hercegovina. Geol. gazette, 8, 5-27, Sarajevo (in Bosnian).<br />
Pamić, J. (1969): The Mid-Triassic spilite-keratophyre series in the Dinarides and its<br />
placement within the Alpine magmatic-tectonic cycle. Geol. gazette, 13, 205-216,<br />
Sarajevo (in Bosnian).<br />
Pamić, J. (1969a): The ultramafic-amphibolitic series of Mt. Skatavica in the ophiolite<br />
zone of the Dinarides (Bosnia). Journal of the National Museum of Bosnia and<br />
Hercegovina, new series vol. VIII, 35-46, Sarajevo (in Bosnian).<br />
Pamić, J. (1969b): High-temperature feldspars from the Middletriassic spilite-keratophyre<br />
association of the Dinarides. Bull. Sci. Cons. Acad. Yugosl. A/14, No. 1-2, Zagreb.<br />
Pamić, J. (1970): Basic petrological characteristics of the chromite-bearing area of Duboštica<br />
in Bosnia. Geol. gazette, 14, 135-148, Sarajevo (in Bosnian).<br />
Pamić, J. (1970a): Syenite and granite rocks associated with talc deposit on Ozren ultramafic<br />
massif. Bull. Sci. Cons. Acad. Yougosl., A15, No. 9-10, 515, Zagreb.<br />
Pamić, J. (1971): Some petrological features of Bosnian peridotite-gabbro complexes in the<br />
Dinaride zone of Yugoslavia. Tschermak’s Min. Petr. Mitt., 15, 14-42.<br />
Pamić, J. (1971a): Amphibolites associated with the large Krivaja-Konjuh ultramafic massif<br />
(Yugoslavia). Bull. Sci. Cons. Acad. Yugosl. A/16, No. 1-2, Zagreb.<br />
Pamić, J. (1971b): Corundum-bearing amphibolites from the southern edge of the Krivaja-<br />
Konjuh ultramafic massif. Geological Annals of the Balkan Peninsula, 35, 399-408,<br />
Belgrade (in Croatian).<br />
Pamić, J. (1972): Stuctural and textural characteristics of Bosnian peridotites as a background<br />
for discussions about their origin. Proceedings of the VII Congress of Yugoslav<br />
Geologists, Vol. II, 271-296, Zagreb (in Croatian).<br />
339
SILICATES<br />
Pamić, J. (1972a): Metamorphic grade of the Jurassic magmatic-sedimentary ‘Diabasehornstein’<br />
formation of the Dinaridic ophiolitic zone (Yugoslavia). Bull. Sci. Cons.<br />
Acad. Yugosl. A/17, No. 5-6, Zagreb.<br />
Pamić, J. (1972b): The spilite-keratophyre series in the Dinarides contains albite whose<br />
optical constants – based on available microscopic measurements on a rotating stage<br />
– indeed show a tendency towards high-temperature optics. Proceedings of the VII<br />
Congress of Yugoslav Geologists, Vol. II, 43-58, Zagreb (in Croatian).<br />
Pamić, J. (1972c): The ultramafic-amphibolite mass of the Skatavica in the ophiolite zone of<br />
the Dinarides. Journal of the National Museum of Bosnia and Hercegovina, new<br />
series vol. 11, 39-47, Sarajevo.<br />
Pamić, J. (1972d): A new contribution to the knowledge of igneous rocksin the Rudo area (SE<br />
Bosnia). Geol. gazette, 16, 123-132, Sarajevo (in Bosnian).<br />
Pamić, J. (1973): Amphibole peridotite (cortlandite) from the Vijenac amphibolite-ultramafic<br />
mass in the ophiolite zone of Bosnia, Yugoslavia. Bull. Sci. Cons. Acad. Yugosl.<br />
A/18, No. 4-6, Zagreb.<br />
Pamić, J. (1974): Alpine-type gabbros within the Krivaja-Konjuh massif in the ophiolite zone<br />
of the Dinarides, Yugoslavia. Tschermak’s Min. Petr. Mitt., 21, 261-279.<br />
Pamić, J.(1974a): Middle Triassic spilite-keratophyre association of the Dinarides and its<br />
position in the Alpine magmatic-tectonic cycle. Spilites and spilitic rocks, 161-174,<br />
edited by G. C. Amstutz, Springer Verlag, Berlin – Heidelberg – New York.<br />
Pamić, J. and Antić, R. (1964): Enclaves of peridotitic rocks in the gabbroid complex of the<br />
Gostovička Rijeka near Zavidovići (Bosnia). Geol. gazette, 9, 5-12, Sarajevo (in<br />
Bosnian).<br />
Pamić, J. and Antić, R. (1968): Serpentine-websterite with magnesian spinel from Mt. Čavka<br />
in Bosnia. Geol. gazette, 12, 139-144, Sarajevo (in Bosnian).<br />
Pamić, J. and Buzaljko, R. (1966): Mid-Triassic spilites and keratophyres in the Čajniče area<br />
(south-easter Bosnia). Geol. gazette, 11, 55-78, Sarajevo (in Bosnian).<br />
Pamić, J., Dimitrov, P. and Zec, F. (1964): Geological characteristics of dacito-andesites in<br />
the Bosna river valley. Geol. gazette, 10, 241-250, Sarajevo (in Bosnian).<br />
Pamić, J. and Đorđević, D. (1974): On the problem of acidic and intermediary intrusive rocks<br />
in the Bosnian serpentine zone. III Symposium of Dinaric Associations, 2, 127-140,<br />
Zagreb (in Croatian).<br />
Pamić, J. and Jurić, M. (1962): Development of Triassic formations south of Jajce. Geol.<br />
gazette, 6, 107-110, Sarajevo (in Bosnian).<br />
Pamić, J. and Kapeler, I. (1969): The gabbro-doleritic series of the Kozarački Potok in<br />
the Prijedor area. Acta Geologica, VI, 27-44, Yugosl. Acad. Sci. Arts, Zagreb (in<br />
Croatian).<br />
Pamić, J. and Kapeler, I. (1970): Corundum-bearing amphibolites from the southern edge of<br />
the ultramafic Krivaja-Konjuh complex. Geological Annals of the Balkan Peninsula,<br />
35, 399-408, Belgrade (in Croatian).<br />
Pamić, J. and Maksimović, V. (1968): Mid-Triassic quartz-albite-diabases in Skythage<br />
sediments from Bijela near Konjic. Geol. gazette, 12, 131-137, Sarajevo (in<br />
Bosnian).<br />
Pamić, J. and Olujić, J. (1969): Albite-bearing granites from Gostilje near the asbestos deposits<br />
of Bosansko Petrovo Selo. Geol. gazette, 13, 199-204, Sarajevo (in Bosnian).<br />
Pamić, J. and Olujić, J. (1974): Hydrothermal-metasomatic rocks (listvenites) from the<br />
northern border of the Ozren ultramafic massif (Yugoslavia). Acta Geologica 7/6,<br />
239-255, Yugosl. Acad. Sci. Arts, Zagreb.<br />
340
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Pamić, J. and Papeš, J. (1969): Products of Ladinian volcanism in the broader area of<br />
Kupreško Polje. Geological Annals of the Balkan Peninsula, 34, 555-576, Belgrade<br />
(in Croatian).<br />
Pamić, J., Šćavničar, S. and Međimorec, S. (1973): Mineral assemblages of amphibolites<br />
associated with Alpine-type ultramafics in the Dinaride ophiolite zone (Yugoslavia).<br />
Journal of Petrology, 14/1, 133-157, Oxford.<br />
Pamić, J. and Tojerkauf, E. (1970): Occurrence of granite at the edge of the Mt. Borja<br />
ultramafic complex. Geol. gazette, 14, 149-153, Sarajevo (in Bosnian).<br />
Pamić, J. and Trubelja, F. (1962): Basic geological and petrological features of Mt. Ozren<br />
in north-eastern Bosnia. 5th Conference of Geologists of Yugoslavia, II, 117-123,<br />
Belgrade (in Serbian).<br />
Panić, B. and Ristić, P. (1972): Sepiolites from Mt. Konjuh. Mining and Technology Archive,<br />
X/2-3, 39-43, Tuzla (in Bosnian).<br />
Papeš, J., Trubelja, F. and Slišković, T. (1973): Effet de la repartition terre/mer sur la formation<br />
des gisements de bauxite en Bosnie-Herzegovine (Yougoslavie). ICSOBA 3eme<br />
Congres International, 175-183, Nice.<br />
Paul, K.M. (1872): Geologische Notiz aus Bosnien. Verhandlungen der Geol. Reichsanstalt,<br />
16, 326-329, Wien.<br />
Paul, C.M. (1879): Beiträge zur Geologie des nördlichen Bosnien. Jahrbuch der K.K. Geol.<br />
Reichsanstalt, XXIX, Heft 4, 759-778, Wien.<br />
Paul, C.M. (1879a): Aus der Umgebung von Doboj und Maglaj. Verhandlungen der Geol.<br />
Reichsanstalt, 23, 205-208, Wien.<br />
Pavlović, F. (1975): Analysis of the phase composition of clays from Prijedor and their<br />
physico-chemical characteristics. MSc thesis (unpublished), 1-81, Sarajevo (in<br />
Bosnian).<br />
Pavlović, P.S. (1889): Comments on the paper by B.Walter: ‘Beitrag zur Kentniss<br />
der Erzlagerstätten Bosniens’ – published in 1887 in Sarajevo. Geological Annals<br />
of the Balkan Peninsula, I, 206-224, Belgrade (in Serbian).<br />
Pavlović, P.S. (1890): Comments on the paper by F. Poech: ‘Über den Manganerzbergbau<br />
von Čevljanović in Bosnien’ – published 1888 in Österr. Ztschrift. f. Berg- und<br />
Hüttenwesen, 20 und 21, Geological Annals of the Balkan Peninsula, II, 196-198,<br />
Belgrade (in Serbian).<br />
Pavlović, P.S. (1891): Comments on the paper by V. Radimsky: ‘Serpentines of Bosnia and<br />
their inclusions, especially sepiolite’. Geological Annals of the Balkan Peninsula,<br />
III, 355-356, Belgrade (in Serbian).<br />
Pavlović, S. (1953): Manganese in Yugoslavia and around the world. First Conference of<br />
Yugoslav Geologists, 65-109, Zagreb (in Croatian).<br />
Pavlović, S. (1962): The mineralogy and petrography of ore and rocks of Fe and Mn deposits<br />
in Bosnia and Hercegovina. Unpublished report of the Geological Survey in<br />
Sarajevo, Belgrade (in Serbian).<br />
Pavlović, S. (1963): The mineralogy and petrography of ore and rocks of Fe and Mn deposits<br />
in Bosnia and Hercegovina. Unpublished report of the Geological Survey in<br />
Sarajevo, Belgrade (in Serbian).<br />
Pavlović, S. (1964: The mineralogy and petrography of ore and rocks of Fe and Mn deposits in<br />
Bosnia and Hercegovina. Unpublished report of the Geological Survey in Sarajevo,<br />
Belgrade (in Serbian).<br />
341
SILICATES<br />
Pavlović, S. and Milojković, R. (1958): Crocidolite asbestos from Halilovac in Bosnia.<br />
Memoirs of the Serbian Academy of Sciences and Arts, 235/17, 19-25, Belgrade<br />
(in Serbian).<br />
Pavlović, S., Ristić, P. and Likić, J. (1970): The quartz sands of the Tuzla basin (‘Miladije’<br />
and ‘Bukinje’ deposits) as a raw material for the production of gas-concrete. Geol.<br />
gazette, 14, 217-236, Sarajevo (in Bosnian).<br />
Pavlović, S., Nikolić, D., Babić, D. and Poharc, V. (1976): Investigations on dickite from the<br />
Vlasenica bauxite. Presentation at the IV Yugoslav Symposium on the prospecting<br />
and exploitation of bauxite, 11-15.10.1976, Herceg Novi (in Serbian).<br />
Pavlovich, M.S. (1937): Les roches eruptives de Zlatibor (Yougoslavie) et leurs relations<br />
avec les formations cristallophylliennes et sedimentaires environnantes. Bull. Soc.<br />
Franc. de Mineralogie, 60/1-3, 5-137, Paris.<br />
Petković, M. (1961/62): The Triassic-age metallogenic area of Vareš. Annals of the Faculty<br />
of Mining and Geology in Belgrade, 8, 153-175, Belgrade (in Serbian).<br />
Petrović, J. (1957): Mineralogical investigations of alluvial deposits at Mt. Motajica. Library<br />
of documents, Inst. Geol. Mining and Nucl. Mat. Min. Resources, Belgrade (in<br />
Serbian).<br />
Pilar, Gj. (1882): Geological observations in western Bosnia in 1879. Memoirs (Rad) Yugosl.<br />
Acad. Sci. Arts, 61, 1-68, Zagreb (in Croatian).<br />
Podubsky, V. (1955): A preliminary report on the investigation of argillaceous schists and<br />
kaolinite-montmorillonite clays from some deposits in Bosnia and Hercegovina.<br />
Geol. gazette, 1, 33-41, Sarajevo (in Bosnian).<br />
Podubsky, V. (1968): The lithostratigraphy of Paleozoic formations in north-western Bosnia.<br />
Geol. gazette, 12, 165-200, Sarajevo (in Bosnian).<br />
Podubsky, V. (1970): Petrographic characteristics of Paleozoic formations in eastern Bosnia.<br />
Geol. gazette, 14, 155-180, Sarajevo (in Bosnian).<br />
Podubsky, V. and Pamić, J. (1969): Igneous rocks in the Paleozoicum of the Sana river area<br />
and their position in the geological sequence. Acta Geologica, 6, 45-54, Yugosl.<br />
Acad. Sci. Arts, Zagreb (in Croatian).<br />
Poech, F. (1888): Über den Manganerzbergbau von Čevljanović in Bosnien. Österr. Ztschrift.<br />
f. Berg- und Hüttenwesen, 36, No. 20 (253-255) und No. 21 (267-268), Wien.<br />
Poech, F. (1900): L’ industrie minerale de Bosnie-Hercegovine. 56 p. avec 1 carte geologique<br />
et 10 gravures en texte, Vienne.<br />
Pogatschnig, L. (1890): Ancient ore mines in Bosnia. Journal of the National Museum of<br />
Bosnia and Hercegovina, vol. II, 125-130, Sarajevo (in Bosnian).<br />
Polić, A. (1938): Occurrences of magnesite at Dubnica near Višegrad. Journal of the National<br />
Museum of Bosnia and Hercegovina, vol. L/2, 37-47, Sarajevo (in Bosnian).<br />
Polić, A. (1940): Occurrence of manganese ore at Mt. Ozren near Sarajevo. Journal of<br />
the National Museum of Bosnia and Hercegovina, vol. LII/2, 5-12, Sarajevo (in<br />
Bosnian).<br />
Polić, A. (1951): On the exploration of ore bodies in the schist mountains of central Bosnia.<br />
Geol. gazette, 9, 343-348, Belgrade (in Serbian).<br />
Popović, Ž. (1930): On the copper ore deposit at Sinjakovo (Bosnia). Mining and Metallurgy<br />
gazette, II/5, 214-217, Belgrade (in Serbian).<br />
Potier, R. (1879): Die Produktions-Verhältnisse in Bosnien und der Hercegovina, 1-58, Wien.<br />
Primics, G. (1881): Zur petrographischen Kenntniss von Bosnien. Földtany Közlöny, 11,<br />
195-199, Budapest.<br />
342
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Radimsky, V. (1889): The serpentines of Bosnia and Hercegovina and their inclusions,<br />
especially sepiolite. Journal of the National Museum of Bosnia and Hercegovina,<br />
vol. I, 88-92, Sarajevo (in Bosnian).<br />
Ramović, M. (1957): Review of the deposits of Zn and Pb minerals in Bosnia and Hercegovina.<br />
Geol. gazette, 3, 9-123, Sarajevo (in Bosnian).<br />
Ramović, M. (1957a): Deposits of mineral resources of Bosnia and Hercegovina. II Congress<br />
of Yugoslav Geologists, 84-91, Sarajevo (in Bosnian).<br />
Ramović, M. (1961): The forms, distribution, structures and textures of ore veins at<br />
Srebrenica. Geol. gazette, 5, 163-197, Sarajevo (in Bosnian).<br />
Ramović, M. (1962): Plagioclase diagrams in igneous rocks of Srebrenica. Geol. gazette, 6,<br />
31-42, Sarajevo (in Bosnian).<br />
Ramović, M. (1963): The ore parageneses in the Srebrenica area (eastern Bosnia). Geol.<br />
gazette, special editions, Vol. 1, 1-96, Sarajevo (in Bosnian).<br />
Ramović, M. (1966): Jurassic-Cretaceous-Paleogene metallogenic zones and belts. Geol.<br />
gazette, 11, 103-129, Sarajevo (in Bosnian).<br />
Ramović, M. (1968): Principles of Metallogeny. Geographical Institute of the Natural Science<br />
Faculty, University of Sarajevo (in Bosnian).<br />
Ramović, M. and Kulenović, E. (1964): New results of exploration activities and geological<br />
investigations of the mercury ore deposit at Draževići near Čevljanovići and the<br />
polymetallic deposit at borovica near Vareš. Geol. gazette, 10, 181-196, Sarajevo<br />
(in Bosnian).<br />
Ristić, P., Likić, J. and Stanišić, N. (1968): Sedimnetological investigations of the Tuzla<br />
basin. Mining and Technology Archive, VI/3, 3-24, Tuzla (in Bosnian).<br />
Ristić, P., Panić, B. and Janjić, S. (1965): The magnesites from Mt. Konjuh. Mining and<br />
Technology Archive, III/2-3, 63-70, Tuzla (in Bosnian).<br />
Ristić, P., Panić, B., Mudrinić, Č. and Likić, J. (1967): The volcanism and geochemistry of<br />
Mt. Konjuh. Mining and Technology Archive, V/3-4, 3-16, Tuzla (in Bosnian).<br />
Ristić, S., Antić-Jovanović, A. and Jeremić, M. (1965): The content of alkali metals in some beryls<br />
with a general overview of the spectrochemistry and geochemistry of this mineral. I<br />
Symposium on Geochemistry, 18-20 January, 409-429, Belgrade (in Serbian).<br />
Ritter, H. (1878): Das Kohlenvorkommen von Dolni Tuzla in Bosnien. Verhandlungen der<br />
Geol. Reichsanstalt, 17, 375-377, Wien.<br />
Roskiewicz, J. (1868): Studien über Bosnien und die Hercegovina. Wien – Lepzig.<br />
Roy, N.N. (1965): The mineralogy of the potassium-barium feldspar series. I. The<br />
determination of the optical properties of natural members. Min. Magazine, 35, No.<br />
271, 508-518.<br />
Rücker, A. (1893): Über die bosnischen Salinen. Österr. Ztschrift. f. Berg- und Hüttenwesen,<br />
LIX, No. 20, 249-254, Wien.<br />
Rücker, A. (1893): Einiges über das Goldvorkommen in Bosnien. Monographische Skizze,<br />
1-101, Wien.<br />
Rzehak, A. (1879): Mitteilungen über die geognostischen Verhältnisse auf der Route Brod-<br />
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Sakač, K. (1969): On the stratigraphy, tectonics and bauxites of Mt. Grmeč in western Bosnia.<br />
Geol. gazette, 22/1968, 269-302, Zagreb (in Croatian).<br />
Schafarzik, F. (1879): Diabas von Doboj in Bosnien. Földtany Közlöny, 9, 439-442, Budapest.<br />
343
SILICATES<br />
Schiller, J. (1905): Über den Gabbro aus dem Flysch bei Višegrad in Bosnien und die<br />
Verteilung von Fe und Mg in Olivin- und rhombischen Pyroxen-enthaltenden<br />
Gesteinen. Tschermak’s Min. Petr. Mitt., Bd. XXIV, 309-320, Wien.<br />
Sendtner, O. (1848): Reise nach Bosnien. Das Ausland, 82-479.<br />
Sijarić, G. (1975): Bauxites of north-western Bosnia. Journal of the National Museum of<br />
Bosnia and Hercegovina, new series vol. 14, 11-126, Sarajevo (in Bosnian).<br />
Sijarić, G. and Šćavničar, S. (1972): Investigations of serpentine minerals from the magnesite<br />
mine Miljevica near Kladanj. Proceedings of the VII Congress of Yugoslav<br />
Geological Societies, II, 319-334, Zagreb (in Croatian).<br />
Sijarić, G. and Trubelja, F. (1974): Quantitative X-ray powder diffraction analysis of<br />
bauxites from Srnetica mountain in west Bosnia. Report of the Yugoslav Center for<br />
Crystallography, 9/1974, 72, Yugosl. Acad. Sci. Arts, Zagreb.<br />
Sijarić, G. and Trubelja. F. (1974a): Quantitative X-ray powder diffraction analysis of<br />
bauxites from Srnetica mountain in west Bosnia. Journal of the National Museum<br />
of Bosnia and Hercegovina, new series vol. 13, 13-22, Sarajevo (in Bosnian).<br />
Sijarić, G., Trubelja, F. and Šćavničar, S. (1976): Diaspore bauxites of the Grmeč mountain<br />
(Bosnia). Travaux du Comite international pour l’etude des bauxites, de l’alumine<br />
et d’aluminium (ICSOBA), No. 13, 115-124, Academie Yougoslave des Sciences et<br />
des Arts, Zagreb.<br />
Sijerčić, Z. (1972): Sedimentological and petrographical characteristics of the first horizon<br />
of Eocene ‘flysch’ from the western flanks of Mt. Majevica. Geol. gazette, 16, 103-<br />
121, Sarajevo (in Bosnian).<br />
Sijerčić, Z. (1972a): Igneous rocks of the diabase-chert series of Mt. Kozara (north-western<br />
Bosnia). Geol. gazette, 16, 145-155, Sarajevo (in Bosnian).<br />
Sijerčić, Z., Pamić, J., Jovanović, Č. and Šljukić, M. (1974): Analcimolites in the Tuzla salt<br />
series (Bosnia). Bull. Sci. Cons. Acad. Yougoslavie, A19, 5-6, Zagreb.<br />
Simić, M. (1964): Basic igneous rocks in the area of the Rača creek north of Sarajevo. Geol.<br />
gazette, 10, 251-263, Sarajevo (in Bosnian).<br />
Simić, M. (1966): Petrology of basic effusive rocks from Babin Dol and Durmiševica on Mt.<br />
Bjelašnica. Geol. gazette, 11, 371-388, Sarajevo (in Bosnian).<br />
Simić, M. (1968): Petrography of basic potassium-rich effusive rocks from Presjenička<br />
Rijeka and Željeznica (Bosnia). First Symposium on the Geology of Dinarides, I,<br />
187-194, Ljubljana (in Serbian).<br />
Simić, M. (1972): Mineral facies in Triassic clastic rocks from the wider area of Sarajevo.<br />
Proceedings of the VII Congress of Yugoslav Geological Societies, II, 335-344,<br />
Zagreb (in Croatian).<br />
Simić, V. (1956): Occurrence of ore at Crni Potok near Busovača in Bosnia. Journal of the<br />
Museum of Natural History in Belgrade, A 7, 97-104, Belgrade (in Serbian).<br />
Soklić, I. (1957): The Cenozoicum of Bosnia and Hercegovina. II Congress of Yugoslav<br />
Geologists, 64-72, Sarajevo (in Bosnian).<br />
Stangačilović, D. (1956): Primary kaoline from Mt. Motajica. Journal of the Museum of<br />
Natural History in Belgrade, A 7, 1-11, Belgrade (in Serbian).<br />
Stangačilović, D. (1956a): Tertiary-age clays from Kobiljača (Bosnia) – Bravesite, a mixture<br />
of illite and meta-hallyosite. Journal of the Museum of Natural History in Belgrade,<br />
A 7, 21-30, Belgrade (in Serbian).<br />
Stangačilović, D. (1969): Genetic and stratigraphic classification of the deposits of illite clays<br />
in Yugoslavia with emphasis on their mineralogy. Memoirs (Rad) of the Yugosl.<br />
Acad. Sci. Arts, 6, 161-174, Zagreb (in Croatian).<br />
344
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Stangačilović, D. (1970): Properties of yugoslav illite clays. Journal of the Museum of<br />
Natural History in Belgrade, A 25, 189-207, Belgrade (in Serbian).<br />
Sterneck, H, (1877): Geographische Verhältnisse, Communicationen und das Reisen in<br />
Bosnien, der Hercegovina und Nord-Montenegro, 1-56, Wien.<br />
Stevanović, S. (1903): Comments on the paper ‘Sepiolite from Mt. Ljubić near Prnjavor’ –<br />
published 1893 in the Journal of the National Museum of Bosnia and Hercegovina,<br />
vol. 5, 99-105. Geological Annals of the Balkan Peninsula, VI/1, 346-347, Belgrade<br />
(in Serbian).<br />
Stojanović, D. (1973): X-ray powder pattern for suolunite from Kulashi, Bosnia, Yugoslavia.<br />
Report of the Yugoslav Center for Crystallography, 8/1973, 58-60, Yugosl. Acad.<br />
Sci. Arts, Zagreb.<br />
Stojanović, D., Đorđević, D. and Đerković, B. (1974): Suolunite and tobermorite in diabase<br />
rocks from Kulaš near Doboj, Bosnia, Yugoslavia. Journal of the Museum of Natural<br />
History in Belgrade, A 29, 5-15, Belgrade (in Serbian).<br />
Sunarić, O. and Olujić, J. (1968): Basic geological features of the chromite deposit of<br />
Duboštica. Geol. gazette, 12, 261-271, Sarajevo (in Bosnian).<br />
Šćavničar, B. and Jović, P. (1961): Differentiation of Pliocene sands of the Kreka coal basin<br />
on the basis of heavy mineral analysis. Bull. Sci. Cons. Acad. Yougoslavie, 6/2, 36,<br />
Zagreb.<br />
Šćavničar, B. and Jović, P. (1962): Differentiation of Pliocene sands of the Kreka coal basin<br />
on the basis of heavy mineral analysis. Geol. gazette, 15/1961, 53-74, Zagreb (in<br />
Croatian).<br />
Šćavničar, S. (1965): Serpentine from Bosansko Petrovo Selo. Acta Geologica, 4, 251-264,<br />
Yugosl. Acad. Sci. Arts, Zagreb (in Croatian).<br />
Šćavničar, S. and Trubelja, F. (1969): The talc-serpentine-chlorite vein from Kupres in the<br />
schist mountains of central Bosnia. Geol. gazette, 22, 445-467, Zagreb (in Croatian).<br />
Šćavničar, S., Trubelja, F. and Sijarić-Pleho, G. (1969): Mineralogical and chemical<br />
properties of hercegovinian bauxites. Travaux du Comite international pour l’etude<br />
des bauxites, de l’alumine et d’aluminium (ICSOBA), No. 5, 45-62, Academie<br />
Yougoslave des Sciences et des Arts, Zagreb.<br />
Šibenik-Studen, M. (1972/73): Scolezite from the Ribnica creek near Višegrad. Journal of<br />
the National Museum of Bosnia and Hercegovina, new series vol. 11-12, 33-41,<br />
Sarajevo (in Bosnian).<br />
Šibenik-Studen, M. (1974): Stilbite from the Ribnica creek near Višegrad. Journal of the<br />
National Museum of Bosnia and Hercegovina, new series vol. 13, 53-60, Sarajevo<br />
(in Bosnian).<br />
Šibenik-Studen, M. and Trubelja, F. (1967): A new contribution to the knowledge on the<br />
volcanism of the river Vrbas valley. Journal of the National Museum of Bosnia and<br />
Hercegovina, new series vol. 6, 5-13, Sarajevo (in Bosnian).<br />
Šibenik-Studen, M. and Trubelja, F. (1971): An occurrence of thomsonite and prehnite<br />
from the village of Kovačići on the eastern flanks of Mt. Konjuh. Journal of the<br />
National Museum of Bosnia and Hercegovina, new series vol. 10, 29-38, Sarajevo<br />
(in Bosnian).<br />
Šibenik-Studen, M., Sijarić, G. and Trubelja, F. (1976): Project on the mineralogy of Bosnia<br />
and Hercegovina – Vol. 2: Results of laboratory investigations. Report to the<br />
Republican Fund for Science, Sarajevo (in Bosnian).<br />
Šinkovec, B. and Babić, V. (1973): Chemical and mineralogical composition of Cretaceous claybearing<br />
bauxites from Mt. Grmeč. Geol. gazette, 25/1971, 245-253, Zagreb (in Croatian).<br />
345
SILICATES<br />
Tajder, M. (1936): Sphalerite from Ljubija near Prijedor. Memoirs (Rad) of the Yugosl. Acad.<br />
Sci. and Arts, Vol. 254, 229-232, Zagreb (in Croatian).<br />
Tajder, M. (1951/53): Biotite-bearing dacites from Sasa near Srebrenica in Bosnia. Geol.<br />
gazette, 5-7, 63-72, Zagreb (in Croatian).<br />
Tajder, M. (1953): Petrography of the Srebrenica ore province in Bosnia. Memorial volume<br />
of Mišo Kišpatić, Yugoslav Academy of Sciences and Arts, 119-173, Zagreb (in<br />
Croatian).<br />
Tajder, M. (1960): Dacite from Potočari near Srebrenica. Geol. gazette, 12/1959, 145-148,<br />
Zagreb (in Croatian).<br />
Tajder, M. and Herak, M. (1972): Petrology and geology. Školska knjiga, Zagreb (in Croatian).<br />
Tajder, M. and Raffaelli, P. (1967): Metamorphosed porphyre-keratophyres in the schist<br />
mountains of central Bosnia. Geol. gazette, 20, 153-170, Zagreb (in Croatian).<br />
Tasić, Ž. (1975): Investigations on some clays from the basins of Prijedor and Sarajevo-<br />
Zenica. MSc thesis (unpublished), 1-134, Sarajevo (in Bosnian).<br />
Trubelja, F. (1957): Some results of investigations of igneous rocks from Vareš in eastern<br />
Bosnia. II Congress of Yugoslav Geologists, 311-325, Sarajevo (in Bosnian).<br />
Trubelja, F. (1960): Petrography and origin of igneous rocks from the Višegrad area in eastern<br />
Bosnia. Acta Geologica, 2, 5-65, Yugosl. Acad. Sci. Arts, Zagreb (in Croatian).<br />
Trubelja, F. (1961): Igneous rocks from the south-eastern part of Mt. Kozara. Geol. gazette,<br />
5, 241-262, Sarajevo (in Bosnian).<br />
Trubelja, F. (1962): Albitized rocks in the area of Bosanski Novi. Geol. gazette, 6, 23-29,<br />
Sarajevo (in Bosnian).<br />
Trubelja, F. (1962a): Igneous rocks of south-eastern Bosnia. 5th Conference of Geologists of<br />
Yugoslavia, II, 79-84, Belgrade (in Croatian).<br />
Trubelja, F. (1963): Effusive rocks from the Čajniče area with a short review of similar rocks<br />
from the Lim river area. Geol. gazette, 15/2, 475-500, Zagreb (in Croatian).<br />
Trubelja, F. (1963a): Granite rocks from the Čajniče area. Geol. gazette, 7, 21-25, Sarajevo<br />
(in Bosnian).<br />
Trubelja, F. (1963b): A new occurrence of albite-bearing effusive rocks at Mt. Ljubić in<br />
Bosnia. Geol. gazette, 8, 29-32, Sarajevo (in Bosnian).<br />
Trubelja, F. (1963c): A new contribution to the knowledge on the igneous rocks from<br />
Višegrad. Geol. gazette, 7, 5-7, Sarajevo (in Croatian).<br />
Trubelja, F. (1966): Montmorillonite from the village of Podhum south of Livno. Geol.<br />
gazette, 11, 347-350, Sarajevo (in Bosnian).<br />
Trubelja, F. (1966a): Igneous and pyroclastic rocks from the northern flanks of Mt. Kozara.<br />
Journal of the National Museum of Bosnia and Hercegovina, new series vol. 5,<br />
5-21, Sarajevo (in Bosnian).<br />
Trubelja, F. (1967): A finding-site of sericite near Kreševo in Bosnia. Bull. Sci. Cons. Acad.<br />
Yougoslavie, A12, No. 5-6, Zagreb.<br />
Trubelja, F. (1967a): Fundamentals of general and special mineralogy, second edition.<br />
University of Sarajevo, Sarajevo (in Bosnian).<br />
Trubelja, F. (1969): Petrological characteristics of some rock types in the Borovica area near<br />
Vareš. Journal of the National Museum of Bosnia and Hercegovina, new series vol.<br />
8, 55-58, Sarajevo (in Bosnian).<br />
Trubelja, F. (1970): Diaspore bauxite at the village of Ljuša in the environs of Jajce (Bosnia).<br />
Bull. Sci. Cons. Acad. Yougoslavie, A15, No. 3-4, 74, Zagreb.<br />
346
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Trubelja, F. (1970a): Kaolinized sanidine-bearing dacites from Bratunac near Srebrenica in<br />
Bosnia. Proceedings of the VII Congress of Yugoslav Geological Societies, 122-<br />
123, Zagreb (in Croatian).<br />
Trubelja, F. (1971): Two different bauxite types in the area of Jajce, Bosnia. Proceedings of<br />
the Second International Symposium of ICSOBA, Vol. 2, 53-62, Budapest.<br />
Trubelja, F. (1971a): Mineralogical investigations of the kaolinized dacite from Bratunac.<br />
Enamel, ceramics and glass, 7/1, 38-44, Zagreb (in Croatian).<br />
Trubelja, F. (1971b): Xonotlite – a rare mineral from the Višegrad area in Bosnia. Report<br />
of the Yugoslav Center for Crystallography, 6/1971, 52, Yugosl. Acad. Sci. Arts,<br />
Zagreb.<br />
Trubelja, F. (1972): Kaolinized sanidine-bearing dacites from Bratunac near Srebrenica in<br />
Bosnia. Proceedings of the VII Congress of Yugoslav Geological Societies, Vol. 2,<br />
371-382, Zagreb (in Croatian).<br />
Trubelja, F. (1972a): The petrological characteristics of some rock types in th region<br />
of Borovica near Vareš. Wiss. Mitteilungen des Bosnisch-Herzegowinischen<br />
Landesmuseums, Bd. II, Heft C, 57-60, Sarajevo.<br />
Trubelja, F. (1972/73): Xonotlite in fissures within basic rocks from the Višegrad area in<br />
eastern Bosnia. Journal of the National Museum of Bosnia and Hercegovina, new<br />
series vol. 11-12, 43-51, Sarajevo (in Bosnian).<br />
Trubelja, F. (1973): Mineralogy of bauxites of Bosnia and Hercegovina as a function of their<br />
geological age. II Yugoslav Symposium on the exploration of bauxites, A2, 1-12,<br />
Tuzla (in Bosnian).<br />
Trubelja, F. (1973a): Infrared spectra of hecegovinian bauxites. II Yugoslav Symposium on<br />
the exploration of bauxites, A2, 1-7, Tuzla (in Bosnian).<br />
Trubelja, F. (1975): Xonotlite from crevices of basic rocks from vicinity of Višegrad. Wiss.<br />
Mitteilungen des Bosnisch-Herzegowinischen Landesmuseums, Bd. IV-V, Heft C,<br />
91-99, Sarajevo.<br />
Trubelja, F. and Barić, Lj. (1970): Glauconite from the Hrčavka valley near Tjentište. Geol.<br />
gazette, 23/1969, 265-272, Zagreb (in Croatian).<br />
Trubelja, F. and Barić, Lj. (1970a): Glauconite from the Hrčavka valley near Tjentište in<br />
Bosnia. Proceedings of the VII Congress of Yugoslav Geological Societies, 123-<br />
124, Zagreb (in Croatian).<br />
Trubelja, F. and Barić, Lj. (1976): On the distribution and structural characteristics of albite<br />
in various rocks of Bosnia and Hercegovina. Journal of the National Museum of<br />
Bosnia and Hercegovina, new series vol. 15, Sarajevo (in Bosnian).<br />
Trubelja, F. and Barić, Lj. (1976a): Project on the Mineralogy of Bosnia and Hercegovina,<br />
Vol. 1 – Descriptions of minerals and literature references. Report to the Republican<br />
Fund for Science, Sarajevo (in Bosnian).<br />
Trubelja, F. and Miladinović, M. (1969): An overview of the geology of the Tjentište and<br />
Sutjeska areas in south-eastern Bosnia. Special editions of the Academy of Sciences<br />
of Bosnia and Hercegovina, Vol. 11, 31-38, Sarajevo (in Bosnian).<br />
Trubelja, F. and Pamić, J. (1956): A new contribution to the knowledge of dacitic<br />
rocks in the Maglaj area. Geol. gazette, 2, 59-66, Sarajevo (in Bosnian).<br />
Trubelja, F. and Pamić, J. (1957): An overview of magmatism in Bosnia and Hercegovina. II<br />
Congress of Yugoslav Geologists, 73-83, Sarajevo (in Bosnian).<br />
Trubelja, F. and Pamić, J. (1965): Petrology of Mt. Ozren. Acta Geologica, 4, 265-314,<br />
Yugosl. Acad. Sci. Arts, Zagreb (in Croatian).<br />
347
SILICATES<br />
Trubelja, F. and Paškvalin, Lj. (1962): A lamprophyre dyke from Sasa near Srebrenica in<br />
Bosnia. Geol. gazette, 6, 61-64, Sarajevo (in Bosnian).<br />
Trubelja, F. and Ristić, P. (1973): Fundamentals of crystallography and mineralogy. University<br />
of Sarajevo, Sarajevo (in Bosnian).<br />
Trubelja, F. and Sijarić, G. (1970): A contribution to the knowledge on the mineralogy and<br />
chemistry of schists in the mountains of central Bosnia. Geol. gazette, 23, 273-284,<br />
Zagreb (in Croatian).<br />
Trubelja, F. and Sijarić, G. (1976): A new occurrence of bauxitic clay near Miljevine (Bosnia).<br />
Presentation at the IV Yugoslav Symposium on the prospecting and exploitation of<br />
bauxite, 11-15.10.1976, Herceg Novi (in Bosnian).<br />
Trubelja, F. and Slišković, T. (1967): The stratigraphic position and mineralogical composition<br />
of the igneous rocks of Sutjeska National Park. Bull. Sci. Cons. Acad. Yougoslavie,<br />
12/7-8, 182-183, Zagreb.<br />
Trubelja, F. and Šibenik-Studen, M. (1965): Effusive rocks from the Vrbas river valley and<br />
granites from Komar. Journal of the National Museum of Bosnia and Hercegovina,<br />
vol. 3-4, 99-103, Sarajevo (in Bosnian).<br />
Trubelja, F., Šibenik-Studen, M. and Sijarić, G. (1974): Minerals of fissures within basic<br />
igneous rocks in Bosnia and Hercegovina. 8th Congress of Geologists of Yugoslavia,<br />
Ljubljana.<br />
Trubelja, F., Šibenik-Studen, M. and Sijarić, G. (1975): Prehnite in the rocks of Bosnia and<br />
Hercegovina. Report of the Yugoslav Center for Crystallography, 10/1975, 65,<br />
Yugosl. Acad. Sci. Arts, Zagreb.<br />
Trubelja, F., Šibenik-Studen, M. and Sijarić, G. (1975a): Occurrences and origin of prehnites<br />
in Bosnia and Hercegovina. Journal of the National Museum of Bosnia and<br />
Hercegovina, new series vol. 14, 133-150, Sarajevo (in Bosnian).<br />
Trubelja, F., Šibenik-Studen, M. and Sijarić, G. (1976): Occurrence of zeolites in Bosnia and<br />
Hercegovina. Geol. gazette, 21, 323-380, Sarajevo (in Bosnian).<br />
Trubelja, F., Šibenik-Studen, M., Sijarić, G. and Šljukić, M. (1974): Investigations of zeolites<br />
in Bosnia and Hercegovina. Report of the Yugoslav Center for Crystallography,<br />
9/1974, 73, Yugosl. Acad. Sci. Arts, Zagreb.<br />
Trubelja, F. and Vasiljević, R. (1968): Bauxite from the area of Barać (Jajce) – a geological<br />
and mineralogical investigation. Journal of the National Museum of Bosnia and<br />
Hercegovina, new series vol. 7, 139-158, Sarajevo (in Bosnian).<br />
Trubelja, F. and Vasiljević, R. (1971): Bauxites of the Baraći region (Jajce) – a geomineralogical<br />
study. Wiss. Mitteilungen des Bosnisch-Herzegowinischen<br />
Landesmuseums, Bd. I, Heft C, 149-168, Sarajevo.<br />
Tscherne, M. (1892): Meerschaum von Bosnien und von Mähren. Verhandlungen der K.K.<br />
Geol. Reichsanstalt, 4, 100-108, Wien.<br />
Tućan, F. (1911): Die Kalksteine und Dolomite des kroatischen Karstgebietes. Geological<br />
Annals of the Balkan Peninsula, VI/2, 609-813, Belgrade (in Croatian).<br />
Tućan, F. (1912): Terra rossa, deren Natur und Entstehung. Neu. Jahrb. f. Mineralogie,<br />
Geologie und Paläontologie, Beilage Bd. 34, 401-430, Stuttgart.<br />
Tućan, F. (1919): Our ore resources. Matica Hrvatska, Zagreb (in Croatian).<br />
Tućan, F. (1922): A contribution to the knowledge on minerals of Yugoslavia. Titanite from<br />
gabbros at Jablanica in Hercegovina. Memorial volume for S.M. Lozanić, 193-198,<br />
Belgrade (in Croatian).<br />
Tućan, F. (1928): The andesite eruption in the karst of Hercegovina. Gazette of the Geological<br />
Survey in Zagreb, II (for 1927/28), 178-188, Zagreb (in Croatian).<br />
348
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Tućan, F. (1930): Special mineralogy. Belgrade (in Croatian).<br />
Tućan, F. (1930a): Mišo Kišpatić. Memoirs (Rad) Yugosl. Acad. Sci. Arts, Vol. 238, 97-271,<br />
Zagreb (in Croatian).<br />
Tućan, F. (1947): The ores of Bosnia. Priroda (Nature), 34/6, 201-208, Zagreb (in Croatian).<br />
Tućan, F. (1957): Special mineralogy. Second revised edition. Školska knjiga, Zagreb (in<br />
Croatian).<br />
Vakanjac, B. (1964): The origin of chrysotile-asbestos deposits around Bosansko Petrovo<br />
Selo. Geol. gazette, 10, 197-225, Sarajevo (in Bosnian).<br />
Vakanajc, B. (1965): On the magnetite-chrysotile-asbestos paragenesis in deposits of<br />
Bosansko Petrovo Selo. Technologica Acta, III/2-3, 45-53, Tuzla (in Bosnian).<br />
Vakanjac, B. (1968/69): Types of chrysotile-asbestos deposits and basic theory of their<br />
occurrence and distribution in Yugoslavia. Annals of the Faculty of Mining and<br />
Geology in Belgrade, 11-12, 135-153, Belgrade (in Serbian).<br />
Varićak, D. (1955): A petrological description of the Maglaj granite. Geol. gazette, 1, 43-57,<br />
Sarajevo (in Bosnian).<br />
Varićak, D. (1956): Quartzporphyres of Mt. Prosara (Bosnia). Geol. gazette, I, 199-206,<br />
Cetinje (in Serbian).<br />
Varićak, D. (1957): The metamorphic rocks of Mt. Prosara and their relationship to<br />
metamorphic facia. Memoirs of the Serbian Geological Society (for 1956), 31-38,<br />
Belgrade (in Serbian).<br />
Varićak, D. (1966): The petrology of the Mt. Motajica granite massif. Geol. gazette, special<br />
editions vol. 9, 1-170, Sarajevo (in Bosnian).<br />
Varićak, D. (1971): Crystalline quartz in Bosnia and Hercegovina. Geol. gazette, 15, 163-<br />
167, Sarajevo (in Bosnian).<br />
Vasiljević, R. (1969): Sedimentary quartzites from Podrašnica near Mrkonjić Grad. Geol.<br />
gazette, 13, 319-322, Sarajevo (in Bosnian).<br />
Veljković, D. (1971): Results of the geological exploration of the Veovača barite and PbZn<br />
deposit near Vareš. Geol. gazette, 15, 211-231, Sarajevo (in Bosnian).<br />
Vrba, K. (1885): Realgare from Bosnia. Memoirs of the Geological Survey in Prague, p. 41,<br />
Prague (in Czech).<br />
Vrba, K. (1889): Realgare from Bosnia. Journal of the Royal Czech Scientific Society,<br />
yearbook for 1889, vol. 1, 10-13, Prague (in Czech).<br />
Vujanović,V. (1962): Mineralogy and origin of the manganese deposit at Čevljanović<br />
(Bosnia). Journal of the Museum of Natural History in Belgrade, A 16-17, 219-255,<br />
Belgrade (in Serbian).<br />
Walter, B. (1887): Beitrag zur Kenntniss der Erzlagerstätten Bosniens, mit einer Karte und 33<br />
Abbildungen, 1-122, Sarajevo.<br />
Weisse, J.G. de (1948): Les bauxites de l’Europe centrale (Province dinarique et Hongrie).<br />
Bull. des Laboratoires de Geologie etc., de l’Universite de Lausanne, No. 87,<br />
Lausanne.<br />
Wolf, D. (1847): Ansichten über die geognostischen-montanistischen Verhältnisse Bosniens,<br />
1-30, Graz.<br />
Zarić, P., Đorđević, D. and Vilovski, S. (1971): Bravoite and vaesite from Slatina near<br />
Banja Luka. Geological Annals of the Balkan Peninsula, 36, 215-222, Belgrade (in<br />
Serbian).<br />
Živanović, D. (1968): The geologic and economic characteristics of the principal magnesitebearing<br />
series at Mt. Konjuh. Geol. gazette, 12, 217-229, Sarajevo (in Bosnian).<br />
Živanović, M. (1963): A short review of basic information on igneous rocks of the schist<br />
mountains of central Bosnia. Geol. gazette, 8, 249-251, Sarajevo (in Bosnian).<br />
349
SILICATES<br />
350
Index<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
A<br />
Actinolite 3, 22, 32, 37, 64, 78, 81, 88, 105,<br />
115-118, 136-142, 154, 174, 237, 280, 286,<br />
302, 304<br />
Africite 102<br />
Albite 5, 44-46, 51, 67, 76, 78-79, 81-82,<br />
84, 89, 96, 106, 120, 123-124, 126, 141, 151,<br />
155, 174-176, 182, 186, 188, 190, 211-213,<br />
219, 245-246, 248-250, 259-264, 268, 274-<br />
285, 287-298, 300, 303, 305, 319, 322, 326,<br />
328-329, 331, 334, 337, 340, 346-347<br />
Allanite 3, 85-87<br />
Almandine 39, 41-43, 45, 47<br />
Amphibole 28, 32-33, 37-38, 40-42, 44, 54,<br />
59, 64, 78-79, 88, 90, 110, 113-116, 119-120,<br />
122-123, 127, 136-151, 153-156, 174, 184,<br />
189, 211, 215, 229, 236, 254, 257, 260, 265,<br />
277, 281, 287, 291, 293-295, 297-298, 304,<br />
307, 309, 320, 331, 340<br />
Analcime 247-248, 254-255, 309-310, 314-<br />
316, 323, 331, 344<br />
Anatase 182<br />
Andalusite 3, 55-57, 66, 187, 213<br />
Andesine 5, 23, 42, 257, 259, 276, 278, 280,<br />
286-301<br />
Andradite 39, 42-43, 45-46<br />
Anorthite 5, 22, 255, 268, 274, 291, 297,<br />
302-304, 306-307<br />
Anorthoclase 257, 262-264<br />
Antigorite 225, 228, 231-232, 234-236<br />
Apatite 22, 44, 49, 101, 106, 185, 187, 195,<br />
257, 259, 263<br />
Apyre 102<br />
Aquamarine 91, 99<br />
Augite 3, 22, 37, 53, 82, 89, 111, 116, 121-<br />
127, 139-140, 150-151, 190, 209-210, 334<br />
Axinite 3, 90<br />
B<br />
Bagrationite 85<br />
Baryte 21, 23, 25, 141, 169, 176-177<br />
Basalt 38, 111, 115, 125-126, 142, 145, 209-<br />
210, 248, 286, 290, 297, 300, 305<br />
Beidellite 4, 200, 202-205, 329<br />
Beryl 3, 24, 91-97, 99-100, 103, 105, 171,<br />
188, 327-328, 331, 336, 338, 343<br />
Biotite 4, 22, 43-44, 50-51, 54, 56-57, 66,<br />
68, 78-80, 86-87, 101, 104, 110, 121-122,<br />
136, 173, 180, 182-191, 195, 197, 203, 206,<br />
209, 211-213, 219-220, 254-255, 257, 259,<br />
263, 283-284, 289, 293-294, 301, 346<br />
Bixibiite 91<br />
Bodenite 85<br />
Braunite 3, 60-63<br />
Bronzite 3, 128-129, 133-134<br />
Bytownite 5, 136, 184, 296-307<br />
C<br />
Calcite 22-23, 28, 45-46, 61, 67, 70. 76-77,<br />
80, 82, 84, 90, 107, 125, 159, 162, 165, 182,<br />
195, 198, 200, 203, 209-211, 245-248, 250,<br />
255, 257, 264, 276, 278, 283, 293-294, 305,<br />
310<br />
Celladonite 181<br />
Chabasite 311, 313, 317, 319-320, 323,<br />
325-326<br />
Chalcedony 23<br />
Chalcopyrite 23-25, 46, 170, 225, 265, 283<br />
Chamosite 207, 217<br />
Chlorite 4, 22, 40, 43-44, 76, 80-84, 90, 106,<br />
118, 120, 122-123, 125-127, 136, 141, 155,<br />
167, 169-170, 174, 177, 179, 185, 187-189,<br />
191, 198, 203, 206-217, 219-220, 229, 234-<br />
235, 244-246, 248-250, 255, 264-265, 276,<br />
278, 281, 283-285, 301, 319-320, 326, 345<br />
Chloritoid 3, 49, 68-69, 175<br />
351
SILICATES<br />
Chromite 23, 25, 34, 36, 43, 114, 131, 146,<br />
217, 229, 234, 329, 339, 345<br />
Chrysocolla 4, 224, 225<br />
Chrysotile 23, 171, 225, 231, 233, 236-237,<br />
241, 332, 334, 338, 349<br />
Clinochlore 206-207, 211-214<br />
Clinozoisite 3, 44, 46, 75, 75-83, 145, 155,<br />
229, 244-245, 250<br />
Cordierite 100, 101<br />
Corundophyllite 206, 209<br />
Crocydolite 155-157<br />
Cryptomelane 61<br />
D<br />
Daphnite 206-207, 217<br />
Datolite 3, 69-71, 245, 255, 309, 316, 331<br />
Diallage 3, 22, 111-112, 115-121, 123-124,<br />
135, 138-139, 143, 150, 209, 281<br />
Dickite 4, 220, 224, 342<br />
Diopside 3, 24, 42-43, 111-116, 121, 136,<br />
171, 182, 229, 291<br />
Disthene 57<br />
Dolomite 23, 47, 109, 157, 165, 169, 175,<br />
229, 231, 348<br />
E<br />
Edenite 42, 135, 142, 146, 148-150, 298,<br />
304, 307<br />
Emerald 91, 97-99<br />
Enstatite 3, 34-36, 128-133, 138, 171, 229<br />
Epidote 3, 22, 28, 44-46, 67, 75-85, 88-90,<br />
105, 107, 109-110, 141, 155, 157, 174, 185,<br />
188-189, 198, 213, 220, 145, 249-250, 259,<br />
279, 281, 301, 305<br />
F<br />
Fayalite 30, 35-38<br />
G<br />
Gabbro 6, 22, 28, 31-33, 35-38, 41, 45, 65,<br />
76-77, 79, 82, 89-90, 107, 112-113, 115-121,<br />
123-125, 131, 134-140, 142-143, 145, 149-<br />
152, 155, 183-184, 186, 190, 197, 208-212,<br />
227, 235-236, 243-245, 247-250, 258, 260,<br />
279, 281, 286, 288, 290, 292, 295-300, 302-<br />
307, 309-311, 313, 317-320, 322-323, 329,<br />
331-332, 334, 336-337, 339-340, 344, 348<br />
Galene 21, 25, 27<br />
Garnets 3, 22-23, 39-47, 82, 90, 101, 107,<br />
110, 113-114, 128, 135, 151, 155, 157, 160,<br />
173, 182, 187, 195, 203, 209, 211-213, 247,<br />
254, 280, 291, 304, 307, 309<br />
Garnierite 225, 234<br />
Gibbsite 182, 217, 221-222, 238, 313<br />
Glauconite 4, 179-182, 347<br />
Glaucophane 4, 148, 155-157<br />
Gneisse > Gneiss 43-44, 49-50, 52, 54, 56,<br />
66, 78, 80, 86, 87, 102, 104, 154-155, 172-<br />
174, 183, 187-188, 212-213, 259, 261-262,<br />
275, 281, 289, 294-295<br />
Goethite 26, 199, 205, 220, 229<br />
Goshenite 91, 99<br />
Grossular 39, 42-43, 45-46<br />
H<br />
Halloysite 4, 194-195, 201, 224, 237-238,<br />
337<br />
Harzburgite 24-37, 115, 120, 129-132, 138,<br />
150, 227<br />
Hausmannite 61<br />
Hedenbergite 111<br />
Heliodor 91, 99<br />
Hematite 23, 25-26, 62, 101, 110, 118, 121,<br />
221, 259<br />
Hemimorphite 3, 71-72<br />
Hibschite 48<br />
Hornblende 4, 22, 41-44, 78, 83, 113-114,<br />
352
117, 120-121, 124, 135-137, 140-146, 148-<br />
155, 174, 182, 211, 213, 244, 248, 287, 294,<br />
298, 304, 307, 319, 332<br />
Hornblendite 41, 78, 113, 151, 154, 174,<br />
294, 304, 307<br />
Hyalophane 4, 177, 264-274, 330<br />
Hydrobiotite 4, 197<br />
Hydromica 44, 46, 50, 165, 179, 189, 192,<br />
Hydromuscovite 4, 166, 192, 196-197, 285,<br />
329<br />
Hypersthene 3, 128-129, 134-136, 138,<br />
153, 301, 305, 309, 336<br />
I<br />
Illite 4, 165, 191-196, 199, 201, 218-219,<br />
222, 238, 344-345<br />
Ilmenite 22, 56, 64-66, 101, 145, 155, 195<br />
K<br />
Kaemmererite 206, 217<br />
Kalinite 218<br />
Kaolinite 4, 165, 171, 194-196, 201, 206,<br />
217-219, 221-224, 237-238, 249, 259-260,<br />
279, 293-294, 329, 337, 342<br />
Ksantorite 85<br />
Kyanite 3, 7, 57-58, 67, 182, 203<br />
L<br />
Labradorite 5, 22, 33, 42, 79, 190, 259, 278,<br />
281, 288, 290-293, 295-303, 305, 334<br />
Lazurite 5, 308<br />
Lepidomelane 188<br />
Lherzolite 32-36, 112-115, 129-134, 171,<br />
227, 241, 302-303, 307<br />
Limonite 23, 25, 50, 71, 110, 165, 167, 194,<br />
224<br />
Lizardite 225, 228-231, 326<br />
M<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Magnesite 21, 28, 36, 38, 228-229, 236,<br />
239-241, 338, 342-344, 349<br />
Magnetite 22-23, 32-33, 35, 37, 43-46, 59,<br />
82-83, 89, 101, 105, 107, 120-121, 125, 136,<br />
141, 151, 157, 177, 185, 190-191, 203, 211,<br />
216, 219, 264-265, 329, 331, 338, 349<br />
Marble 45, 76, 174-175, 188, 248<br />
Mesolite 5, 310, 313<br />
Metahalloysite 201, 237<br />
Micaschist 43, 50, 56, 66, 80, 104, 173-174,<br />
183, 187-188, 213, 242, 281<br />
Microcline 4, 172, 258-259, 261-262<br />
Montmorillonite 4, 165, 171, 192, 194-195,<br />
198-206, 218, 342, 346<br />
Morganite 91, 99<br />
Muromonite 85<br />
Muscovite 4, 22, 43, 50-51, 54, 56, 67, 69,<br />
86-87, 93, 96, 101, 103-104, 165-166, 172-<br />
179, 187, 192-193, 195, 203, 219, 238, 258-<br />
259, 261, 273, 284-285, 288<br />
N<br />
Nacrite 4, 224<br />
Natrolite 5, 70-71, 210, 247, 255, 309-311,<br />
313-314, 316, 322-323, 325-326, 331<br />
Nepheline 4, 254<br />
Nontronite 4, 203-206, 220<br />
O<br />
Oligoclase 5, 22, 51, 223, 260, 278, 280-<br />
281, 286-289, 292, 295, 298, 300, 330<br />
Olivine 3, 22, 30-38, 117-120, 129-132, 134-<br />
136, 138-140, 143, 145, 150, 155, 167, 171,<br />
186, 190, 206, 226-227, 229, 235-236, 243-<br />
245, 260, 296, 298-299, 302-304, 306, 344<br />
Omphacite 3, 41, 113, 127-128, 184, 309<br />
Orthoclase 4, 22, 80, 104, 171-172, 195,<br />
353
SILICATES<br />
219, 258-261, 264-265, 268, 279<br />
Ottrelite 3, 68-69<br />
P<br />
Pargasite 42, 135, 142, 146, 148-150, 298,<br />
304, 307<br />
Pennine 28, 44, 206-207, 211, 213<br />
Periclase 182<br />
Phlogopite 4, 182<br />
Pigeonite 3, 111, 119<br />
Pistazite 75, 77, 79, 85<br />
Plagioclase 5, 32, 37, 41, 43-44, 52, 76-77,<br />
79, 101, 114, 120, 123, 125-126, 135, 138-<br />
139, 163, 182, 185-186, 192, 209, 218-220,<br />
244, 247, 250, 255, 257-259, 274, 276-178,<br />
280-281, 284, 286, 300, 302-304, 306-309,<br />
316-317, 320, 323, 325, 327-328, 343<br />
Prehnite 4, 28, 43-44, 66, 71, 76-77, 79-80,<br />
83, 90, 114, 124, 145, 161, 163, 211, 227,<br />
242-250, 255, 276, 281, 291, 303-304, 307,<br />
309, 314, 316-317, 319-320, 323, 345, 348<br />
Pumpellyite 3, 90, 249, 319<br />
Pyrite 23-25, 44-46, 96, 103, 105, 145, 170,<br />
203, 220-222, 225, 253, 265, 273, 279, 330<br />
Pyrope 39, 41-43, 45, 47<br />
Pyrophyllite 4, 165-166, 175, 194, 198, 285,<br />
329<br />
Pyroxene 28, 33, 37-38, 40-41, 44, 64, 78,<br />
110-116, 118, 120-121, 127-129, 131-135,<br />
138-140, 145, 150-151, 167, 171, 208, 211,<br />
213, 226-227, 236, 287, 296, 302, 304-305,<br />
307, 331, 344<br />
Q<br />
Quartz 12, 21-24, 26, 28, 38, 40, 47, 49, 50,<br />
52, 54, 56-58, 61, 66-67, 69, 81-82, 84, 89,<br />
94-96, 99, 101, 103-110, 127, 141, 153-155,<br />
164-165, 169, 173-179, 184-185, 187-196,<br />
198-199, 201-203, 209, 211-213, 216, 219-<br />
220, 222-223, 238, 248-249, 254, 257-258,<br />
260, 263, 265, 273-274, 276-277, 283-285,<br />
288, 292, 308, 317, 320, 330, 332, 334, 340,<br />
342, 349<br />
R<br />
Rhipidolite 71, 206-207, 245<br />
Rhodochrosite 26-27<br />
Rhodonite 4, 164<br />
Riebeckite 155-157<br />
Romanechite 61<br />
Rubelite 102, 108<br />
Rutile 41, 43, 49, 64, 67, 106, 110, 182, 192,<br />
203<br />
S<br />
Sanidine 4, 22, 185, 220, 224, 256-258, 261-<br />
264, 347<br />
Saponite 4, 206<br />
Scapolite 5, 308-309<br />
Scolecite 5, 311-313, 322-323<br />
Searlesite 4, 250-254, 325-326, 328-329<br />
Sepiolite 4, 21, 23-25, 33, 134, 220, 238-<br />
242, 336, 341, 343, 345<br />
Sericite 44, 56-57, 76, 81, 101, 106-107,<br />
110, 165, 172-179, 195-197, 211, 216, 219-<br />
220, 238, 248-249, 259-260, 265, 276, 279,<br />
282, 291, 346<br />
Serpentine zone 22-23, 30-34, 38, 40-41,<br />
48-49, 51, 56-57, 64, 70-72, 76, 79-80, 89,<br />
112, 114, 116-117, 121-123, 127, 129, 133-<br />
134, 137-138, 143, 147, 155, 158, 164, 167,<br />
168, 171, 178, 183, 186, 197, 199, 205, 208,<br />
210, 226-227, 236, 243, 249, 254, 255, 275,<br />
279, 286, 287, 290, 295, 296, 299, 302, 304,<br />
306-307, 309, 313, 316, 322-323, 326-327,<br />
330, 336-337<br />
Sheridanite 206-207<br />
Shorl 105<br />
Siberite 102<br />
Spessartine 39, 42, 45, 47<br />
354
Sphalerite 25, 27, 72, 107, 346<br />
Sphene 63<br />
Sporogelite 183<br />
Staurolite 3, 59-60, 203<br />
Stilbite 5, 28, 90, 103, 281, 311, 317-319,<br />
322, 345<br />
Stilpnomelane 4, 84, 198<br />
Sudoite 206-207, 217<br />
Suolunite 3, 72-75, 158-159, 345<br />
Syenite 51, 53, 210, 247, 258, 261, 275, 280,<br />
331<br />
T<br />
Talc 4, 96, 103, 130, 166-172, 201, 209-210,<br />
214-215, 234-235, 332, 339, 345<br />
Tautolite 85<br />
Thomsonite 5, 245, 255, 310, 313-315, 322,<br />
323, 345<br />
Thorite 3, 53-55, 86<br />
Titanite 3, 28, 63-67, 101, 116, 155, 248,<br />
320, 348<br />
Tobermorite 4, 73, 75, 158-159, 345<br />
Tourmaline 3, 28, 49, 52, 67, 80, 89, 96,<br />
101-110, 182, 189, 195, 203, 259, 283, 320,<br />
330, 334, 337<br />
Tremolite 3, 32, 37, 136-139, 142, 237, 245<br />
Troctolite 31-33, 35, 37, 79, 112, 117, 119-<br />
120, 138, 140, 145, 206, 227, 243-244, 295,<br />
302-303, 306<br />
Tschermakite 148-149<br />
Tuff 51, 66, 110, 127, 180-181, 184, 186,<br />
191, 199-201, 206, 210, 212, 251, 254-255,<br />
257, 277, 281, 286, 289, 290, 292, 294-295,<br />
300, 328, 337<br />
V<br />
<strong>MINERALS</strong> of Bosnia and Herzegovina<br />
Vermiculite 4, 206<br />
Vesuvianite 3, 90<br />
Vorobievite 91, 99<br />
W<br />
Wasite 85<br />
Wollastonite 4, 74, 107, 157-158, 161<br />
X<br />
Xonotlite 4, 74, 159-164, 244, 281, 331,<br />
337, 347<br />
Z<br />
Zeolite 66, 70, 76, 105, 163, 241, 244, 250,<br />
255, 313, 316, 322-327, 348<br />
Zircon 3, 41, 43, 58-53, 101-102, 106, 108,<br />
182, 195, 203, 219, 259<br />
Zoisite 3, 22, 67, 79, 81-82, 84, 87-90, 109,<br />
139, 154, 244, 249<br />
U<br />
Uvarovite 39, 42-43, 47<br />
355
SILICATES<br />
This book was published with financial support of:<br />
ZA IZDAVAŠTVO<br />
SARAJEVO<br />
Engineering<br />
Consulting<br />
Design<br />
Road Directorate of Federation<br />
of Bosnia and Herzegovina<br />
Geoinvest d.o.o. Sarajevo, Department for Transport, Faculty of Civil Engineering in<br />
Sarajevo, Ministry of Civil Affairs of Bosnia and Herzegovina, Federal Ministry of<br />
Physical Planning, Institute for Geology, Faculty of Civil Engineering in Sarajevo,<br />
Construction Institute of the Canton Sarajevo, Federal Directorate for Building, Managing<br />
and Maintaining Motorways, Federal Institute for Geology, INTRADE energija, Institute<br />
for Hidrotechnics, Faculty of Civil Engineering in Sarajevo<br />
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