Budapest 1977 - Magyar Természettudományi Múzeum

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Budapest 1977 - Magyar Természettudományi Múzeum

ANNALES HISTORICO-NATURALES

MUSEI NATIONALIS HUNGARICI

A TERMÉSZETTUDOMÁNYI MÚZEUM

ÉVKÖNYVE

TOMUS LXIX.

ADIUVANTIBUS:

D. JÁNOSSY, I. KOVÁCS, S. MAHUNKA,

J. PAPP, J. SZUJKÓ-LACZA, T. TÓTH

REDIGIT:

: Z. KASZAB

Ann. Hist. -nat. Mus. Nat. Hung., 69, 1977.

[


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ANNALES HISTORICO-NATURALES

MUSEI NATIONALIS HUNGARICI

A TERMÉSZETTUDOMÁNYI MÚZEUM

ÉVKÖNYVE

TOMUS LXIX. 1977.

ADIUVANTIBUS:

D. JÁNOSSY, I. KOVÁCS, S. MAHUNKA,

J. PAPP, J. SZUJKÓ-LACZA, T. TÓTH

REDIGIT:

Z. KASZAB

Ann. Hist.-nat. Mus. Nat. Hung., 69, 1977.


ISSN 0521 — 4726

Felelős Kiadó: Nemes Iván igazgató — Műszaki szerkesztő: Sugár László

Készült az MSZ 5601 — 59 szabvány szerint B/5 alakban, 311,25 A/5 ív terjedelemben,

1000 példányban, NPI tsz. 6026/77

77/4907. Franklin Nyomda, Budapest. Felelős: Vágó Sándornó igazgató


CONSPECTUS MATERIARUM

Pars Petrograpüica

EMBEY-ISZTIN, A.: The Szigliget amphibolite/lherzolite compound xenolith as an

evidence for diapiric uprise in the mantle below Hungary 5

NOSKE-FAZEKAS, G. : Feldspatuntersuchungen am Andesitvorkommen des Róka-

Berge bei Szokolya (Ungarn) 13

Pars Palaeontologiea

HABLY, L. & CSABA, A. : A new Smilax L. species from the upper Oligocène of

Vértesszőlős (Hungary) 23

Pars Botanica

P.-KOMÁROMY, Zs. : The algal flora of the Ördöglyuk cave at Szoplak (Hungary) .... 29

HAJDTJ, L. : Über die Wiederaufstellung von Coelastrum astroideum De Not. (Chlorophyta,

Chlorococcales) 37

BORHIDI, A. & MUNIZ, O.: Revision del género Croton L. (Euphorbiaceae) en Cuba 41

SZUJKÓ-LACZA, J. & SEN, S.: Correlation coefficient study in some character pairs of

the Hungarian Gentiana (Gentianaceae) 57

Pars Zoologica

BETSCH, J.-M. : Collemboles Symphypléones de la Mongolie (Collembola) 59

STEINMANN, H.: A study on the higher taxa of Carcinophoridae (Dermaptera) ... 89

GOMY, Y.: Histeridae nouveaux de la faune orientale et de la Nouvelle-Guinée

(Coleoptera) 101

KASZAB, Z.: Neue Tenebrioniden (Coleoptera) von den Galapagos und Antillen,

sowie aus Südamerika und Ostasien 117

KASZAB, Z. & MEDVEDEV, G. S. : Tentyrüni (Coleoptera, Tenebrionidae) aus der Mongolei,

III . 133

HALSTEAD, D. G. H. : Further records of Palarus and description of a new species

from Ghana and Zaire (Coleoptera, Tenebrionidae) 145

SKOPIN, N. G. : Über Blaps transversimsuleata Ball, und ihre nähere Verwandten (Coleoptera,

Tenebrionidae) 149

LOPATIN, I.: Weitere Beiträge zur Kenntnis der Chrysomeliden-Fauna der Mongolei

(Coleoptera) 153

NIKOLAJEV, G. V. & SHUKRONAJEV, S. : Zwei neue Scarabaeidae aus Tadshikistan

(Coleoptera) 157

BAJTENOV, M. S. : Tychiinae (Coleoptera, Curculionidae) aus der Mongolei 159

VOJNITS, A. M. : Archiearinae, Rhodometrinae, Geometrinae II, Sterrhinae II and Ennominae

III (Lepidoptera, Geometridae) from Mongolia 165

DELY-DRASKOVITS, A. : Lasiopleura. brevivenosa sp. n. aus der paläarktischen Region

(Diptera, Chloropidae) 177

MIHÁLYI, F. : A new key for Hungarian Lucilla species (Diptera, Calliphoridae) 181

PAPP, L. : Notes on some Becker's types (Diptera, Carnidae and Risidae fam. n.) .... 185

ZOMBORI, L.: New sawfly species in the Hungarian fauna (Hymenoptera, Symphyta),

III 191

HORSTMANN, K.: Campopleginae aus Jordanien und Libanon (Hymenoptera, Ichneumonidae)

195


PAPP, J. : New Apanteles Först. species from Hungary (Hymenoptera, Braconidae :

Microgasterinae), V 201

PAPP, J. : Braconidae (Hymenoptera) from Mongolia, VIT 219

SZELÉNYI, G. : New Palaearctic Chalcid flies (Hymenoptera, Eulophidae) 241

FABRITITJS, K. : Beitrag zur Kenntnis der Platygasteriden Ungarns (Hymenoptera,

Proctotrupoidea) 249

MÓCZÁR, L. : Angaben zur Ceropaliden-Fauna (Hymenoptera) der Mongolei 253

TstJNEKi, K. : H. Sauter's Sphecidae from Formosa in the Hungarian Natural History

Museum (Hymenoptera) 261

BAYOUMI, B. M. : Two new Oribatid mites (Acari) from Egypt 297

MAHUNKA, S. : Ctenobelba csiszarae sp. n. und einige Bemerkungen über die Gattung

Ctenobelba Balogh, 1943 (Acari, Oribatida) 301

MAHUNKA, S. & RACK, G.: Zwei neue Arten der Familien Acarophenacidae und Pygmephoridae

( A carina, Tarsonemida) 305

ATHIAS-FIENRIOT, C: Untersuchungen über die Gattung Neogamasus Tikhomirov mit

zwölf neuen Arten aus Korea (Parasitiformes, Gamasida) 311

VARGA, A. : Beiträge zur Kenntnis der Gattung Carpathica A. J. Wagner, 1895 (Gastropoda)

343

Pars Anthropologics

TÓTH, T. : Neolithic and Paleometallic populations in the Central Danubian Basin 347

LoTTERHor, E. : On the problem of gracilization in the Central Danubian Basin, II. 357

TjiaAKOBa, T. R\. & TOT, T.: O pacnpeAejieHHH KOJKHMX ysopoB Ha TepnpopnH

BeHrpnH (HOBbie ßaimbie H3 Kapuar) 361

Pars Museologica

List of scientific publications of the Hungarian Natural History Museum in the

Year 1976 373

Scientific staff of the Hungarian Natural History Museum in the Year 1977 379


ANNALES HISTORICO-NATURALES MUSEI NATIONALIS HUNGARICI

Tomus 69. Budapest 1977.

The Szigliget Amphibolite, lherzolite

Compound Xenolith as an Evidence for

Diapiric Uprise in the Mantle Below Hungary

by A. EMBEY-ISZTTN, Budapest

Abstract — On the basis of similarities between the Szigliget amphibolite/lherzolite

compound xenolith and the lherzite veins of Etang de Lherz (Pyrenees, France) it has

been argued that the origin of the amphibolite is connected with diapiric uprise of

mantle material. Other evidences are also discussed. With 4 figures.

BASCT (1975) has recently underlined the interesting fact that the peridotite-bearing

alkali undersaturated basalts are constantly associated with Wilson-Morgan hot-spots,

both in the ocean basins and on the continents. The Wilson-Morgan hypothesis of hotspots

or eonvection plumes is very useful because it may explain the source of energy

that drives the lithospheric plates. The hot-spots are surface representations of hot upwelling

mantle material or mantle diapir. According to WILSON (1973) the hot-spots are

characterized by gravity highs, and high heat flows, as well as by shallow seismicity. In

the ocean basins they are associated with mid-oceanic ridges and on the continents they

are near the rift valleys. BASU (loc. cit.) has given a list of such continental rift zones each

of which is reputed by the presence of periodite inclusion-bearing alkali basalts. According

to him these rift systems are as follows: 1. Ethiopia and eastern Africa, 2. Rhine Graben

(GFR), 3. Lake Baikal (USSR), 4. Auvergne (Massif Central, France). I hold the view

that the list is incomplete, for I think that it should be completed at least by another region

of Europe: the Pannonian Basin in Hungary.

The following facts strengthen the view that the Pannonian Basin may be similar to

the rift systems of the world: a) Extensional tectonics in young Cenozoic times; b) Eruption

of inclusion-bearing alkali undersaturated basaltic lavas and tuffs in the Upper Pliocene;

c) Shallow seismicity and high heat flow; 4) Elevated position of the LVZ; e) Thin

crust (24-26 km).

In the following passages an account is given of a peculiar amphibolite/lherzolite

composite xenolith which in the author's opinion may be considered as an evidence for

mantle diapirism below the Pannonian Basin. The xenolith in question has been found

in an outcrop of basaltic tuff near the village of Szigliget north of Lake Balaton. Here the

tuff contains numerous nodules of CV-dipside, Cr-spinel lherzolite replaced to varying

degrees by carbonate. Besides peridotites, clinopyroxene megacrysts have also been found.

Petrography

The amphibolite/lherzolite compound xenolith (Fig. 3) is slightly elongated in one

direction and measures approximately 6 X 4.5 X 4 cm. It is incompletely covered by a

thin layer of basalt. In the middle of the nodule there is a black vein, 2 cm in width, cutting

the CV-diopside-spinel lherzolite. The black vein is a coarse-grained amphibolite and

its contacts toward the lherzolite are sharp. The lherzolite is replaced to a high degree by

a carbonate. However, the replacement must have been selective, affecting mostly olivine

and having little influence on the other constituents. On the basis of the presence of

large strained orthopyroxenes and interstitial spinel the texture may be called porphroclastic

according to the classification of MERCIER & NICOLAS (1975). — The amphibolite

vein is composed almost entirely of a coarse-grained amphibole aggregate. The grain

size may attain 5 mm, but at the borders it is generally smaller. The texture is panxeno-


morphic and no evidence for or against a cumulus origin could be found. While large domains

seem tectonically undisturbed, other domains show abundant signs of cataclysis

such as tiny crystals due to recrystallization or distorted twin lamellae. However, it is evident

that this texture has nothing in common with that of the lherzolite: the amphibolite

must have intruded into the lherzolite long after this last one had metamorphosed. Besides

large amphibole crystals, the amphibolite contains n i.ior euhedral opaque inclusions,

probably ilmenite, and very subordinate grains of spinel. This spinel diffeis from the lherzolite

spinel in its greenish colour. (The lherzolite spinel is chest-nut brown.)

In addition to the primary mineral association, a secondary one has also to be mentioned.

This secondary association is apparently due to a partial melting of small degree.

It is composed of newly formed amphibole, jolagioclase crystals and a vitrous matrix.

In contrast to large primary amphiboles, the small secondary ones have perfect crystal

faces and show optical zoning.

Chemical Mineralogy

Electron microprobe analyses have been carried out on minerals of amphibolite

and lherzolites by the aid of a MS-46 type microanalyzer in the B. R. G. M., Orléans, La

Source, (France) (EMBEY-ISZTIN 1976bj.

Lherzolite silicates are high in Mg and low in Fe, therefore they characterize an environment

depleted in basaltic constituents (KUNO & AOKI 1970, CARTER 1970). The composition

of olivine is: Mg 90.20-90.29 Fe 9. 8 0-9 71, that of the orthopyroxene: Mg 8 9 1 Fe9 2 Ca17 and that of the clinopyroxene Mg49.o Fe 5. 7 Ca45 3.

2 +

The spinel with a composition of Mg78 Fe|J as well as Al|J Fef + Cr^+ (the ¥e (

3 +

Fe has been calculated from structural formula), falls into the field of magnesio-picotite,

near the field of magnesio-chrom-picotite in SOKOLOV'S classification. —• The carbonate

which replaces olivine is a very pure calcite.

The amphibolite is in sharp contrast to the lherzolite because its minerals are rich

in basaltic constituents. As its accessories are quite subordinate, the chemical composition

of the whole amphibolite is well represented by the primary amphiboles. The primary

amphibole is a pargasite rich in Ti, the number of Ti being slightly smaller than 0.5

per half unit cell. Mg/27Fe = 2.62; 100 Mg/Mg + TFe = 72.39. No evidence could be

detected in favour of chemical zoning traversing primary amphiboles by electron beam.

Fig. 1. Microprobe scans for Fe and Ti accros a secondary amphibole.— Fig. 2. P —T diagram

of Hungarian and French nodules (in prep.). Closed circles Hungarian, crosses

French nodules. A, B, C fields of plagioelase, spinel and garnet-lherzoiite. Ps: dry peridotite

solidus, Go: oceanic geoterm, Gc: shield geotberm.

2


The centre of secondary euheral amphiboles is chemically very similar to the primary

ones (Mg/27Fe = 2.70; 100 Mg/Mg + 2Fe = 72.70) but at the borders the composition

becomes different; higher in Ti, Fe, Ca and lower in Si, Al, Mg, Na and K. Accordingly,

the Mg/i:Fe = 1.68; 100 Mg/Mg + £Fg = 62.64 ratios become smaller. As the

number of Ti per half unit cell becomes 0.82, it is no more a titaniferous pargasite but a

kaersutite. The traversing of a secondary amphibole crystal by electron beam shows clear

chemical zoning (Fig. 1).

The green spinel differs from the brown spinel of the lherzolite in having higher Al,

Ti and especially Fe, and smaller Mg and Cr, this last one becoming only a trace element.

In SOKOLOV'S classification the green spinel (Alf,J Fe% +

CTQ +

; Mgj-J Fell is a magne-

3 +

sianpicotite (Fe /Fe 2+

calculated from structural formula).

Because of its heterogeneity, the glass has been analyzed with wide electron beam

moved across the sample. It is highly oversaturated, high in Si, Al and K, low in in Na,

Mg.

Discussion

The Szigliget amphibolite/lherzolite composite xenolith is an extreme curiosity.

Strictly speaking, it has only one exact equivalent petrographically ; the

amphibolite type-LZA in lherzolite at Lherz (Pyrenees, France) described by

CONQUERE (1971). However, the geological environment is different; Lherz is an

alpino-type peridotite body that has been elevated high in the crust. Here we have

a very complicated vein system among which there are both complex and simple

veins. The complex veins may contain anhydrous rock types (pyroxenites without

amphibole) and amphibole-bearing rocks such as garnetiferous amphibole ariegite

or garnetiferous amphibole-bearing websterite. The different rock-types of veins

are arranged in a symmetric manner (CONQUÉRÉ 1971). Amphibolites ("lherzites"

in the French literature) which only contains essentialy hydrous minerals may

occur in two different manners : either in complex veins generally in a central

position, or as distinct simple veins cutting the host lherzolite. This last one may

again be one of the following two types: Amphibolites without mica (CONQUÉRÉ'S

type-LZA) and amphibolites with mica: type-LZB. Between the Szigliget amphibolite/lherzolite

composite xenolith and the type-LZA of the ultrabasic massif of

Lherz there is petrographically an astonishing similarity. In both cases the width

of the amphibolite veins are of the same order : the texture with signs of cataclysis,

the lack of evidence in favour of a cumulus origin, the proportions of its minerals,

the sharp contacts toward the host lherzolite are all identical. Even the occurrence

of small opaque inclusions is a common feature, like that of the green spinel:

however, this last one has only been detected in the type-LZB of the Pyrenees.

Another find, very similar to the Szigliget one, is described by DICKY (1968) from the

Kakanui (New Zealand) mineral breccia, which is a composite amphibolite/lherzolite

xenolith, like the Szigliget one, but the amphibolite is clearly of a LZB-type (60% amphibole,

38% phlogopite, 2% opaque).

From the amphibole-bearing xenoliths of the Grand Canyon (Arizona), BEST mentions

the presence of 7 amphibolite inclusions from basanitic lava. BEST'S sample (BEST

1973, Nor. 29, Fig. 9) is also a coarse-grained amphibolite of type-LZB. Amphibolites of the

Grand Canyon are thought to have originated in a somewhat different manner from those

of Lherz, judging from their larger size and cumulus fabric.

Very interesting mode of occurrence of amphibole, yet different from the former ones

and to a smaller extent that of phlogopite, apatite, and plagioclase, are described by VYTL-

SHTRE and TRASK (1971) from peridotite inclusions of Dish Hill, California. Among them

there are very thin amphibole selvages and veins, and interstitial amphiboles. A common

mode of occurrence of this last one is as thin mantles on spinel grains. (The author found


such araphibole-mantled spinel grains in a peridotite nodule from Marais de Limagne.) The

amphibole is thought to be a product unrelated to the original crystallization of the peridotite.

All the amphiboles from different localities treated above are chemically

more or less similar. They represent highly undersaturated olivine nephelinitic to

olivine melilite nephelinitic compositions. Contrary to expectation, the compositions

of the amphibole from the Szigliget xenolith is nearer to that of the type-

LZB from Lherz. The type-LZA has markedly higher 100 Mg/Mg+2Te (82.99)

than the type-LZB (70.25) or Szigliget (72.39). However, the Szigliget amphibole

differs from both in having a higher K content; K 20/Na 20 = 0.86 (Szigliget),

0.27 (LZA, Lherz), 0.50 (LZB, Lherz).

Unfortunately, the comparison with the amphibole of Kakanui composite xenolith

could not be executed, because of lack of chemical analysis. However, judging from optical

determinations DICKEY 1968) this amphibole must also be a titaniferous pargasite

or a kaersutite with a composition not much different from those mentioned above.

Besides the amphibole of type-LZB Lherz, that of the Grand Canyon amphibolite

is also very similar to the Szigliget amphibole, though it is also lower in K (K 20/Na 20 =

0.57) and slightly bigher in Al (100 Mg +ZFe = 73.92). The amphibole of lherzolite of

Siberia Crater, California (No. 2 inWILSHIRE & TRASK 1971) is more ferrous and less

magnesian similarly to the secondary amphibole of Szigliget (100 Mg/Mg + XFe = 63.90

Siberia Crater; 62.64 secondary amphibole Szigliget).

To reconstruct the probable physical conditions that existed at the time of

formation of the Szigliget amphibolite vein is not an easy task. The understanding

of stability relations of amphiboles is still incomplete. For example, kaersutites

of the same composition have been crystallized experimentally from nepheline

mugearite in the presence of 2 to 5 percent water at pressures ranging from 2.2

to 22.5 kbar (MERILL & WYLLIB 1975).

VARNE describes a hornblende lherzolite where the amphibole, a Ti-poor Naand

Cr-rich pargasite, is thought to be stable within a hydrous mantle to a depth

of 100 km or more (VARNE 1970). The amphibole is thought to be a primary phase

here in the lherzolite, in contrast to all occurrences that have been mentioned so far.

The amphibole-bearing material that intrudes lherzolite at Lherz, Kakanui,

Szigliget or elsewhere may be regarded as high pressure heteromorphs of nephelinitic-basanitic

lavas (BEST 1970, MASON 1968, VARNE 1968). However, certain

features of their chemistry may be due to processes such as subsolidus and wall-rock

reactions (BEST 1973).

On the basis of the surprising similarity between the amphibolite of Lherz

and that of the Szigliget xenolith, it may be concluded that their histories might

have been also similar to some extent. To the formation of highly undersaturated

nephelinitic liquids entrapped at depth, represented by the chemistry of amphibolites,

large scale differentation processes must be admitted. Rock-types originated

from differentiating hydrous liquids are excellently represented —• with possibility

to evaluate chronological order—-in the symmetric complex vein systems of theul

trabasic massif of Lherz. CONQUÉRÉ, using data of experimental work (KORNPROBST

1970, BOYD 1959, GREEN & RINGWOOD 1967, KTJSHIRO 1968, YODER & TILLEY

1962, O'HARA 1967), has concluded that in the hydrous adiabatic rising diapir

{a term of GREEN and RINGWOOD) an important partial melting took place at

about a pressure of 27 kbar, which had resulted in 20% liquid, probably an olivinericfi

tholeiite. With falling temperature and pressure, the anhydrous rock-rypes

crystallized (about 27-16 kbar), followed by amphibole-bearing rocks (about


Fig. 3. The Szigliget composite xenolith. — Fig. 4. Exolution lamellae of clinopyroxene

in orthopyroxene, Magyarbánya, North Hungary.

16-11 kbar). The last alkali-rich strongly undersaturated liquids would have been

crystallized as amphibolites in the lower level of the crust about 8 kbar.

It is evident that the vein systems of Lherz cannot serve as a precise model

for the conditions of igneous bodies at great depth below the Pannonian Basin.

However, here we have also evidences of an active diapiric rise of the upper mantle

(see in STEGENA et al. 1975) in the Pliocene. The Moho discontinuity is in an elevated

position at a depth of 22-26 km only (MITTTCH 1967). The heat flow is markedly

greater than the average value. Therefore I conclude that the Szigliget

amphibolite vein — like at Lherz in the Pyrenees — is a last product of the differentiation

of liquids, the origin of which is due to partial melting of hydrous rising

material from the upper mantle, and probably it crystallized at a pressure of 8-10

kbar. — In the Szigliget amphibolite, a partial remelting also took place, probably

due to subsequent rapid ascending in the basanitic lava. As the centre of the

secondary amphibole is chemically similar to the primary one, it may be concluded

that the remelting originated at a considerable depth.

However, the Szigliget composite xenolith is not the only petrological evidence

for upwelling mantle below Hungary. The examination of inclusions (mostly

4-phase lherzolites) has revealed some facts indicating the complex cooling history

of the inclusions (EMBEY-ISZTIN in prep.). First of all, the exolution lamellae

of clinopyroxene in enstatite (Fig. 4) can be mentioned. The reverse case is uncommon.

Furthermore, it seems probable that not only the clinopyroxene but the

spinel can also be an exolution product in the lherzolites. According to these textúrái

relationships the following reaction can be assumed:

Ca, Al-rich pyroxene —- enstatite -f-clinopyroxene -f- spinel. It is evident that

on the left of the equation the t must have been higher than on the right. According

to BEST (1975) the Ca, Al-rich pyroxene is stable at 1400 °C, NICOLAS et al. (1972)

assume also 1400 °C and 18 kbar. The lherzolites have re-equilibrated at 850-1050 °C

and at a pressure range of 10-18 kbar (EMBEY-ISZTIN in prep.). The mechanism

that transported these rocks from an environment of higher p, t to another of

lower p, t must have been a convection in the mantle.

In this regard, another interesting fact may be mentioned. Namely the position

of the Hungarian lherzolite «xenoliths in the p-t diagram is very instructive

(Fig. 2). One part of the lherzolites is on or near to the oceanic geotherm along with

lherzolites of Auvergne (Massif Central, France). Another part of the Hungarian

samples shows a clear departure from the oceanic geotherm (EMBEY-ISZTIN in


prep.). As the p becomes smaller (that is at shallower and shallower depth) the

t does not fall. Therefore, this picture may reflect an adiabatic diapiric rise, in the

sense of GREEN & RINGWOOD (1967).

References

BASU A. R. (1975): Hot-spots, mantle plumes and a model for the origin of ultramafic

xenoliths in alkali basalts. —• Earth and Planet. Sei. Lett., 28: 261-274.

BEST, M. G-. (1970): Kaeräutite peridotite inclusions and kindred megacrysts in basanitic

lavas, Grand Canyon, Arizona. —Gontr. Mineral. Petrol., p. 27-44.

BEST, M. G. (1975): Amphibole-bearing cumulate inclusions, Grand Canyon, Arizona and

their bearing on silica-undersaturated hydrous magmas in the upper mantle. — J.

Petrology, 16: 212-236.

BEST, M. G. (1974) : Contrasting types of chromium-spinel peridotite xenoliths in basanitic

lavas, Western Grand Canyon. Arizona — Earth and Planet. Sei. Lett., 23: 229-237.

BOYD, F. R. (1959): Hydrothermal investigation of amphiboles. — Researches in geochemistry

(Abelson P. H. ed.), London, p. 377-396.

CARTER, J. L. (1970): Mineralogy and chemistry of the earth's upper mantle based on

the partial fusion-partial crystallization model. —Geol. Soc.Am. Bull., 81: 2021-2034.

CONQUÉRÉ, F. (1971): Les pyroxenolite et les amphibolites associées aux lherzolites du

gisment de Lherz, Ariege, France : un exemple du role de l'eau au cours de la fusion

partielle de lherzolites. —Gontr. Mineral. Petrol., 33: 32-61.

DICKEY, J. S. (1968): Eclogitic and other inclusions in the mineral breccia member of

the Deborah volcanic formation at Kakanui, New Zealand, — Am. Mineral., 53:

1304-1319.

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Author's address: DR. ANTAL EMBEY-ISZTIN

Mineralogical Department

Hungarian Natural History Museum

H-1088 Budapest, Múzeum körút 14-16

Hungary

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