biostratigraphy and paleoecology of cretaceous/tertiary boundary in ...

BIOSTRATIGRAPHY AND PALEOECOLOGY OF 

CRETACEOUS/TERTIARY BOUNDARY IN THE 

SULAIMANI REGION, KURDISTAN, NE-IRAQ 

A THESIS 

SUBMITTED TO THE COLLEGE OF SCIENCE, UNIVERSITY 

OF SULAIMANI, IN PARTIAL FULFILLMENT OF THE 

REQUIRMENTS FOR THE DEGREE OF DOCTORATE OF 

PHILOSOPHY IN GEOLOGY 

By 

Khalid Mahmood Ismael Sharbazheri 

M. Sc. In Geology , Mosul University, 1983 

Supervised by 

Dr. Qahtan A. M. Al Nuaimy 

Assistant Professor 

Dr. Imad M. Ghafor 

Assistant Professor 

Jan. 2008 A.D 

Bafranbar. 2707 KU

III

IV 

Dedicated: 

To 

My Wife 

My Daughters 

And 

My Sons

V 

ACKNOWLEDGEMENTS 

I am deeply indebted to Dr. Qahtan A. Mohammed Al Nuaimy and Dr.Imad 

Mahmood Ghafor for their undertaking the task of supervising this 

dissertation and for offering many suggestions and corrections during all stages 

of the work. My best thanks to the Head of the Department of Geology Dr. Kamal 

Haji Karim and the Dean of the College of Science (Dr. Parykhan M. Jaf ), for 

their generous help and assistance throughout this work especially offering the 

available facilities . I would like to express my gratitude to the University 

presidency for providing the financial support for transportation (during 

fieldwork) and printing the draft and final copy of this work. 

I am indebted also to Dr. Rund Al Hammoody / Department of Geology, 

University of Mosul for her pioneering in providing me the internet key for 

application the catalogue and atlas of Paleocene planktonic foraminifera. 

My genuine thanks to my friends; Dr. Bakhtear Muhammad Ameen , Dr. Dler 

Hussen Baban , Mr. Musher Mustafa, Mrs. Razawa Hama Rasheed , Mr. Serwan 

Hama Ahmed , and Mr Jabar Muhammad from the Department of Geology, 

University of Sulaimani for helping me in the fieldwork and the software 

programming in this dissertation. 

My sincere thank goes to Prof. Dr. Martin Langer at the Institute for 

Paleontology, University of Bonn/Germany for offering available facilities in the 

library, the references and scanning electron microscope photo processing. Also 

I would like to express my gratitude to Prof. Dr. Basim Al- Qayim for his 

contributions and discussion during this work. 

Finally, I would like to express my special appreciation for my wife, Shina 

Darwesh, for her endurance during the preparation of this effort. 

Khalid 

Jan. 2008

VI 

Abstract 

The Cretaceous / Tertiary (K/T) boundary section, which crop out in the 

studied regions are located within the High Folded zone (Dokan and Smaquli 

area), Imbricated Zone (Sirwan valley, Barzinja and Qala Cholan area) in 

Northeastern Iraq. Is extended in northwest-southeast direction as narrow trend 

near and parallel to the Iraqi/ Iranian border. These units mainly consist of flysch 

and flysch type successions of thick beds of clastic rocks of Tanjero / Kolosh 

Formations in (Sirwan, Qulka and Gali sections) or flysch to molasses 

Tanjero/Red bed series (Swaiss group) in (Kato and Qishlagh sections). 

The study is specially focused on analysis of all the uncertain aspects of the 

boundary zones, such as lithostratigraphy, biostratigraphy, paleoenvironment 

reconstruction, paleoecology nature of contact, age determination, local and 

regional correlation in order to answer many of the questions raised naturally 

through different researches and studies since decades by different authors in 

and outside Iraqi regions about lithostratigraphic, biostratigraphic nature of the 

contact, age, paleoecology, paleoenvironment reconstruction, correlation with 

regional, continental and intercontinental similarities. 

The detail lithostratigraphic study achieved on the cropped upper most part of 

the Upper Cretaceous successions (upper part of Tanjero Formation) in Sirwan 

valley, Kato, Qishlagh And Qulka sections, with the lower most part of Kolosh 

Formation and Red Bed Series of the Early Tertiary, while in the Gali section 

(Smaquli area) the studied stratigraphic units include the upper part of Shiranish 

Formation, Shiranish-Tanjero transition unit, Tanjero Formation and Kolosh 

Formation. 

Eight biozones were recorded in the studied area, based on identified 

planktonic foraminiferal assemblages within uppermost part of Shiranish 

Formation, Shiranish-Tanjero transition unit (Reddish to pale brown succession), 

Tanjero Formation in Smaquli area (Gali section) and upper part of Tanjero 

Formation in all other studied sections, and also four biozones are recorded

VII 

within the lower part of Kolosh Formation (Lower Paleocene) in Smaquli, Dokan 

and Sirwan areas. 

The biostratigraphic correlations on the studied sections are based on 

planktonic foraminiferal zonations. The correlation showed a comparison 

between the biostratigraphic zones established in this study with other equivalent 

of the commonly used planktonic zonal scheme around the Cretaceous/Tertiary 

boundary in and outside of Iraq. 

The paleoenvironment of Cretaceous/Tertiary boundary sequences in the 

Sulaimani region, NE-Iraq, Kurdistan are determined by using foraminifera 

especially planktonic through Late Maastrichtian and Early Danian. Lithologically 

it is concerned with Tanjero and Kolosh Clastic Formations regionally, and 

Tanjero-Red Bed Series in the studied area. 

Paleobathymetric and paleoecological factors are studied through the 

distribution patterns of planktonic and benthonic foraminifera and include the total 

numbers of foraminiferal species, the diversity and statistical analysis of planktonic, 

benthonic forams, the Planktonic/Benthonic ratio and the Agglutinated/Calcareous 

ratio. 

The available data on distinguished planktonic foraminifera evidenced that 

the Cretaceous/Tertiary nature in the present study displays both gradual and 

sudden catastrophic extinction pattern approximately halve number in 

planktonic foraminiferal species before the K/T boundary and complete 

species extinction at or near the K/T boundary which indicates no Cretaceous 

planktonic foraminiferal survivorship into the Danian except (Guembelitria 

cretacea) and (Hedbergella monmothensis) in the lower most Danian. 

The recorded planktonic foraminiferal biozones in the studied area reveal 

the continuous sedimentation without evidence of any hiatus, in addition that the 

appearance of the new lower most Danian planktonic forams indicates gradual 

sedimentation especially at Smaquli, Dokan and Sirwan area, 

The sedimentation rate mean in graphical method by using biozone 

(m/myr) or years/meter was estimated for total studied stratigraphic

VIII 

successions from the upper part of Tanjero Formation and lower part of Kolosh 

Formation around K/T boundary, reveals the continuations and increasing the 

sediment accumulation rate without interruption or any gaps to be disclosed.

Subject 

1- Chapter One: 

IX 

LIST OF CONTENTS 

Introduction 

Page 

1 

1.1- Preface ................................................................................................................................................. 1 

1.2- Location and Geomorphology.............................................................................................................. 2 

1.3- Geological Setting …………………………………………………………………………………………….. 3 

1.4- general stratigraphy ............................................................................................................................. 5 

1.4.1- Upper Cretaceous formations …………………………………………………………………………….. 6 

1.4.1.1- Shiranish Formation ………………………………………………………………………………….….. 6 

1.4.1.2-Tanjero Formation …………………………………………………………………………………………. 8 

1.4.2- Lower Tertiary formations …………………………………………………………………………………. 10 

1.4.2.1- Kolosh Formation …………………………………………………………………………………………. 11 

1.4.2.2- Red Bed Series (Suwais Group) ………………………………………………………………………... 14 

1.5- previous biostratigraphic studies on Shiranish - Tanjero Formations ……………………………... 15 

1.6- Review on the Upper Cretaceous – Lower Tertiary Contact on Iraq ………………………………… 17 

1.7- Methodology ……………………………………………………………………………………………………. 19 

1.7.1- Studied Sections …………………………………………………………………………………………….. 19 

1.7.2- Samples collection and preparation …………………………………………………………………….. 20 

1.8 The aim of the Study ………………………………………………………………………………………….. 22 

2- Chapter Two: 

23 

Lithostratigraphy 

2.1- Preface …………………………………………………………………………………………………………. 23 

2.2- Lithostratigraphy of Sirwan sections ……………………………………………………………………… 23 

2.3- Lithostratigraphy of Kato section …………………………………………………………………………... 28 

2.4- Lithostratigraphy of Qishlagh section ……………………………………………………………………. 29 

2.5- Lithostratigraphy of Qulka section (Dokan area) ………………………………………………………... 33 

2.6- Lithostratigraphic of Gali section (Smaquli area) .............................................................................. 37 

3- Chapter Three: 

42 

Biostratigraphy 

3.1-Preface …………………………………………………………………………………………………………… 42 

3.2- Biostratigraphy ………………………………………………………………………………………………… 42 

3.2.1- Biostratigraphy of the Upper Cretaceous Formations……………………………………………… 47 

3.2.1.1- Globotruncana aegyptiaca Interval Zone (CF8) ……………………………………………………... 50 

3.2.1.2- Gansserina gansseri Interval Zone (CF7)…………………………………………………………….. 52 

3.2.1.3- Contusotruncana contusa Interval Zone (CF6)……………………………………………………… 54

3.2.1.4- Pseudotextularia intermedia Interval Zone (CF5)……………………………………………………. 55 

3.2.1.5- Racemiguembelina fructicosa Interval Zone (CF4)………………………………………………….. 60 

3.2.1.6- Pseudoguembelina hariaensis Interval Zone (CF3)…………………………………………………. 63 

3.2.1.7- Pseudoguembelina palpebra Interval Zone (CF2)…………………………………………………… 66 

3.2.1.8- Plummerita hantkeninoides Total Range Zone (CF1)……………………………………………….. 68 

3.2.2- Biostratigraphy of the Early Paleocene Formations………………………………………………….. 71 

3.2.2.1- (P0) Gumbelitria cretacea Interval Zone........................................................................................ 71 

3.2.2.2- ( Pá) Parvularugoglobierina eugubina Total Range Zone............................................................ 72 

3.2.2.3- ( Pá & P0 ) in Dokan and Sirwan valley.......................................................................................... 76 

3.2.2.4- (P1) Parvularugoglobigerina eugubina- Praemurica uncinata Interval Zone…………………… 77 

3.2.2.4.1- (P1a) Parvularugoglobierina eugubina – Subbotina triloculinoides Interval Subzone.......... 78 

3.2.2.4.2- (P1b) Subbotina triloculinoides- Globanomalina compressa/Praemurica inconstans 

Interval Subzone........................................................................................................................................... 79 

X 

4- Chapter Four: 

Depositional environment and paleoecology 

86 

4.1-Preface .................................................................................................................................................... 86 

4.2- Planktonic species diversity or species richness ……………………………………………………… 87 

4.3- Signor- Lipps Effect............................................................................................................................... 89 

4.4- Planktic/Benthic foraminiferal ratio and Benthic Foraminiferal Assemblage………………………. 90 

4.4.1- Maastrichtian...................................................................................................................................... 93 

4.4.2- Paleocene........................................................................................................................................... 100 

4.5- The Nature of Maastrichtian/Paleogene boundary………………………………………………………. 103 

4.6- Method of graphical correlation…………………………………………………………………………….. 105 

4.7- Sedimentation rate around Cretaceous/Tertiary boundary……………………………………………. 108 

6- CHAPTER FIVE 

conclusions 

112 

References 

122 

Plates 

List of Figures and Table 

Figure No. Title Page 

Fig (1.1) Location and Geological map of the studied area (modified from Sissakian, 2000) 4 

Fig (1.2) General stratigraphy of Cretaceous/Tertiary boundary at the studied sections 5

XI 

Fig (1.3) Upper Campanian - Maastrichtian facies map of Middle East (Buday, 1980) with 

general location of the studied area. 

7 

Fig (1.4) A: Modification of the time expanded stratigraphic column of Bellen et al (1959) to 

showing the gradational contact between Kometan and Shiranish Formations. 

B: original column of the above author without modification. (After Karim et al., 2007) 

Fig (1.5) Paleocene –Lower Eocene facies map of Middle east (Buday, 1980 with general 

location of the studied area. 

Fig (1, 6) Correlation of the previous biostratigraphic zonation on Cretaceous/Tertiary boundary 

in the studied region and different localities of Iraq. 

Fig (2.1) Lithostratigraphic column of studied section in Sirwan valley showing 

conventional lithologic constituent. 

Fig (2.2) Schematic geologic cross section of the studied section (Sirwan valley) 

8 

13 

18 

24 

26 

Fig (2.3) Image showing the Cretaceous/Tertiary contact between Tanjero- Kolosh Formations 

and three ridge forming conglomerate beds at the lower part of Kolosh Formation 

Fig (2.4) Image showing a- conglomerate bed. b- Systematic sampling within the upper part of 

Tanjero Formation, Sirwan valley 

27 

27 

Fig (2.5) Lithostratigraphic column of Kato section showing conventional lithologic 

constituent. 

Fig (2.6) Lithostratigraphic column of Qishlagh section showing conventional lithologic 

constituent. 

28 

31 

Fig (2.7) Schematic geologic cross section of the Qishlagh Section Qala Cholan area 32 

Fig (2. 8) (a) showing reworked fossils of large foram. of Loftusia, Omphalocyclus and 

Orbitoides in the transitional zone between Tanjero and Red Bed Series. 

(b) Showing the conglomerate bed of 3 m. thick, which contain reworked and dwarfed fossils 

at the base of Red Bed Series. 

33 

Fig (2.9) Schematic geologic cross section of the Qulka Section Dokan area 35 

Fig (2.10) Lithostratigraphic column of Qulka section in Dokan area showing 

conventional lithologic constituent. 

36 

Fig (2. 11) Photo image (a) Showing the conglomerate bed of 1.5 m. thick, which previously 

concluded to be the contact line of Cretaceous/Tertiary boundary in Dokan area by different 

authors. (b) Soft, friable and weathered intraformational conglomerate and pebbly sandstone 

from the lower part of Kolosh Formation, rich in reworked fossils of Corals. Gastropods, 

Pelecypods, Echinoids and Brachiopods 

37 

Fig (2.12) Schematic geologic cross section of the (Gali Section) Smaquli area 39 

Fig (2.13) Lithostratigraphic column of Gali section in Smaquli area showing conventional 

lithologic constituent. 40 

Fig (2.14) Image showing the graditional contact (change in color) between Shiranish Formation 

and Reddish to pale brown succession 

41

XII 

Table No. Title Page 

Table (3.1) Showing the number of planktonic and benthonic foraminiferal Genera and species 

identified in the studied sections from the Tanjero and Kolosh Formations 44 

Figure No. Title Page 

Fig ( 3.1) Biostratigraphic range chart of planktonic foraminifera at Cretaceous/Tertiary boundary, 

Sirwan area, (Sirwan section) 45 

Fig (3.2 ) Biostratigraphic range chart of benthonic foraminifera at Cretaceous/Tertiary boundary, 

Sirwan area, (Sirwan section) 46 

Fig (3.3) Biostratigraphic range chart of planktonic and benthonic foraminifera, Cretaceous 

/Tertiary boundary in Kato area (Kato section) 

48 

Fig (3.4 ) Biostratigraphic range chart of planktonic and benthonic foraminifera Cretaceous 

/Tertiary boundary, Qala cholan area, (Qishlagh section) 49 

Fig (3.5) Biostratigraphic range chart of planktonic foraminifera at Cretaceous/Tertiary boundary, 

Dokan area, (Qulka section) 56 

Fig (3.6 ) Biostratigraphic range chart of benthonic foraminifera at Cretaceous/Tertiary boundary, 

Dokan area, (Qulka section) 57 

Fig (3.7) (in 2 parts). – Part 1: Biotratigraphic range chart of planktonic foraminifera at Cretaceous 

/Tertiary boundary in Smaquli area (Gali section) 58 

Fig (3.7) Part 2:- Biostratigraphic range chart of planktonic foraminifera at Cretaceous/Tertiary 

Boundary in Smaquli area (Gali section) Continued. 59 

Fig (3.8) Biostratigraphic range chart of benthonic foraminifera at Cretaceous/Tertiary boundary in 

Smaquli area (Gali section) 

Fig (3.9) Genetic radiation, Phylogenetic relationship and Geologic ranges of Paleocene serial 

& low to high trochospiral microperforate wall structure planktonic foraminifera (From 

Olsson et. al, 2000) 

65 

73 

Fig (3.10) Genetic radiation, Phylogenetic relationship and Geologic range of Paleocene 

muricate, smooth walled, non-spinose and spinose concellate wall structure of 

trochospiral planktonic foraminifera (From Olsson et. al, 2000) 

Fig (3.11) Genetic radiation and phylogenetic reconstruction of the Early Paleocene 

microperforate planktonic foraminifera (From Liu & Olsson 1992) 

74 

75 

Fig (3. 12 ) Correlation chart showing the planktonic foraminiferal biostratigraphic zones of 

Upper Cretaceous (Maastrichtian) of the studied sections with the planktonic foraminiferal 

zonation commonly used in low, middle and high latitudes, in the new zonal scheme, and 

inside the Iraq. The age of planktonic foraminiferal datum events shown. (Modified from 

different authors) 

82 

Fig ( 3. 13) Correlation chart showing the planktonic foraminiferal biostratigraphic zones of 

Upper Maastrichtian/lower Danian of the studied sections with the planktonic foraminiferal 

zonation commonly used in low, middle and high latitudes, in the new zonal scheme. The 

age of planktonic foraminiferal datum events shown. (Modified from different authors) 

83

XIII 

Fig (3.14). High resolution planktonic foraminiferal biozone for the Maastrichtian and Early 

Danian (Cretaceous/Tertiary) boundary at Gali section (Smaquli area) and other studied 

localities. Note that this biozones significantly refines the resolution for the upper 

Maastrichtian, by replacing the Abathomphalus mayaroensis zone by four biozones. 

84 

Fig (3.15) Correlation of the previous Planktonic foraminiferal biostratigraphic zonation on 

Cretaceous/Tertiary boundary with the present study in the studied region and different 

localities of Iraq. 

85 

Fig (4.1) Planktonic foraminiferal species richness across the Tunisian continental shelf-slope 

based on data from the inner shelf Seldja section (Keller and other,1998) , middle shelf Elles 

section ( Abramovich and Keller,2002), and outer shelf to upper slope El Kef section (Li and 

Keller 1998c,). Note: The species richness increase with increasing depth across the shelf 

and is a function of available ecological niches and depth habitats (from Keller 2004) 

89 

Fig (4.2) Upper depth limits and paleobathymetric distribution of Upper Cretaceous and Lower 

Paleogene benthonic foraminifera (1): van Morkhoven et al.(1986), fold out, p.8, fig,5; (2): 

Speijer (1994), p. 84,fig.6; (3):Tjalsma and Lohmann (1983); (4): Widmark (2000), p.376; 

(5): Berggren and Aubert (1975); (6):R. Speijer, press. Comm., 2001; (7): Widmark and 

Speijer 1997a; (8): Kaminski et al.1988;(1c): modified after van Morkhoven et al.(1986), 

(from Alegret and Thomas 2001) 

92 

Fig (4.3): The main Foraminiferal parameters derived from the quantitative analysis with the 

proposed paleodepth curve in the Late Cretaceous/Early Paleocene succession in Gali 

section (Smaquli area) 

94 


proposed paleodepth curve in the late Cretaceous/Early Paleocene succession in Qulka 

section (Dokan area) 

96 


proposed paleodepth curve in the late Cretaceous/Early Paleocene succession in Sirwan 

section (Sirwan valley) 

97 


proposed paleodepth curve in the late Cretaceous/Early Paleocene succession in Qishlagh 

section (Qala Cholan area) 

99 

Fig (4.7: The main Foraminiferal parameters derived from the quantitative analysis with the 

proposed paleodepth curve in the late Cretaceous/Early Paleocene succession in Kato 

section (Barzinja area) 

101 

Fig (4.8): Graphic correlation shows the depositional rate of sediment between Smaquli and 

Qulka sections, Note: Change in the gradient in the early stage (dog-Leg) indicate highest 

rate of deposition in Qulka section than Smaquli section 

106 


Sirwan sections. Note: Change in the gradient in the early stage (dog-Leg) indicate highest 

rate of deposition in Sirwan section than Smaquli section 

107 

Fig (4.10): Graphic correlation shows the depositional rate of sediment between Qulka and 

Sirwan sections. Note: NO Change in the gradient o observed, a best-fit line constructed 

completely which indicate similar rate of deposition in Qulka and Sirwan section 

107

XIV 

Fig (4.11): Sedimentation rate of the Upper Cretaceous/Lower Tertiary Succession from 

gali section Smaquli area plotted vs. planktonic foraminiferal zonal scheme. The age (Time) 

of foraminiferal datum events shown (in MY) 

110 


Qulka section Dokan area plotted vs. planktonic foraminiferal zonal scheme. The age (Time) 

of foraminiferal datum events shown (in MY) 

110 


Sirwan section plotted vs. planktonic foraminiferal zonal scheme. The age (Time) of 

foraminiferal datum events shown (in MY) 

111

Chapter one 

Introduction 

CHAPTER ONE 

Introduction 

1.1- Preface 

The Tanjero, Kolosh and Red Bed Series basin, as a part of the Neotethys, 

was strongly deformed by the Alpine orogeny during their activity continued 

from Jurassic to Miocene where a huge thickness of sediments was 

accumulated. These successions are generally well exposed in different 

localities and different types of stratigraphic units in Zagros mountain regions 

such as the Balambo, Qulqula, Qamchuqa, Aqra-Bekhme, Kometan, Shiranish 

and Tanjero Formations, in addition to the Kolosh, Gercus Formations and 

Red Bed Series. The basins of these units have a complicated history of 

development and tectonics, this history was demonstrated by different 

characteristics of these stratigraphic units. 

Biostratigraphic analysis involves the interpretation of the nature of 

contact between Tanjero / Kolosh and Tanjero / Red Bed series, evolution, 

estimation the age of biozones by high resolution planktonic foraminiferal 

zonation and paleoenvironmental interpretation in accordance to planktonic 

and benthonic foraminiferal assemblages relationship by examining different 

geologic variables associated in this study. The geologic variables in the 

present study include the traditional and biostratigraphic analysis based on 

detail study of (5) exposed sections throughout the studied area. The detailed 

field and lab studies were directed towards planktonic foraminiferal zonation 

and paleoenvironmental interpretation to interpret architecture and 

biostratigraphic relation, in addition to the correlation and comparisons with 

similar and related studies achieved in this field regionally or globally. 

During the last decades the analysis of the Cretaceous/ Tertiary (K/T) 

boundary has been one of the most frequently mentioned topics in the earth 

science and several hypotheses have been suggested to explain the causes 

behind the global mass extinction in several groups of organism across this 

boundary, both marine and terrestrial forms were affected by the extinction 

event, which implies a multitude of causes for the Late Cretaceous extinctions, 

1

Chapter one 

Introduction 

such as plate tectonics' (continental rifting) the asteroid-impact, volcanisms, 

acid rains, iridium increase and CO 2 release and the resulting climate changes. 

The K/T boundary has been studied in different localities and regions in the 

world for different sense and purposes by different methods, such as tectonic, 

geochemical, stratigraphic, and biostratigraphic. The Cretaceous/ Tertiary 

Boundary in Kurdistan Region were not studied completely, especially in 

Sulaimani region which represents an important part of Zagros area. 

This study deals with the biostratigraphy and paleoenvironment of 

Cretaceous/Tertiary boundary sequences in the Sulaimani region, NE-Iraq, 

Kurdistan, depending on planktonic foraminifera through Late Maastrichtian 

and Early Paleocene. Lithologically it is concerned with Tanjero and Kolosh 

clastic Formations, Tanjero-Red Bed Series or Shiranish-Kolosh Formations 

regionally in the studied area. 

The study is specially concentrated on analysis of all the uncertain aspects 

of the formations, such as stratigraphy, biostratigraphy, paleoenvironment, 

paleogeography, basin analysis, age and regional geology. In the present 

study there are attempts to answer many of the questions raised naturally 

through different researches and studies since this decade by different 

authors in and outside Iraqi regions about stratigraphy, biostratigraphy, nature 

of the contact, age determination, paleoecology, paleogeographic 

reconstruction, and correlation with regional, continental and intercontinental 

similarities. 

1.2- Location and Geomorphology 

The studied area is located within the Imbricated Zone (proximal area) was 

represented by Qishlagh, Kato and Sirwan valley sections (High Folded 

Zones) and in the High and Low Folded Zones (distal area) represented by 

Qulka and Gali sections. The studied area is located within Sulaimani and near 

by Erbil Governorates in northeastern Iraq. It extended from Halabja town 

in southeast to Koy Sinjaq town in the northwest. This area is located between 

latitude (35 0 10 - ) and (36 0 30 - ) north and longitude (46 0 10 - ) and (44 0 40 - ) 

east, (Fig.1.1 ). The main outcrop of the studied sections is located at Smaquli 

2

Chapter one 

Introduction 

area north of Koy Sinjaq town by about 25 Km. This area is represented 

geomorphologically by mountain series and narrow or wide subsequent (strike) 

valleys trending northwest—southeast. The Mountains and valleys are 

dissected by, at least, two large consequent valleys and tens of smaller ones. 

The large valleys are those in which the Little Zab and Diala Rivers. The 

outcrops of the studied sections consist mainly of alternation of thick beds of 

flysch type marl, shale, marly limestone, claystone and sandstone of Tanjero- 

Kolosh Formations, ridge forming massive pale grey tough recrystalized 

occasionally dolomitized, siliclastic limestone of interfingering Aqra Formation 

and thick beds of red claystone, sandstone and conglomerate molasses type 

of Red Bed Series. 

1.3- Geological Setting 

The studied area is located at the southern boundary (in front) of the Zagros 

Thrust Belt, which is developed from the basin fill of the Neo-Tethys and 

colliding of the Iranian and Arabian plates (Buday 1980). Structurally, the 

studied area is located within two different zones. The outcrops of Qishlagh 

section ( Qala Cholan area), Kato section (Barzinja area) and Sirwan valley 

section (Halabja area) are located in the Imbricated Zone while that of Dokan 

section ( Dokan area) and Gali section (Smaquli area) are located exactly on 

the high folded Zone, as divided by Buday and Jassim (1987) (Fig.1.1 and 

1.2). 

Because of intense imbrications, the studied area in Qishlagh, Kato and 

Sirwan valley is characterized by obscured anticlines and synclines which 

have been stacked together as very thick and tight packages which were 

overturned toward southwest (Karim 2004). These imbrications include 

Qulqula, Balambo, Aqra, and other units such as Kometan, Shiranish, Tanjero, 

Kolosh Formations and the Red Bed Series. 

3

Chapter one 

Introduction 

Fig. (1.1) Location and geological map of the studied area (from Sissakian et al., 2000). 

4

Chapter one 

Introduction 

The Tanjero Formation underlies the Red Bed Series directly; Numan 

(2000) and Karim (2004) regarded the basin of latter formation and Kolosh 

Formations as Zagros Early Foreland Basin. In the Tagaran, Qala Cholan, 

Qishlagh, Sura Qqalat and Mawat area, the Tanjero Formation overlied by 

Red Bed Series graditionaly. Lawa et al., (1998), Karim (2004) and 

Sharbazheri, (2007). mentioned that the contact is gradational in some places 

and unconformable in others. 

Even as in the other three studied sections (Sirwan valley, Dokan and 

Smaquli Gali sections), the Tanjero Formation underlies directly the Kolosh 

Formation, and the nature of the contact explained briefly in subsequent 

chapters. 

1.4- General stratigraphy 

The general stratigraphy of the Cretaceous/Tertiary boundary of Upper 

Campanian-Maastrichtian and Paleocene-Lower Eocene cycles of the studied 

sections was shown in Fig (1.2), the studied sections in the Sulaimani area 

Fig (1.2) General stratigraphy of Cretaceous/Tertiary boundary at the studied sections. 

comparatively comprise wide distribution and show rapid lateral variation in 

depositional environment, consequently the present study will include several 

5

Chapter one 

Introduction 

lithologic units during Upper Cretaceous-Lower Tertiary. The following is a 

review on the previous studies about lithostratigraphy and biostratigraphy of 

the incorporated formations. 

1.4.1- Upper Cretaceous Formations 

Bellen et al., (1959), Ditmar et al., (1971),Kassab (1974 & 1975), Buday 

(1980),Karim (2004), Jassim & Goff (2006) and others defined the Upper 

Cretaceous cycles as the Upper Campanian –Maastrichtian sedimentary cycle 

based on the ages attributed to the Shiranish and Tanjero Formations at their 

type localities and the other similar rock units. Fig (1.3) 

1.4.1.1- Shiranish Formation 

The Shiranish Formation was first defined by Henson (1940) from the High 

Folded Zone of North Iraq, near the village of Shiranish Islam, Northeast of 

Zakho. The formation belongs among the most widespread units to the Upper 

Campanian- Maastrichtian cycle in North Iraq. It is represents distal portion of 

deeper foreland basin near by its neighboring Tanjero Formation too Karim 

(2004). The Formation, in its type area, comprises thin bedded argillaceous 

limestones (locally dolomitic) overlain by blue pelagic marls (Owen and Nasr, 

1958; Bellen et al., 1959, in Jassim & Goff. 2006). Al Qayim, (1992), divided 

the formation into three lithologic units in its type locality. 

The Shiranish Formation is also recognized in NE Syria (Dubertret, 1966 

and Brew et al., 2002 in Jassim & Goff. 2006). Maastrichtian foraminiferal 

limestone and marl in central Syria can be partly correlated with the Shiranish 

Formation (Ponicarov et al., 1967 in Jassim & Goff. 2006). Al Mutwali and Al 

Juboury (2005) studied Shiranish Formation from Sinjar area, northwestern 

Iraq and lithologically they are divided into three units; these units embrace an 

alternation of marl, marly limestone, limestone, sandy limestone and lenses of 

breccia. In SE Turkey the Shiranish Formation is equivalent to the Kermav 

marls of the Mardin area (Beer 1966 in Buday, 1980). Towards, the SE of Iran 

the formation is equivalent to the upper part of pelagic Grupi Formation 

(James & Wynd 1965), and the Upper Cretaceous Marl Group it is equivalent 

to Tayrat Formation from Kuwait and Upper part of Aruma Formation in Saudi 

6

Chapter one 

Introduction 

Arabia (Kent et al.,1951 in Jassim & Goff . 2006). Abdel-Kireem (1983 - 

1986b) studied the lithostratigraphy and paleoecology of exposed Shiranish 

Formation in Sulaimani-Dokan region, and subdivided the formation into two 

lithologic members. 

Fig (1.3) Upper Campanian- Maastrichtian facies map of Middle East (Buday 1980) with general 

location of studied area 

7

Chapter one 

Introduction 

The Shiranish Formation in the studied area overlies Kometan Formation 

conformably. This evidence was studied in the recent years and during 

fieldwork, new observations are recorded in many different localities that show, 

distinct character in opposite to previous studies, like gradational contact 

between the Kometan and Shiranish Formations. The gradation contact can 

be seen as the regular alternating of beds of white limestone and bluish white 

marl. Fig (1.4) (Karim et al., 2007). 

In the studied area the Shiranish Formation overerlain by Tanjero 

Formation graditionally and the contact is marked by the first appearance of 

gray sandstone or siltstone beds at the top of Shiranish Formation (bluish 

white marl and marly limestone) and starting of olive green lithology of Tanjero 

Formation. 

Fig. (1.4) A: Modification of the time expanded stratigraphic column of Bellen et al (1959) 

showing the gradational contact between Kometan and Shiranish Formations. 

B: Original column of the above authors without modification. (After Karim et al., 2007) 

1.4.1.2- Tanjero Formation 

According to Bellen et al. (1959), Tanjero Formation is first defined and 

described under the name of Tanjero Formation by Dunnington (1952). From 

the selected type section at Sirwan valley, 2 km to the south of Kani 

Karweshkan village, near Halabja town (Fig 1.1 ) and at the right bank of 

8

Chapter one 

Introduction 

Sirwan river (upstream of Dialla river). The type section comprises two 

divisions. The lower division comprises pelagic marl, and occasional beds of 

argillaceous limestone with siltstone beds in the upper part (Bellen et al. 

1959).The upper division comprises silty marl, sandstone, conglomerate, and 

sandy or silty organic detrital limestone, it interfingers with the Aqra Limestone 

Formation. The sandstone is composed predominantly of grains of chert and 

green igneous and metamorphic rocks. The conglomerates contain pebbles of 

Mesozoic limestones, dolomites, recrystalized limestones and radiolarian 

chert. The thickness of the formation is highly variable. The maximum 

thickness of the formation is about 2000 meters between Rowandus and 

Chwarta (Jassim and Goff 2006) 

The Tanjero Formation outcrop extends into Southeast Iran where it was 

referred to as the Maastrichtian flysch by (Kent et al., 1952 in (Jassim and Goff 

2006), and described as chert conglomerate by James and Wynd (1965). In 

Turkey, the Cretaceous parts of the Garmav Formation are equivalent to the 

Tanjero Formation (Buday 1980) 

In the study area, the formation has great variation in thickness which 

reflects tectonic activity and character of foreland depositional basin, in the 

Barzinja- Kato proximal area only the lower part of 50m remained, the other 

part is eroded and represented by incised valley and Kato conglomerate. 

(Karim, 2004). In the Smaquli area the thickness is reduced to 72m which 

represents the distal part of the basin and completely vanished by about 5Km 

south of Shaqlawa city. 

Al-Mehaidi (1975) discussed briefly the stratigraphy and tectonic of the 

formation within the Chuarta area and mentioned the occurrence of the Aqra 

Formation in the upper part of Tanjero Formation as a lens. AI-Rawi (1981) 

studied in detail the sedimentology, and petrology of the formation in selected 

sections (Sulaimani, Dokan and Rawandoz). He mentioned that the lower part 

at Sulaimaniya has shallow environment of deposition and concluded that the 

paleocurrent is toward northwest and flow parallel to the axis of the Tanjero 

trough. 

9

Chapter one 

Introduction 

Abdel-Kireem(1986 a) studied the formation within stratigraphy of Upper 

Cretaceous and Lower Tertiary of Sulaimaniya- Dokan Region, and suggested 

to remove the word "clastic" from the name of the formation and to add its 

lower part within the Shiranish Formation. Abdel-Kireem (1986b) studied 

planktonic forams and stratigraphy of Tanjero Formations, and subdivided the 

formation into three units according to the microfacies and lithofacies. 

Jaza (1992), recognized the turbidite and submarine fan (as depositional 

feature of the basin) during the sedimentary facies analysis of the formation in 

selected sections from Sulaimaniya district , and divided the rock body of the 

formation into sixteen lithofacies and suggested further detailed study of the 

formation to reconstruct depositional model for the whole basin and its relation 

to tectonics. Minas (1997), studied sequence stratigraphy of the formation and 

laid Tanjero Formation in deeper environment than Shiranish Formation. Al- 

Rawi and Al-Rawi (2002), studied the formation as turbidite example of flysch 

type in a northeast and north of Iraq, and concluded that the formation 

deposited in deeper environment, except the limestone beds, which are 

deposited in shallower condition. 

Karim (2004 and 2006); Karim and Surdashy (2005a, 2005b, and 2006) 

studied in detail the basin analysis, paleocurrent, tectonic history and 

sequence stratigraphy of Tanjero Formation. They indicated an unconformity 

at the lower part of Tanjero Formation which was represented by about 500m 

of boulder and gravel conglomerate, and found about four main incised valleys 

in the Sulaimani area during Maastrichtian. They mentioned that this 

conglomerate is deposited during sea level fall (lowstand system tract) 

1.4.2- Lower Tertiary Formations 

The lower Tertiary Formations are the most widespread and well known 

lithologic units in both surface and subsurface sections throughout almost all 

structural units of Iraq Figure 1.5 However, the Tertiary sediments have a 

small areal distribution in the High Folded, Imbricated, and Northern Thrust 

Zones Units. (Buday 1980) 

10

Chapter one 

Introduction 

Ditmar et al., (1971) subdivided the Tertiary Group into two sedimentary 

cycles, the Paleocene- Lower Eocene Cycle and the Middle Eocene cycle. The 

Paleocene- Lower Eocene units in the studied locations represented by thick 

sequence clastic rocks of Kolosh Formation and Suwais Group (Red bed 

Series) where it overlies the Tanjero Formation. 

1.4.2.1- Kolosh Formation 

The formation was first described by Dunnington (1952, in Bellen et al., 

1959) at Kolosh village, north of Koy Sinjaq in the High Folded Zone; Ditmar et 

al., (1971) mentioned the occurrence of Sinjar Formation too at its upper part 

in the type locality. The formation according to the original description consists 

of shale and sandstones composed of green rock, chert, and radiolarite. 

Bellen et al., (1959) described the following units from Kolosh type locality 

from the top to the base: 

1- 144m of limestone and marl with Miscellanea miscella, ostracods and 

miliolids; 

2- 30m of limestone with Dictyokathina simplex Smout, Lokhartia sp. 

Valvulinids, miliolids, ostracods; 

3- 113.5m of limestone and shales, red shales and sandstone with the same 

fossils but without Dictyokarhina simplex Smout; 

4- 6m of limestone with Saudia labyrinthia; miliolids and rotalids, 

5- 410m of blue shale and green sand. 

According to Ditmar et al., (1971), the following fossils were distinguished in 

the type locality: Ammodiscus incertus, Globorotalia angulata, Globigerina 

bulloides, Gyroidina soldanii, Loxostoma applinae, Nodosaria zippei, 

Nuttalides trumpyi, Pseudovalvulineria sp, Teredolites sp, Ovulites morlleti, O. 

cf elongate, Trinocladus perplexuz, Griphoporella arabica. Funcoporella 

diplopora, Cymoporella sp. 

Toward the west, the formation comprises distal lithologic character of 

mudstone, siltstone, and argillaceous limestone beds in subsurface sections at 

the Chamchamal, Taq Taq and Mushorah region. (Jassim & Goff, 2006) 

11

Chapter one 

Introduction 

The Kolosh Formation extends into Turkey, where it is represented by the 

clastic facies of the Garmav Formation (Altinli, 1966 in Jassim & Goff, 2006). 

In southeast of Iran, the upper part of the Amiran Formation of the (James and 

Wynd,1965) and the purple shales of the Lower Pabda Formation can be 

correlated with the Kolosh Formation. (Jassim & Goff, 2006) 

The biostratigraphy of Kolosh Formations were studied by Kassab (1972, 

1974, 1975, 1976 and 1978) and Kassab et al., (1986) at the type locality and 

other locations in north and northeast of Iraq. They recognized the planktonic 

foraminiferal Zones of Lowermost Middle Paleocene, represented by 

Globorotalia uncinata partial range Zone. Fig (1.6) 

Munim (1976) and Jacob (1978) recorded the Late Lower Paleocene at 

Zandour village, by recognizing Globorotalia trinidadensis Zone in Kolosh 

Formation. Al-Mutwali (1983) and Al-Omari et al., (1988), through their study of 

biostratigraphy of Kolosh Formation at Shaqlawa area, they recognized 

Globorotalia trinidadensis Zone which is indicated to the Late Lower 

Paleocene age. Fig (1.6) 

Al-Shaibani et al., (1986) during their stratigraphic analysis on the 

Tertiary-Cretaceous contact in Dokan area, (North Iraq), they placed the 

contact in Zone P3 ( Middle Thanetian), based on overlapping of the range of 

Globorotalia (T.) trinidadensis Bolli, 1957, and Subbotina velascoensis 

Cushman,1925 and other species. Fig (1.6) 

Raffo (1989) recorded the following Danian species Eoglobigerina 

appressa, Eoglobigerina edita praeedita, Globorotalia (Tu.) compressa 

planocompressa; Grt. (Tu.) archaeocompressa; Grt. (Tu.) rainwateri; Grt. (Tu.) 

sp. Type VII, during his study on planktonic foraminifera and biostratigraphy of 

Aaliji Formation and the nature of the contact with underlying Shiranish 

Formation at Mushorah well (No.1) (northwest Iraq) Fig (1.6 ) 

Ghafor and Karim (1999), studied the biostratigraphy of the upper part of 

Kolosh Formation from Sartaq-Bamo in northeastern Iraq and they recognized 

the Globororalia velascoensis Zone of Upper Paleocene age. 

12

Chapter one 

Introduction 

Fig (1, 5) Paleocene – Lower Eocene facies map of Middle East (Buday 1980) with general 

location of studied area 

13

Chapter one 

Introduction 

1.4.2.2- Red Bed Series (Suwais Group) 

The Series was first described by Bolton (1958) as a Suwais Red Beds (the 

name comes from Suwais village) in the Imbricate Zone about 20km to the 

north of Sangasar town and to the north of the Ranyia city. The lithology of the 

series at the type section is divided into four units; they are as follows from 

bottom to top: 

-Unit 1, Consists of different types of limestone beds (fossiliferous, detrital 

and conglomeratic limestone) 

-Unit 2, this unit consists of fine clastic (ferruginous red shale and blue 

siltstone) with some interlayer of limestone and conglomerate. The 

thickness of this unit is about 300m. 

-Unit 3, Polymictic conglomerate is containing boulder and blocks of 

limestones, chert, igneous and metamorphic rock fragments. 

-Unit 4, Composed of marly shale and sandstone with some conglomerate. 

Al-Mehaidi (1975), divided the Series at Chwarta area into four parts. 

Karim (1975) studied the Series paleontologically and claimed that the age of 

the series is Miocene. Buday (1980), reviewed the earlier studies about the 

series with illustration of the regional distribution and interpretation of different 

lithology. Al-Ameri et al., (1990), investigated the palynology of Unit one of 

Suwais Red Beds in Chwarta Area; they concluded that this unit deposited 

during Santonian. Lawa et al. (1998), recorded gradational contact between 

Red Bed Series and Tanjero Formation in Chwarta area; while Karim 

(2004), recorded both gradational and unconformable contact in different 

localities in Chwarta and Qandil area. 

Al-Qayim (2000) studied the sedimentation and tectonic environment of 

the Suwais Red Beds from northeast margin of the Arabian plate, and 

concluded that the unit indicates flysch type sequence with variable facies. 

Lawa 2004, in Al-Barzinjy, 2005 showed by sketch that the Red Bed 

Series have been deposited during Paleocene and in an intermountain basin 

above the sea level where the Kolosh Formation located to the southwest of 

the series, and separated both basins from each other by mountain ranges. 

14

Chapter one 

Introduction 

Al-Barzinjy (2005) during the study of stratigraphy and basin analysis of 

Red Bed Series at northeast Iraq, claimed that the depositional basin of lower 

Tertiary sequences of Red Bed, Kolosh, and Gercus Formations are the same 

and there were no paleohigh at the time of deposition to separate these units. 

1.5 - Previous biostratigraphic works on Shiranish –Tanjero Formations 

Bellen et al. (1959) has described briefly the distribution, age, lithology, 

fossil content, and stratigraphy of the Shiranish and Tanjero Formations, in 

addition to geographic distribution at different localities. 

The most representative fossils foraminifera of Shiranish Formation 

recorded in the type locality are: - Globigerina cretacea, Globotruncana 

tricarinata, G. lapparenti pendens, G. fornicata, G. stiwarti, G. Leopoldi, G. 

arca, G. gagnebini, G. gansseri, G. cf.rosetta, and Pseudotextularia spp., 

Anomalina ammonoides, Bolivina incrassata, Bulimina sp., Buliminella laevis, 

Bolivinoides dracco, Cibicides beaumontianus, Gyroidina 

naranjoinsis,Gyroidina sp., Marsonella oxycona, Nodosaria sp., Textularia 

cretosa.(Buday 1980) 

The fossils reported by (Bellen et al., 1959) in Tanjero Formation are:- 

Gryphaea vesiclaris, Hippurites cf.morgani, H, nov. spp., Prairadiolites 

cylindraceous, Turbo clathratus, vaccinates cf. gallopryincialis, Loftusia 

morgani, L. elongata, L. persica, L. nov.sp., Omphalocyclus macropora, 

Siderolites calcitrapoides, Globigerina cretacea, G. sp., Globigerinella cf. 

aspera, Globotruncana stuarti, G. leupoldi, G. lapparenti bulloides, G. 

lapparenti tricarnata, G. arca , G. fornicata, G. marginata, Gumbelina 

spp.,Pseudotextularea elegans, Pseudolithothamnium album, Trinocladus. sp., 

Ovulites sp. 

Two planktonic foraminiferal zones and five subzones are recognized by 

Kassab (1972, 1974, 1975c, 1975d, 1976b) and Kassab et al (1986) during 

their biostratigraphy study of the Shiranish and Tanjero Formations at their 

type localities and six other sections in north and northeast Iraq . They 

deducted the Late Campanian –Maastrichtian age to the both Formations in 

Iraq, these zones as follow from base to the top: 

15

Chapter one 

Introduction 

a- Globotruncana fornicata –stuartiformis-elevata-roseta- ventricoza Zone. 

1- Globotruncana calcarata-- elevata--aegyptiaca Subzone (Late Campanian) 

2- Globotruncana arca – tricarinata - subcircumnodifer Subzone (Early 

Maastrichtian) 

b - Globotruncana contusa- esnehensis- duwi Zone 

1- G. gansseri- bahijae- Gublerina cuvillieri Subzone (Middle Maastrichtian) 

2- Abathomphalus mayaroensis Subzone (Late Maastrichtian) 

3- Globotruncana falsocalcarata Subzone (Late Maastrichtian) 

Abawi et al., (1982) and Abdel-Kireem (1986a &b) included both formations 

within stratigraphy of Upper Cretaceous in northeast Iraq, and they recognized 

five planktonic foraminiferal subzones under two zones as follow from the base 

to the top: 

a- Globotruncana fornicata-arca-stuarti Assemblage Zone 

Globotruncana calcarata Subzone (Late Campanian) 

b- Globotruncana aegyptiaca –lapparenti-stuarti Assemblage Zone. 

1- Rugotruncana subcircumnodifer Subzone (Early Maastrichtian) 

2- Globotruncana gansseri Subzone (Middle Maastrichtian) 

3- Globotruncana contusa Subzone (Middle Maastrichtian) 

4- Abathomphalus mayaroensis Subzone (Late Maastrichtian) 

Al-Mutwali and Al-Jubouri (2005) determined the age of Shiranish 

Formation by Late Campanian—Late Maastrichtian through the biostratigraphy 

of the following biozones 

1- Globotruncana calcarata (Late Campanian) 

2- Globotruncanella havanensis- Roseta fornicata Zone (Early Maastrichtian) 

3- Globotruncana aegyptiaca Zone (Early Maastrichtian) 

4- Globotruncana gansseri Zone (Late Maastrichtian) 

Bakkal et al., (1993), studied biostratigraphy of Shiranish Formation in 

Higran area, and determined the age of Shiranish Formation as Middle —Late 

Maastrichtian, by recognizing two planktonic foraminiferal subzones of 

Globotruncana gansseri gansseri and Kassabiana falsocalcarata subzones 

under the Globotruncana contusa stuartiformis biozone. 

16

Chapter one 

Introduction 

Lawa et al. (1998) argued the interfingering carbonate layers in the upper 

part of the Tanjero Formation at Chwarta-Mawat area and concluded that 

these layers belong to Aqra Formation with Late Maastrichtian age according 

to existence of Abathomphalus mayaroensis Subzone. 

Sharbazheri (2007) estimated the age of unconformity within Tanjero 

Formation, by about (1.23 my) duration through thick succession of 500m 

conglomerate and red claystone layers at the lower part of Tanjero Formation 

at Chwarta area, depending on describing the following planktonic 

foraminiferal biostratigraphic zones from the base upward: Globotruncana 

aegyptiaca Interval Zone (CF8), Gansserina gansseri Interval Zone (CF7) 

Racemiguembelina fructicosa Interval Zone (CF4), Pseudoguembelina 

hariaensis Interval Zone (CF3) with missing zones of Contusotruncana 

contusa Interval zone (CF6) and Pseudotextularia intermedia Interval zone 

(CF5). 

1.6 – Review on the Upper Cretaceous- Lower Tertiary Contact in Iraq. 

The Upper Cretaceous and Lower Tertiary sedimentary rocks in Iraq have 

been the subject of numerous stratigraphic and paleontological investigations. 

Such sediments are well developed in both surface and subsurface exactly the 

exposed part at north and northeastern territory 

The Upper Cretaceous and Lower Tertiary boundary is marked by one of 

the most dramatic extinction of different groups of organism; especially the 

planktonic foraminifera, the recognition of the major paleoclimatic change 

during the late Maastrichtian has focused new attention on global climate 

changes and their effect on marine organism. 

In particular the last half million years of the Maastrichtian is increasingly 

recognized as a time of rapid and extreme climatic changes characterized by 

maximum cooling at about 65, 5 Ma, followed by (3-4 0 ) C greenhouse warming 

and major Deccan volcanic activity between 65.4 and 65.2 Ma. (Li & Keller, 

1998a) (Keller 2001) (Barrera, 1994; Courtillot et al., 1996, Hoffman et al., 

2000, in Keller, 2004) 

17

Chapter one 

Introduction 

Fig (1, 6) Correlation of the previous biostratigraphic zonation on Cretaceous/Tertiary 

boundary in the studied region and different localities of Iraq. 

18

Chapter one 

Introduction 

Dunnington (1955, 1957), recorded the indication of great gap in the 

stratigraphic column, in his biostratigraphic studies about the nature of the 

Cretaceous/Tertiary contact in Dohuk, Aqra and northern Iraq, evidenced by 

the period of great regression of the ocean during Late Maastrichtian and Early 

Paleocene time followed by the uplifting of the area due to the tectonic 

orogeny, consequently this region undergone the process of erosion and 

period of non deposition. This phenomenon is applied for almost greater area 

of Iraq, exactly in the region of the northern and northeastern part. 

Al-Omari (1970) during his study on foraminifera of Mesozoic and Cenozoic 

at wells Butmah-9 and Ainzala 16, 17 from the northwestern part of Iraq, 

confirmed that the Aaliji Formation overlies the Shiranish Formation 

unconformably. 

Other biostratigraphic studies carried out in Iraq and especially in the area of 

study are summarized in Fig (1.6). 

1.7 - Methodology 

1.7.1 - Studied Sections 

Five sections were selected for foraminiferal biostratigraphic study of the 

Cretaceous / Tertiary boundary (Fig1.1 and.1.2). The general stratigraphy and 

structural condition of these sections are represented either by photos or 

diagrams. These sections are as follow: 

1- Gali section: It is located within Smaquli area about 25 Km. north of Koy 

Sinjaq town on the northeast limb of Awagird mountain at plunging of Safeen 

anticline in the direction of southeast, at the latitude (36 0 10 - 51.3 = ) and 

longitude (44 0 36 - 40.8 = ) and for distance 1 km. south east of Gali village. 

(Fig. 1, 1 and 1, 2) 

2- Dokan section: Is directly located to the southwest direction of about 3 km 

from Dokan Dam along the left bank of Qulka valley. (Fig .1, 1 & 1,2). At 

latitude (35 0 56 - 22.0 = ) and longitude (44 0 56 - 13.6 = ) 

3- Qishlagh section: It is located directly north of Qala Cholan, 15 Km. west 

of Chwarta Town, at the latitude (35 0 43 - 69.2 = ) and longitude (45 0 29 - 

03.0 = ) (Fig.1.1 & 1. 2) 

19

Chapter one 

Introduction 

4- Kato section: This section is located at 8 km to the southeast of Chwarta 

town, (Barzinja area) Kato mountain, at latitude (35 0 40 - 39.1 = ) and longitude 

(45 0 37 - 25.7 = ) near Suerala village (Fig.1, 1 & 1, 2) 

5- Sirwan Section: located at the Sirwan valley, on the right bank of Sirwan 

river (upstream of Diyala river), (2) km to the south of Kani Karweshkan 

village, near Halabja Town at latitude (35 0 07 - 26.7 = ) and longitude 

(45 0 52 - 34.7 = ). Most of the base part of type section for Tanjero Formation 

was covered under water mass of Darbandekhan Dam. (Fig.1, 1 & 1, 2) 

1.7.2 - Samlpe collection and preparation 

All samples were collected from the studied sections at the field after 

removing the surface contaminated soil and trying to obtain fresh and un 

weathered materials. Samples were collected at interval range between (20 – 

50) cm at or near the Cretaceous / Tertiary contact and at interval of 50cm to 

3m away from the contact. 

572 samples from five sections (Figs. 4.1-7) were analyzed for planktonic 

and benthonic foraminifera, by using (50) gm from each sample. Three special 

techniques were chose for the preparation and extraction of foraminiferal 

content in this study: 

1- Acetic acid method: The sample here was broken down into small 

fragments of about 3 - 5 mm in diameter, placed in beaker. The small fragment 

(soaked) in acetic acid. The prepared solution termed as ethanoic acid solution 

CH 3 COOH, made up of (80%) acetic acid and (20%) H 2 O for the duration time 

between (1 – 6) hours. The proposed technique based on cold-disaggregating 

with acetic acid. The acetic acid causes a very slow reaction that 

disaggregates the rocks without destroying and corroding fossil content. This 

method firstly was used by (Lirer 2000). The time of desegregations varies 

with the type of rock (amount of % CaCO 3 ) ranged between 1 – 2 hours for 

marl , claystone and shale, 2 – 3 hours for shale and marly limestone, 4 – 6 

hours are sufficient for limestone, this indicates that the porosity and degree 

of lithification play an important role on disaggregation time. 

20

Chapter one 

Introduction 

2- Hydrogen peroxide method: Another preparation method was introduced in 

this research is hydrogen peroxide oxidation method,( H 2 O 2 ) , oxidizes organic 

mater and producing (CO 2 ) pressure in the pore spaces proved to be winning 

and it is the most favored method to separate foraminiferal test from the rock 

type of soft, friable, porous and permeable rocks. The method used H 2 O 2 

(concentration of 20 - 30% ) and water with duration time between 2 – 3 

hours. 

3-The third method is more classical and traditional preparation for extraction 

foraminifera from the rock matrix, in which the particles were boiled in water 

for 3 – 5 hours with addition of few grams of Sodium hydroxide ( Na OH) or 

Sodium carbonate (Na 2 CO 3) which produces CO 2 as well as crystals of salt 

within the pore spaces. 

-The disaggregated samples were washed under tap water through a 63-µm 

sieve until clean foraminiferal residues were recovered. Then to remove the 

residual encrustations and clay materials the residue is dipped again in beaker 

with water diluted desogen and placed into an ultrasonic vibrator for half hour. 

The use of ultrasonic cleaner proved to be successful in mechanical cleaning 

of individual specimens without breaking them. The final washed residue was 

dried in an oven at 50 C o or by using the sand bath, Planktonic and benthonic 

foraminifera are well preserved in the Smaquli area for both Upper Cretaceous 

and Lower Tertiary (Danian) forams, but in other sections the preservation is 

moderate, although original calcite shells are recrystallized in some samples 

of Sirwan section. 

For each sample about 200—300 specimen were picked from 

representative sample split. Population counts for each sample are based on 

random split, of specimens from 63 µm and 150 µm fraction respectively. 

Planktonic and benthonic foraminifera were picked from each sample and 

mounted. The remaining samples were used to searching for rare species. 

A- Laboratory analysis and scanning electron microscope photography 

were processed in the Institute for Paleontology, University of Bonn, Germany. 

21

Chapter one 

Introduction 

1.8 -The aim of the study: 

The aim of this study includes the following aspects: 

1- Complete and high resolution biostratigraphic zonation of the sections in 

the studied area. 

2- Regional biostratigraphic correlation of the sections within the area of the 

study and global correlation with other similar sequences 

3- Indicating the age of the sequences, by using the new zonal scheme and 

the age of planktonic foraminiferal datum events with correlative and relative 

methods. 

4- Depositional and paleoenvironmental study of the units based on sequence 

analysis of the formations along the studied section. 

5- Paleogeobathymetric interpretation of the studied sections. 

6. To establish the relations between the Red Bed Series and 

contemporaneous Kolosh Formation in the high and low folded zones. 

7- The nature of the contact between Late Maastrichtian and early Paleocene. 

8- Interpretation and determination of depositional rate and Graphical 

correlation between the studied sections. 

22

Chapter Two 

CHAPTER TWO 


LITHOSTRATIGRAPHY 

2.1-Preface 

In this chapter, a detailed study of the exposed uppermost part of the 

Upper Cretaceous successions (upper part of Tanjero Formation) and the 

Early Tertiary (lower most part of Kolosh Formation and Red Bed Series) were 

carried out in Sirwan valley, Kato, Qishlagh, Dokan and Gali section (Smaquli 

area). The studied stratigraphic sections include the upper part of Shiranish 

Formation, (Shiranish-Tanjero transition unit), Tanjero, Red Bed Series and 

Kolosh Formations. 

2.2- Lithostratigraphy of Sirwan section 

The studied section in Sirwan valley represents the uppermost part of 

Tanjero Formation and the lower part of Kolosh Formation, only 255m from 

the upper portion of Tanjero Formation were studied from the rest of (1500 m.) 

thickness and 65m from the lower part of Kolosh Formation, including the 

description and detailed lithologic constituent, and fieldwork investigation is 

inferred and shown in figs (2.1, 2.2, 2.3). The most characteristic lithologic 

component of Tanjero Formation comprises alternation of bluish marl, marly 

siltstone, dark grey weathered sandstone, pebbly sandstone, dark grey shale, 

sometime organic rich shale, and seven weathered friable intraformational 

conglomerate beds distributed along this interval, they range in thickness from 

0.5m to 2m, the pebble component of these conglomerate beds consists of 

chert, limestone, and metamorphic particles Fig (2.4a). The lateral distribution 

of conglomerate beds ranges between 200 – 2000m. 

23

Chapter Two 


Fig (2.1) Lithostratigraphic column of studied section in Sirwan valley showing lithologic 

characters. (Not to scale, the thickness shown on each portion of discussion) 

24

Chapter Two 


The thickness, alternations between fine and coarse sediments, with 

different distinctive lithologic composition and abundant reworked high 

diversity species richness of radiolarian microfossils, silica sphere and 

microtectites?, reveal that these sediments were eroded and derived from 

short distance of hinterland source area of Qulqula Formation in the eastern 

side of the Tanjero foreland basin, and great deformation during later phases 

of the Laramide orogeny along the Arabian and Iranian plate margin. The 

foraminifera commonly represented in this interval of Tanjero Formation with 

three diluted foraminiferal survivorships, both planktonic and benthonic 

moderately preserved, restricted to fine clastics of marl, shale, marly limestone 

and clay siltstone, without any interruptions of deposition evidenced by 

continuation of foraminiferal biozones. It is worthy to mention that the 

intraformational conglomerate beds were formed by submarine fans during 

cyclic pulses of tectonic activity (Karim 2004). 

The Lower Tertiary lithostratigraphic unit is represented by Kolosh 

Formation which overlies the Tanjero Formation marked by 3m thick of 

conglomerate bed at the base, Figs (2.1, 2.2 2.3), which is in the lithologic 

characteristic point of view, while the biostratigraphic investigation results in 

this criterion indicate the most probable new condition of conformable contact. 

Only 65m of the lower part of Kolosh Formation investigated. The most 

characteristic lithologic component of Kolosh Formation comprises alternation 

of dark grey shale, bluish green marl, organic rich shale, with thin layer of 

siltstone, occasionally intervened by thin marly limestone layers and fine 

weathered sandstone, and three ridges forming diagnostic pale grey yellowish 

slightly weathered conglomerate beds distributed vertically along the lower 

part of the Kolosh Formation, with the thickness of 3.0m, 10.0m and 13m, 

respectively Fig (2.3). The distribution of foraminiferal content was recorded 

from twenty samples from sample 185 to sample 205 after the Tanjero- 

Kolosh contact by 14m thickness, which indicates barrens from foraminifera, 

otherwise the reworked radiolarians frequently observed in all samples of 

Kolosh Formation with rare reworked planktonic foraminifera of Tanjero 

Formation. 

25

Chapter Two 


Fig (2.2) Schematic geologic cross section of the studied section (Sirwan Valley) 

26

Chapter Two 


Fig (2.3) Image showing the Cretaceous/Tertiary contact between Tanjero- Kolosh Formations, 

Sirwan valley section and three ridge forming conglomerate beds at the lower part of Kolosh 

Formation 

As mentioned above, 

the activations of Laramide Orogeny along the 

Arabian and Iranian plate margin and great deformation during later phases 

were still continuous for the period of lower Tertiary (Paleocene) time (Karim 

2004). Moreover, the Kolosh Formation was overlained by Sinjar Formation 

gradually in the studied sections and marked by the regular change from fine 

clastic sediment of Kolosh Formation to non clastic limestone beds of Sinjar 

Formation. 

Fig (2.4) Image showing a- conglomerate bed within upper part of Tanjero Formation, Sirwan 

Valley. b- Systematic sampling within friable greenish grey silty marlstone of upper part of 

Tanjero Formation, Sirwan Valley 

27

Chapter Two 


2.3- Lithostratigraphy of Kato section 

The Kato section is located in Barzinja area, lithostratigraphically includes 

the upper part of Tanjero Formation and the lowermost part of Red Bed 

Series. The lower part of Tanjero Formation was previously studied by 

Sharbazheri (2007) in order to determine the age of the barren zone belonging 

to the 500m intraformational Kato Conglomerate which estimated by (1.23 

m.y). Only 98m of remaining part from Tanjero Formation have been 

studied in this section, with 12m from the lower part of Red Bed Series, the 

description and lithologic constituent and fieldwork investigation is inferred as 

shown in fig (2.5). 

Fig (2.5) Lithostratigraphic column of Kato section showing conventional lithologic 

constituent. (Not to scale, the thickness shown on each portion of discussion) 

28

Chapter Two 


In the Kato section Tanjero Formation is underlained by Shiranish 

Formation gradationally, as a rule the contact is marked at the first appearance 

of gray sandstone or siltstone beds at the top of Shiranish Formation. The 

Red Bed Series overlies the Tanjero Formation conformably with a transitional 

contact. The studied Cretaceous part in Kato section is divided into three units. 

Unit one comprises 40m of thick bedded succession of fossiliferous limestone 

and interbedded calcareous shale, the limestone forming a ridge of massive 

pale grey, tough, recrystallized, occasionally dolomitized, and characterized by 

several bands rich in rudist, gastropods, pelecypods, brachiopods, and other 

macro and microfossils. This unit was mentioned previously as interfingering 

Aqra limestone by Al-Mehaidi (1975) and Lawa et. al., (1998). The Aqra unit is 

overlained by 35m of alternation of thin bedded pale grey limestone, grey 

shale, marl, friable sandstone and calcareous fossiliferous sandstone with 

claystone and detrital fossiliferous limestone of second unit (Tanjero 

Formation). The third unit represents a transitional interval between Tanjero 

Formation and Red Bed Series; it comprises 23m of alternation of thin bedded 

pale gray unfossiliferous limestone, olive green sandstone, red clay, friable 

reddish sandstone, siltstone, and detrital sandy reworked fossiliferous 

limestone at lower part, and dark organic rich shale bed of 20 cm thickness at 

the base of this interval. The lower part of the Red Bed comprises alternation 

of thick bedded, red claystone, friable red bed of sandstone and siltstone, with 

lenses of conglomerate. The contact placed on the line when the olive green 

colour of sediment is vanished and the appearance of completely red colour of 

sediment and conglomerate beds. 

2.4 - Lithostratigraphy of Qishlagh section 

The exposed rocks of Qishlagh section appeared in Qala Cholan area figs 

(2.6, 2.7) which includes the upper part of Tanjero Formation and the lower 

most part of Red Bed Series, the lithologic nature comprises of 45m of flysch 

type of Tanjero clastic sediments with dark grey to olive green marl, shale, and 

bluish white calcareous marl and thin layer of fossiliferous friable sandy 

limestone intervened by streak of limestone at the base of this interval, this 

unit followed by 115m of interfingering Aqra Limestone which consists of 

29

Chapter Two 


medium to massive well bedded ridge forming recrystalized pale grey 

limestone and sandstone to silty limestone occasionally dolomitized rich in 

rudist and other macro and microfossils intercalated by with beds of shale and 

calcareous shale at the lower and upper part of this interval. The Aqra 

Limestone interval overlained by 67m of Tanjero Formation with alternation of 

bluish white marl, marly siltstone, thin bedded recrystalized fossiliferous 

limestone and weathered pale grey friable sandstone layer with some pebbly 

sandstone, clay ball and pillow structure. 

The third unit of this section is transitional zone 35m of clastic increasing 

upward consists of reddish weathered friable sandstone pebbly sandstone 

rich in reworked Loftusia, Omphalocyclus and Orbitoides fig(2.8a) at the base 

and followed by alternation grey shale, marl, friable detrital sandy limestone 

with purple to reddish claystone, and two conglomerate beds at the upper part 

of this interval, the conglomerate genetically comprises igneous, metamorphic 

and sedimentary origin of the pebbles and they extended laterally for limited 

short distances. This interval is characterized by shell debris of macrofossils 

such as solitary corals cyclolites, echinoids, dwarfed gastropods, and 

pelecypodes.The transition interval overlained by typical molasses of Red Bed 

Series in this section marked by 3m of friable brownish weathered 

conglomerate of metamorphic and sedimentary pebbles and complete reddish 

color (fig 2.8b) with reworked dwarfed fossils of corals, brachiopod, echinoid, 

gastropod and pelecypods, followed by red beds of claystone, sandstone, 

pebbly sandstone. It is important to mention that in addition to Kato and 

Qishlagh sections, other three preliminary outcrops were taken into 

consideration for sampling on Tanjero/ Red Bed contact like (Zardabee, 

Tagaran and Shakha Sur) sections in order to get high foraminiferal 

survivorship recovery, but it proved useless result from the foraminiferal 

recovery point of view. 

30

Chapter Two 


Fig (2.6) Lithostratigraphic column of Qishlagh section showing lithologic characters. 

(Not to scale, thicknesses shown opposite each unit) 

31

Chapter Two 


Fig (2.7) Schematic geologic cross section of the Qishlagh locality in Qala Cholan area 

32

Chapter Two 


Fig (2. 8) (a) showing reworked fossils of large foram. of Loftusia, Omphalocyclus and 

Orbitoides in the transitional zone between Tanjero and Red Bed Series. (b) Showing the 

conglomerate bed of 3 m. thick, which contain reworked and dwarfed fossils at the base of Red 

Bed Series. 

2.5 - Lithostratigraphy of Qulka section (Dokan area) 

The measured part of studied section covered 163m of upper part of 

Tanjero Formation and 54m from the lower part of Kolosh Formation. The 

detailed stratigraphic section is shown in Figs (2.9, 2.10, & 2.11) on both side 

of conglomerate bed, which formerly supposed to be the contact or key marker 

for Cretaceous/Tertiary boundary in the studied area by different authors. The 

well exposed rocks of studied section of Tanjero Formation at Qulka section 

represented by 63m of olive green to pale grey marl and bluish white 

calcareous marl intervened by streak of limestone veins and 3m dark grey to 

olive green soft, friable sandstone occasionally with siltstone, clay ball and 

pillow structure at the middle part of this interval. Followed by 59m of 

interfingering Aqra Limestone unit which consists of well bedded ridge forming 

recrystalized pale grey to yellowish limestone and sandstone to silty limestone 

occasionally dolomitized intercalated by thin beds of shale, calcareous shale, 

marl and sandstone beds through this interval. The Aqra Limestone interval in 

this section varies from its equivalent at Qishlagh and Kato sections, by very 

low frequency of macrofossils and short lateral distribution. The interfingering 

Aqra limestone unit overlained by 41m of Tanjero flysch type emergence again 

by alternation of olive green to dark grey calcareous shale, marl, thin bedded 

sandy limestone ,friable weathered sandstone, some pebbly sandstone bluish 

33

Chapter Two 


white marl, marly siltstone, thin bedded recrystalized limestone and with clay 

ball and pillow structure. In this section, it is significant to mention that there 

are 3 conglomerate beds at the upper part of this unit, with the thickness of 

(0.5 m., –1.5 m., – 0.2 m.) respectively, the conglomerate bed with thickness 

of 1.5m is previously concluded to be the marker bed of Cretaceous/Tertiary 

boundary at studied section by different authors, Fig (2.11a). Whereas the 

negate event is that the exact Cretaceous/Tertiary contact comes after 14m 

above the previously mentioned contact, without any obvious change in 

lithologic characters between Tanjero and Kolosh Formations at sample No. of 

K20 with the first appearance of Paleocene index foram. taxon .and 

disappearance of the Upper Cretaceous planktonic foraminifera of 

Globotruncanids, Heterohelicids and Rugoglobigerinids. The contact line 

placed at the base of friable, soft and weathered fine sandstone and silty 

sandstone of (5m.) thickness with dilution of foraminiferal content by abrupt 

change and without more Cretaceous planktonic foraminifera, and the 

recognition of the major paleoclimatic transform during the late Maastrichtian 

has focused new attention on climate changes and their effect on marine 

organisms, this was reflected on foraminiferal survivorship in the studied area. 

The Kolosh Formation consists of 5m soft, friable, weathered sandstone, 

siltstone at the base, followed by dark grey shale, olive green marl and organic 

rich shale alternate with thin layer of siltstone, fine sandstone occasionally 

intervened thin marly limestone layers, and 2m of sandstone, pebbly 

sandstone and friable conglomerate Fig (2.11b) rich in reworked fossils of 

solitary corals, and small gastropods, pelecypod and brachiopods at the 

middle part of studied interval. 

34

Chapter Two 


Fig (2.9) Schematic geologic cross section of the Qulka Section in Dokan area 

35

Chapter Two 


Fig (2.10) Lithostratigraphic column of Qulka section in Dokan area showing lithologic 

characters. (Not to scale, the thickness shown on each portion of discussion) 

36

Chapter Two 


Fig (2. 11) Photo image (a) Showing the conglomerate bed of 1.5 m. thick, which is previously 

concluded to be the contact line of Cretaceous/Tertiary boundary in Dokan area by different 

authors. (b) Soft, friable and weathered intraformational conglomerate and pebbly sandstone 

from the lower part of Kolosh Formation, rich in reworked fossils of corals. gastropods, 

pelecypods, echinoids and brachiopods. 

2.6 - Lithostratigraphy of Gali section (Smaquli area) 

The well exposed rocks of measured part of studied Gali section, in 

Smaquli Mountain area covered 15m of the upper most part of Shiranish 

Formation, then 74m of the reddish to pale brown succession (Shiranish- 

Tanjero transition unit), 72m Tanjero Formation and 49m Kolosh Formation 

and 10m of the lower most part of Gercus Formation. The detailed 

lithostratigraphic section is shown in Figs (2.12, 2.13, and 2.14). 

In the studied section, the reddish to pale brown succession (Shiranish- 

Tanjero transition unit) consists of 74m alternation of thin well bedded 

fossiliferous reddish to pale brown clay, marl alternate with thin reddish shale 

and papery shale intercalated by thin pale brown some time to pale grey 

calcareous marl of 5cm to 10cm thickness from the base to the top of this 

interval. Throughout the studied area the reddish to pale brown succession 

(Shiranish-Tanjero transition unit) is underlained by Shiranish Formation. It is 

likely forming a normal stratigraphic boundary of conformable gradational 

contact from bluish white marl and marly limestone of Shiranish Formation to 

the first appearance of reddish to pale brown clay or marl beds of the 

transitional unit Fig (2.14). 

37

Chapter Two 


The upper contact of the red unit marked by starting of olive green and dark 

grey lithology with the first appearance of 20cm hard well bedded sandstone at 

the base of Tanjero Formation. The Tanjero Formation is represented by 72m 

and subdivided lithologically into three distinct units based on field observation 

Figs (2.12, 2.13) .These three units are described briefly as follows from the 

base to the top. 

- Unit A: 24m thick consists of olive green to dark grey shale alternate with 

grey marl and claystone , with three layers of hard, fine to medium grain 

sandstone at the base of 20cm thickness, middle part of 15cm thickness and 

the upper part of 10cm. thickness. 

- Unit B: 20m Consists of alternation of thin olive green beds of marl, dark 

grey organic shale, papery calcareous shale and thin limestone beds of 3-6 cm 

thickness, repeated in cyclic way every two meter in this interval and two 

limestone beds of 20cm thickness at the middle and the upper part of this unit. 

-Unit C: 28m Consists of dark organic papery shale and interlayred by thin 

beds of dark grey marl with oily impregnated friable soft and weathered pale 

brown three sandstone beds of 3m , 1.8m and 1m thickness at the upper part 

of this unit respectively. 

The overlying formation is Kolosh Formation of 49m thick consists mainly of 

dark grey organic rich shale alternate with marl and thin layer of siltstone and 

hard sandstone beds of 5cm to 10cm thickness, occasionally intercalated with 

thin marly limestone layers and 5 red claystone beds at the last 10 meters of 

the upper most part of Kolosh formation, which starts from 30 cm to 2m 

respectively. 

38

Chapter Two 


Fig (2.12) Schematic geologic cross section of the Gali section in Smaquli area 

39

Chapter Two 


Fig (2.13) Lithostratigraphic column of Gali section in Smaquli area showing conventional 

lithologic constituent. (Not to scale, the thickness shown on each portion of discussion) 

40

Chapter Two 


Fig (2.14) Image showing the graditional contact (change in color) between Shiranish 

Formation and Reddish to pale brown succession 

The Kolosh Formation overlained by the Gercus Formation, the contact is 

seems to be conformable by lithologic evidence of graditional change from 

dark grey organic rich sediments of Kolosh Formation to red, purple mudstone, 

sandstone, gritty marl, pebbly sandstone and conglomerates. The contact 

placed on the line where the sediment colour mainly began with red lithology. 

paleontologically there were no significant fossils recorded in this interval of 

lower most part of Gercus Formation in which six samples were studied for 

both foraminiferal and palynomorphs evidence. 

41

Chapter Three Biostratigraphy 

CHAPTER THREE 

BIOSTRATIGRAPHY 

3.1: Preface 

The comprehensive studies of planktonic foraminiferal biostratigraphy during 

the last five decades have proved to be more useful and more accurate way 

among the large number of micropaleontological branches, especially than 

benthonic foraminifera for regional, interregional and intercontinental correlation 

over the Cretaceous and Tertiary periods. A number of datum events and series 

of zonation for different regions have been proposed. ( e.g. Bolli 1966; Postuma 

1971; Blow 1979; Caron 1985; Berggren & Miller 1988; Berggren et al.,1995; 

Berggren & Norris 1997; Keller 1988 , 2002, 2004; Keller et al 1995; Li & Keller 

1998a,b; Abramovich et al., 2002; and Olsson et al., 2000). That is due to wide 

geographic distribution, their occurrence in the deeper marine environment, 

short geologic range as well as known morphological feature of the index 

species. 

3.2: BIOSTRATIGRAPHY 

The samples which contain microfossils collected from the studied sections 

yielded rare, predominant to extremely abundant groups, bad to well preserved, 

according to different localities of studied sections. It is looked as the radiation 

stage of biotic evolution and high diversity of globotruncanids, rugoglobigerinids, 

globigerinids and heterohelicids planktonic foraminifera in Smaquli area (Gali 

section), high to moderate occurrence in Qulka section (Dokan area), moderate 

in Sirwan section and low occurrence, low diversity in both Kato and Qishlagh 

sections with moderate calcareous and agglutinated benthonic forams in general 

Table (3.1), (Figs.3.1 – 3.8). The foraminifera occurs continuously in the 

sedimentary succession of the all studied sections, generally shows incessant in 

sedimentary sequence without any interruptions, except of Sirwan section which 

is evidenced by three diluted intervals of foraminiferal survivorship in the studied 

upper part of Tanjero Formation, and the fourth one at the base of Paleocene 

just after the extinction catastrophe of organism at the uppermost part of 

Maastrichtian. The Upper Maastrichtian –Lower Paleocene interval in general 

attracted particular attention because of the foraminifera is relatively moderate 

42


and is mostly well preserved, especially in Smaquli area which showed highest 

species diversity than other sections, at the contact of Cretaceous/Tertiary 

boundary 

Table 3.1 shows the statistics of identified planktonic and benthonic 

foraminiferal genera and species belonging to all studied localities were 

recorded from the studied sections (Figs. 3.1 - 3.8). The planktonic foraminifera 

of globotruncanids, heterohelicids, rugoglobigerinids, globigerinelloidids and 

globigerinids are the most prevalent planktonic forams in the studied area and 

they show the best indication of typical Tethyan fauna type. 

The comprehensive and motif plan in this work was deduced from the 

recently planktonic foraminiferal zonation and correlation for the sediments in 

tropical/subtropical regions, are widely based on that of Berggren & Miller 

(1988), Li and Keller (1998a & b), Liu and Olsson (1992), Berggren et al., 

(1995), Berggren & Norris (1997), Olsson et al., (2000), Arenillas et al., (2001), 

Elnady & Shahin (2001), Samir (2002), Abramovich et al., (2002), Keller (2002) 

and (2004), Abramovich and Keller (2003), Obaidalla (2005), Smit (2005), and 

Sharbazheri (2007), and used exclusively as the biostratigraphic framework in 

this study. Fortunately, this zonation proved satisfactory successful results 

essentially achieved in different localities of the world. 

Li and Keller (1998a) subdivided the Maastrichtian zonal scheme into eight 

Cretaceous Foraminiferal (CF) zones labeled (CF8) to (CF1) from the base to 

the top; this new biozonation provides accurate and significantly higher 

biostratigraphic resolution than previous zonal schemes. They calibrated their 

ranges to the paleomagnatic time scale in the DSDP Site 525A, and on 

Tunisian sections (Li and Keller 1998b), their age estimation were also 

correlated with magnetochron ages by Berggren et al (1995), and consequently 

the criteria for age estimation and determination rate of sedimentation can be 

proved easily through biostratigraphic correlation and datum event comparison. 

The genetic classification and identification used in this study for the 

Maastrichtian and Lower Paleocene sediments respectively follow that of Boli 

(1966), Postuma (1971), Kassab (1974), (1975d) and (1976), Masters (1977), 

Blow (1979), Jenkins and Murray (1981), Caron (1985), Loeblich and Tappan 

43


(1988), Berggren & Miller (1988), Berggren et al., (1995), Georgescu (1996 and 

2002), BouDagher-Fadel et al (1997), Berggren & Norris (1997), Olsson et 

al., (2000), Elnady & Shahin (2001), Arenillas et al., (2001). 

The biostratigraphic correlation of the studied sections is based on 

planktonic foraminiferal zonations (Figs.3.12 - 3.13), which shows a comparison 

between the biostratigraphic zones established in this study with other 

equivalent of the commonly used planktonic zonal scheme 

around the 

Cretaceous/Tertiary boundary in and outside of Iraq. 

Table (3.1) Showing the number of planktonic and benthonic foraminiferal Genera and species 

identified in the studied sections from the Tanjero and Kolosh Formations 

Location Formation Epoch Foram type 

Total Total 

Genera Species 

Genera Species 

No. No. 

No. No. 

Sirwan Tanjero Late Maas. Pl. 20 62 

Sirwan Kolosh 

Early 

30 79 

Pl. 11 18 

Paleocene 

Sirwan Tanjero Late Maas. Ben. 36 58 

Sirwan Kolosh 

Early 

40 62 

Ben. 32 52 

Paleocene 

Kato Tanjero Late Maas. Pl. 14 30 14 30 

Kato Tanjero Late Maas. Ben. 25 38 25 38 

Qishlagh Tanjero Late Maas. Pl. 13 26 13 26 

Qishlagh Tanjero Late Maas. Ben. 28 42 28 42 

Dokan Tanjero Late Maas. Pl. 18 53 

Dokan Kolosh 

Early 

26 68 

Pl. 9 16 

Paleocene 

Dokan Tanjero Late Maas. Ben. 36 52 

Dokan Kolosh 

Early 

38 57 

Ben. 31 43 

Paleocene 

Gali 

Trunsit.unit 

Maas. Pl. 23 82 

+ Tanjero 

35 101 

Gali Kolosh 

Early 

Paleocene 

Pl. 14 21 

Gali 

Trunsit.unit 

Maas. Ben. 38 66 

+ Tanjero 

38 71 

Gali Kolosh 

Early 

Paleocene 

Ben. 30 50 

44


C R E T A C E O U S T E R T I A R Y PERIOD 

L A T E M A A S T R I C H T I A N P A L E O C E N E EPOCH--AGE 

T A N J E R O F O R M A T I O N K O L O S H Fn. FORMATION 

1 40 80 100 110 120 130 140 150 160 177 180 185 195 200 210 SAMPLE No 

LITHOLOGY 

1 63 110 140 160 170 180 190 210 230 255 280 300 320 THICKNESS m. 

P0 

CF.zones 

CF 5 CF 4 CF 3 CF 2 CF 1 

& P 1a P1b (Li&Killer,1998a) 

P. 

intermedia 

R. fructicosa P. hariaensis 

P. 

palpebra 

P. 

hantk. 

- ---- ----- ----- ------ ------------------ ---------- ----- --- ---- --- -- -- - 

-- --- ----- -- ------- ------------------ -- -------- --- --- --- --- ---- -- 

--- ----- ------- ------ -------- ---- ---------- ---- 

- ----- ---- ---------------- ----------------- ------------------ 

- --- ---- ---- ---------------- ------------ ----- ---------------- 

------- ------------------------- ---- -- ---- 

-- ----- ----- ---------- -------------- ---- ----------- ------ ------ ------ --- 

---- -- --------------- --------- -- ---------------- -- -- - - - - 

----- -- ---- --- -- -- --- --- --- ------------------------- -- -- -- -- --- - ---- 

- -- - -- ---- ---- -- -- ----------------- --- -- -- -- - - -- -- --- - -- 

--- -- - - --- --- --- -- --- --- --- --- ---- -- -- - - - 

----- - -- -- -- - -- --- -- - - - -- ------------------------------------ ---- --- 

--- ----------------------- --- --- -- - -- - --- - - 

------------------------- ---- -- --- -- - -- - - 

-- ---- -- -- ---------------- ------------ --- -------------------0 

---- ----- ---------------- ---- 

- ---- ------ ----- --- 

------ ------- ---------------- ---------- ----- -------------------- --- --- - -- --- -- --- -- 

--- ------- ---------------- ------ ----- ---- ----------------------------------- ---- - --- -- - 

---- - ---- ----------------- ------ ---- ----- ----------------------- 

---- ------ ---------------- ----- ------- --- -- 

--- - --- -------- ------- ----- ----- ----- --------------- ---- --- -- -- 

----- ----- ------ 

---- ---- ---- - -- 

----- ------ ---- ----- ------- ------- ---------------- --- -- ---- - --- --- 

------ ------ ----------------- --- ----- ---- -- ---------------- --- -- --- --- ----- 

----- ------ --------- -- ----- --- -- ---------- ------ ------- -------- 

-- ------ ----- ------------------ ---- ---------- ---------------- ----- 

--- ---- ----- 

---- ------ -------- 

--- ------- ---------- 

- - ------ ----------------- ------ ---- --------------- - ------- --- - - ------ 

---- ------ -- - -- - 

--- -- -- --- ------------- ---- ---- ---- ---- -- --- - 

---------------------------- -- --- 

- ---- ---- ------- ----- --- ---- ------ ------------ --- -- --- --- ---- --- -- - 

--- ------- ------- --- ---- --- ----- ------- ----- --- ---- -- -- --- --- 

---------------- -------- --- --- -- --- --- -- ------------------ ---- ---- --- 

----- ---- ------------ -- ---- ---- -- --- - - - 

--- ------ ------ ------ ---- ---- ------ 

---- -------- ---- ------ ----- --------- --- --- ---- --- -- -- 

-- ----- -------- ------ -------- ------ ---- 

-- ----- -------- ---------------- -- ------- ------ ------------------- ------ ------ ------ ----- ---- 

-- ---- -- ----- ---------------- -- ------ ------- ---- ----- --- ---- ----- --- ---- 

- ---- ------- ------- ----- - ----- ---- ----------- ---- 

0----- --------- ------ ---------- ---- -------- -------- ------ ----- ---- -- ---- ----- ------ -- 

---- --- --- --- ---- 

--- --- - ---- ----------------- 

0------ ------------------ -- --- - ---- -- --- -- 

----- ----------- -------- ---- --- ----- ---- ---- -- --- -- -- 

--- ------ ----- ------ ----------------- ----- ------ ----- ------ ---- -- - - - - - 

- - ---- - -------- ----------------- ------- ----- --- ------ ---- ---- - ---- -- -- 

- --- -- -------- - ---------------- ---------------- -- ------- --- ----- ---- 

-- -- -- -- -- -- -- -- -- 

----------------- -- 

------ ------ 

------- 

-- ---- ----- -------- - --- -------- - - ----------- --- 

----- ---- --- -------- ------------------- ---- --- - -- ---- ------- 

-- ------ --- --------- 

0----------0 

pá 

Heterohelix navarroensis Loeblich 

= globulosa (Ehrenberg) 

= striata (Ehrenberg) 

= punctulats (Cushman) 

= pulchra (Brotzen) 

Laeviheterohelix glabrans (Cushman) 

Planoglobulina carseyae (Plummer) 

= acervulinoides (Egger) 

Rugoglobigerina rugosa (Plummer) 

= scotti (Bronnimann) 

= hexacamerata Bronnimann 

= macrocephala Bronnimann 

= pennyi Bronnimann 

= reicheli Bronnimann 

Gansserina gansseri (Reuss) 

= wiedenmayeri (Gandolfi) 

Globotruncanita stuarti (de Lapparent) 

= stuartiformis Dalbez 

= conica White 

= pettersi Gandolfi 

= angulata Tilev 

Globotruncana aegyptiaca Nakkady 

= orientalis El-Naggar 

= falsocalcarata Kerdany & Abdelsalam 

= falsostuarti Sigal 

= dupeublie Caron et al. 

= lapparenti Boli 

= arca (Cushman) 

= bulloides Vohgler 

= rosetta Carsey 

= insignis (Gandolfi) 

Contusotruncana contusa (Cushman) 

= fornicata Plummer 

= plicata White 

= walfischensis Todd 

Rugotruncana circumnodifer (Finlay) 

= subcircumnodifer (Gandolfi) 

Globotruncanella petaloidea (Gandolfi) 

= pschadae (Keller) 

Globigerinelloides volutes (White) 

= multispinata (Lalicker) 

= prairiehillensis Pessango 

= bolli Pessango 

Pseudotextularia elegans (Rzehak) 

= deformis (kikoine) 

= intermedia (De Klasz) 

Racemiguembelina fructicosa (Egger) 

= poweli Smith & Pessango 

Pseudoguembelina costulata (Cushman) 

= hariaensis Nederbragt 

= palpebra 

= excolata (Cushman) 

Hedbergella monmothensis (Olsson) 

= holmdelensis Olsson 

Abathomphalus mayaroensis (Bolli) 

Archaeoglobigerina carteri (Kassab) 

= blowi Pessango 

= cretacea (d Orbigny) 

Gublerina cuvillieri Kikoine 

Gumbelitria cretacea Cushman 

= dammula (Voloshina) 

Plummerita hantkeninoides (Bronnimann) 

SUBZONE 

Cretaceous planktonic foraminifera 

Parvularugoglobigerina alabaminsis (Liu & Olsson) 

Rectoguembelina cretacea Cushman 

Woodringina clytonensis (Loeblich & Tappan) 

= hornerstownensis (Olsson) 

Chiloguembelina morsei (Kline) 

= midwayensis (Cushman) 

Globoconusa daubjergensis (Bronnimann) 

Parasubbotina pseudobulloides (Plummer) 

Subbotina trivalis (Subbotina) 

= triloculinoides (Plummer) 

Globanomalina archeocompressa (blow) 

= planocompressa (Shutskaya) 

Eoglobigerina edita (Subbotina) 

= eobulloides Morozova 

= simplicissma Blow 

Praemurica taurica (Morozova) 

= pseudoinconstans (blow) 

Guembelitria cretacea Cushman 

-------------------------------------------- 

-------------------------------------------- 

--------------------------------------- 

-------------------------------------------- 

-------------------------------------------- 

-------------------------------------------- 

----------------------------- 

-------------------------------------------- 

-------------------------------------------- 

0----------- 

-------------------------------------------- 

-------------------------------------------- 

-------------------------------------------- 

------------------------------------------ 

------------------------------- 

------------------------------------- 

-------------------------------------------- 

----------------------------- 

Fig (3.1) Biostratigraphic range chart of planktonic foraminifera at Cretaceous/Tertiary boundary, Sirwan 

area, (Sirwan section) 

Paleocene planktonic 

foraminifera 

45



L A T E M A A S T R I C H T I A N P A L E O C E N E EPOCH--AGE 

T A N J E R O F O R M A T I O N Kolosh FORMATION 

1 40 80 100 110 120 130 140 150 160 177 180 185 195 200 210 SAMPLE No 

LITHOLOGY 

1 63 110 140 160 170 180 190 210 230 255 280 300 320 THICKNESS m. 

P0 

CF.zones 

CF 5 CF 4 CF 3 CF 2 CF 1 

& P 1a P1b (Li&Killer,1998a) 

P. 

P. P. 

R. fructicosa P. hariaensis 

intermedia. 

palpebra hant. 

Pá 

SUBZONE 

---- - -------- --- --------------- -- 

-------- --- ---- --- - - - - - - - - - - - 

------------ ------- -- -- 

-------- ---------- - ------- - 

--- ------ ---------- -- ---- ------ ----- 

-- -- - ----- ---- -------- -------- ----- 

-------- -------- ------- ----- ------ ---- -------- 

---- --- ------ ------ -- - ----- 

-------- --------- --------- - ---- ---- ---- ---- 

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-- --- --- 

---- -------- ------ --- -------- - - - - - 

-------- ----- ---- ------- - ---- - -- - 

------ ----- 

---------- ----- --- - - - 

-- -- -- ---- ---- ------- - - ---- - - - 

-------- ------ ----- --- --- -- -- - - -- 

-- --- ----- -------- ------- ---- -- - - - - 

-------- - ------- -- ----- ------- - 

------- ----- - - - 

-------- -------- ------ ------- --------- ----- - - - - - - - - - - - 

---- --- ---- ---- --------- ----- ---- - 

---- -------- ----- - -- --- -- - ---- -- -- 

---- - - ---- --------------- ---- - - ---- 

-- -- --- -- ----------- - -- ----- 

----- -------- ------- ------- --- - - -- 

------ -- - - - -- - 

----- ------- - - - - - - 

-- -- ---- --- 

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-------- -------------- ---------------- ---- --- ---- - - - 

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-------- ------------ -- ---- ----- - - - - - 

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---- - ------- ------------- - ---- --- - - - - 

-------- ----- ---- -------- -- --- - - - - - - 

-------- -------- ------- --- --- ----- - 

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---- ------ -------- ----- ----------- 

-- -------- --- -- -------- - ----- ---- - - - 

---- ------ -------- ---- -- - - - - - 

-------- -------- -- --- -- -- --- --- 

-- -- 

--- -------- -------- -------- ---- -- 

---------------- ----- ------ ----- 

------ 

---- -------- ------- --- ----- --- 

-------- ---- ------ -- -- --- -- -- - - - 

-------- ------ ------- ------------- ----- --- - - - - - 

--- -------- ------ ------ 

-------- -------- ------ ---------- ----- - 

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------ ----- 

--------- ---- ----- ------ --- 

-- -- -- -- -- -- -- -- - - - 

-- --- - -- -- -- -- -- - -- - 

---- --- ---- ---- 

--- --- - -- 

--- -- -- 

----- --- - -- -- 

------ ----- ---- 

-- -- -- 

---- ----- ------- 

-- - ---- - --- -- 

-- 

--- --- -- -- - 

------ - --- 

----- ---- --- 

--- - --- --- - 

-- - -- 

- --- -- - - -- 

--- -- -- - - 

--- -- -- -- -- 

--- --- -- - 

---- - --- ---- ---- 

---- - -- 

--- --- 

-- --- ------- ---- --- 

----- ------- 

--- -- - -- 

- -- - --- --- 

--- --- -- -- 

------ ---- 

-- -------- 

--- --- ---- 

------ - 

--- ---- -- -- --- 

----- 

--- ---- ------ 

----- -- -- 

---- ------- 

--- -- --- -- 

- --- ---- -- -- 

---- -------- --- 

---- ---- ----- 

--- ------ 

----- --- --- 

---------- --- 

--------- 

- ------ - --- 

--- -------- 

----- ----- 

------ --- - ----- 

---- ---- -- - 

----- 

------- 

--- --- ---- --- 

--- ------ 

FORAMINIFERA 

BENTHONIC 

Bolivina incrassata Reuss 

Bolivinoides draco (Marsson) 

= delicates Cushman 

= miliaris Hittcrmar & Koch 

Astacolua sp. 

Rzehakina epigone (Rzehak) 

Cibicidoides dayi (White) 

= subcarinatos Cushman & Deaderick 

Osangularia navarrana (Cushman) 

Pullenia jarvisi Cushman 

Pyrulinoides sp. 

Neoflabellina rugosa (d Orbigny). 

= delicatissima (Plummer) 

Bulimina ovulum Reuss 

= midwayensis 

Praebulimina ovulum (Reuss) 

= aspera (Cushman &Parker) 

Uvigerina graciliformis 

Oolina apiculata Reuss 

Globorotalites michelinianus (d Orbigny) 

Ammodiscus cretaceous (Reuss) 

= preuvianus 

Marsonella oxycona (Reuss) 

Dorothia smokynensis Wall 

= retusa 

= rosetta 

Textularia astutia. Lalicker 

Spiroplectamina laevis. (Roemer) 

= spectabilis (Grzybowski) 

= dentata (Alth) 

= navicula (d Orbigny) 

Stilomella midwayensis. (Cushman &Todd) 

Nodosaria minor Hantken 

= affinis Reuss 

= cf. limbata d'Orbigny. 

Pseudonodosaria sp. 

= appressa Loeblich & Tappan 

Dentalina elegans d Orbogny 

= inornata (d Orbogny) 

Dentalinoides canulina Marie 

Noneonella insecta (Schwager) 

Pleurostomella paleocenica (Cushman) 

Paralabamina hillebrndti (Fisher) 

= laevis. (Beissel) 

Lenticulina muennsteri 

= navicula. (d Orbigny). 

= gunderbookaensis. Crespin 

Gavelinella micra. 

= danica 

Lagena hispida Reuss 

Fissurina? sp. 

Coryphostomata midwayensis. (Cushman) 

Gyroidina girardana (Reuss) 

Gaudryna pyramidata. Cushman 

= pulvina 

Gyroidinoides globosus. (Hagenow) 

= exsertus (Belford) 

Clavulinoides globulifera.Ten Dam &Sigal 

Conicospirilina sp. 

Rotalia spp 

Omphalocyclus macroporus (Lamark) 

Orbitoides medius (d Archiac) 

. 

Fig (3.2) Biostratigraphic range chart of benthonic foraminifera at Cretaceous/Tertiary boundary, Sirwan 

area, (Sirwan section) 

46


It is important to mention that the conventional index species Abathomphalus 

mayaroensis of Late Maastrichtian recorded very rare presentation and it is 

frequently absent in shallow continental shelf sections in all studied regions 

which may be due to paleoenvironment condition of the deeper and more 

basinal oceanic environment around low latitudes restrictions of the species 

Canudo et al., (1991), and in high latitudes disappear prior to K/T boundary 

(Blow, 1979). Therefore the A. mayaroensis Biozone is geographically and 

ecologically restricted. In such cases it is better to replace the A. mayaroensis 

Biozone by other biozones to avoid any ambiguous and vague situation about 

first appearance and last extinction datum event. (Figs 3.12 and 3.13) 

For the Paleogene subdivisions zonal scheme previously have been 

developed in two widely separated geographic areas: the eastern hemisphere 

(Caucasus mountains, e.g. Subbotina, 1953; Krasheninikov, 1969), and in the 

western hemisphere (Trinidad, e.g. Bolli, 1957 a, b in Samir, 2002). 

A discussion of all subsequent modifications of the original zonal scheme 

proposed by Bolli (1966), Blow (1979), Berggren & Miller (1988), Berggren et al., 

(1995), Berggren & Norris (1997), Olsson et al., (2000), represent the base of 

Paleocene zonal scheme for this study with other mentioned authors in Fig 

(3.13) which shows a comparison between this zonal scheme and earlier 

developed schemes. It is worthy to remember that the original, genetic radiation, 

phylogenetic reconstruction relationship and geologic ranges of Paleocene 

planktonic foraminifera were established by Liu & Olsson (1992), and Olsson et 

al., (2000), which form the base principles datum event of working group up on 

the( Atlas of Paleocene Planktonic Foraminifera) by Olsson et al.,(2000), figs 

(4.9 -4.11) 

3.2.1- Biostratigraphy of the Upper Cretaceous Formations: 

According to identified planktonic foraminiferal assemblages within upper 

most part of Shiranish Formation, Reddish to pale brown succession, Tanjero 

Formation in Smaquli area in addition in upper part of Tanjero Formation in all 

other sections, eight biozones are recorded from the studied sections. The 

biostratigraphic zones of the studied area are described from the bottom to the 

top as below: 

47


U P P E R C R E T A C E O U S PERIOD 

LATE MAASTRICHTIAN EPOCH--AGE 

1 10 20 25 30 40 45 SAMPLE NO. 

LITHOLOGY 

1 10 20 30 40 50 60 70 80 90 100 110 THICKNESS m. 

(Interfingering Aqra Lst.) Tanjero Formation Transitional unit Red Bed FORMATION 

CF4 CF 3 --------- 

Planktonic foram.CF. 

zones(Li&Killer,1998a) 

R. fructicosa P.hariaensis--------------------?? SUBZONE 

------------------------------------------------------ 

------------------------------------------------------ 

------------------------------------------------------ 

--- -------------------------------------------------- 

------------------------------------------------------ 

------------------------------------------------------ 

-------------------------------------------------- --- 

------------------------------------------------------ 

- -- ----------------------- -------------------------- 

-------- 

-------------------------------------- 

------------------------------------------------------ 

------------------------------------------------------ 

------------------------------------------------------ 

------------------------------------ 

------------------------------------------------------ 

------------------------------------------------------ 

------------------------------------------------------ 

------------------------------------------------------ 

-------------- --------------------------------------- 

---- - -- - - -- - - - - - - - 

------------------------------------------------------ 

------------------------------------------------------ 

------------ ----------------------------------------- 

------------------------------------------------------ 

------------------------------------------------------ 

------------------------------------------------------ 

------------------------------------------------------ 

-------------- 

------------------------------------------------------ 

--------------------------------------------------------------- 

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--------------------------------------------------------------- ---- --- 

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--------------------------------------------------------------- --- ----- 

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--------------------------------------------------------------- ---------- ---------- 

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------------- -------------------------------------------------- ---- 

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--------------------------------------------------------------- ------------------------------- 

--------------------------------------------------------------- ----------------------- 

Reworked Foram. 

-------------------------- 

-------------------------- 

-------------------------- 

------------------------- 

-------------------------- 

-------------------------- 

-------------------------- 

-------------------------- 

-------------------------- 

---------------------- 

N o r e c o r d s o f foraminifera 





= brazoensis Martin 





Gansserina gansseri (Reuses) 








= gagnebini Tilev 








= intermedia De Klasz). 







Cibicides dayi (White) 

= subcarinatos Coshman &Deaderick 

= excavate Brotzen 






Praebulimina quadrata 

= ovulum 



= pruvianus 




Globorotaloides sp. 

Spiroplectamina israelskyi Hillebrandt 


= sp. 

Ammospaeroidina pseudoapiculata. 




Dorothia crassa 

= smokynensis Wall 

= retusa 

Gyroidijna girardana (Reuss) 




= tissoti Shlumberger 

Loftusia elongata Brady 

= morgani Douville 

= persica Brady 

= minor Coxi 

FORAMINIFERA 

PLANKTONIC FORAMINIFERA 

BENTHONIC FORAMINIFERA 

Fig (3.3) Biostratigraphic range chart of planktonic and benthonic foraminifera, Cretaceous /Tertiary boundary 

in Kato area (Kato section) 

48


UPPER C R E T A C E O U S TERTIARY PERIOD 

E-MAAS. L A T E M A A S T R I C H T I A N PALEOCENE EPOCH--AGE 

Tanjero Interfinguring Aqra lst.. Tanjero Transitional Red Bed FORMATION 

1 5 11 18 23 29 33 38 41 46 47 50 52 53 58 SAMPLE No 

LITHOLOGY 

1 20 45 75 100 130 160 200 225 245 265 275 THICKNESS M. 

CF 5 CF 4 ------ 

Planktonic foraminiferal. CF. 

zones (Li&Killer,1998a) 

P.intermed. R .fructicusa ----- SUBZONE 

FORAMINIFERA 

------------------------ 

------------------------ 

------------------------ 

------------------------ 

----------------------- 

-------- --------------- 

---------- ------------- 

------------------------ 

------------------------ 

------------------------ 

------------------------ 

------------------------ 

------------------------ 

----------------------- 

------------------------ 

------------------------ 

------------------------ 

------------------------ 

------------------------ 

----------------------- 

------------------------ 

------------------------ 

------------------------ 

----------------------- 

----- 

------------------------ 

----------------------- -- -- 

----------------------- - - -- -- -- 

----------------------- 

---------------------- --- --- - -- --- -- -- 

------------------------ - - --- --- --- -- 

----------------------- --- --- -- 

------------------------ - --- - -- -- 

----------------------- -- - - - - -- ---- - 

------------------------- --- --- 

-------------------------- -- - - 

------------------------------ --- --- - - -- - 

---------------------- --- ------ ----- ---- ---- ---- -- -- ----- 

--------------------------- ---- ---- ------- ---- --------- ---- 

-------------------------- --- -- -- -- ---- ----- -------------------- ---- 

-------------------- ------------------- ----- --- --- --- ----- ---- ------------------ 

---- ---------- ------ ----- --- --- - --- ----- -- --- -- 

---------------------- ---- ---- ---- --- ------ -- -------------- 

------------- -------- -- --- -- -- -- ----- -------------------- 

---- ------ - - - ------ ---- --- ------ ---- ----- ----------------- 

- -- --------- --- -- --- --- --- ---- ---- ----- ----------- 

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--------------------------------------- -------------- ---------------- ----------- 

------------------- ---- ------ ---- --- ---- ---- ------ --------------- 

------------------------------------ -- --- ------------- --------- ---- --------- 

------------------- -- ----- ---- ----- ------ --------- ----------- 

------------------------------- ---- ---------- ------------------ ----------- 

---------------------------------------- -------- -------- ----------- ----------- 

----------------------- --------- --- ---------- ---------- -------------------------- -------- ----------- 

---- --- ------ ----------------------------------------------- - -------------------------- 

-------------------------------------- ----------------- -------------------------- 

------------------------------------------------------- -------------------------- 

------------------------------------- ---------------- ---------------------------- 

----------------------------------------------------------------------------------- 

-------------------------------------- -------------- ---------------------------- 

------------------------------------------------------------------------------- 

-------------------------------------- --------------- ----------------------- 

-------------------------------------------------------------- --------------- 

------------------------------------------------------------------------------- 

-------------------------------------- --------------- ----------------------- 

-------------------------------------------------------------- --------------- 

------------------------------------------------------------------------------- 

Rewor 

ked 

Foram 

inifera 

---------- 

---------- 

---------- 

---------- 

---------- 

---------- 

---------- 

---------- 

---------- 

---------- 

---------- 

---------- 

---------- 

no r e c o r d s of foraminifera 



















Globotruncana arca (Cushman) 












= excavate Brotzen 









= pruvianus 



= retusa 

= rosetta 



= laevis. (Roemer) 

= sp. 

Ammospaeroidina pseudoapiculata. 






Rotalia sp. 

Valvulammina sp. 




= apiculatus Shlumberger 

Lepidorbitioides socialis (Leymerie) 

Siderolites sp. 

Loftusia elongata Brady 

= morgani Douville. 

= persica Brady 


= coxi Henson 

= sp. 

PLANKTONIC FORAMINIFERA 

BENTHONIC FORAMINIFERA 

Fig (3.4) Biostratigraphic range chart of planktonic and benthonic foraminifera Cretaceous /Tertiary 

boundary, Qala Cholan area, (Qishlagh section) 

49


3.2.1.1- Globotruncana aegyptiaca Interval Zone (CF8) 

The Globotruncana aegyptiaca (CF8) zone was originally established and 

described by Caron (1985).It is marked by the interval from the First Appearance 

Datum (FAD) of the nominate species to the First Appearance Datum (FAD) of 

Gansserina gansseri (Bolli). In the studied Gali section (Smaquli area) is defined 

by the first appearance FAD of index taxon (Globotruncana aegyptiaca 

Nakkady,)within the first sample taken from the upper part of Shiranish 

Formation at the base to the FAD of Gansserina gansseri (Bolli) at sample No.8 

(plate. 2, Figs. 10-12) within reddish unit at the top. This zone covers frequent 

occurrence of the nominate species for 15m. interval in the upper part of the 

Shiranish Formation and 8m. from the lower part of reddish unit. This interval 

may not represent all interval of the biozone because the first sample of our 

section may not fit within the FAD of the nominate species. This part of 

Globotruncana aegyptiaca zone indicates early Maastrichtian for the cropped 

interval, and corresponds to that of Caron (1985), in tropical regions, Shahin 

(1992), in Egypt, it is equivalent to the same zone recorded in the south Atlantic 

DSPT Site 525A and Tunisia by Li and Keller (1998a,b), Abramovich et al., 

(2002), in Madagascar, Al-Mutwali and Al-Jubouri, (2005), north Iraq, 

Sharbazheri (2007). In the studied section a well diversified planktonic 

foraminiferal species are recorded, e.g. Heterohelix navarroensis Loeblish, H. 

globulosa (Ehrenberg), H. striata (Ehrenberg), H. reussi (Cushman), H. 

nauttalli (Voorwijk), H. punctulats (Cushman), H. pulchra (Brotzen), 

Planoglobulina carseyae (Plummer), P. brazoensis Martin, Rogoglobigerina 

rugosa (Plummer), R. scotti (Bronnimann), R. hexcamerata Bronnimann, 

R. macrocephala Bronnimann, R. rotundata Bronnimann, R. milamensis Smith 

& Pessango, Gansserina wiedenmayeri (Gandolfi), Globotruncanita stuarti (de 

Lapparent), G. stuartiforms Dalbez, G. conica White, Rugotruncana 

subcircumnodifer ( Gandolfi), R. circumnodifer ( Finlay), Globotruncana 

aegyptica Nakkady, Glt. orientalis El-Naggar, (Carsey), Glt. falsostuarti Sigal, 

Glt. mariei Banner & Blow, Glt. arca (Cushman), Glt. gagnebini Tilev, Glt. 

bulloides Vohgler, Glt. linneiana (d Orbigny), Glt. ventricosa White, Glt. 

insignis (Gandolfi), Glt. dupeublie Caron et al., Glt lapparenti Boli, 

50


Contusotruncana fornicata Plummer, Globotruncanella petaloidea (Gandolfi), G. 

havanensis (Voorwuk), Pseudotextularia elegans (Rzehak), P. Deforms 

(Kekoine), P.intermedia (De Clasz), Pseudoguembelina costulata (Cushman), 

Globigerinelloides voluta (White), G. multispiinata (Lalicker), G. prairiehilleinsis 

Pessango, G. subcarinatus Bronnimann, G. bolli Pessango, G. ultramicra 

(Subbotina), Archaeoglobigerina cretacea (d Orbigny), A. blowi Passango, 

Gublerina cuvillieri Kikoine, Gumbelitria cretacea Cushman, G. Dammula 

(Voloshina) Hedbergella monmothensis (Olsson). 

Beside these planktonic foraminiferal assemblages moderate benthonic 

foraminiferal species were recorded (Fig. 4.8) e.g: Bolivina incrassata Reuss, 

Bolivinoides draco (Marsson), B. miliaris Hitt & Koch, Cibicidoides dayi 

(White), C. subcarinatos Cushman & Deaderick , C. excavata Brotzen, 

Osangularia navarrana (Cushman), Pullenia jarvisi Cushman, Pyrulinoides sp., 

Neoflabellina rugosa (d Orbigny), N. delicatissima (Plummer), Bulimina 

midwayensis, Uvigerina graciliformis, Oolina apiculata Reuss, Globorotalites 

michelinianus (d Orbigny), Ammodiscus cretaceous (Reuss), A. pruvianus, 

Marsonella oxycona (Reuss), Dorothia smokynensis Wall, D. retusa, D. rosetta, 

Textularia astutia. Lalicker, Spiroplectamina israelskyi Hillebrandt, S, laevis. 

(Roemer), Stensioina excolata (Cushman), Nodosaria minor Hantken, N. affinis 

Reuss, N. cf. limbata d'Orbigny, Pseudonodosaria sp., P. appressa Loeblich & 

Tappan, Dentalina elegans d Orbogny, D.inornata (d Orbogny), Dentalinoides 

canulina Marie, Noneonella insecta (Schwager), Pleurostomella subnodosa 

(Reuss), Paralabamina hillebrndti (Fisher), P. laevis. (Beissel), P. carseyae 

(Plummer), Lenticulina muennsteri, L. navicula. (d Orbigny),. L. 

gunderbookaensis. Crespin, Gavelinella danica , Lagena sp., Coryphostomata 

midwayensis. (Cushman), Gyroidina girardana (Reuss), Gaudryna pyramidata. 

Cushman, G. pulvina, Gyroidinoides globosus. (Hagenow), Clavulinoides 

globulifera.Ten Dam & Sigal, 

According to the all above mentioned authors, and Khalil and Mashally 

(2004), SW Sinai Egypt, (Elnady and Shahin 2001), N E Sinai, Martines (1989), 

South America, Abdel-Kareem & Samir (1995), Western Desert Egypt, Fars 

(1984), Egypt. Al-Mutwali (1996), (Al Mutwali and Al Jabouri, 2005), Iraq. The 

51


age estimation of this biozone indicates Early Maastrichtian age. Li and Keller 

(1998a), recorded the time span of this biozone from 72.48Ma to 70.39 Ma 

estimated by absolute ages based on magnetochron ages. Premoli Silva et al., 

(1998), in their study of bio-isotope stratigraphy on eastern Mediterranean, and 

Maestas et al., (2003), recorded the Globotruncana aegyptiaca Zone from the 

Upper Campanian age. 

The Geologic Time Scale (GTS2004) by Gradstein et al., (2004), (Fig.3.12), 

accompanying International Stratigraphic Chart, issued under auspices of the 

International Commission on Stratigraphy (ICS), shows the current 

chronostratigraphic scale and ages with estimation of uncertainty for all stage 

boundaries, placed this span of time 72.48Ma to 70.39 Ma under the upper limit 

of Campanian. The chronostratigrapic duration age was estimated based on 

different techniques and methods to construct a GTS (2004) placed the 

Maastrichtian stage between time intervals of (70.6 - + 0.6 Ma) at the base, and 

to (65.5 + - 0.3 Ma) at the top. 

3.2.1.2- Gansserina gansseri Interval Zone (CF7) 

The Gansserina gansseri (CF7) zone was introduced by Bronnimann (1952), 

as Globotruncana gansseri Zone for the first time and placed into the Early 

Maastrichtian of Trinidad in (Samir, 2002). In the studied section, this Biozone is 

defined by the interval between the FAD of nominate species Gansserina 

gansseri (Bolli) and the FAD of Contusotruncana contusa (Cushman), (plate. 2, 

Figs. 1-3) at Gali section (Smaquli area), lower part of reddish to pale brown 

succession. This zone covered abundant occurrence of the nominate species for 

(20m.). Most of the workers in the zonal scheme placed Gansserina gansseri 

zone informally at the middle- lower Maastrichtian (Li and Keller, 1998a), and 

(Abramovich et al., 2002) in DSDP Site 525A. (Fars, 1984), (Abdel-Kareem & 

Samir, 1995), (Luning et al., 1998), (Elnady and Shahin, 2001), and (Samir, 

2002), Egypt. (Kassab 1974, 1975c, 1975d & 1976b), (Abawi et al., 1982) 

(Abdel-Kareem, 1986a, b), (Kassab et al., 1986), (Al-Mutwali, 1996), (Al-Mutwali 

and Al-Jubouri, 2005), and (Sharbazheri 2007), Iraq. (Chacon and Martin- 

Chivelet, 2005), Spain. (Premoli Silva et al., 1998), Italy. (Changkham and Jafar, 

1998), India. While (Khalil and Mashally, 2004), in Egypt, and Caron (1985), in 

52


general this zone has been recorded from Middle Maastrichtian. Obaidalla 

(2005), Egypt, placed this zone on the base of Late Maastrichtian. Maestas et 

al., (2003), from California Mexico placed this Zone at upper Campanian- Lower 

Maastrichtian. 

Note: it is worthy to pay attention to the first appearance of A. mayaroensis 

which occurs 25m. above the first appearance of G. gansseri, therefore the A. 

mayaroensis not used as a zonal marker because of many studies have shown 

that both (FA) and (LA) of this species are diachronous. In addition, this taxon is 

rarely present in continental shelf due to its deeper environmental habitat. (Li 

and Keller, 1998), (Huber, 1992), (Nederbragt, 1991). 

In addition to the index species, the planktonic assemblages of this zone 

include: 

Heterohelix navarroensis Loeblish, H. globulosa (Ehrenberg), H. striata 

(Ehrenberg), H reussi (Cushman), H. nauttalli (Voorwijk), H. punctulats 

(Cushman),H. pulchra (Brotzen), Planoglobulina carseyae (Plummer), P. 

brazoensis Martin, Rogoglobigerina rugosa (Plummer), R. hexcamerata 

Bronnimann, R. macrocephala Bronnimann, R. milamensis Smith&Pessa, 

Gansserina gansseri (Reuss), G. wiedenmayeri (Gandolfi), Globotruncanita 

stuarti (de Lapparent),Globotruncanita stuartiforms Dalbez, Globotruncanita 

conica White, Globotruncanita pettersi Gandulfi, Rugotruncana 

subcircumnodifer ( Gandolfi) R. circumnodifer ( Gandolfi), ,Globotruncana 

aegyptica Nakkady, Glt. orientalis Elnaggar, Glt. rosetta (Carsey), Glt. 

falsostuarti Sigal, Glt. mariei Banner & Blow, Glt. arca (Cushman), Glt. 

gagnebini Tilev, ,Glt. bulloides Vohgler, Glt. linneina (d 

Orbigny),Glt. ventricosa White, Glt. insignis (Gandolfi), Glt. dupeublei 

Caron et al., Glt. lapparenti Boli, Contusotruncana fornicata (Plummer) 

,Abathomphalus mayaroensis (Bolli), Abathomphalus intermedius (Boli), 

Globotruncanella petaloidea (Gandolfi), Globotruncanella havanensis 

(Voorwuk), Pseudotextularia elegans (Rzehak),Pseudotextularia deformis 

(kikoine), P. intermedia (De Clasz), Pseudoguembelina costulata (Cushman), 

Gublerina cuvillieri kikoine, Globigerinelloides voluta (White), G. multispiinata 

(Lalicker), G. prairiehilleinsis Pessagno, G. subcarinatus Bronnimann, G. bolli 

53


Pessango, G. ultramicra (Subbotina),, Archaeoglobigerina cretacea (d 

Orbigny), A. blowi Passango, Gublerina cuvillieri Kikoine, Gumbelitria cretacea 

Cushman, G. dammula (Voloshina) Hedbergella monmothensis (Olsson). In 

addition to these planktonic foraminiferal assemblages moderate benthonic 

foraminiferal Species were recorded (Fig 3.8). The age estimation of this 

biozone by (Li and Keller 1998a), records the time span of 70.39Ma to 69.56 Ma 

830 Ky estimating absolute ages based on magnetochron ages with 41ky/m, 

moderate rate of deposition (Fig.4.11) 

Age: early Maastrichtian. 

3.2.1.3- Contusotruncana contusa Interval Zone (CF6) 

Dalbeiez (1955) proposed the Globotruncana contusa Zone for the Upper 

Maastrichtian of Tunisia. Biostratigraphic interval of this zone is defined by the 

FAD of Contusotruncana contusa (Cushman) at the base and last appearance 

(LAD) of Globotruncana linneniana (d Orbigny) at the top. (plate. 1, Figs. 6-8). In 

the present study at Gali section, this Zone (CF6) covers an interval of 25 

meters. This Zone yielded an assemblage of planktonic foraminifera which 

totally resembles that of the underlying Gansserina gansseri Zone (CF7), except 

for the first appearance of Contusotruncana contusa (Cushman), 

Contusotruncana plicata White, C. patelliformis (Gandolfi), , Globotruncana 

rosetta Carsey, Racemiguemelina powli Smith and Pessango, Hedbergella 

holmdelensis Olsson, Rugoglobigerina scoti (Bronnimann), and mark the 

termination of Guembelitria dammula (Voloshina), Globotruncana gagnebini 

Tilev, Globotruncana bulloides Vohgler, Glt. insignis (Gandolfi), Glt. mariei 

Banner & Blow, Glt. ventricosa White, Globotruncanella havanensis 

(Voorwuk),Globigerinilloides boli Passango, Archaeoglobigerina blowi 

Pessango, A. cretacea (d Orbigny). 

As defined above, the present Biozone (CF6) is correlatable with the Zone 

recorded by (Li and Keller, 1998a and b),and (Abramovich et al., 2002), at 

DSDP Site 525A. (Samir 2002), from Egypt. (Sharbazheri 2007), NE Iraq. To 

the lower part of Rosita contusa Zone recorded in the Northeast of Iraq by 

(Abawi et al., 1982 and Abdel-Kareem 1986), in Italy (Premoli Silva and Sliter 

1995, 1999) (Premoli Silva et al 1998), (Abdel-Kareem & Samir 1995) Egypt, 

54


and it is correlated with the middle part of Gansserina gansseri Zone of (Al- 

Mutwali 1996), Hammoudi 2000 and Al-Mutwali and Al-Jubouri 2005), Iraq. 

(Chacon and Martin-Chivelet 2005) Spain and other different localities of the 

world (Robaszynski et al.,1984) and (Caron, 1985) general, (Maestas et al 

2003), USA. (Obaidalla 2005), Egypt. (Figs. 4.12 - 4. 13). 

Magnetochron records of this biozone by (Li and Keller 1998a show that the 

age estimation of the time span from (69.56 Ma) to (69.06Ma) 500 Ky/25meters 

estimating absolute ages based on magnetochron ages with 20 Ky/meter 

which indicate higher rate of deposition than (CF7) (Fig. 5.11) 

Age: Late early Maastrichtian. 

3.2.1.4- Pseudotextularia intermedia Interval Zone (CF5) 

The Pseudotextularia intermedia Zone (CF5) is defined by the LAD of the 

Globotruncana linneiana (d Orbigny) at the base and the FAD of 

Racemiguembelina fructicosa (Egger) at the top (plate 2, Fig 9). Nederbragt 

(1990), originally introduced this Biozone as the interval from the FAD of 

Planoglobulina acervulinoides at the base and the FAD Racemiguembelina 

fructicosa at the top. In the present study, the definition is constrained according 

to Li and Keller (1998 a and b).The interval of this Zone is 19 meters thick in Gali 

section. 

The recorded planktonic foraminiferal assemblages in this biozone 

represented by well diversified forms of Heterohelix navarroensis Loeblish, H. 

globulosa (Ehrenberg), H. striata (Ehrenberg), H. punctulats (Cushman), H. 

nauttalli (Voorwijk), H. reussi (Cyshman), H. pulchra (Brotzen), Planoglobulina 

carseyae (Plummer), P. brazoensis Martin, P. acervulinoides (Egger), 

Rugoglobigerina rugosa (Plummer), R. scotti (Bronnimann), R. 

hexacamerata Bronnimann , R. macrocephala Bronnimann, R. milamensis 

Smith & Pessango, Gansserina gansseri (Reuss), G. wiedenmayeri 

(Gandolfi), Globotruncanita stuarti (de Lapparent), G. stuartiformis Dalbez, 

G. conica White, G. pettersi Gandolfi, G. angulata Tilev, Globotruncana 

aegyptiaca Nakkady, Glt.orientalis El-Naggar, Glt. falsostuarti Sigal, Glt. 

dupeublie Caron et al., Glt. lapparenti Boli, Glt. arca (Cushman), Glt. rosetta 

Carsey, Contusotruncana contusa (Cushman), C. plicata White, C. 

55


Patelliformis (Gandolfi), Rugotruncana circumnodifer (Gandolfi), R. 

subcircumnodifer (Gandolfi), Globotruncanella petaloidea (Gandolfi), 


L A T E - M A A ST R I C H T I A N P A L E O C E N E EPOCH--AGE 

Tanjero Interfingering (Aqra Lst) Tanjero Kolosh FORMATION 

T48 T40 T35 T28 T22 T14 T10 T1 K1 K7 K11 K16 K20 K30 K45 K55 K65 SAMPLE No 

LITHOLOGY 

1 30 60 90 110 125 135 140 145 150 160 170 200 217 THICKNESS m. 

P 

CF.zones 

CF 5 CF4 CF3 CF2 CF1 

0 P 1a 

P1b (Li&Killer,1998a) 

P.inter. R. fructicosa P. hariaensis P. palpebra P.hant. á 

SUBZONE 

------------------------- ------ ------ ------ ----------------------------- ---------- --------------------- 

------------------- ----------- ------- -------- ---------------------------- ---------- ------------------ 

---------------------------------- ------- ------ ---------- ----------- ---------- ----- 

---------------------------- ---------- ----------- 

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--------- ---- ------ ---- -------- ---------- ----- ----- ----- 

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-------------------------------------------------------------------------------------------------------------------------------------------------------- 

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-------------------------------- ----- --- 

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------------------------------------------------------ 

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------------------------------------ ---- ---- --- --- -------- ---- --- --- ---- 

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----------------------------- ----------- ---- -------- --------- ------------------------------------------------------------ 

-------------------------------------- ------- --------- ------- ------- -------- --------------------------------------------------- 

---- ----- ---- -- -- -- -- 

-------- -------- ----- 

------------ ----- ----- ------ --- --- ------------ -------------------------- 

---------- --- -- 

0-------------0 

Heterohelix navarroensis Loeblish 












= rotundata Bronnimann 
















Rugotruncana circumnodifer (Finlay) 



= havanensis (Voorwuk) 



= subcarinata Bronnimann 










= palpebra 

= excolata (Coshman) 







Plumeri. hantkeninoides (Bronnimann) 

Cretaceous planktonic foraminifera 



Chiloguembelina Morse (Kline) 














-------------------------- 

--------------------------------- 

------------------------------------------------ 

------------------------------------------------ 

--------------------- 

------------------------------------------------ 

------------------------------------------------ 

---------------- 

------------------------------------------------ 

------------------------------------------------ 

------------------------------------------------ 

------------------------------------------------ 

------------------------------------- 

------------------------------------- 

------------------------------------------------ 

------------- 

Paleocene planktonic 


Fig (3.5) Biostratigraphic range chart of planktonic foraminifera at Cretaceous/Tertiary 

boundary in Dokan area (Qulka section) 

56



L A T E M A A ST R I C H T I A N P A L E O C E N E EPOCH--AGE 

Tanjero Interfin. (Aqra Lst) Tanjero Kolosh FORMATION 

T48 T40 T35 T28 T22 T14 T10 T1 K1 K7 K11 K16 K20 K30 K45 K55 K65 SAMPLE No 

LITHOLOGY 

1 30 60 90 110 125 135 140 145 150 160 170 200 217 THICKNESS m. 

P 

CF.zones 

CF 5 CF4 CF3 CF2 CF1 

0 P 1a P1b (Li&Killer,1998a) 

P.inter. R. fructicosa P. hariaensis P. palpebra P.hant. á 

SUBZONE 

-------------- ---- --- ------ ------ ------------------------ ------- -- 

--------- --- ------------- --------------------- ---- ---- --- ---- 

----------------- ---- ---- --- 

- ---- - ------ ---- --- - ----- -- --- ---- --- --- --- 

------ ---- ---- ---- -- --- ---- ---- -- ----- --- - 

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------------------------ ------------------ ---- 

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--------------------------------------------------------- --- 

----------------------------------- 

--------------------------------------- 

--- ---- 

--- - ---- - ---- 

--- -- ---- --- --- 

--- --- ----- 

---- -- - ----- 

---- --- -- - --- 

-- --- -- - --- -- --- 

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- -- ---- --- -- 

-- -- - -- - -- - -- 

---- -- ---- 

- -- - -- -- --- -- 

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----- 

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-- -- -- -- -- - -- 

- -- -- - 

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----- 

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--- - --- -- -- 

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---- 

---- - --- - --- 

----- - -- -- -- - - 

--- --- --- 

-- -- -- -- -- 

- ---- - ---- 

----- - ---- - ---- 

--- --- --- 

- ---- --- 

Benthonic 





= sp. 

Rzehakina epigone (Rzehak) 







Ellipsonodosaria plumerae (Cushman) 


= midwayensis 

Praebulimina ovulum 





= pruvianus 



= retusa 

= rosetta 













Pleurostomella subnodosa (Reuss) 



= carseyae (Plummer) 




= danica 

Lagena sp. 






Rotalia spp. 

Valvulammina sp. 

Omphalocyclus macroporus (Lamar) 



Loftusia morgani Douville 


Fig (3.6) Biostratigraphic range chart of benthonic foraminifera at Cretaceous/Tertiary 

boundary in Dokan area (Qulka section) 

57



LATE CAMP. EARLY Y MAASTRICHTIAN ----- LA TE MAASTRICHTIAN P A L E O C E N E EPOCH--AGE 

Shiranish Shiranish/Tanjero transition unit Tanjero Kolosh FORMATION 

1 3 5 10 15 20 25 30 35 40 45 50 55 60 70 80 90 100 110 115 120 130 140 146 SAMPLE No 

58 

LITHOLOGY 

1 15 30 50 70 89 100 113 143 171 200 230 THICKNESS m. 

CF.zones 

CF 8 CF 7 CF 6 CF 5 CF 4 CF 3 CF 2 CF 1 P 

pá P 1a 

(Li&Killer,1998a) 

Glt. G. C. P. 

P. 

P. 

P. 0 

P1b 

R. fructicosa 

aegyptiaca. gansseri contusa interm. 

hariaensis palpebra hantk. 

SUBZONE 

------------------------------------------------- -------------- ------ ----------------------------- --------- ---- --- ----- --- 

------------------- ------------- ----------- --- --------------- -------- ---- ---------------------------- ----- -- -- --- --- --- --- --- - 

---------------------------------- -- ------- ------ ----- ---------- ----- ----------- -------- ---- -- ---- ---- ---- ---------- -- --- 

---------------------------------------------------------------------------------------------------------------------------------------- 

----------------------------------------------------------------------------------------------------------------------------------------------------------- 

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----------------------------------------- --------- - - - 

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0--------0 

Heterohelix navarroensis Loeblish 




= nauttalli (Voorwijk) 

= reussi (Cyshman) 

= pulchra (Brotzen) 

Laeviheterohelix glabrans (Coshman) 









= rotundata Bronnimann 

= milamensis Smith & Pessango 

= reicheli Bronnimann 


= wiedenmayeri (Gandolfi) 




= pettersi Gandolfi 

= angulata Tilev 


= linneina (d Orgigny) 

= orientalis El-Naggar 








= rosetta Carsey 

= insignis (Gandolfi) 

= mariei Banner & Blow 

= ventricosa White 

= sp. 




= Patelliformis (Gandolfi) 

= walfischensis Todd 

= sp. (nov. sp?) 

Rugotruncana circumnodifer (Gandolfi) 



= havanensis (Voorwuk) 

= pschadae (Keller) 

= sp. 



= subcarinatus Bronnimann 



= ultramicra (Subbotina) 








= palpebra 

= excolata (Cushman) 




= intermedius (Bolli) 

Kuglerina rotundata (Bronnimann) 

Costellagerina cf. bulbosa Belford 

Archaeoglobigerina carteri (Kassab) 

= blowi Pessango 

= cretacea (d Orbigny) 




Trinitella scotti Bronnimann 

Plummerita hantkeninoides (Bronnimann) 

Fig (3.7) – Part 1: Biostratigraphic range chart of planktonic foraminifera at 

Cretaceous/Tertiary boundary in Smaquli area (Gali section) 

Cretaceous planktonic foraminifera



LATE CAMP. EARL Y MAASTRICHTIAN ----- LA TE MAASTRICHTIAN P A L E O C E N E EPOCH--AGE 

Shiranish Shiranish/Tanjero transition unit Tanjero Kolosh FORMATION 

1 3 5 10 15 20 25 30 35 40 45 50 55 60 70 80 90 100 110 115 120 130 140 146 SAMPLE No 

LITHOLOGY 

1 15 30 50 70 89 100 113 143 171 200 230 THICKNESS m. 

CF.zones 

CF 8 CF 7 CF 6 CF 5 CF 4 CF 3 CF 2 CF 1 P 


Glt. 

aegyptiaca. 

G. 

gansseri 

C. 

contusa 

P. 

interm. 

R. fructicosa 

P. 

hariaensis 

P. 

palpebra 

P. 

hantk. 

0 

pá P 1a P1b 

SUBZONE 

Parvularugoglobigirina eugubina (Luterbacher & Premoli Silva) 

Parvularugoglobigirina extensa (Blow) 

Rectoguembelina cretacea Cushman 

Hedbergella monmouthensis (Olsson), 



Chiloguembelina morsei (Kline) 



Parasubbotina aff pseudobulloides (Olsson et al) 












---------- 

---------- 

------------------ 

---- 

----------------- 

------------------------------------------ 

---------------------------- 

------------------------------------------ 

- ---------------------------------------- 

---------- 

-------------------------------- 

------------------------------------------ 

--------- 

-------------- --------- ------------------ 

------------------------------------------ 

------------------------------------------ 

------------------------------------------ 

------------------------------- 

------------------------------------------ 

-------------------------------- 

----------------------- 

Paleocene planktonic foraminifera 

Fig (3.7) Part 2:- Biostratigraphic range chart of planktonic foraminifera at 

Cretaceous/Tertiary boundary in Smaquli area (Gali section) Continued. 

Globigerinelloides volutes (White), G. subcarinatus Bronnimann, G. 

prairiehillensis Pessango, Pseudotextularia elegans (Rzehak), P. 

59 

deformis 

(kikoine), P. intermedia (De Klasz), Racemiguembelina poweli Smith & 

Pessango, Pseudoguembelina costulata (Cushman), P. 

excolata (Cushman), 

Hedbergella monmothensis (Olsson), P. holmdelensis Olsson, 

Abathomphalus intermedius (Bolli), Archaeoglobigerina carteri (Kassab), 

Gublerina cuvillieri Kikoine, Gumbelitria cretacea Cushman. 

Due to high similarities of foraminiferal occurance, the present Zone (CF5) 

is equvalent to that of Li and Keller (1998a,b), (Abramovich et al., 2002), (Samir 

2002) , it is most likely equivalent to the upper part of Gansserina gansseri 

Zone recorded in the North and Northeast of Iraq and different regions of the 

world (Al-Mutwali and Al-Jubouri, 2005), (Al-Mutwali, 1996), (Hammoudi, 2000), 

(Caron 1985), (Ubaidalla, 2005), (Robaszynski et al., 1984), (D Hont & Keller, 

1991), and it is equivalent to the upper part of Glt. contusa Zone of (Abawi et al., 

1982, and Abdel-Kareem, 1986), and Glt.contusa-R. fructicosa Zone of (Premoli


Silva and Sliter, 1995, 1999) from Italy. (Abdel-Kareem & Samir. 1995), Egypt. 

(Fig. 3.12) 

The Pseudotextularia intermedia Zone spans about 0.73Myr (69.06- 

68.33Ma), (730Ky/19) meters estimating absolute ages based on magnetochron 

ages with (38.5 Ky/meter) of moderate rate of deposition (Fig.3. 12 – 3. 13), 

(Fig,5.11) 

Age: Late Early Maastrichtian. 

Note: it is important to mention that the Pseudotextularia intermedia Zone was 

recorded also from the other studied sections (only the upper part) in which the 

lower limit not studied. This biozone represented by moderate diversity of 

planktonic foraminiferal assemblage by 43 species in Sirwan section, (Fig.3.1), 

44 species in Qulka section (Fig.3.5) and Low diversity planktonic foraminiferal 

assemblage by (27) species in Qishlagh section, (Fig.3.4) 

3.2.1.5- Racemiguembelina fructicosa Interval Zone (CF4) 

Racemiguembelina fructicosa zone (CF4) was introduced by Li and Keller 

(1998 a and b) as a biostratigraphic interval between FAD of Racemiguembelina 

fructicosa (Egger) at the base and the FAD of Pseudoguembelina hariaensis at 

the top. The FAD of Racemiguembelina fructicosa (Egger) in the studied section 

recorded from the upper most part of reddish to pale brown unit and covers the 

basal part of the Tanjero Formation (sample no.38) to the FAD of 

Pseudoguembelina hariaensis Nederbragt within Tanjero Formation (sample 

no.58). (plate. 1, Fig. 9). Attaining a thickness of 23m. at Gali section (Fig 3.7) 

110 meters Sirwan section (Fig 3.1) 32 meters Kato section (Fig 3.3) 83 meters 

Qulka section (Fig 3.5), while the upper limit of this zone in Qishlagh section not 

recorded due to change of environmental parameters which is represented by 

thick bedded interfingering limestone of Aqra Formation at the upper part of 

Tanjero Formation 

It is important to mention that the zonal scheme of Cretaceous foraminifera 

(CF) proposed by Li and Keller (1998 a&b), which replaces the Abathomphalus 

mayaroensis zone with four zones (R. fructicosa zone, P. hariaensis Zone, P. 

palpebra Zone, P. hantkeninoides Zone), for a much improved age estimate for 

60


the late Maastrichtian (Fig. 3.12). The total range zone of A. mayaroensis Zone 

characterized the Upper Maastrichtian in low latitude regions as well as the 

Tethyan paleogeographic realm. However it has been found that A. mayaroensis 

is very rare or absent in high latitude regions (Blow, 1979) and in the present 

section also, consequently it is more accurate to use the new zonal scheme. 

Most of the workers in the zonal scheme placed Racemiguembelina 

fructicosa zone at the lower Late Maastrichtian (Li and Keller, 1998a&b), 

(Abramovich et al., 2002), at DSDP Site 525A. (Keller et al., 1995), from Tunisia. 

(Obaidalla 2005), and (Samir 2002), Egypt. As defined above, the present 

Biozone (CF4) is correlatable with the lower part of A. mayaroensis of (Abawi et 

al., 1982 and Abdel-Kareem 1986), (Premoli Silva and Sliter 1995, 1999),Italy. 

(Caron 1985), and (Robaszynski et al., 1984), general. (Fig. 3.12). 

This zone covered abundant occurrence of the nominate species, in addition 

to the index planktonic 55 species identified from Gali section, e.g: Heterohelix 

navarroensis Loeblish, H. globulosa (Ehrenberg), H. striata (Ehrenberg), H. 

punctulats (Cushman), H. nauttalli (Voorwijk), H. reussi (Cyshman), H. pulchra 

(Brotzen) , Planoglobulina carseyae (Plummer), P. brazoensis Martin, P. 

acervulinoides (Egger), Rugoglobigerina rugosa (Plummer), R. scotti 

(Bronnimann), R. hexacamerata Bronnimann, R. macrocephala Bronnimann, 

R. pennyi Bronnimann, R. milamensis Smith & Pessango, R. reicheli 

Bronnimann, Gansserina gansseri (Reuss), Globotruncanita stuartiformis 

Dalbez, G. conica White, G. pettersi Gandolfi, G. angulata Tilev, 

Globotruncana aegyptiaca Nakkady, Glt. falsostuarti Sigal, Glt. dupeublie 

Caron et al., Glt. lapparenti Boli, Glt. arca (Cushman), Contusotruncana 

contusa (Cushman), C. plicata White, C. Patelliformis (Gandolfi), C. 

walfischensis Todd, C. sp. (nov. sp?), Rugotruncana circumnodifer (Gandolfi), 

R. subcircumnodifer (Gandolfi), Globotruncanella petaloidea (Gandolfi), G. 

pschadae (Keller), Globigerinelloides volutes (White), G. subcarinatus 

Bronnimann, G. prairiehillensis Pessango, Pseudotextularia elegans (Rzehak), 

P. deformis (kikoine), P. intermedia (De Klasz), Racemiguembelina 

fructicosa (Egger), R. poweli Smith & Pessango, Pseudoguembelina 

costulata (Cushman), P. palpebra, P. excolata (Cushman), Hedbergella 

61


monmothensis (Olsson), H. holmdelensisOlsson, Abathomphalus mayaroensis 

(Bolli), A. intermedius (Bolli), Kuglerina rotundata (Bronnimann), 

Archaeoglobigerina carteri (Kassab) Gublerina cuvillieri Kikoine, Gumbelitria 

cretacea Cushman, 

The planktonic foraminiferal assemblages represented by moderate number 

of species diversities in both Sirwan and Qulka section represented by 45 

species (figs. 3.2 and 3.5), while this number was reduced to 30 species in Kato 

section and 26 species in Qishlagh section , in Qishlagh the same assemblage 

and number of species continued from previous P. Intermedia Biozone to R. 

fructicosa zone with addition to the nominate species of R. fructicosa, at the 

lower part of 10 meters only, after that all planktonic foraminiferal assemblages 

disappeared and replaced by larger foraminiferal community with other smaller 

benthonic forams for the total remaining interval of Tanjero Formation till the 

transitional interval between Tanjero Formation and Red Bed series which is 

characterised by concentration of reworked larger foraminiferal assemblage and 

dwarfed macrofossils of pelecypods, gastropodes, brachiopodes and solitary 

corals like Cyclolites. planktonic forams represented by: Heterohelix 

navarroensis Loeblish, H. globulosa (Ehrenberg), H. striata (Ehrenberg), H. 

punctulats (Cushman), Planoglobulina carseyae (Plummer), P. brazoensis 

Martin, Rugoglobigerina rugosa (Plummer), R. scotti (Bronnimann), R. 

hexacamerata Bronnimann, R. macrocephala Bronnimann, Gansserina 

gansseri (Reuss), Globotruncanita stuarti (de Lapparent), G. stuartiformis 

Dalbez , G. conica White, Globotruncana aegyptiaca Nakkady, 

Contusotruncana contusa (Cushman), C. fornicata Plummer, C. plicata White, 

Globotruncana arca (Cushman), Glt. gagnebini Tilev Globotruncanella 

petaloidea (Gandolfi), Globigerinelloides volutes (White), Pseudotextularia 

elegans (Rzehak), P. deformis (kikoine), Racemiguembelina fructicosa (Egger), 

Pseudoguembelina costulata (Cushman), 

The benthonic forams represented by : Bolivina incrassata Reuss, 

Bolivinoides draco (Marsson), Cibicidoides dayi (White), C. subcarinatus 

Cushman & Deaderick, C. excavata Brotzen, Osangularia navarrana 

(Cushman), Pullenia jarvisi Cushman, Pyrulinoides sp. Neoflabellina rugosa (d , 

62


Orbigny), Bulimina ovulum Reuss, Oolina apiculata Reuss, Globorotalites 

michelinianus (d , Orbigny), Ammodiscus cretaceous (Reuss), A. pruvianus, 

Marsonella oxycona (Reuss), Dorothia smokynensis Wall, D. retusa, D. 

rosetta, Textularia astutia. Lalicker, Spiroplectamina israelskyi Hillebrandt, S. 

laevis. (Roemer), Gyroidina girardana (Reuss), Gyroidinoides globosus. 

(Hagenow), Gaudryna pyramidata. Cushman, Clavulinoides globulifera.Ten Dam 

&Sigal, Conicospirilina sp. Rotalia sp. Valvulammina sp. Omphalocyclus 

macroporus (Lamark), Orbitoides medius (d Archiac), O. tissoti Shlumberger, O. 

apiculatus Shlumberger, Lepidorbitioides socialis (Leymerie), Siderolites sp. 

Loftusia elongata Brady, L. morgani Douville, L. persica Brady, L. minor Cox , L. 

coxi Henson, L. sp.These assemblages of benthonic foraminifera in addition to 

macrofossils like echinoides, gastropods, cephalopods, brachiopods, corals and 

pelecypods (coral like rudistids ),indicate the fundamental variation in lithology 

and Faunal assemblages from Tanjero clastics to the interfingering interval of 

Aqra Limestone represents quite graditional change to reefal facies, probably 

formed due to the presence of submerged high within the Tanjero foreland 

basin at the end of the Maastrichtian resulted from the termination of 

Paraxysmal phases of Laramide orogeny. ( Lawa et al.,1998, Al Omari et al., 

1989, Al Mutwali and Abawi, 2005) 

The age estimation of this biozone by (Li and Keller, 1998a), records the 

time span between (68.33 Ma) to (66.83 Ma) (1500 KY) estimating absolute 

ages based on magnetochron ages with (62 ky/m) low rate of deposition in Gali 

section, (13, 5 ky/m) high rate sedimentation in Sirwan area. (18 ky/m) high rate 

of deposition in Qulka section Dokan area. (Figs. 3.10 -3.11). 

Age: Early Late Maastrichtian. 

3.2.1.6- Pseudoguembelina hariaensis Interval Zone (CF3) 

The Pseudoguembelina hariaensis zone was defined by Li and Killer, (1998a) 

as a partial range of the nominate species between the FAD of 

Pseudoguembelina hariaensis Nederbragt and the LAD of Gansserina gansseri 

(Bolli). In the studied area this zone also marked by the FAD of the nominate 

species to the last occurrence of Gansserina gansseri (Bolli). (Plate 16; Fig. 6).It 

is covers the intervals of (21)meter in Gali section, (23) meters in Qulka section 

63


and 30 meters in Sirwan section. This zone shows reliable abundance of 

Pseudoguembelina hariaensis Nederbragt and other assemblages' planktonic 

foraminifera which totally resembles that of the underlying Racemiguemblina 

fructicosa zone (CF4), in Gali section with the following planktonic forams of 50 

species like: Heterohelix navarroensis Loeblish, H. globulosa (Ehrenberg), H. 

striata (Ehrenberg), H. punctulats (Cushman),H. nauttalli (Voorwijk), H. reussi 

(Cyshman), Laeviheterohelix glabrans (Cyshman), Planoglobulina carseyae 

(Plummer), P. brazoensis Martin, P. acervulinoides (Egger), Rugoglobigerina 

rugosa (Plummer), R. scotti (Bronnimann), R. hexacamerata Bronnimann, R. 

macrocephala Bronnimann, R. pennyi Bronnimann,R. reicheli Bronnimann, R. 

rotundata Bronnimann, Gansserina gansseri (Reuss), Globotruncanita 

stuartiformis Dalbez, G. conica White, G. pettersi Gandolfi, G. angulata 

Tilev, Globotruncana aegyptiaca Nakkady, Glt. falsostuarti Sigal, Glt. 

dupeublie Caron et al., Glt. lapparenti Boli, Contusotruncana contusa 

(Cushman), C. plicata White, C. Patelliformis (Gandolfi), C. walfischensis 

Todd, C. sp. (nov. sp?), Rugotruncana circumnodifer (Gandolfi), 

Globotruncanella petaloidea (Gandolfi), G. pschadae (Keller), Globigerinelloides 

volutes (White), G. subcarinatus Bronnimann, Pseudotextularia elegans 

(Rzehak), P. deformis (kikoine), Racemiguembelina fructicosa (Egger), 

Pseudoguembelina costulata (Cushman), P. palpebra, P. excolata (Cushman), 

Hedbergella monmothensis (Olsson), H. holmdelensisOlsson, Abathomphalus 

mayaroensis (Bolli), Kuglerina rotundata (Bronnimann), Costellagerina cf. 

bulbosa Belford, Gublerina cuvillieri Kikoine, Gumbelitria cretacea Cushman. 

The species number of planktonic foraminifera in this zone is reduced to 45 

species at Sirwan section (Fig. 3.1) and 40 species in Qulka section Dokan area 

(Fig. 3.5). While this number shows its relative decreasing to 27 species in Kato 

section (Fig. 3.3). This zone is recorded only from the marly and shaley 

limestone layers between the last 12 meters of Aqra interfingering Limestone 

within Tanjero Formation which is interrupted 10 meters of unfossiliferous 

sandstone and marl. In the upper part of Tanjero Formation at Kato section. 

64



LATE CAM.----EARLY MAASTRICHTIAN ----------- LATE MAASTRICHTIAN P A L E O C E N E EPOCH--AGE 

Shiranish Shiranish/Tanjero trans. unit Tanjero Kolosh FORMATION 

1 3 5 10 15 20 25 30 35 40 45 50 55 60 70 80 90 100 110 115 120 130 140 146 SAMPLE No 

65 

LITHOLOGY 

1 15 30 50 70 89 100 113 143 171 200 230 THICKNESS m. 

CF.zones 

CF 8 Cf 7 CF 6 CF 5 CF 4 CF 3 CF 2 CF 1 

P 

P P 


P 1a 1 

P. 

P. P. P. 0 

Glt, 

C. 

R. 

á 

G. gansseri 

intermed 

hariaens palpe hantk 

aegyptiaca 

contusa 

fructicosa 

b SUBZONE 

ia. 

is bra ini. 

- --- -- -- ---- --- ----- ---- --- --- -- -- 

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- ------ ----- -- -- 

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- --- -- -- 

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- - - -- --- 

-- ---- -- --- 

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------ --- ---- ----- 

--- --- ---- ----- 

-- ---- ----- -- 

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---- - ----- -- 

-- -- -- 

-- ----- -- -- 

- -- ---- --- -- --- 

--- - --- -- -- 

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-- --- - - --- --- 

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-- --- ---- - -- 

------- ---------- 

-- ---- ------ 

--- ---- -- ---- 

----- 

- ---- 

--- --- -- ---- 

-- ------ ----- --- 

Fig (3.8) Biostratigraphic range chart of benthonic foraminifera at Cretaceous/Tertiary 

boundary in Smaquli area (Gali section) 

FORAMINIFERA 

BENTHONIC 




= miliaris Hitt & Koch 

= sp. 



= excavata Brotzen 



= quinqueloba (Reuss) 





= midwayensis 

Praebulimina ovulum (Reuss) 

= aspera (Cushman &Parker) 

= laevis (Beissel) 

= carseyae (Plummer) 



= golbosa (Montagu) 


= sp. 


= pruvianus 



= retusa 

= rosetta 

= sp. 





= navicula (d Orbigny) 

Stilomella midwayensis. (Cushman &Todd) 

Stensioina excolata (Cushman) 


= affinis Reuss 








Pleurostomella subnodosa (Reuss) 

= paleocenica (Cushman) 




= gunderbookaensis. Crespin 

= sp. 


= danica 

Lagena hispida Reuss 

= sp. 

Palliolattella sp. 




= pulvina 


= exsertus (Belford) 

= subangulatus (Plummer) 



Saracenaria navicula (d Orbigny) 

Ellipsodimorphina sp.


There is no any evidence of planktonic foram occurrence except of some larger 

foraminifera and smaller benthonic till the interval of Tanjero -- Red Bed 

transition unit which characterized by the presence of reworked larger forams. 

The benthonic foraminifera identified from the uppermost part of Tanjero 

Formation are: Praebulimina quadrata, Oolina apiculata Reuss, Nodosaria 

minor Hantken, Globorotaloides sp. Spiroplectamina israelskyi Hillebrandt, 

Lenticulina muennsteri,Dorothia crassa, D. smokynensis Wall, D. retusa, 

Omphalocyclus macroporus, Orbitoides medius (d Archiac), O. tissoti 

Shlumberger, Loftusia elongata Brady, L. morgani Douville, L. persica Brady, L. 

minor Coxi, 

As defined above, the present Biozone (CF3) is correlatable with the Zone 

recorded by (Li and Keller, 1998a,b), (Abramovich and Keller,2003) in DSDP 

Site 525A. Abramovich et al., (2002) Madagascar. (Keller et al., 1995) from 

Tunisia. (Keller, 2004) Eastern Tethys. (Samir, 2002), (Keller, 2002), (Obaidalla, 

005) Egypt. (Sharbazheri, 2007) NE Iraq, and it is correlated with the middle 

part of Abathomphalus mayaroensis zone recorded in the Northeast of Iraq 

(Abawi et al., 1982, and Abdel-Kareem,1986), in Italy (Premoli Silva and Sliter, 

1995, 1999) (Premoli Silva et al., 1998), (Abdel-Kareem & Samir, 1995) Egypt, 

and (Robaszynski et al., 1984) (Caron, 1985) general.(Figs. 3.12 - 3.14) . 


Middle Late Maastrichtian, with the time span of (66.83Ma) to (65.45Ma) 

estimating absolute ages based on magnetochron ages. (1380 Ky) estimating 

absolute ages based on magnetochron ages with 66ky/m low rate of deposition 

in Gali section. (60 ky/m) low rate of deposition in Qulka section Dokan area.(46 

ky/m) low to moderate rate of sedimentation in Sirwan valley.(Figs. 3.12 & 3.13) 

Age: Middle Late Maastrichtian. 

3.2.1.7- Pseudoguembelina palpebra Interval Zone (CF 2) 

This Zone (CF2) defines the interval between the LAD of Gansserina 

gansseri at the base to the FAD of Plummerita hantkeninoides at the top. Li & 

Keller, (1998 a and b) introduced this zone from DSDP Site 525A and Tunisia, 

respectively. At Gali section in Smaquli area, the Zone (CF2) covers spans 24 

66


meters (Fig. 3.7) (Plate.16; Figs. 7, 8). The recorded planktonic assemblage of 

this zone is characterized by the same number 50 species diversity with 

underlying Pseudoguembelina hariaensis zone, and marked by the extinction of 

Heterohelix punctulatus (Cushman), Gansserina gansseri, Globigerinelloides 

volutes (White), and Laeviheterohelix glabrans (Cyshman), at the upper part of 

this zone. Besides, the planktonic foraminiferal species enduring from the 

underlying Biozones, some species shows their first appearance, e.g. 

Globotruncana Falsoscalcarata Kerdany & Abdelsalam, Globotruncanella sp. 

and Trinitella scotti Bronnimann were appeared for the first time with this zone. 

In Qulka section at Dokan area, the Zone (CF2) covers spans (9) meters 

(Fig. 3.5) this zone represented by 37 species with the extinction of Gansserina 

gansseri (Reuss), Globigerinelloides prairiehillensis Pessango at the base and 

Globigerinelloides volutes (White), G. subcarinata Bronnimann at the upper part 

of this zone. The first appearance of Rugoglobigerina rotundata Bronnimann at 

the base and Globotruncana Falsoscalcarata Kerdany & Abdelsalam, at the 

upper part of this zone. 

The Pseudoguembelina palpebra Interval Zone (CF 2) in Sirwan valley 

displays spans 25 meters (Fig. 3.1), biostratigraphically represented by 

decreasing species number from 49 to 38 species and there is no any distinctive 

appearance of new species with this zone. The planktonic foraminiferal 

assemblages of this zone in Sirwan section represented by Heterohelix 

navarroensis Loeblish, H. globulosa (Ehrenberg), Laeviheterohelix glabrans 

(Coshman), Planoglobulina carseyae (Plummer), P. acervulinoides (Egger), 

Rugoglobigerina rugosa (Plummer), R. scotti (Bronnimann) , R. hexacamerata 

Bronnimann, R. macrocephala Bronnimann, R. pennyi Bronnimann, R. reicheli 

Bronnimann, Globotruncanita stuartiformis Dalbez , G.conica White , 

Globotruncana aegyptiaca Nakkady, Glt. Falsocalcarata Kerdany & 

Abdelsalam, Glt. falsostuarti Sigal, Glt. dupeublie Caron et al., Glt. lapparenti 

Boli, Contusotruncana contusa (Cushman), C. plicata White, C. walfischensis 

Todd, Rugotruncana circumnodifer (Gandolfi), R.subcircumnodifer (Gandolfi), 

Globotruncanella petaloidea (Gandolfi), G. pschadae (Keller), Globigerinelloides 

prairiehillensis Pessango, Pseudotextularia elegans (Rzehak), P.deformis 

67


(kikoine), Racemiguembelina fructicosa (Egger), Pseudoguembelina hariaensis 

Nederbragt, P. palpebra, P. excolata (Cushman), Hedbergella monmothensis 

(Olsson), H. holmdelensis Olsson, Gublerina cuvillieri Kikoine, Gumbelitria 

cretacea Cushman. 

As defined above, the present zone (CF2) of studied area is equivalent to the 

same zone of the P. palpebra Zone of South Atlantic DSDP Site 525A (Li & 

Keller, 1998a), (Abramovich et al.,2002); and Tunisia (Li & Keller, 1998b), 

(Arenillas et al.,2000); eastern Tethys (Keller, 2004), the present P. palpebra 

Zone is equivalent to the upper part of Abathomphalus mayaroensis Zone 

recorded from different parts of the world (Premoli Silva & Sliter, 1995 & 1999), 

(Molina et al., 1996) Canudo et al., 1991); from Spain; Premoli Silva et al.,1998 

eastern Mediterranean; (Robaszynski et al., 1984; Caron, 1985), general; 

(Maestas et al., 2003), USA California; and Egypt (Obaidalla, 2005; Samir 2002; 

Elnady &Shahin, 2001; Luning et al.,1998). The present P. palpebra Zone is 

equivalent to the upper part of Abathomphalus mayaroensis Zone recorded from 

different localities from Iraq, (Al-Mutwali and Al Juboury, 2005; Al-Mutwali, 1996; 

Hammoudi, 2000; Abawi et al., 1982; Abdel-Kireem, 1986; Kassab, 1972, 1974, 

1975, 1976, 1979, and Kassab et al., 1986) (Figs 3.10 -12) 


Upper Late Maastrichtian, with the time span of (65.45Ma) to (65.30Ma) 


absolute ages based on magnetochron ages with (6 ky/m) high rate of 

deposition in Gali section. (17 ky/m) high rate of deposition in Qulka section 

Dokan area.(6 ky/m) high rate of sedimentation in Sirwan valley. (Figs. 3.12 -14) 

Age: Upper Late Maastrichtian. 

3.2.1.8- Plummerita hantkeninoides Total Range Zone (CF 1) 

The biostratigraphic interval of this zone defined by the total range of the 

nominate taxon, Plummerita hantkeninoides (Bronnimann). Pardo et al. (1996) 

introduced the P. hantkeninoides Zone for the latest Maastrichtian of Spain. It 

marks the uppermost Cretaceous biozones. As its top marks the K/P boundary. 

The upper limit of this zone coincides with the mass extinction of large tropical-- 

68


subtropical taxa. At Studied sections, this zone covers the top (25) meters of the 

Maastrichtian in Sirwan area (Plate.16, Fig.12). (Plate.21, Figs.10, 11). (13) 

meters in Qulka section. And (15) meters in Gali section. The Characteristic 

recorded planktonic foraminiferal assemblage of this zone shows gradual 

decreasing in both species and individual numbers from Pseudoguembelina 

palpebra Zone to Plummerita hantkeninoides Zone. (50) to (37) species in Gali 

section (Smaquli area), (37) to (29) species in Sirwan section and (38) to (24) 

species in Qulka section (Figs. 3.1, 3.5 and 3.7), at this zone. In addition, the 

planktonic foraminiferal species enduring from the underlying biozones, only two 

species Plummerita hantkeninoides (Bronnimann) and Trinitella scotti 

Bronnimann show their first appearance in Gali section and Plummerita 

hantkeninoides (Bronnimann) in both Sirwan and Qulka section. The planktonic 

foraminiferal assemblages in Qulka section comprise 

Heterohelix navarroensis Loeblish, H. globulosa (Ehrenberg), H. striata 

(Ehrenberg), Rugoglobigerina rugosa (Plummer), R. scotti (Bronnimann), R. 

macrocephala Bronnimann, R. pennyi Bronnimann, R. rotundata 

Bronnimann, Globotruncanita stuartiformis Dalbez, G. conica White, 

Globotruncana falsocalcarata Kerdany & Abdelsalam, Glt. falsostuarti Sigal, 

Glt. dupeublie Caron et al., Contusotruncana contusa (Cushman), C. plicata 

White, Globotruncanella petaloidea (Gandolfi), Pseudotextularia elegans 

(Rzehak), Pseudoguembelina costulata (Cushman), P. hariaensis Nederbragt, 

P. palpebra, P. excolata (Coshman), Hedbergella monmothensis (Olsson), H. 

holmdelensis Olsson, Gumbelitria cretacea Cushman, Plummerita 

hantkeninoides (Bronnimann), (Fig. 4.5). 

As defined above and based on the associated planktonic foraminiferal 

assemblage, the present Plummerita hantkeninoides Total Range Zone (CF 1) 

is equivalent to the same zone recorded from Tunisia (Li & Keller, 1998b); 

Eastern Tethys Israel (Keller 2004), Egypt (Keller, 2002), ( Samir 2002 and 

Obaidalla 2005), (Pardo et al. 1996), (Keller 1996); Tunisia (Arenillas et 

al.,2000); to the upper part of Zone (CF 1-2) from South Atlantic DSDP Site 

525A (Li & Keller, 1998a); and Madagascar (Abramovich et al.,2002); DSDP 

Site 525A (Abramovich and Keller, 2003); USA (Stinnesbeck et al., 2004). The 

69


present Plummerita hantkeninoides Zone is equivalent to the upper most part 

of Abathomphalus mayaroensis Zone recorded from different parts of the world 

(Canudo et al., 1991), (Smit 2005),and (Chacon & Martin-Chivelet 2005) Spain; 

(Premoli Silva & Sliter, 1995 & 1999),Italy; (Premoli Silva et al., 1998), eastern 

Mediterranean ; (Govindan et al., 1996), India; (Robaszynski et al., 1984, and 

Caron, 1985), general; (Maestas et al., 2003), USA, California; (Martinez, 1989; 

Luning et al., 1998), south USA. And equivalent to Plummerita reicheli Zone of 

(Elnady & Shahin, 2001, and Shahin, 1992,), from Egypt. The present 

Plummerita hantkeninoides Zone is equivalent to the Kassbiana falsocalcarata 

Zone recorded from Shalki village and Sirwan valley (Kassab et al., 1986), 

(Kassab 1976). Tel Hajar.1 (Ghafor 1988), (Figs 3.12-14) 


Upper most Late Maastrichtian, with the time span of (65.30Ma) to (65.00Ma), 


absolute ages based on magnetochron ages with (20 ky/m) high rate of 

deposition in Gali section. (23 ky/m) high rate of deposition in Qulka section 

Dokan area.(12 ky/m) high rate of sedimentation in Sirwan valley. (Figs. 3.12-14) 

Age: Latest Maastrichtian. 

It is reliable to pay attention that the decreasing in the number of species 

within the Plummerita hantkeninoides Zone is continued to the end of this 

zone at K/T boundary as observed in Gali section from (37) to (28) species, (24) 

to (20) species in Qulka section and (29) to (23) species in Sirwan section. The 

large subtropical high diversities Maastrichtian planktonic foraminiferal 

assemblages suddenly disappeared at the stratigraphic level that corresponds to 

the top of this biozone. On paleontological criterion the Cretaceous/Tertiary 

boundary is placed either at the mass extinctions of Cretaceous planktonic 

foraminiferal assemblages as in all studied sections, or at the first occurrence of 

Paleocene species. It is convenient to assume that the stratigraphic intervals of 

transitional unit (at Tanjero – Red bed contact) in both Qishlagh and Kato 

sections in Qala-Cholan and Barzinja area respectively (Figs. 3. 3 - 4), which 

located on border line and represent the proximal area of Tanjero basin, 

characterized by reworked fossils of different types (macro and microfossils) 

70


from predeposited sediment of Tanjero basin to be the transitional time interval 

from Cretaceous to Tertiary, the second estimation is that the transitional unit 

may represent time interval of latest Maastrichtian or Earliest Danian of 

deposition, or the upper most part of Tanjero Formation chronostratigraphically 

may extended to the lower Paleocene while the another contradictory 

assumption is that the Red Bed Series may began from the upper Maastrichtian. 

The most important sedimentological evidence is Tagaran conglomerate 

within the upper part of Tanjero formation, shows the same sedimentological 

origin of that of transitional unit and conglomerate beds within the lower part of 

Red Bed Series. (Karim, 2004 and Al-Barzinjy, 2005), The K/T contact in the 

studied areas has been interpreted as conformable contact. 

3.2.2- Biostratigraphy of the Early Paleocene Formations: 

According to identified planktonic foraminiferal assemblages within Lower 

part of Kolosh Formation, in Smaquli, Dokan and Sirwan area, four biozones 

recorded in the region. The biostratigraphic zones of the studied area are 

described from the bottom to the top as below: 

3.2.2.1- P0. Guembelitria cretacea interval Zone. 

The contact line between Tanjero and overlying Kolosh Formation in Gali 

section placed on the last oily impregnated friable soft and weathered pale 

brown fine sandstone beds of 1 meter thickness barren of foraminifera except 

for few forms of Guembelitria cretacea Cushman. This fine sandstone bed 

overlied by 25cm dark organic papery shale and interlayred by thin beds of dark 

grey marl which evidenced by the record of Hedbergella monmothensis (Olsson) 

with Guembelitria cretacea. This interval is 1,25 meter thick representing the 

Guembelitria cretacea (P0) zone and marks the K/T boundary and defined as 

interval between the extinction of Cretaceous planktonic foraminifera, Last 

appearance Datum (LAD) of (Globotruncana, Rugoglobigerina, 

Globigerinelloides, Heterohelicids) at the base and the first appearance datum 

(FAD) of Parvularugoglobigerina eugubina (loterbacher & Premoli Silva) at the 

top. (Plate.26, Figs. 17-18) (Fig. 3. 7 part. 2). The Guembelitria cretacea 

Biozone is comparatively very well expanded (1, 25 meter) and lithologically 

71


characterized by similar sediment constituent between both Tanjero and 

overlying Kolosh Formation in which no one can observe the contact line 

between these two formations in the field especially in Smaquli and Dokan area. 

Another important point to be mentioned is the lack of any reworked 

foraminiferal evidence to be observed within (P0) Guembelitria cretacea zone 

and overlying biozones in mentioned areas. The K/T contact in the studied areas 

has been interpreted as conformable contact because of the absence of any 

sedimentological break, or erosional surface, no condensed section no 

mineralogical record observed in addition to uninterrupted biostratigraphic 

record. 

As defined above and based on the associated planktonic foraminiferal 

assemblage, the Guembelitria cretacea zone coincides with the same zone 

recorded from Tunisia (Li & Keller, 1998 b); from Egypt (Keller, 2002); Eastern 

Tethys Israel (Keller, 2004); general (Olsson et al., 2000), (Berggren & Norris, 

1997), (Berggren et al.,1995), (Keller, 1996); DSDP Site 525A (Abramovich and 

Keller, 2003) ; Spain (Pardo et al., 1996), (Smit, 2005). P0 is also equivalent to 

the Lower part of Guembelitria cretacea zone from Egypt by (Obaidalla, 2005) 

and Tunisia (Arenillas et al., 2000) and Canudo et al., 1991, Caravaca and 

Agost from Spain. 

The age estimation of this biozone by (Olsson et al., 2000) (Keller, 2002, and 

2004), records the earliest Paleocene (Danian), with the time span of (65.00Ma) 

to (64.97Ma) estimating absolute ages based on magnetochron ages. (30 Ky) 

ages with (24 Ky/m) high rate of deposition in Gali section. (Figs. 3.12 -13) 

Age: Earliest Paleocene (Danian). 

3.2.2.2- (Pá) Parvularugoglobigerina eugubina Total Range Zone 

Definition: Biostratigraphic interval is characterized by the total range of the 

nominate taxon. (Liu, 1993, emended. of Pá of Blow, 1979; Luterbacher and 

Premoli Silva, 1964). (Plate .24, Figs.9-14) 

Luterbacher & Premoli Silva (1964) firstly used the Globigerina eugubina 

Zone for the Early Paleocene of Central Italy. Blow, (1979) used 

Parvularugoglobigerina longiapertura to characterize the earliest Paleocene 

Zone P? (Globorotalia (Turborotalia) longiapertura). However, this assemblage 

72


seems to be close to those of the Pv. eugubina Zone. Moreover, in (Samir 

2002), most workers have included Pv. longiapertura with Pv. eugubina group 

(e.g. Olsson et al., 1992). In the studied section of Smaquli area, this zone 

covers the interval of 18 meters is characterized by a small-sized planktonic 

foraminiferal assemblage of a worldwide distribution, that represented by 

Parvularugoglobigirina eugubina (Luterbacher & Premoli Silva), 

Parvularugoglobigirina extensa (Blow), Hedbergella monmouthensis (Olsson), 

Rectoguembelina cretacea Cushman, Woodringina clytonensis (Loeblich & 

Tappan), W. hornerstownensis (Olsson), Chiloguembelina morsei (Kline), Ch. 

midwayensis (Cushman), Globoconusa daubjergensis (Bronnimann), 

Parasubbotina aff pseudobulloides (Olsson et al), Subbotina trivalis (Subbotina), 

Globanomalina archeocompressa (blow), Gl. planocompressa (Shutskaya), 

Eoglobigerina edita (Subbotina), E. eobulloides Morozova, E. simplicissma 

Blow, Praemurica taurica (Morozova), Guembelitria cretacea Cushman, 

( Fig.3.7 part.2) 

Fig (3.9) Genetic radiation, Phylogenetic relationship and Geologic range of Paleocene serial & low to high 

trochospiral microperforate wall structure planktonic foraminifera (From Olsson et. al, 2000) 

73


Fig (3.10) Genetic radiation, Phylogenetic relationship and Geologic range of Paleocene 

muricate, smooth walled, non-spinose and spinose concellate wall structure of 

trochospiral planktonic foraminifera (From Olsson et. al, 2000) 

74


Fig (3.11) Genetic radiation and phylogenetic reconstruction of the Early Paleocene 

microperforate planktonic foraminifera (From Liu & Olsson 1992) 

Based on faunal similarities, the present Pv. eugubina Zone is equivalent to 

the same zone recorded from Tunisia (Keller, 1998 b); Egypt (Elnady & Shahin, 

2001, Samir 2002 , Luning et al, 1998, Shahin 1992); Spain (Smit 2005); Ain 

Settara ,Tunisia (Arenillas et al., 2000); (Li & Keller, 1998 b); (Abramovich and 

Keller, 2003); Egypt (Keller, 2002); Eastern Tethys Israel (Keller, 2004), general 

(Olsson et al.2000); (Berggren & Norris 1997); (Berggren et al.1995); (Keller 

1996); to P1a of (Pardo et al. 1996), (Fig 3. 13-14) 

The age estimation of this biozone by Olsson et al., 2000, Li and Keller 

1998a, Keller, 2002, 2004, records the earliest Paleocene (Danian), with the 

time span of (64.97Ma) to (64.90Ma) estimating absolute ages based on 

magnetochron ages. 70Ky ages with 4 Ky/m high rate of deposition in Gali 

section. (Figs. 3.12 -14) 

Age: Earliest Paleocene (Danian). 

75


3.2.2.3- (Pá & p0) in Dokan and Sirwan valley. 

In the present study, the earliest Paleocene P0 (Guembelitria cretacea) 

Zone, and Pá Parvularugoglobigerina eugubina Zone) which is well observed 

in Smaquli area, was not recorded completely or continuously in both Qulka and 

Sirwan sections 

The Cretaceous/Tertiary boundary in Dokan area placed on the base of soft 

weathered friable fine sandstone and claystone of 5 meter thickness with very 

rare occurrence (Few individuals) of Guembelitria cretacea Cushman and 

Globoconusa daubjergensis (Bronnimann) recorded from the upper most part of 

this sandstone unit (Fig.3.5). As in Gali section, the base of this fine sandstone 

marks the extinction (Datum event) or disappearance of Cetaceous planktonic 


While in Sirwan valley, the Cretaceous/Tertiary boundary placed on the 

base of 3 meters of pale grey to yellowish, weathered friable conglomerate. This 

conglomerate and overlying 12 meters of dark grey organic rich shale alternate 

with marl, marly limestone and thin layer of siltstone, sandstone, are barren of 

foraminifera, as mentioned previously in Chapter Two that the sedimentary 

succession of the studied sections in Sirwan valley shows evidence of three 

diluted intervals of foraminiferal survivorship in the studied upper part of Tanjero 

Formation, and the fourth one at the base of Paleocene just after the extinction 

catastrophe of organism at the uppermost part of Maastrichtian. 

The age estimation of this interval depending on Magnetic polarity and 

recorded datum events by (Olsson et al., 2000), (Keller 2002, 2004), with the 

time span of (65.00Ma) end of Plummerita hantkeninoides to 64.90Ma last 

occurrence of Parvularugoglobigerina eugubina, estimating absolute ages based 

on magnetochron ages. 100 Ky with 20 Ky/m high rate of deposition in Qulka 

section. And with 6.5 Ky/m high rate of deposition in Sirwan section (Figs. 3.12- 

13) 

Sedimentologically any evidence of erosional surface, condensed section or 

mineralogical record, trace fossils or hard ground was not observed beside 

these significant points, the great lithologic similarity between both Tanjero and 

overlying Kolosh Formations in which no one can observe or distinguished the 

76


contact line of K/T boundary in the field. As there is no sign for the presence of 

an unconformity, we propose that this interval may be equivalent to both P0 & 

Pá (G. cretacea - P. eugubina Zone). In addition to these categories the 

sedimentation rate of deposition in all studied sections particularly in Sirwan 

section, closely at Cretaceous/Tertiary boundary recorded high to very high rate 

of sedimentation which reveals continuous uninterrupted sedimentary 

sequences. Otherwise the significant amount of conglomerate beds within the 

studied upper part of Tanjero Formation represented by 7 repeated beds of 0.5 

to 2 meters thickness) and three conglomerate beds within the lower part of 

Kolosh Formation. That reveals the intraformational conglomerate beds of 

limited lateral extensions. (Figs. 2.3 & 2.4), this could be attributed to either its 

extremely short duration, or its restriction to near shore, or diluted in 

foraminiferal survivorship rather than open ocean environments as outlined by 

Berggren & Norris, (1997). Entirely the presence of three local conglomerate 

beds in the upper most part of Tanjero Formation in Qulka section sustain and 

displays the same valid conception. (Fig.2.11) 

3.2.2.4- P1. Parvularugoglobigerina eugubina - Praemurica uncinata 

Interval Zone 

(P1; defined in Berggren et al., 1995, emend. of Berggren & Miller, 1988). 

Definition: Biostratigraphic interval between the LAD of Parvularugoglobigerina 

eugubina at the base and the FAD of Praemurica uncinata at the top. 

According to Berggren & Norris (1997) and Olsson et al.,( 2000) the P1 zone is 

subdivided into three subzones based on the sequential appearances of 

Subbotina triloculinoides (P1a/P1b boundary) and Globanomalina compressa 

/Praemurica inconstans (P1b/P1c boundary). In the studied area of (Gali, Qulka 

and Sirwan) sections only, P1a Zone and Lower part of P1b Zone encountered. 

(Fig. 3.13) 

77


3.2.2.4.1- (P1a) Parvularugoglobigerina eugubina - Subbotina 

triloculinoides interval subzone 

Definition: Biostratigraphic interval between the LAD of Parvularugoglobigerina 

eugubina and the FAD of Subbotina triloculinoides. (P1a; defined in Berggren et 

al., 1995; emendation of Parasubbotina pseudobulloides Subzone (P1a) in 

Berggren and Miller, 1988) 

In the present study, the P1a Subzone attains a thickness of 35 meter in 

Sirwan section, 40 meter in Qulka section and 25 meter in Gali section, (Figs.3. 

1, 3. 5 and 3. 7 part 2) (Figs. 3.12-14). The associated planktonic foraminiferal 

assemblage in Gali section is generally similar to that recorded from the 

underlying Pá Zone except for the absence of Parvularugoglobigirina eugubina 

(Luterbacher & Premoli Silva), Parvularugoglobigirina extensa (Blow), 

Hedbergella monmouthensis (Olsson), and Parasubbotina aff pseudobulloides 

(Olsson et al), in the lower part. While the Woodringina clytonensis (Loeblich & 

Tappan), Rectoguembelina cretacea Cushman, and Guembelitria cretacea 

Cushman were disappeared in the middle interval of this biozone, this Zone 

characterized by the first appearance of Parasubbotina pseudobulloides 

(Plummer) and Praemurica pseudoinconstans (Blow) at the beginning of this 

Biozone in Smaquli area. 

The associated planktonic foraminiferal assemblage is represented by 

complete occurrences of the following species in Sirwan area: 

Parvularugoglobigerina alabaminsis (Liu & Olsson), Rectoguembelina cretacea 

Cushman, Woodringina clytonensis (Loeblich & Tappan), W. hornerstownensis 

(Olsson), Chiloguembelina morsei (Kline), Ch. midwayensis (Cushman), 

Globoconusa daubjergensis (Bronnimann), Parasubbotina pseudobulloides 

(Plummer), Subbotina trivalis (Subbotina), Globanomalina archeocompressa 

(blow), G. planocompressa (Shutskaya), Eoglobigerina edita (Subbotina), E. 

eobulloides Morozova, E. simplicissma Blow, Praemurica taurica (Morozova), 

P. pseudoinconstans (blow), Guembelitria cretacea Cushman, in Qulka section 

the assemblages comprise (15) species belonging to (9) Genus like: 

Woodringina clytonensis (Loeblich & Tappan), W. hornerstownensis (Olsson), 

Chiloguembelina Morse (Kline), W. midwayensis (Cushman), Globoconusa 

78


daubjergensis (Bronnimann), Parasubbotina pseudobulloides (Plummer), 

Subbotina trivalis (Subbotina), Globanomalina archeocompressa (blow), S. 

planocompressa (Shutskaya), Eoglobigerina edita (Subbotina), E. eobulloides 

Morozova, E. simplicissma Blow, Praemurica taurica (Morozova), P. 

pseudoinconstans (blow), Guembelitria cretacea Cushman. In which the 

Guembelitria cretacea Cushman is represented in the lower part and 

Woodringina clytonensis (Loeblich & Tappan), and Globoconusa daubjergensis 

(Bronnimann) is prolonged to the middle part of this biozone. 

Based on faunal similarities, the combined P1a Subzones of studied sections 

could be equivalent to the lower part of Morozovella pseudobulloides Zone of 

Bolli (1966), Caron (1985),P1a Subzone of Blow, (1979); Elnady & Shahin 

(2001), from Egypt; Arenillas et al.,(2000) Tunisia; present subzones are 

correlatable with P1a Subzones of Berggren & Miller, (1988); Samir, (2000) In 

Egypt; to the P1b of Keller, (1988) and Keller et al., (1995), in Tunisia; to the P. 

pseudobulloides of Obaidalla, (2005), Egypt; and also it is equivalent to the P1a 

of Berggren and Norris, (1997),Berggren et al.,(1995); Keller, (2002, 2004), 

Abramovich et al.,(2002); Olsson, (2000); Smit, (2005), SE Spain. 


recorded datum events by (Olsson et al., 2000), (Keller 2002, 2004) with the 

time span of (64.90Ma) from the end of Parvularugoglobigerina eugubina to 

(64.50Ma) first occurrence of, Subbotina triloculinoides, estimating absolute 

ages based on magnetochron ages. (400 Ky) with (10 Ky/m) high rate of 

deposition in Qulka section. And with (11.5 Ky/m) high rate of deposition in 

Sirwan section and (16 Ky/m) high rate of deposition in Gali section. (Fig. 3.13). 

The estimated age is Early Paleocene (Early Danian). 

3.2.2.4.2- (P1b). Subbotina triloculinoides- Globanomalina compressa / 

Praemurica inconstans Interval Subzone 

Definition: Biostratigraphic interval between the FAD of Subbotina triloculinoides 

at the base and FAD of Globanomalina compressa and/or Praemurica 

inconstans at the top. 

Remarks: Berggren et al., (1995) introduced this subzone to emend P1b 

79


(Subbotina triloculinoides) Subzone of Berggren & Miller, (1988). At studied 

sections only the lower part of this subzone is studied which attains a thickness 

of 15 meters in Sirwan section, 10 meter in Qulka and Gali sections. The 

associated planktonic assemblage of this subzone differs from the underlying 

P1a Subzone by the presence of S. triloculinoides (Plummer), in addition to the 

following in Gali section like: 

Woodringina hornerstownensis (Olsson), Chiloguembelina midwayensis 

(Cushman), Globoconusa daubjergensis (Bronnimann), Parasubbotina 

pseudobulloides (Plummer), Subbotina trivalis (Subbotina), Globanomalina 

archeocompressa (blow), G. planocompressa (Shutskaya), Eoglobigerina edita 

(Subbotina), E. eobulloides Morozova, Praemurica taurica (Morozova), 

P.pseudoinconstans (blow). In Qulka section slight different were existed in 

planktonic assemblage as below: Chiloguembelina morse (Kline), Ch. 

midwayensis (Cushman), Parasubbotina pseudobulloides (Plummer), Subbotina 

trivalis (Subbotina), Globanomalina archeocompressa (blow), G. 

planocompressa (Shutskaya), Eoglobigerina edita (Subbotina), E. eobulloides 

Morozova, E. simplicissma Blow Praemurica taurica (Morozova), 

P.pseudoinconstans (blow). In Sirwan section similar assemblages were 

observed like: Parvularugoglobigerina alabaminsis (Liu & Olsson), 

Rectoguembelina cretacea Cushman, Woodringina clytonensis (Loeblich & 

Tappan), W. hornerstownensis (Olsson), Chiloguembelina morsei (Kline), CH. 

midwayensis (Cushman), Parasubbotina pseudobulloides (Plummer), Subbotina 

trivalis (Subbotina), S. triloculinoides (Plummer), Globanomalina 

archeocompressa (blow), G. planocompressa (Shutskaya), Eoglobigerina edita 

(Subbotina), E. eobulloides Morozova, Praemurica taurica (Morozova), P. 

pseudoinconstans (blow), 

Based on faunal similarities, the combined P1 b Subzones of studied 

section could be equivalent to the upper part of Morozovella pseudobulloides 

Zone of Bolli, (1966), and Blow, (1979). To Caron (1985); Elnady & Shahin, 

(2001), Samir, (2002) from Egypt; Arenillas et al.,(2000) Tunisia; to the P1c of 

Keller, (1988), and Keller et al., (1995), in Tunisia; to the S. triloculinoides by 

Obaidalla, (2005) in Egypt; and also it is equivalent to the P1b of Berggren and 

80


Norris (1997),Berggren et al.,(1995); Keller, (2002, and 2004), Abramovich et 

al.,(2002), Olsson (2000); and Smit (2005) SE of Spain. 


recorded datum events by (Olsson et al., 2000), (Keller, 2002, 2004) with the 

time span of 64.50Ma from first occurrence of, Subbotina triloculinoides, to FAD 

of Globanomalina compressa and/or Praemurica inconstans at the top of 63.00 

Ma. Estimating absolute ages based on magnetochron ages (Figs. 3.13 -14). 

The estimated age is Early Paleocene (Early Danian). 

81


Fig (3. 12 ) Correlation chart showing the planktonic foraminiferal biostratigraphic zones of Upper 

Cretaceous (Maastrichtian) of the studied sections with the planktonic foraminiferal zonation commonly 

used in low, middle and high latitudes, in the new zonal scheme, and inside the Iraq. The age of 

planktonic foraminiferal datum events shown. (Modified from different authors) 

82


Fig ( 3. 13) Correlation chart showing the planktonic foraminiferal biostratigraphic zones of Upper 

Maastrichtian/lower Danian of the studied sections with the planktonic foraminiferal zonation commonly 

used in low, middle and high latitudes, in the new zonal scheme. The age of planktonic foraminiferal datum 

events shown. (Modified from different authors) 

83


Fig (3.14). High resolution planktonic foraminiferal biozone for the Maastrichtian and 

Early Danian (Cretaceous/Tertiary) boundary at Gali section (Smaquli area) for Early 

Maastrichtian and other studied localities. Note that this biozones significantly refines the 

resolution for the upper Maastrichtian, by replacing the Abathomphalus mayaroensis zone 

by four biozones. 

84


Fig (3.15) Correlation of the previous Planktonic foraminiferal biostratigraphic zonation 

on Cretaceous/Tertiary boundary with the present study in the studied region and 

different localities of Iraq. 

85

Chapter Four 

Depositional Environmenment and Paleoecology 

CHAPTER FOUR 

DEPOSITIONAL ENVIRONMENT AND PALEOECOLOGY 

4.1- Preface 

Paleoecology is defined as the study of the interaction of organisms with one 

another and with the environment in the geological past, and the study of the 

causes of patterns of distribution and abundance of organisms. It is concerned 

with interaction between individuals and their physical, chemical and biological 

parameters of the environment, consequently through high resolution studies of 

these important parameters with lithologic characters of lithofacies, textures, and 

sedimentary structures. 

The most important group of organisms used in this study is planktonic and 

benthonic foraminifera, which play an important role in interpretation of 

depositional environment and paleoecology of most of the sedimentary basin of 

Mesozoic and Cenozoic Era in the world. 

The paleontologists continuously faced the problem of how the fossil communities 

reveal the paleoenvironment in which they lived. The worthy approach to solve such 

problem has been answered through the quantitative evolution of the planktonic and 

benthonic foraminiferal species and their abundance patterns. The variations in the 

relative abundance of these assemblages are used to document the rate and nature 

of the planktonic foraminiferal evolution and diversification through the Cretaceous/ 

Tertiary boundaries. 

In the present studied area , the encountered parts of Maastrichtian, Early 

Paleocene planktonic as well as benthonic foraminiferal assemblages developed 

not only to construct the biostratigraphic zones but also their species communities 

could reflect the nature of the biotope controlled by abiotic sedimentary 

environments. Paleobathymetric and paleoecological factors are studied through 

the distribution patterns of planktonic and benthonic foraminifera, where the total 

numbers of foraminiferal species, the diversity and statistical analysis of planktonic, 

86

Chapter Four 


benthonic forams, the Planktonic/Benthonic ratios and the 

Agglutinated/Calcareous ratios are the most important parameters in this chapter. 

4.2- Planktonic species diversity or species richness 

Species diversity is the total number of species in an assemblage, whereas 

species richness reflects the actual number of species present at a given time 

and is therefore a measure of environmental variability (e.g., climate, seasonality, 

nutrient fluctuations), but may be influenced by fossil preservation (e.g., 

dissolution, breakage of shells). Species richness may be significantly less than 

species diversity as a result of sample preservation, climate variations and/or 

local environmental conditions. (Keller 2004) 

Species richness at Smaquli, Dokan and Sirwan sections is unusually low 

during the latest Maastrichtian which starts from the end of Pseudoguembelina 

palpebra Zone (CF2) around 65.5 Ma and upward, it fluctuates about 30-20 

species in Plummerita hantkeninoides Zone, except for the lower and middle 

part of the studied sections where 40-50 species are present and across the 

Cretaceous/Tertiary contact at Kolosh Formation where it drops down to 17-14 

species (Figs. 4. 3 - 4.7). Even lower species richness was observed at Kato 

and Qishlagh sections with 25-28 species in Pseudotextularia intermedia and 

Racemiguembelina fructicosa Zones CF5 -CF4. While the planktonic 

foraminiferal assemblages interrupted their occurrences due to environmental 

changes in both Kato section from the lower part of Pseudoguembelina 

hariaensis (CF3) and lower part of Racemiguembelina fructicosa Zone in 

Qishlagh section, and replaced by shallow benthonic larger foraminiferal 

assemblages of platform biotope communities. (Figs 4.3-4) 

There is the fact that increasing distances from the shoreline, the turbidity 

decreases , enabling principal production to increase. In addition, the complex 

pelagic ecosystem, with many nutrient chains, is only developed at a certain 

water depth around the total photic zone and has noted that planktonic 

87

Chapter Four 


foraminiferal diversity (species richness) increases from shallower to deeper 

waters across shelf areas. (Van Der Zwaan et al., 1990) 

Sediment deposition at these localities occurred at outer neritic upper 

bathyal and middle-outer neritic depth, respectively. Comparable depth 

localities in Tunisia, Spain, and Mexico average 45-55 species (Lopez and 

Keller, 1996 in Keller, 2004; Pardo et al., 1996; Abramovich and Keller, 2002). 

Fossil preservation is excellent at Smaquli sections and relatively good in other 

studied localities and does not account for the low species richness, which 

appears to be regional throughout the studied area. To recognize these 

abnormally poor species assemblages exactly at the uppermost Maastrichtian 

Plummerita hantkeninoides zone (CF1), it is available to study species richness 

patterns across the Cretaceous/Tertiary boundary within high resolution 

biostratigraphic researches of all studied localities previously in Iraq and 

neighboring countries. 

Species richness and diversity tend to be highest in outer shelf-upper slope 

environments (250-500m) and gradually decrease in shallower waters across 

the continental shelf. (Keller, 2004), this can be confirmed in the present studied 

area. 

In the upper Maastrichtian zones (CF1 to CF3), species richness varies 

between 42-54 species at the outer shelf-upper slope section at El Kef (Keller, 

1988; Li and Keller, 1998c: Keller et al., 2002b in Keller, 2004). At the shallower 

middle neritic trends (Abramovich. and Keller, 2002), the lowest species 

richness is found at the innermiddle neritic locality of Seldja in southern Tunisia 

where on average only (10-15) species are present. Species richness is directly 

related to niche availability, which is related to water depth and watermass 

stratification. In shallow inner neritic environment, species richness is lowest 

because ecological niches are largely restricted to the surface mixed layer (50m) 

of the upper photic zone (Keller,2004) (Fig 4,1) 

88

Chapter Four 


Fig (4.1) Planktonic foraminiferal species richness across the Tunisian continental shelf-slope 

based on data from the inner shelf Seldja section (Keller and other,1998) , middle shelf Elles 

section ( Abramovich and Keller,2002), and outer shelf to upper slope El Kef section (Li and Keller 

1998c,). Note: The species richness increase with increasing depth across the shelf and is a 

function of available ecological niches and depth habitats (from Keller 2004) 

4.3- Signor- Lipps Effect 

Abundance: relative abundance refers to the proportion of species (or group 

of fauna) of the entire assemblages, e.g. percentage. While an absolute 

abundance refers to the number of individuals in a unit sample or assemblages. 

It is important to realize that relative and absolute abundance measurements 

give different information. Despite these difficulties the relative abundance is 

better for dead assemblages because of several effective parameters, which are 

known as Signor- Lipps Effect, Based on reasonable interactions between 

method of sampling, sampling density, sample size, preparation methods, 

relative abundance, precision amount and omission in statistical measurements, 

occurrence pattern, fossil preservations, and observation about last appearance 

datum event LAD (or first appearance datum FAD) provide an accurate estimate 

of the true LAD or FAD (Signor and Lipps, 1982, in MacLeod 1996). It does 

89

Chapter Four 


enable much more sophisticated testing of those observations in such 

biostratigraphic analysis nevertheless on high resolution results for favorites. 

Consequently to avoid and reduce the effect of such variability we tried to get rid 

of these sophisticated cases by organization and systematic work with relevant 

and accurate documentation of biostratigraphic evidences. 

4.4- Planktonic/Benthonic foraminiferal ratio and Benthic Foraminiferal 

Assemblage 

In the present study, among the most important paleoecological and 

depositional environment factors, the abundance of planktic foraminifera, 

planktonic species richness, Planktic/Benthic foraminiferal ratios, Benthic 

Foraminiferal assemblage, and Agglutinated/Calcareous ratios are used as 

important parameters to interpreting paleoecological changes and 

paleobathymetric determination of Maastrichtian/Lower Paleocene 

succession in Sulaimani region (Figs 4.3 - 4.8) 

Nyong & Olsson, 1984 (in Samir, 2002) have noticed that the inner shelf 

depth 10-50m is characterized by low planktonic percentage with low 

species diversity and high benthic foraminiferal assemblages, whereas 

higher 8-25% planktonic foraminifera and diversity characterize the middle 

shelf depth 50-100m. In addition, the outer shelf depth 100-200m is 

characterized by 30-70% planktonic foraminifera, while the middle slope 

depth 400-800m is characterized by 90% planktonics and a slight increase 

in benthonic diversity. 

The ratios of Planktonic/Benthonic foraminiferal species are a valuable 

indicator of paleobathymetry. The general conventional pattern for benthonic 

foraminiferal raises from the nearshore environment to the continental edge, 

further downward decreases significantly towards bathyal depths (Van Der 

Zwaan et al., 1990). 

According to benthonic foraminiferal assemblages, many authors 

recognized two main cosmopolitan distinct, depth-controlled benthic 

90

Chapter Four 


foraminiferal assemblages that enjoyed a widespread geographic dispersal 

and equitable climatic conditions during Maastrichtian and Paleocene. The 

continental shelf fauna, termed as "Midway-type fauna" (MF), and a lower 

continental slope and abyssal plain fauna termed as "Velasco-type fauna" 

(VF). (Alegret and Thomas, 2001; Samir, 2002) 

The paleodepth indicated by benthonic foraminiferal assemblages are 

clearly of great value for the interpretation of the environment of deposition 

of the Cretaceous/Tertiary clastic unit (Alegret et al. 2003) 

The paleobathymetric estimation in this study also depends on the 

occurrence and abundancy of depth-dependent benthonic foraminiferal 

assemblages. The paleodepth can be derived from previous studies of other 

authors (Fig 4.2) which show the main patterns of occurrence of benthonic 

foraminifera at different depths, as well as the distribution of Midway and 

Velasco-type faunas. 

In the present study, the qualitative and quantitative foraminiferal 

counting is carried out in detail for about 50gm of the residue of some 

selective sample in each biozones, the Agglutinated / Calcareous ratios and 

the quantity of both planktonic and benthic forams are calculated for each 

sample to determine the environmental conditions that prevailed during the 

deposition of the Maastrichtian - Early Paleocene sequence in the studied 

area. In addition, their lithologic characters are significant indicators for the 

paleodepth. Moreover, the pattern of sea-level oscillations is also inferred by 

calculating the P/B ratio, the Aggl. /Calc. ratio, the planktonic diversity and 

distribution of the planktonic groups as well as the benthonic associations. 

The foraminiferal distribution is a function of the water depth available over 

the shelf during any particular interval, (Canud et al, 1991); Elnady & 

Shahin, 2001; Samir, 2002; Maestas et al., 2003; Chacon and Martin- 

Chivelet, 2005) 

91

Chapter Four 


Fig (4.2) Upper depth limits and paleobathymetric distribution of Upper Cretaceous and Lower 

Paleogene benthonic foraminifera (1): van Morkhoven et al. fold out (1986), p.8, fig,5; (2): Speijer 

(1994), p. 84,fig.6; (3):Tjalsma and Lohmann (1983); (4): Widmark (2000), p.376; (5):Berggren and 

Aubert (1975); (6):R. Speijer, press. Comm., 2001; (7): Widmark and Speijer 1997a; (8): Kaminski et 

al.1988 ;( 1c): modified after van Morkhoven et al.(1986),(from Alegret and Thomas 2001) 

92

Chapter Four 


4.4.1- Maastrichtian 

The Maastrichtian succession represented by upper most part of 

Shiranish Formation (samples 1-5), Reddish to pale brown succession 

(Shiranish-Tanjero transition unit), (Samples, 6-40) and Tanjero Formation 

(samples, 41-113) in Smaquli area, while in the other localities, the studied 

part of Late Maastrichtian succession, represented by the upper part of the 

Tanjero Formation (in Dokan, Qala Cholan, Barzinja and Sirwan valley) is 

characterized by the following parameters: 

1- The most diverse assemblage of planktonic foraminiferal species 

richness ranged from 45 – 55, P/B ratios from 65-80% and Aggl/Calc 

percent from 15-25% (From CF8 – CF2) Zones, with decreasing the species 

richness in (CF1) Zone which is being 34-27 and slightly increasing in 

Agglutinated/Calcareous percent to 35%, In Smaquli section (Fig. 4, 3). 

2- Planktonic foraminifera species richness from 35 – 45, P/B ratios from 

50-70% and Aggl/Calc percent from 15-20% with decrease in species 

richness in (CF1) Zone from 24-20 and slight increase of 

Agglutinated/Calcareous percent to 30%, In Qulka section (Fig. 4 ,4). 

3- Planktic foraminiferal species richness is ranged between 35 -45, P/B 

ratios between 55-70% and Aggl./Calc. percent from 18-30%, with decreasing 

the species richness from (CF2 &CF1) Zones from 30-22 and slightly 

increasing in Aggl./Calcar. Percent 50% within the upper most part of (CF1), 

In Sirwan section (Fig. 4, 5). 

4- Planktonic foraminiferal species richness is 25, P/B ratios are 45% and 

Aggl./Calc. Percent ranged between 35-40% in the lower part of Qishlagh 

section (sample 1-11) with decreasing in Agglu./Calc. percent 10–20 in the 

middle part (sample 12-33) and increasing to 35-40% in (samples 35-46) (Fig. 

4 ,6). 

5- Planktonic foraminifera species richness is 30, P/B ratios are 45% and 

Aggl/Calc percent is 23% in the lower part of Kato section (samples, 1-19) 

93

Chapter Four 


with decreasing in Agglu./Calc. Percent between 15 – 20 in the middle part 

(samples, 23-29) 


proposed paleodepth curve in the Late Cretaceous/Early Paleocene succession in Gali section 

(Smaquli area) 

The typical Tanjero and kolosh Formations characteristically are poor in 

macrofauna's exactly at Smaquli, Sirwan and Dokan area, which is abundant in 

94

Chapter Four 


neritic deposits as in upper part of Tanjero Formation in Qala Cholan and 

Barzinja area. 

The planktonic assemblages of the lower part in Smaquli area from Zone 

(CF8) to (CF1) and (CF5) to (CF2) Zones at Dokan and Sirwan valley are 

characterized by high values in the percentages of planktonic foraminifera, P/B 

ratios, species richness, low Agglutinated percentages and general benthonic 

morphotypes of Upper Cretaceous/Early Paleocene Paleodepth indicators 

reveal deeper water bathymetry of upper bathyal around 300-600m depth. In 

Smaquli area and the outer neritic-upper bathyal around 200-400m depth in 

Dokan and Sirwan area, (Depending on all the above mentioned references 

evaluation). The paleobathymetric curve shows regular trend in their values 

where they exhibit high to moderate percentages values, since the 

preservation of foraminiferal species is generally good. 

The terminal decreases in species richness 34 starts from the base to the 

end of Zone CF1 (Gali section) and continued upwards till the upper most part 

of Cretaceous biozone Zone CF1, where the species richness becomes 

27. This decline coincides with the LA of Plummerita hantkeninoides and 

reaches to 20 in Qulka section and 22 in Sirwan section. The decline is also 

coupled with the trend of decrease in species richness, in the percentages 

of planktonic foraminifera and p/b ratios. On the other hand, a slight 

increase is recorded in the percentages of arenaceous morphotypes. 

These criteria indicate shallowing regressive phase in the end of 

Maastrichtian basin where the estimated water depth according to Van Der 

Zwaan et al.,(1990) ranges from middle to outer shelf, around 50 to 150m 

depth. 

The present paleobathymetric interpretation is further confirmed and 

sustained by the components of the cosmopolitans associated benthonic 

assemblage, which resembles that recorded by Van Morkhoven et al.(1986); 

Speijer (1994; Tjalsma and Lohmann (1983); Widmark (2000; Berggren and 

Aubert (1975); R. Speijer, press. Comm., 2001; Widmark and Speijer 1997a; 

95

Chapter Four 


Kaminski et al.1988; van Morkhoven et al.(1986), fold out; modified after Van 

Morkhoven et al.(1986),(from Alegret and Thomas 2001) (Fig 4. 2) 


proposed paleodepth curve in the late Cretaceous/Early Paleocene succession in Qulka section 

(Dokan area) 

The planktonic assemblages of the lower part in Qishlagh section from (CF5) 

Zone to lower most part of (CF4) Zone (samples 1-10) (Fig 4. 6) are 

characterized by low to moderate values in planktonic foraminiferal 

percentage, p/b ratios are 45, species richness 25, low to moderate 

96

Chapter Four 


Agglutinated percentages 40-45 and general benthonic morphotypes of Upper 

Cretaceous/Early Paleocene Paleodepth indicators reveal middle to outer 

shelf bathymetry around 100 to 200m. depth. The paleobathymetric curve 

shows the regular trend in its values where it exhibits low to moderate 

percentages values, since the preservation of foraminiferal species is 

generally good. 


proposed paleodepth curve in the late Cretaceous/Early Paleocene succession inSirwan section 

(Sirwan valley) 

97

Chapter Four 


The remaining interval of this section is represented by thick succession 

115m. of Aqra limestone Formation ,characterized by common occurrence of 

coral like rudists which constitute the original part of the carbonates with other 

great number of bivalve pelecypods, in addition to the echinoids, gastropods, 

brachiopods, coral and large foraminiferal assemblages with common smaller 

benthonic too. (Fig. 4.6) It is convenient to mention that the occurrence of 

Planktonic foraminifera not observed till the end of this section except for the 

lowermost few meters of this interval. It is well known that rudist growth and 

their nourished during late Cretaceous shallow marine quiet environment with 

low agitation or dynamic action of watermass within depositional environment, 

the bathymetry not exceeds than 30m depth. The Aqra interfingering limestone 

represents submerged high reefal facies relatively represent a time span of 

quite and shallowing within the mobile foreland basin of Tanjero trough. (Al- 

Omari 1989, Al-Mutwali 1992, Lawa et al., 1998.) 

The Aqra Limestone Formation followed by 67m. of alternation of bluish 

white marl, marly limestone, siltstone, recrystallized fossiliferous limestone 

sandy limestone, with weathered friable sandstone, olive green sandstone, 

dark grey shale and calcareous shale. This interval characterized by 

continuation of the same benthonic foraminiferal assemblages of Aqra 

Limestone without macrofossils growth in situ ,it is characterized by increasing 

in agglutinated percent from 20 to 45 in the middle and upper part of this 

interval. The depositional environment and paleobathymetry of this unit may 

represent upper part of inner neritic shoal from 10 to 30m. depth. This interval 

characterized by no evidence of any porcelaneous foraminiferal assemblages 

which indicate no restriction, high agitation of watermass, and high rate of 

deposition which may cause the dilution of planktonic foraminiferal 

survivorship. 

The planktonic assemblages of the lower part in Kato section from (CF4) 

Zone to lower most part of (CF3) Zone (Fig. 4. 7) are characterized by low to 

moderate values in the percentages of planktonic foraminifera, P/B ratios 

98

Chapter Four 



proposed paleodepth curve in the late Cretaceous/Early Paleocene succession in Qishlagh 

section (Qala Cholan area) 

Between 42-45, species richness is between 25-30, low to moderate 

agglutinated percentages 20-30 and general benthonic morphotypes of Upper 

Cretaceous/Early Paleocene paleodepth indicators reveal middle to outer 

shelf bathymetry around 100 to 200m depth. But controversy to the above 

mentioned conception it is appropriate to emend this abstraction because the 

99

Chapter Four 


occurrence of these foraminiferal assemblages (all planktonic and most of 

benthonic foraminifera) are restricted to the thin beds of shale, marl and marly 

limestone intercalation within thick beds of interfingering Aqra Limestone 

Formation which is famous by its components of macro and microfossils as 

mentioned in Qishlagh section. Consequently the reliable bathymetry of this 

unit is not greater than 30m. depth with cyclical deepening during the 

deposition of shale or marly limestone intercalations. 

The Aqra Limestone Formation followed by 35m. of alternation of bedded 

limestone grey shale, marl, friable sandstone, marly limestone, calcareous 

fossiliferous sandstone sandy limestone, with detrital fossiliferous limestone 

and claystone. This interval characterized by little benthonic foraminiferal 

assemblages of larger size without macrofossils growth in situ ,it is 

characterized by decreasing in agglutinated percent from 20 to 10 in the upper 

part of this interval. The depositional environment and paleobathymetry of this 

unit may represent upper part of inner neritic shoal from 10 to 30m depth. This 

interval characterized by no evidence of any porcelaneous foraminiferal 

assemblages as Qishlagh section which indicates no restriction, high agitation 

of watermass, and high rate of deposition which may cause the dilution of 

planktonic foraminiferal survivorship. 

4.4.2- Paleocene 

A progressive shallowing of depositional environment started from the 

Pseudoguembelina palpebra Zone (CF2) in all studied sections especially at 

Gali, Qulka and Sirwan section from 65.5my upward and continued to the lower 

Paleocene through Plummerita hantkeninoides Zone (CF1),Guembelitria 

cretacea Zone (P0), Parvularugoglobigerina eugubina Zone (Pá), 

Parvularugoglobigerina eugubina-Subbotina triloculinoides Zone (P1a) and 

Subbotina triloculinoides-Praemurica inconstans (P1b). This trend of 

shallowing integrated and contributed with stacking pattern of high rate 

sedimentation which display extreme climax rate around Cretaceous/Tertiary 

boundary with the rate of deposition about 100m/my. (Figs 4. 11, 12 & 13) 

100

Chapter Four 


Fig (4.7: The main Foraminiferal parameters derived from the quantitative analysis with the 

proposed paleodepth curve in the late Cretaceous/Early Paleocene succession in Kato section 

(Barzinja area) 

In the studied area, the nature of Cretaceous-Tertiary contact characterized 

by vanishing, obliteration and complete extermination of planktonic foraminiferal 

assemblages, except of two species(Hedbergella monmothensis & 

Guembelitria cretacea) which they turnover the K/T boundary and forming the 

new chain of genetic radiation and phylogenetic reconstruction of the Early 

101

Chapter Four 


Paleocene planktonic foraminifera (Liu & Olsson 1992 and Olsson et al., 2000) 

consequently the biotic parameters or factors which play an important role on 

the environmental output based on quantitative analysis of planktonic 

foraminiferal assemblages is of little values when it is compared with qualitative 

investigation in the base of Paleocene age. 

1-The Early Paleocene episode characterized by low Planktonic 

foraminiferal species richness 18 in Pá decreased to 12 species in P1b, P/B 

ratios are 65 in Pá and 40 in P1b, Aggl./Calc. percent ranged between 40-25- 

in Gali section. 

2- In Qulka section species richness is 14 in P1a decreased to 11 species in 

P1b, P/B ratios are 45 in P1a and 50 in P1b, Aggl. /Calc. percent ranged 

between 30-20- . 

3-Species richness is 17 in P1a decreased to 15 species in P1b, P/B ratios 

are 50 and Aggl. /Calc. percent is 35 in P1a and 25 in P1b in Sirwan section. 

The planktonic assemblages of the lower Danian in (P0) in Smaquli, and (P0 

& Pá) from Dokan and Sirwan valley are characterized by no recording of 

planktonic foraminiferal assemblage except for (Hedbergella monmothensis & 

Guembelitria cretacea), in the last 25cm of (P0) at Smaquli section. Little 

increase in Agglutinated percent at Smaquli and Sirwan valley refers to the 

shallowing episode around 10-50m. (Olsson & Nyong, 1984 in Samir, 2002), 

(Keller, 1988; Li and Keller, 1998c: Keller and others, 2002b in Keller, 2004), 

(Abramovich. and Keller, 2002). Afterward the planktonic foraminiferal species 

richness was recognized from Smaquli, Sirwan and Dokan are 18, 17, and 14 

species respectively from (Pá, P1a), it decreased to 11, 15 and 12 in (P1b). 

P/B ratios shows normal percent varied between 40 to 50% during the total 

interval low Agglutinated percentages around 20 to 25. These environmental 

parameters and general benthonic morphotypes of Upper Cretaceous/Early 

Paleocene Paleodepth indicators reveal shallow water bathymetry of innermiddle 

neritic around 50 - 70m depth. (Keller, 1988; Li and Keller, 1998c: Keller 

102

Chapter Four 


and others, 2002b in Keller, 2004), (Abramovich. and Keller, 2002). (Samir, 

2002), 

4.5- The Nature of Maastrichtian/Paleogene boundary 

At Smaquli, Qulka and Sirwan valley extremely rich in microfauna especially 

planktonic foraminifera. High resolution biostratigraphic analysis of these 

sections indicates a major biotic change in planktonic foraminiferal 

assemblages. Neither burrows (trace fossils) nor sedimentary structures, 

condensed sections, hard ground, mineralization bed of glauconitic, Iron 

oxide, silicate, silica spheres, microtectites or any Phosphatic minerals 

have been found at the K/T boundary. In addition, the great similarities in 

the lithologic components below and above the contact line between 

Tanjero and Kolosh Formations, in which impossible to distinguish or to 

differentiate between them lithologically in the field. The planktonic 

foraminiferal biozones recorded in the studied area reveals continuous 

sedimentation without evidence of any hiatus (Figs 3.1-3.8) in addition to the 

appearance of the new lower most Danian Planktonic forams which indicate 

the gradual contact at Smaquli area. These data are similar to those 

identified from El Kef in Tunisia (Keller et al., 1995); Agost, Caravaca, 

Zumaya, in Spain (Canudo et al., 1991: Pardo et al., 1996: Molina et al., 

1996, 1998); Ain Settara in Tunisia (Arenillas et al.. 2000); Caravaca SE Spain 

( Smit, 2005); Egypt (Shahin, 1992), (Samir, 2002), ((Keller, 2002),(Obaidalla, 

2005) and Israel (Keller ,2004). 

The extinction pattern of the Late Maastrichtian fauna has been a matter of 

controversy. In this connection, Smit (2005) studied the planktonic foraminiferal 

pattern of extinction across the (K/P) boundary at Caravaca SE Spain, and 

believed that the bolide impact event caused the extinction of all Cretaceous 

fauna, except for one species (G. cretacea) which considered the 

occurrence of Cretaceous individuals above the K/P boundary as due to 

reworking. Keller (1988) in Obaidalla, 2005 proposed that the 14 Cretaceous 

103

Chapter Four 


species became extinct below the (K/P) boundary while l0 species survived 

well into the Danian sediments at El Kef (GSSP) in Tunisia, a phenomena 

which indicate in their opinion that the extinction is unrelated to an impact event. 

In the present study the available data show both gradual and sudden 

catastrophic extinction pattern for partially or halve number in planktonic 

foraminiferal species before the (K/T) boundary and complete species 

extinction at or near the (K/T) boundary which indicate no Cretaceous 

planktonic foraminiferal survivorship into the Danian except of (G. cretacea) 

and (H. monmothensis) in the lower most Danian. 

In contrast, benthonic foraminifera were not affected by major global 

extinction at the Cretaceous/Tertiary boundary, and as fact that could not 

differentiate between the Danian and Maastrichtian in the point of benthonic 

foraminiferal assemblage point of view (Alegret et al., 2003). In the studied 

area, the same document was observed and recorded, in general benthonic 

foraminifera were little affected during the K/T mass extinction which was 

distinguished by reducing the number of benthonic species at Smaquli from 12- 

11 species at Plummerita hantkeninoides Zone (CF1) to 7 species in 

Guembelitria cretacea zone (P0) , then increased again upward to 11 species in 

Parvularugoglobigerina eugubina zone (Pá) becomes 20 species in (P1a) and 

lately 18 species in Subbotina triloculinoides – Praemurica inconstans Zone 

(P1b) (Fig. 3.8) 

In Qulka section (Dokan area), the number of species remains stable 12 

species at the end of Plummerita hantkeninoides Zone (CF1) through Late 

Maastrichtian to (P0 & Pá) Earliest Danian, then increased upward to 18 

species in (P1a) Parvularugoglobigerina eugubina - Subbotina triloculinoides 

Zone. and decreased to 12 species in Subbotina triloculinoides- Praemurica 

inconstans Zone (P1b) (Fig. 3.6) 

104

Chapter Four 


The number of benthonic species at Sirwan valley decreased from 12 

species at Plummerita hantkeninoides Zone (CF1) to 7 species in (P0 & Pá), 

then increased again upward to 20 species in both Parvularugoglobigerina 

eugubina- Subbotina triloculinoides Zone (P1a) and Subbotina triloculinoides- 

Praemurica inconstans Zone(P1b) (Fig. 3.2) 

The benthonic foraminiferal assemblage represented by calcareous tests 

about %80 in all studied sections, except for the lower and middle part of the 

Qishlagh section decreased to %60 while at the Cretaceous/Tertiary boundary, 

from the upper part of Pseudoguembelina palpebra zone (CF2) to (P0 & Pá) 

lowest Danian, there was slightly increasing in agglutinated percent to about 

30-40 in all studied section (Gali, Qulka and Sirwan valley). (Figs. 4.3 - 4.5), 

4.6- Method of graphical correlation 

The American stratigrapher AB. Shaw devised a new technique of semiquantitative 

correlation of biostratigraphical sequences. Shaw's method utilizes 

a single stratigraphical section which is taken as the standard likely present. In 

the study area, the Gali section is selected as standard because it represented 

the most simple continuous section and unaffected tectonically by structural 

complications. From this section, the limit boundary of (First appearance datum 

event FAD and last appearance datum event LAD) for standard zonal scheme 

of biostratigraphic zonation utilized and recorded and constructed in state of 

total ranges of species, with particular importance being assigned to the first 

and last appearance of fossil species. A graph can be constructed using the 

data collected from all stratigraphical section. The first and last datum events of 

the Biozones provide points on the graph, then the best-fit line is constructed. 

Any Changes in the gradient or the graph (dog-legs) indicate changes in the 

rate of sedimentation which is observed in graphical correlation between Gali 

section (Smaquli area) and both Dokan and Sirwan sections (Figs 4. 8, 4. 9) 

which refer to low sedimentation rate in initial part on (R. fructicosa Zone) at 

Smaquli area, compared with highest sedimentation rate at both Qulka and 

105

Chapter Four 


Sirwan sections and later one from P.hariaensis Zone to S. triloculinoides Zone 

(Upper Late Maastrichtian-Lower Danian), the graphical line shows best-fit line 

of 45 0 which indicate similar rate of depositions. If a best-fit line can be 

constructed completely, the sections can be correlated, (Sirwan and Qulka) (Fig 

4.10) which show the same rate of deposition in the same geologic time from 

Late Maastrichtian- Early Danian. This technique provides a clear graphical 

method which aids in the correlation or sequences. 

Fig (4.8): Graphic correlation shows the depositional rate of sediment between Smaquli and Qulka 

sections, Note: Change in the gradient in the early stage (dog-Leg) indicate highest rate of 

deposition in Qulka section than Smaquli section 

106

Chapter Four 



Sirwan sections. Note: Change in the gradient in the early stage (dog-Leg) indicate highest rate of 

deposition in Sirwan section than Smaquli section 

Fig (4.10): Graphic correlation shows the depositional rate of sediment between Qulka and Sirwan 

sections. Note: NO Change in the gradient observed, a best-fit line constructed completely 

which indicate similar rate of deposition in Qulka and Sirwan section. 

107

Chapter Four 


4.7- Sedimentation rate around Cretaceous/Tertiary boundary 

Sediments principally consist of two different components: -Allochthonous 

clastic or detrital sediments which are derived from land sources outside of 

depositional area.-Autochthonous, sediment produced in the depositional area 

mostly biogenic or chemically precipitated sediments. The sedimentation rates 

of clastic sediments are controlled mainly by the size and characteristics of the 

source area. Furthermore, the distances of the depositional area from the site 

of sediment input play a role. The sedimentation rates of sediments on 

siliciclastic shelf or foreland basin were proposed by several authors from low 

rate of deposition by 10m/ma to high rate of deposition by 100m/ma, in (Ensele, 

2000, Fig, 10.3, page. 458) 

The magnetostratigraphy of Maastrichtian and lower Paleocene showed 

magnetochrons 32n to 28n (Figs 3. 12, 3.13). These paleomagnetic data are 

available to determine and calculate the sedimentation rates of the studied 

sections and establishment the chronostratigraphy of the Cretaceous/Tertiary 

boundary events as mentioned in previously discussed chapter three. 

To identify the presence of possible hiatuses, due to the non 

documentation of some zones and the overall poor recovery, high rate of 

sediment accumulation in thick interval of biozones, or thin interval of slow rate, 

non deposition and condensed sections, the high resolution planktonic 

foraminiferal biostratigraphic zonation plays an important role in determining 

such sedimentary rate with the aid of paleomagnetic Chron, the age and 

duration of each faunal event and the age of datum events achieved by several 

authors in the study of high resolution biostratigraphic zonations around 

Cretaceous/Tertiary boundary in different localities of the global Earth.( e.g: 

Berggren et al., 1995; Berggren & Norris, 1997; Li & Keller,1998a,b; 

Abramovich et al., 2002; Olsson et al., 2000); Keller, 2002, 2004; (Figs 3.12-13) 

The mean sedimentation rate or average sediment rate by biozone 

(m/myr) or years/meter was estimated previously. In this chapter just try to 

108

Chapter Four 


point out the general sedimentation rate of total studied stratigraphic 

successions from the upper part of Tanjero Formation and lower part of Kolosh 

Formation around K/T boundary. Based on the time scale as shown in (Figs 

4.11 - 4.13) the sedimentation rate varies from zone to zone. In particular, low 

rates of sediment accumulations in the Gali section were observed from the 

base of Maastrichtian at upper most part of Globotruncana aegyptiaca Zone 

(CF8) to the end of Pseudoguembelina hariaensis Zone (CF3) (Fig4.11) Low 

to moderate rate of depositions recorded in both Qulka and Sirwan 

sections for Racemiguembelina fructicosa zones CF 4.and Pseudoguembelina 

hariaensis Zone (CF3) (Figs, 4.-12, 4.13) 

In the sequences above, the Pseudoguembelina hariaensis Zone(CF3), 

and from the base of Pseudoguembelina palpebra zone (CF2) in all three 

mentioned localities the sedimentation rate rapidly increased and recorded high 

rate sedimentation just 0.5myr below the K/T boundary to the lower Paleocene 

age through out the Pseudoguembelina palpebra zone (CF2, Plummerita 

hantkeninoides zone (CF1),Guembelitria cretacea (p0), Parvularugoglobigerina 

eugubina (pá), Parvularugoglobigerina eugubina-Subbotina triloculinoides 

(P1a) and Subbotina triloculinoides – Praemurica inconstans (P1b). It is worthy 

to mention that the sedimentation rates in all three mentioned studied sections 

from 65.5my to 64.5my were around 75 -100m/ma. 0.5my below and above the 

Cretaceous/Tertiary boundary, which reveal continuations and increasing the 

sediment accumulation without interruption or any gaps to be disclosed along 

the contact of K/T boundary. 

Note: The depositional rate of studied sequences in Qulka and Qishlagh 

sections was not introduced due to incomplete high resolution biostratigraphic 

zonation which was evidenced by interruption of planktonic foraminiferal 

assemblages and change in the environmental and depositional system. 

109

Chapter Four 



Gali section (Smaquli area) plotted vs. planktonic foraminiferal zonal scheme. The age (Time) of 



Qulka section Dokan area plotted vs. planktonic foraminiferal zonal scheme. The age (Time) of 


110

Chapter Four 



Sirwan section plotted vs. planktonic foraminiferal zonal scheme. The age (Time) of 


111

Chapter Five 

CHAPTER FIVE 

Conclusion 

CONCLUSIONS 

In the biostratigraphic and paleoecologic study of the Cretaceous-Tertiary 

succession in the studied sections at (Gali, Qulka. Qishlagh, Kato and Sirwan 

valley) in Sulaimani area, Kurdistan region, northeast of Iraq, the consecutive 

preference deductions manifested as the end result of this effort to apprize the 

summit trail which imply the following points: 

1- Choosing the optimum method for preparation and separation 

foraminiferal test from the rock type of soft, friable, porous, and permeable rock 

and used for different lithologic type, e.g (claystone, shale, marl, marly 

limestone and limestone. 

2- A detailed study includes the well description and high resolution lithologic 

constitution and field work investigation carried on the well exposed of the most 

upper part of the Upper Cretaceous/Lower Tertiary successions incorporated 

the upper part of Tanjero Formation in Sirwan valley, Kato, Qishlagh and Dokan 

section included with the lower most part of Kolosh Formation and Red Bed 

Series of the Early Tertiary, while in the Gali section (Smaquli area) the studied 

stratigraphic units include the Upper part of Shiranish Formation, Shiranish- 

Tanjero transition unit (Reddish to pale brown succession), Tanjero Formation 

and Kolosh Formation and the fieldwork at different settings is presented 

towards a reasonable and meaningful subdivision of the studied sections. In 

addition to that, the studied sections included the interfingering of Aqra 

Limestone unit, occurred within the upper part of Tanjero Formation in 

Qishlagh, Kato and Qulka sections. 

3- Due to the great similarities in the lithologic characters between the two 

formal units of Tanjero and Kolosh Formations in the field, it is quit difficult for 

112

Chapter Five 

Conclusion 

any geologist to observe the contact line or differentiated between them exactly 

at Smaquli, Dokan and Sirwan valley. Consequently, it is reliable to conclude 

that the two formations were sharing the same continuous depositional basin 

around Upper Maastrichtian/Lower Paleocene Epochs. 

4- The lateral and vertical relation of reddish to pale brown succession is 

quite conformable with both underlying Shiranish and overlying Tanjero 

Formations. 

5-The well exposed reddish to pale brown succession has its own special 

monotonous, conventional lithologic character differ from both underlying 

Shiranish Formation and overlying Tanjero Formation, geographically extended 

for more than 75Km and it has mapable thickness which reaches 72m.in Smaquli 

Gali Gorge, with relevant feasible geologic age of Lower Maastrichtian about 

2My duration. Consequently I propose the name of Smaquli Formation as a new 

formal lithologic unit to display an incipient effort of formation rank according to 

international stratigraphic nomenclature cod. 

6- The planktonic foraminifera occurs continuously within the Upper 

Cretaceous sequences in the sedimentary succession of the studied section at 

Smaquli, Dokan and Sirwan valley, generally shows incessant in sedimentary 

sequence without any interruptions. 

7- The upper most part of Kolosh Formation in Smaquli area is characterized 

by the attendance of five red claystone beds at the last 10 meters which start 

from 30cm. to 2m. respectively, and overly by Gercus Formation, the contact is 

seemed to be conformable by lithologic evidence of graditional change from dark 

grey organic rich sediments of Kolosh Formation to red, purple mudstone, 

sandstone, gritty marl, pebbly sandstone and conglomerates. The contact is 

placed on the line where the sediment colour mainly began with red lithology. 

113

Chapter Five 

Conclusion 

Paleontologically there were no significant evidences of fossils record in this 

interval of lower most part of Gercus Formation in which six samples were 

studied for both foraminiferal and palenomorphs. Consequently it is convenient to 

mention that the geologic age of the Gercus Formation in Smaquli area, inferred 

conformable gradditional nature, and may began from the Danian (Lower 

Paleocene) instead of Middle Eocene age. 

8- The Tanjero Formation was completely studied in Smaquli area which 

represented by 72m. And subdivided lithologically into three distinct units based 

on field observation and lithologic characters. Chronostratigraphically represents 

Late Maastrichtian Epoch. 

9- The total number of planktonic and benthonic foraminiferal species was 

identified from all studied sections as follow: 

A - Gali section 82 planktonic species were belonging to 23 Genus in Shiranish- 

Tanjero transition unit but in Tanjero Formation 21 planktonic species were 

belonging to 14 Genus in Kolosh Formation, while 66 benthonic species were 

belonging to 38 Genus in Shiranish-Tanjero transition unit and Tanjero 

Formation, 50 benthonic species are belonging to 30 Genus in Kolosh 

Formation. 

B- Qulka section 53 planktonic species were belonging to 18 Genus in Tanjero 

Formation and 16 planktonic species are belonging to 9 Genus in Kolosh 

Formation, but 52 benthonic species were belonging to 36 Genus in Tanjero 

Formation and 43 benthonic species are belonging to 31 Genus in Kolosh 

Formation. 

C - Sirwan section 62 planktonic species were belonging to 20 Genus in 

Tanjero Formation and 18 planktonic species are belonging to 11 Genus in 

Kolosh Formation, but 58 benthonic species was belonging to 36 Genus Tanjero 

Formation and 52 benthonic species are belonging to 32 Genus in Kolosh 

Formation. 

114

Chapter Five 

Conclusion 

D - Qishlagh section 26 planktonic species were belonging to 13 Genus in 

Tanjero Formation, while 42 benthonic species were belonging to 28 Genus in 

Tanjero Formation. 

E - Kato section 30 planktonic species were belonging to 14 Genus in Tanjero 

Formation, while 38 benthonic species were belonging to 25 Genus in Tanjero 

Formation. 

10- Based on the geologic range and relative abundance of Planktonic 

foraminiferal species, the studied sections along (K/T) boundary are precisely 

divided into the numbers of biostratigraphic zones, depending on the new 

zonal scheme as high resolution biostratigraphic studies, which are quietly 

adequate and commonly used in low and middle latitudes. In addition to that, 

these biostratigraphic zones were correlated to their equivalents in and outside 

of the region and with world wide standard biostratigraphic zones with the aid 

of datum events which show the age of planktonic foraminiferal zones. The 

distinguished biostratigraphic zones in the studied sections are the following 

from the base upward. 

A - Gali section (Smaquli area) 

a1 - upper part of Globotruncana aegyptiaca Interval Zone (CF8), (Upper part 

of Shiranish Formation and Lower most part of Reddish to pale brown 

succession) (Early Maastrichtian) 

a2- Gansserina gansseri Interval Zone (CF7), (Reddish to pale brown 

succession) (Early Maastrichtian) 

a3 - Contusotruncana contusa Interval Zone (CF6), (Reddish to pale brown 

succession), (Early Maastrichtian) 

a4 - Pseudotextularia intermedia Interval Zone (CF5) (Reddish to pale brown 

succession), (Early Maastrichtian) 

a5 -Racemiguembelina fructicosa Interval Zone (CF4), (upper most part of 

Reddish to pale brown succession and lower part of Tanjero Formation) 

(Late Maastrichtian) 

a6 - Pseudoguembelina hariaensis Interval Zone (CF3), (Tanjero Formation), 

115

Chapter Five 

Conclusion 


a7 - Pseudoguembelina palpebra Interval Zone (CF2), (Tanjero Formation), 


a8 – Plummerita hantkeninoides total range Zone (CF1), (Tanjero Formation), 


a9 - Guembelitria cretacea Interval Zone (p0), (Kolosh Formation), Earliest 

Paleocene (Danian). 

a10 - Parvularugoglobigerina eugubina total range Zone (pá), (Kolosh Formation), 

Earliest Paleocene (Danian). 

a11 - Parvularugoglobigerina eugubina - Subbotina triloculinoides Interval Zone 

(P1a), (Kolosh Formation), Early Paleocene (Early Danian) 

a12 - Subbotina triloculinoides – Praemurica inconstans Interval Zone (P1b), 

(Kolosh Formation), Early Paleocene (Danian) 

B - Qulka section (Dokan area) 

b1 – Upper part of Pseudotextularia intermedia Interval Zone (CF5) (Tanjero 

Formation), (Late Early Maastrichtian) 

b2 - Racemiguembelina fructicosa Interval Zone (CF4), (Tanjero Formation 

and 

Interfingering Aqra Limestone) (Late Maastrichtian) 

b3 - Pseudoguembelina hariaensis Interval Zone (CF3), (Interfingering Aqra 

Limestone and Tanjero Formation), (Late Maastrichtian) 

b4 - Pseudoguembelina palpebra Interval Zone (CF2), (Tanjero Formation), 


b5 – Plummerita hantkeninoides total range Zone (CF1), (Tanjero Formation), 


b6 - Guembelitria cretacea- Parvularugoglobigerina eugubina Interval Zone (p0 

& pá), (Kolosh Formation), Earliest Paleocene (Danian). 

b7 - Parvularugoglobigerina eugubina - Subbotina triloculinoides Interval Zone 

116

Chapter Five 

Conclusion 


b8 - Subbotina triloculinoides – Praemurica inconstans Interval Zone (P1b), 


C - Sirwan section (Sirwan valley) 

c1 - Pseudotextularia intermedia Interval Zone (CF5) (Tanjero Formation), (Late 

early Maastrichtian) 

c2 -Racemiguembelina fructicosa Interval Zone (CF4), (Tanjero Formation), 


c3 - Pseudoguembelina hariaensis Zone (CF3), (Tanjero Formation), (Late 

Maastrichtian) 

c4 - Pseudoguembelina palpebra Interval Zone (CF2), (Tanjero Formation), 


c5 – Plummerita hantkeninoides total range Zone (CF1), (Tanjero Formation), 


c6 - Guembelitria cretacea and Parvularugoglobigerina eugubina Interval Zone 

(p0 & pá), (Kolosh Formation), Earliest Paleocene (Danian). 

c7 - Parvularugoglobigerina eugubina - Subbotina triloculinoides Interval Zone 


c8 - Subbotina triloculinoides – Praemurica inconstans Interval Zone (P1b), 


D- Qishlagh section (Qala Cholan area) 

d1 - Pseudotextularia intermedia Interval Zone (CF5) (Tanjero Formation), (Late 

early Maastrichtian) 

d2 – Initial interval of Racemiguembelina fructicosa Interval Zone (CF4), (at 

lower most part of Interfingering Aqra Limestone), (Late Maastrichtian) 

117

Chapter Five 

Conclusion 

E- Kato section (Barzinja area) 

e1 – Upper part of Racemiguembelina fructicosa Interval Zone (CF4), 

(Interfingering Aqra Limestone), (Late Maastrichtian) 

e2 - Pseudoguembelina hariaensis Interval Zone (CF3), (Interfingering Aqra 

Limestone), (Late Maastrichtian) 

11– Gali, Dokan and Sirwan sections in the studied area represent the most 

continuous sedimentary sequences across the K/P mass extinction boundary. 

The planktonic foraminiferal assemblages are very rich to moderate diversified 

and an excellent to good state of preservation respectively. These 

assemblages are similar to those of EL Kef, Tunisia and other continuous K/P 

boundary sections. 

12- It is relevant to declare that one of the results within these accessible 

conclusions of this dissertation will sustain the inferred assumption by Al- 

Barzinjy 2005, which proved that the Red Bed Series and Kolosh Formation 

sharing the same depositional basin and having the same tectonic setting. 

Moreover, both are representing lateral facies change of each other, in addition 

to that the foreland basin of Tanjero Formation during the Cretaceous/Tertiary 

boundary extended laterally and transversally in northeast and occupied the 

area from Sirwan, Halabja, Barzinja, Qala Cholan and Sura Qalat representing 

proximal area which gradually changed to the Red Bed Series (Kato and 

Qishlagh section) as conformable boundary in a rapid subsiding costal area. 

While in the southwest distal area of this basin the Tanjero Formation gradually 

changed to the Kolosh basin in Dokan and Smaquli area, the deeper part of 

depositional environment. 

13- Quantitative high-resolution biostratigraphic analysis of planktonic 

foraminifera at studied sections indicates that the extinction occurred over a 

short period of time. At Smaquli area 22 species of the Cretaceous planktonic 

118

Chapter Five 

Conclusion 

foram became extinct below the K/T boundary at lower part or before the P. 

hantkeninoides zone), where as the remaining 28 species became extinct at or 

near the K/T boundary and (G. cretacea) with (H. monmothensis) crossed the 

boundary and survived into the lower most part of Danian sediments. (The 

occasion was applied on both Qulkqa and Sirwan sections also). This sudden 

extinction is a catastrophic event may contain an evidence of asteroid impact. 

The extinct species are from both of the large, complex and small tropicalsubtropical 

forms. While the survivor species are of the small, cosmopolitan 

and simple forms. 

Consequently the data on stratigraphic range chart strongly imply that the 

planktonic foraminiferal record across the K/T boundary transition can be explained 

by earth derived environmental changes and that if an extraterrestrial bolide impact 

occurred, its effect on marine plankton foraminifera was of the catastrophic 

character that is usually assumed, which hesitated and terminated the Cretaceous 

planktonic fauna in the studied area. 

14- In general, benthonic foraminifera were little affected during the K/T 

mass extinction which was distinguished by reducing the number of benthonic 

species at all studied sections, at Plummerita hantkeninoides zone (CF1) and 

increased again upward in (P1a) and (P1b) 

15- The planktonic assemblages of the lower part from (CF8) to (CF1) in 

Smaquli area and (CF5) to (CF2) at Dokan and Sirwan valley are characterized 

by high values in the percentages of planktonic foraminifera, p/b ratios, species 

richness, low Agglutinated percentages and general benthonic morphotypes of 

Upper Cretaceous/Early Paleocene Paleodepth indicators reveal deeper water 

bathymetry of upper bathyal around 300-600m. depth In Smaquli area, the 

outer neritic-upper bathyal depth around 200-400m. depth in Dokan and Sirwan 

area. Middle to outer neritic depth around 100-200m. lower part of Qishlagh and 

inner to middle neritic depth 50-100m. in lower part of Kato section. 

119

Chapter Five 

Conclusion 

16- The terminal decrease in species richness began from the base to 

the end of Zone CF1 (Gali section) and continued upwards till the upper most 

part of Cretaceous biozone Zone CF1, the same thing in Qulka and Sirwan 

sections. The decline is also coupled with the trend of decrease in p/b 

ratios. On the other hand, a slight increase is recorded in the percentages 

of arenaceous morphotypes. These criteria indicate shallowing regressive 

phase in the end of Maastrichtian basin where the estimated water depth 

ranges from middle to outer shelf, around 50 to 150m. depth. 

17- The planktonic assemblages of the lower Danian in (P0) in 

Smaquli area, and (P0&Pá) from Dokan and Sirwan valley are 

characterized by no recording of planktic foraminiferal assemblage 

except for (Hedbergella monmothensis & Guembelitria cretacea), in the 

last 25cm of (P0) at Smaquli section. Little increase in Agglutinated 

percent at Smaquli and Sirwan valley refers to the shallowing episode 

around 10-50m. Afterward planktic foraminiferal assemblage, p/b ratios, 

Agglutinated percentages and species richness from Smaquli, Sirwan 

valley and Dokan in (Pá, P1a &p1b) (Early Paleocene), indicate shallow 

water bathymetry of inner to middle neritic around 50 - 70m. depth. 

18- A graphical method of correlation constructed by using the data 

collected from all stratigraphical section. As indicated, low sedimentation rate in 

initial part on (R. fructicosa Zone) at Smaquli area compared with highest 

sedimentation rate at both Qulka and Sirwan sections. Later one from 

P.hariaensis Zone to S. triloculinoides Zone (Upper Late Maastrichtian-Lower 

Danian), the graphical line shows best-fit line of 45 0 which indicate similar rate 

of depositions. 

19- The mean sedimentation rate or average sediment rate by biozone 

(m/myr) or years/meter was estimated in all studied stratigraphic successions 

120

Chapter Five 

Conclusion 

from the upper part of Tanjero Formation and lower part of Kolosh Formation 

around K/T boundary. Based on the time scale, the sedimentation rate varies 

from zone to zone. In particular, low rates of sediment accumulations in the Gali 

section were observed from the base of Maastrichtian at upper most part of 

(CF8) to the end of (CF3).Low to moderate rate of depositions were 

recorded in both Qulka and Sirwan sections for CF4 .and (CF3). 

In the sequences above the (CF3), and from the base of (CF2) in all 

three mentioned localities, the sedimentation rate rapidly increased and 

recorded high rate sedimentation just 0.5myr below the K/T boundary to the 

lower Paleocene age through out the (CF2, (CF1), (p0), (pá), (P1a) and 

(P1b). It is worthy to mention that the sedimentation rates in all three mentioned 

studied sections from 65.5my to 64.5my were around 75 -100m/ma. 0.5my 

below and above the Cretaceous/Tertiary boundary, which reveal continuations 

and increasing the sediment accumulation without interruption or any gaps to 

be disclosed along the contact of K/T boundary. 

121

REFERENCES 

Abawi, T. S. Abdel-Kireem, M. R. and Yousef G. M., 1982. Planktonic 

foraminiferal stratigraphy of the Shiranish Formation, Sulaimaniah- Dokan 

region Northeastern Iraq. Revista Espanola de Micropaleontologia, 14(1), 

pp.153--164. 

Abdel-Kireem, M. R., 1983. A study of the paleoecology and bathymetry of 

the foraminiferal assemblages of the Shiranish Formation (Upper Cretaceous). 

Northeastern Iraq. Paleogeography, Paleoclimatology, paleoecology. Vol. 43, 

pp. 169-180, 2 figs. 

Abdel-Kireem, M. R., 1986a. Planktonic foraminifera and stratigraphy of the 

Tanjero Formation (Maastrichtian), northeastern Iraq. Micropaleontology,vol. 

32, no.3, pp.215-231. 

Abdel-Kireem, M. R., 1986b. Contribution to the stratigraphy of the Upper 

Cretaceous and Lower Tertiary of the Sulaimaniya – Dokan region, 

Northeastern Iraq. N. Jb. Geol. Paleont. Abh.172 (1) pp.121-139. 

Abdel-Kireem, M. R., 1986c. Microfaunistic parameters of the chalk 

Formations (Upper Cretaceous), Bahariya Oasis, Egypt. Revista Espanola De 

Micropaleontologia, Vol. XVIII, num.1, pp. 27-46. 

Abdel-Kireem, M. R. & Samir, A. M., 1995., Biostratigraphic implications of 

Maastrichtian-Lower Eocene sequence at the north gunna section, Farafra 

Oasis, Western Desert, Egypt. Marine Micropaleontology.vol. 26, pp.329-340. 

Abramovich, S. Keller, G. Adatte, T. Stinnesbek, W. Hottinger, L. 

Stueben, D. Berner, Z. Ramanivosa, B. and Randriamanantenasoa, A., 

2002. Age and paleoenvironment of Maastrichtian to Paleocene of the 

mahajanga Basin, Madagascar: a multidisciplinary approach. Marine 

Micropaleontology.vol. 47, pp.17-70. 

Abramovich, S. and Keller, G., 2003. Planktonic foraminiferal response to 

the Latest Maastrichtian abrupt warm event: a case study from South Atlantic 

DSDP Site 525A. Marine Micropaleontology. vol. 48, pp.225-249. 

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Al-Ameri, T. K., Al-Rawi, I. K. and Khoshaba, B.N., 1990. Palynology of 

Unit one of Suwais Red Beds, Chwarta, Northeast Iraq. 

Science. Vol.31, No.1. 

Iraqi Journal of 

Al-Barzinjy, S. T. M., 2005. Stratigraphy and basin analysis of Red Bed 

Series at Northeast Iraq. Kurdistan region. Unpublised Ph.D. thesis, University 

of Sulaimani University, 159p. 

Alegret, L. and Thomas, E., 2001. Upper Cretaceous and Lower Paleogene 

benthonic foraminifera from northeastern Mexico.Micropaleontology, vol.47, 

no. 4, pp. 269-316, text-figures 1-3, plates 1-10, table 1. 

Alegret, L. Molina, E. and Thomas, E., 2003. Benthonic foraminiferal 

turnover across the Cretaceous /Paleogene boundary at Agost (southeastern 

Spain): Paleoenvironmental inferences. Marine Micropaleontology, Vol. 48, pp. 

251-279. 

Al-Hashimi, H. A. J. and Amer, R. M., 1985. Tertiary microfacies of Iraq. D. 

G. Geol. Surv. Min. Invest. puli., Baghdad, 56 pp, 17 fig., 159 pls. (S. O. M) 

Al-Mehaidi, H. M., 1975. Tertiary Nappe in Mawat Range, N.E Iraq, Jour. 

Geol. Soc. Iraq, vol. 8, pp. 31-44. . 

Al-Mutwali, M. M., 1983. Biostratigraphy of Kolosh Formation and the nature 

of its contact with upper Cretaceous rocks in Shaqlawq area. M.Sc. Thesis. 

University of Mosul, 154p 

Al-Mutwali, M. M., 1992. Foraminifera, Stratigraphy and Sedimentology of the 

Upper Cretaceous – Lower Tertiary in selected boreholes around Khleisia 

Anah- ramadi area. Unpublished PhD. thesis, University of Mosul, Moysl- 

Iraq.300p. 

Al-Mutwali, M. M., 1996. Planktonic foraminiferal biostratigraphy of the 

Shiranish Formation. Khashab well no. 1, Hemren area. Northeastern 

Iraq.Jour. Geol. Sci.Iraq, 7(1) pp. 129-136. 

Al-Mutwali, M. M. and Abawi T. S., 2005. Stratigraphy of the Tayarat 

Formation (Upper Cretaceous) in selected wells, western Iraq. Rafidain Journal 

of Science, Vol. 16, No. 1, Geology, Special Issue. Pp 17-32. (In Arabic) 

Al-Mutwali, M. M. and Al-Jubouri, F. N., 2005.Litho and Biostratigraphy of 

Shiranish Formation (Late Campanian-Late Maastrichtian) In Sinjar area, 



123 




Northwestern Iraq. Rafidain Journal of Science, Vol. 16, No. 1, Geology, 

Special Issue. Pp 152-176. 

Al-Omari, F. S., 1970. Upper Cretaceous and lower Cenozoic foraminifera of 

the three Oil wells in northwestern Iraq. Pd.D. Thesis, university of Missouri at 

Rolla, 208p. 

Al-Omari, F. S. Al-Radwani, M. A. and Al-Mutwali, M. M., 1988. (issued 

1993) Biostratigraphy of Kolosh formation at Shaqlawa area, northeastern 

Iraq. Journ. Geol. Soc. Iraq. Vol. 21, No.2, pp. 91-104. 

Al-Omari, F. S. Al-Radwani, M. A. and Lawa, F. A., 1989. Biostratigraphy of 

Aqra Limestone formation (Upper Cretaceous), northern Iraq. Journ. Geol. 

Soc. Iraq. Vol. 22, No.2, pp. 44-55. 

Al-Omari, F. S., 1995. (Issued in 1997).Biostratigraphy of Upper 

Cretaceous/Lower Tertiary in Butmah Well no.9 North West Iraq. Iraqi 

Geological Journal, Vol.28, no.2, pp.112-119 

Al-Qayim, B. A., 1992. (issued 1993) Bioturbated rhythmite of the Shiranish 

Formation, type-locality,NW Iraq. Iraqi Geological Journal, Vol.25, no. I, 

pp.185-194 

Al-Qayim, B. A., 1994. Evolution of flysch basin along the northestern margin 

of the Arabian plate. 5th Jordan geological conference & 3 rd conference on the 

geology of the Middle East (Geocome III), pp 347-373. 

Al-Qayim, B. A., 2000. Sedimentation and tectonic environment of the Suwais 

Red Beds, NE-Margin of the Arabian plate-5 th international on the geology of 

the Arab world, Egypt. Abstract book, p.112. 

Al-Qayim, B. A. and Al-Shaibahi, S. K., 1989. Stratigraphic anlysis of 

Cretaceous-Tertiary contact, Northwest Iraq.Journ. Geol. Soc. Iraq. Vol. 22, 

No.1, pp. 41-52. 

Al-Qayim, B. A. and Al-Shaibahi, S. K., 1993. Stratigraphic evolution of 

Paleogen sequence. Haibat-Sultan, Northeastern Iraq. Journ. Geol. Soc. Iraq. 

Vol. 21, No.2, pp. 51-65. 

Al- Rawi, I. K., 1981. Sedimentology and Petrography of Tanjero Clastic 

Formation From north and NE, Iraq. Unpub. Ph.D. Thesis, University of 

Baghdad, 295p. 



124 




Al- Rawi, D. and Al-hamadani, T. A., 1985. Microfacies study of Aqra 

limestone in the type section and Gali Zinta section and reconstruction of the 

paleoclimate. Journ. Geol. Soc. Iraq. Vol. 18, No.1, pp. 115-161. 

Al- Rawi, Y. T. and Al-Rawi, I. K., 2002. Tanjero Formation from northeast 


north Iraq.A turbidite example of flysch type. Proceeding of 15 th Iraqi 

Geological Conference, 15-18Dec.2002, Baghdad. 

Al- Shaibahi, S. K., 1973. Microfossils from Shiranish Formation in 

northeastern Iraq, Sulaimania, Asmar region. Journal of Geological Society of 

Iraq, vol.VI, p p 49-65. 

Al-Shaibahi, S. K. Al-Qayim, B. A. and Salman, L., 1986. Stratigraphic 

analysis of Tertiary Cetaceous contact, Dokan area, North Iraq, Journal of 

Geological Society of Iraq, vol.19, no.2.(7 th IGC) p.26. 

Al-Shaibani, S. K., Al- Hashimi, H. A., and Ghafor, I. M., 1993. 

Biostratigraphy of the Cretaceous-Tertiary boundary in well Tel-Hajer No-1, 

Sinjar area, northwest Iraq. Iraqi Geological Journal, Vol.26, no.2, pp.77-97. 

Arenillas, I. Arz, J. A. Molina, E. and Dupis, C., 2000a. An independent test 

of planktonic foraminiferal turnover across the Cretaceouc/Paleocene (K/P) 

boundary at at EL Kef, Tunisia: Catastrophic mass extinction and possible 

survivorship .Micropalentology, vol.46, no.1, pp. 31-49. 

Arenillas, I. Arz, J. A.Molina, E. and Dupis, C., 2000b.The 

Cretaceous/Paleocene (K/P) boundary at Ain Settara, Tunisia: sudden 

catastrophic mass extinction in planktonic foraminifera. journal of foraminiferal 

research, v.30,no.3, pp. 202- 218. 

Bak, K. Bak, M. Geroch, S. and Manecki, M., 1997. Biostratigraphy and 

paleoenvironmental analysis of benthonic foraminfera and radiolarians in 

Paleocene variegated shales in the Skole unit, Polish flysch Carpathians. 

Annales Societatis Geologorum Poloniae, vol. 67. pp 135-154. 

Bakkal, K. K. Ghafor, I. M. and Kassab, I. I. M., 1993. Biostratigraphy of 

Shiranish Formation in Hijran area Northeastern Iraq. journal of Science and 

Nature,(University of Salahaddin) Vol. 2, No. 2, pp. 34-39. 

Bandy, O. L., 1964. Cenozoic planktonic foraminiferal zonation .Micropaleo. 

Vol. 10, no. 1, pp.1-17, tex.figs. 1-6. 



125 




Bandy, O. L., 1967. Cretaceous planktonic foraminiferal zonation 

.Micropaleo. Vol. 13, no. 1, pp.1-31, tex.figs. 1-13. 

Barrera, E. and Savin, S. M., 1999. Evolution of the Late Campanian – 

Maastrichtian marine climates and oceans. in Barrera, E. and Joohnson, C. C. 

eds., Evolution of the Cretaceous Ocean- climate system: Boulder, Colorado, 

Geological Society of America Special paper , 332, pp.245-282. 

Bellen, R. C. Van, Dunnington, H. V., Wetzel, R. and Morton, D., 1959. 

Lexique Stratigraphique, Interntional. Asie, Iraq, vol. 3c. 10a, 333 p. 

Berggren, W. A. and Miller, K. G., 1988. Paleogene tropical planktonic 

foraminiferal biostratigraphy and magnetobiochronology. Micropaleontology. 

Vol. 34, No. 4, pp. 362-380. 

Berggren, W. A., Kent, D. V., Swisher, III, C. C. and Aubry, M.-P., 1995. A 

revised Cenozoic geochronology and chronostratigraphy in Berggren, W. A. 

and Norris, R. D. 1997. Biostratigraphy, phylogeny and systematics of 

Paleocene trochospiral planktonic foraminifera. Micropaleontology, vol.43, 

supplements. 1, pp. 1-116, text figures 1-17, plates 1-16, tables 1-5, and 

appendix 1. 

Berggren, W. A. and Norris, R. D., 1997. Biostratigraphy, phylogeny and 

systematics of Paleocene trochospiral planktonic foraminifera. 

Micropaleontology, vol.43, supplements. 1, pp. 1-116, text figures 1-17, plates 

1-16, tables 1-5, and appendix 1. 

Blow, W, H., 1979. The Cenozoic Globigerinidae, Vol. 1-3, Leiden, E. J.,Brill, 

1413p., 264pls. 

Boersma, A., 1984a. Cretaceous-Tertiary planktonic forams from the south 

Atlantic.Walvis Ridge area, deep Sea Drilling Project leg 74.Init. Rep.DSDP 

74, 501-523. 

Bolli, H. M., 1966. Zonation of Cretaceous to Pliocene marine sediments 

based on planktonic foraminifera. Bol. Inform. Asoc. Vonezolana Geol. Min. 

Ret .En., vol. 9, no.1, pp. 3-32, 4 tables. 

Bolton, C. M. G., 1958. The geology of Ranya area. Site Inv Co. Unpubl. 

Report, SOM. Library. Baghdad. 



126 




Boltovskoy, E. Watanabe, S. Totah, V. I. and Ocampo, J. V., 1992. 

Cenozoic benthonic foraminifers of DSDP Site 548 (North 

Atlantic).Micropaleontology, vol. 38, no. 2, pp. 183-207, plates 1-4, text figs 1- 

5, tables 1-4, appendix 1. 

Boltovskoy, E. Watanabe, S., 1993. Cenozoic monothalamous foraminifers 

from DSDP Site 525 (southern Atlantic) Micropaleontology vol. 37, no.1, pp. 1- 

27, plates 1-7, text figures 1-4, tables 1-4. 

BouDagher-Fadel. M. K, Banner. F. T, and Whittaker. J. E., 1997. The Early 

evolutionary history of planktonic foraminifera. Chapman and Hall. London. 

289 p., 15 Figs., 52 plates. 

Brohi, i. A., 1994. Late Cretaecous and Early Tertiary benthonic foraminiferal 

Biostratigraphy in Khuzdar District, Balochistan, Pakistan, with Special 

reference to the Influence of the Tethyan Sea Closure. Joun. Sci. Hiroshima. 

Univ., Ser. Vol.10, No.1, pp.25-81. 

Buday, T., 1980. Regional Geology of Iraq: Vol. 1, Stratigraphy, I.I.M Kassab 


S.Z. Jassim (Eds) D. G. Geol. Surv. Min. Invest. Publ. 445p. 

Buday, T. and Jassim, S. Z., 1987. The Regional geology of Iraq: Tectonism, 

Magmatism and Metamorphism. I. I. Kassab and M.J. Abbas (Eds), Baghdad, 

445 p. 

Canudo, J. I. Keller, G. and Molino, E., 1991. Cretaceous/Tertiry boundary 

extinction pattern and faunal turnover at Agost and Caravaca, S.E.Spain. 

Marine Micropaleontology .vol, 17. pp, 319-341. 

Caron, M., 1985. Cretaceous planktic foraminifera. In BOLLI, H.M., 

SAUNDERS 

, J.B. and PERCH-NIELSEN, K.,(Eds) Planktonic 

Stratigraphy, pp 17-87., 37 figs. Cambridge Univ. Press. 

Chacon. B. and Martin-Chivelet. J., 2005. Major Paleoenvironmental 

changes in the Campanian to Paleocene sequence of Caravaca (Subbetic 

Zone, Spain) journal of Iberian Geology 31 (2) pp 299-310. 

Chungkham, P. and Jafar, S. A., 1998. Late Cretaceous (Santonian- 

Maastrichtian) integrated Cocolith- Globotruncanid Biostratigraphy of pelagic 



127 




limestone from the accretionary prism of Manipur, northeastern India. 

Micropaleontology, vol. 44, no. 1, pp. 69-83. 

Ditmar, V. 

and Iraqi Soviet team., 1971. Geological conditions and 

hydrocarbon prospects of the republic of Iraq, northern and central part.- 

Technoexport report. INOC Library, Baghdad. 

D , Hont, S. and Keller, G., 1991. Some patterns of planktonic foraminiferal 

assemblage turnover at the Cretaceous/Tertiary boundary. Marine 

Micropaleontology .vol, 17. pp, 77-118. 

Dunnington, H. V., 1955. The Tertiary – Cretaceous boundary problem in N. 

Iraq. No IR/ HVD/ 611. Baghdad. INOC Library, Un published report. Pp.1-66, 

figs1-3. 

Dunnington, H. V., 1957. The Paleocene –Cretaceous unconformity at Aqra. 

Un published report.ivo. IR/ MUD /691. INOC Library.Baghdad, 

Einsele, G., 2000. Sedimentary basins, Evolution, Facies and Sediment 

Budget. Springer-Verlag, Berlin, Heidelberg, New York with 354 figures. 

El-Dawy, M. H., 2001. Paleocene benthonic foraminiferal Biostratigraphy and 

paleobathymetry in the sections between El Sheikh Fadl and Ras Gharib, 

Eastern Desert, Egypt. Micropaleontology, vol. 47, no.1, pp. 23 - 46, textfigures1-8, 

plates 1-3, 

Elnady H. and Shahin A., 2001. Planktonic Foraminiferal biostratigraphiy and 

paleobathymetry of the Late Cretaceous – Early Tertiary succession at 

northeast Sinai, Egypt. Egypt. Jour. Paleontol., Vol. 1, pp. 193-227. 

El-Naggar, Z, R., and Ashour, M. M., 1983. Microbiostratigraphic analysis of 

the Late Cretaceous - Early Paleocene successions in Egypt (typified by the 

Dakhala, Nile vally and Red sea coast sections) Proceed. Lst. Jord. Geol. 

Conf. (1982, Amman) pp.112-180, pls. 1-17, figs. 1-3. 

El-Nakhal, H. A., 1983. The occurance of the foraminiferal Genus 

Rugoglobigerina in the Late Cretaceous succession of Kuwait. Journ. Of Geol. 

Soc.Iraq. Vol. 16-17. pp. 149-183. 

El-Nakhal, H. A., 1984. Kassabella, anew Late Cretaceous planktonic 

foraminiferal Genus with meridional rogosity.Journal of foraminiferal research, 

Vol. 14, no.2, pp.140-141. 



128 




Faris, M., 1984. Biostratigraphy of the Upper Cretaceous-Lower Tertiary 

succession of Duwi Range, Quseir district, Egypt.Revue De 

Micropaleontolocie, Vol. 27, No. 2, pp. 107-112. 

Faris, M., 1985. Stratigraphy of the Late Cretaceous-Early Tertiary sediments 

in the Ghanima and Amur sections, Kharga area, Egypt.Newsl. stratigr.vol.14, 

no.1, pp. 36-47. 

Fluegeman, Jr., R. H. Berggren, W. A. and Briskin, M., 1990.Paleocene 

benthonic foraminiferal biostratigraphiy of the eastern Gulf Coastal Plain. 

Micropaleontoloy, Vol. 36, No. 1, pp. 56-64. 

Ganssen, G. M. and Kroon, D., 2000. The isotopic signature of planktonic 

foraminifera from NE Atlantic surface sediment: implication for the 

reconstruction of past oceanic conditions.Journal of Geological Society, 

London, Vol.157, pp. 693-699. 

Georgescu, M. D., 1996. Santonian –Masstrichtian planktonic foraminifers 

(Globigerinelloididae, Hedbergellidae, Globotrucanidae and 

Rugoglobigerinidae) in the Romanian black Sea offshore. 

Micropaleontology.vol. 42, no.4, pp 305- 333, text-figures 1-7, plates 1-12. 

Georgescu, M. D., 2002. An Interactive Guide to Planktonic Foraminifera; A. 

Cretaceous taxa. Published from Web. www.http://Services.chronos/guide 

plankforam/index.htm. , An HTmL -based illustrated guide to the taxonomy and 

descriptive morphology of Cretaceous planktonic foraminifera. 

Ghafor, I. M., 1988. Planktonic foraminifera and Biostratigraphy of the Aaliji 

Formation and the nature of its contact with the Shiranish Formation in Well 

Tel- Hajar No.1, Sinjar area , Northwestern Iraq. Unpublised MSc. thesis, 

University of Salahaddin-Iraq. 206 p. 

Ghafor, I. M. and Kareem, K. H., 1999. Biostratigraphy of Upper part of the 

Kolosh Formation from Sartaq-Bamo Northeastern Iraq.JDU (Sci)-Special 

issue: The first Scientific Conference of Dohuk University, Vol. 2, No. 4. pp, 

493-510. 

Ghlis, M. and Bellier, et Jean-Pierre., 1989. Comparative distribution of 

planktonic foraminifera and calcareous nanofossils in the Upper most 



129 




Cretaceous of the south Constantine area: a framework for Algeria. Revue de 

Micropaleontologie Vol. 32, no, 4. pp. 261-276. 

Govindan, A. Ravindran, C. N. and Rangaraju, M. K., 1996. Cretaceous 

stratigraphy and planktonic foraminifera Zonation of Cauvery Basin, Soyth 

India. Memoir Geological Society of India. No.37, pp. 155-187. L Roma Rao 

Volume, Cretaceous stratigraphy and Paleoenvironment. Ashok Sahni Editor. 

Gradstein, F. M, Kaminski, M. A. and Berggren, W. A., 1988. Cenozoic 

foraminiferal Biostratigraphy of the central North Sea. Abh. Geol. B.-A. Band. 

41, pp 97-108, with 2 figures and 2 ntables. 

Gradstein, F. M, Kristiansen, I. K. Loemo, L. and Kamniski, M. A., 1992. 

Cenozoic foraminiferal and dinoflagellate cyst Biostratigraphy of central North 

Sea. Micropaleontology vol.38, no.2, pp. 101-137. 

Gradstein, F. M, Kamniski, M. A. Berggren, W. A. Kristiansen, I. L. and D , 

Iorio, M. A., 1994. Cenozoic biostratigraphy of the North Sea and Labrador 

Shelf. Micropaleontology , vol.40, supplement for 1994, pp. 1-152, plates 1-22, 

text figures 1-40, tables 1-17, & A1-A5, appendices 1-4. 

Gradstein, F. M. and Backstrom, S., 1996. Cainozoic Biostratigraphy and 

Paleobathymetry, northern North Sea and Haltenbanken. Norsk Geologisk 

Tidsskrift, Vol. 76, pp. 3-32. Oslo. 

Gradstein, F. M and Kamniski, M. A., 1997. New species of Paleogene 

deep-water agglutinated foraminifera from the North Sea and Norwegian Sea. 

Annales Societatis Geologorum polonoae. Vol.67: pp. 217-229. 

Gradstein, F. M. Ogg. J. G. Smith, A. G. Bleeker, W. And Lourens, L. J., 

(2004). Anew Geologic Time Scale, with special reference to Precambrian 

and Neogene. Episodes, Vol. 27, No. 2, pp. 83-100. 

Grafe, K. U., 2005. Late Cretaceous benthonic foraminifera from the Basque- 

Cantabrian Basin, Northern Spain. Journal of Iberian Geology, vol. 31, no. 2, 

pp. 277-298. 

Hammoudi, R, A., 2000. Planktonic foraminiferal biostratigraphy of the 

Shiranish Formation (Upper Cretaceous) in Jambur well no.13 Northern 

Iraq.Raf.Jour.Sci. vol.11, No. 4, pp. 50-58 



130 




Houston, R. M. Huber, B. T. and Spero, H. J., 1999. Size related isotopic 

trend in some Maastrichtian planktonic foraminifera: methodological 

comparisons, intraspecific variability, and evidence for photosymbiosis. Marine 

Micropaleontology, 36, pp.169-188. 

Hradecka, L. Lobitzer, F. O. Savabenicka, L. and Svobodova, M., 1999. 

Biostratigraphy and Facies of selected Exposures in the Grunbach-Neue Welt 

Gosau-Group (Coal bearing Series, Inoceramus-Marl and Zweiersdorf- 

Formation, Late Cretaceous and Paleocene, Lower Austria): Abhandlungen 

der Geologischen Bundesanstalt, Band 56/2, pp.519- 551. 

Huber. B. T., 1990. Masstrichtian planktonic foraminifer biostratigraphy of the 

Maud Rise (WeddellSea, Antarctica): ODP Leg 113 Hole 689B and 689 C. 

proc. ODP, and Sci. Results 113,489-514. 

Huber. B. T., 1992. Paleobiogeography of Campanian – Maastrichtian 

foraminifera in the southern high latitudes. Paleogeogr., Paleoclimat., 

Paleoecol. 92,325-360. 

Huber. B. T. and Boersma, A., 1994. Cretaceous origination of Zeauvigerina 

and its relationship to Paleocene biserial planktonic foraminifera. Journal of 

Foraminiferal research, vol. 24, no. 4, pp. 268-287. 

Hudson, J. D., 1998. Duscution on the Cretaceous –Tertiary biotic transition. 

Journal of geological sosity, London, vol. 155, pp. 413-419. 

Hulsbos, R. E. Kroom, D. Jansen, H. S. M. and van Hinte, J. E., 1989. 

Lower Eocene benthonic foraminifera and Paleoenvironment of the outer 

Voring Plateau, Norwegian Sea (DSDP Site 338) Micropaleontology, Vol. 35, 

no.3, pp. 256-273, pls 1-3, 

Hunter, R. S. T. Arnold, A. J. and Parker, W. C., 1988. Evolution and 

homeomorphy in the development of the Paleocene planorotalites 

pseudomenardii and the Miocene Globorotalia (Globorotalia) margaritae 

lineages. Micropaleontology, vol.34, no.2, pp. 181-192. 

Jacob, V. S., 1978 Ms. Biostratigraphy and age determination of upper 

Cretaceous rocks (section 2) Dohuk area, North Iraq. S.O.M. (D.G.Geol. Surv. 

Min. Invest.) Library Baghdad. 



131 




James, G. A. and Wynd, J. G., 1965. Stratigraphic nomenclature of Iranian 

Oil Consurtium agreement area.AAPG Bull., Vol. 49, No. 12, pp.2182-2245, 

Figs. 98, Table.1. Tulso, Oklahoma 

Jassim, S. Z and Goff, J, C., 2006. Geology of Iraq. Published by Dolin, 

Brague Moravian Museum, Berno. 345p. 

Jaza, I. M., 1992. Sedimentary facies analysis of the Tanjero Formation in 

Sulaimaniya District, NE-Iraq. Unpubl. M. Sc. Thesis, Salahaddin University, 

121p. 

Jenkins, D. G. and Murray, J. W., 1981. Stratigraphic atlas of fossil 

foraminifera. Ellis Horwood limited publ. 310 p., 48 Figs., 66pls. 

Jones, G. D., 1988. A paleoecological model of Late Paleocene flysch-type 

agglutinated foraminifera using the paleoslope transect approach, Viking 

Graben, North Sea. Abh. Geol. B.-A. Band 41, pp. 143-153. With 5 figures and 

2 plates. 

Kaddouri, N., 1989. Stratigraphy of the Mesozoic and Cenozoic sediments in 

Sinjar depression. . Journ. Geol. Soc. Iraq. Vol. 22, No.2, pp. 35-43. 

Kaminski, M. A. Gradstein, F. M. Berggren, W. A. Geroch, S. and 

Beckmann J. P., 1988. Flysch type agglutinated foraminiferal assemblages 

from Trinidad: Taxonomy, stratigraphy and Paleobathymetry. Abh. Geol. B. - 

A. Band. 41, pp. 155-227, with 8 figures, 10 plates and 4 tables. 

Kaminski, M. A. and Crespo de Cabrera, S., 1999. Anew species of primitive 

Reticulophragmium (foraminifera) from the Paleocene Vidono Formation of 

northeastern Venezuela. Annales Societatis Geologorum Poloniae, vol. 69, pp. 

189-193. 

Karim, K. H., 2004. Basin analysis of Tanjero Formation in Sulaimaniya area, 

NE-Iraq. Unpublised Ph.D. thesis, University of Sulaimani University, 135p. 

Karim, K .H., 2006.Environment of Tanjero Formation as inferred from 

sedimentary structures, Sulaimanyia area, NE-Iraq. JAK, Vol.4, No.1.pp. 1-18. 

Karim, K.H and Surdashy, A. M., 2005a. Paleocurrent analysis of Upper 

Cretaceous Foreland basin: a case study for Tanjero Formation in Sulaimanyia 

area, NE-Iraq, , Journal of Iraqi Science, Vol. 5, No.1, pp.30-44. 



132 




Karim, K. H. and Surdashy, A. M., 2005b. Tectonic and depositional history 

of Upper Cretaceous Tanjero Formation in Sulaimaniya area NE-Iraq. JZS, 

Vol.8, No.1. pp. 47-62. 

Karim, K.H. and Surdashy, A. M., 2006. Sequence stratigraphy of Upper 

Cretaceous Tanjero Formation in Sulaimaniya area, NE-Iraq. KAJ, Vol.4. 

No.1.pp. 19-43. 

Karim, K.H. Sharbazheri, K. M. and Amin, B. M., 2007. Stratigraphic study 

of the contact between Kometan and Shiranish formation (Upper Cretaceous) 

Sulaimaniya Governorate, Kurdistan Region, NE- Iraq. Journal of geological 

society of Iraq Vol.39, No.1 (in press) 

Karim, S. A., 1975. Biostratigraphy of the Red Bed Series, Chwarta, NE-Iraq. 

Jour. Geol. Soc. Iraq, special issue, pp.147-156. 

Karim, S. A. and Jassim. S. Z., 1988. (issued in 1993) Biostratigraphy and 

environmental reconstruction of the Paleocene Phosphatic sequence, Western 

Desert, Iraq. Journ. Geol. Soc. Iraq. Vol. 21, No.2, pp. 129-151. 

Kassab, A, S. and Keheila, E. A., 1994. Paleocene Biostratigraphy and sea 

level change of the Northern Eastern Desert of Egypt. Newsl. Stratigr. 31 (2), 

pp.85-100.Berlin. Stuttgart. 

Kassab, I. I. M., 1972. Ms. Micropaleontology of Upper Cretaceous –Lower 

Tertiary of north Iraq . Univ. london, Phd. Thesis, 310 p, 29pls, 18text-figes., 

14 charts. 

Kassab, I. I. M., 1974a. The genus Heterohelix (Foraminiferida) from 

Northern. Iraq. Journal of Geological Society of Iraq, vol.VII, pp. 75-94 

Kassab, I. I. M., 1974b., Biostratigraphy of Upper Cretaceous – Lower Tertiary 

of North Iraq, v.1, Colloque Africaia de micropaleontology- Tunis.pp 277-325. 

Kassab, I. I. M., 1975a. Globotruncana falsocalcarata Kerdany and 

Abdelsalam from northern Iraq. Micropaleontology, vol.21, no.3, pp. 346-351,2 

pls,2 figs. 

Kassab, I. I. M., 1975b. Biostratigraphic study of the subsurface Upper 

Cretaceous – Lower Tertiary of Well Injana No. 5, Northestern Iraq. Journal of 

Geological Society of Iraq, Special issue, pp.181-199,2 pls, 5 figs. 



133 




Kassab, I. I. M., 1975c. Planktonic foraminifera range in the type Tanjero 

Formation (Upper Campanian-Maastrichtian) of N. Iraq. Journal of Geological 

Society of Iraq, vol.8, pp.73-86, 2figs. 

Kassab, I. I. M., 1975d. The genus Globigerinelloides from Northern. Iraq. 

Journal of Geological Society of Iraq, vol.8 , pp. 8-105. 

Kassab, I. I. M., 1976a. Planktonic foraminiferal ranges in the type Kolosh 

Formation (Middle-Upper Paleocene) of NE Iraq. Journal of Geological Society 

of Iraq, vol.IX, pp. 54-99. 30 text- figs., 4 pls. 

Kassab, I. I. M., 1976b. Some Upper Cretaceous planktonic foraminiferal 

genera from northern Iraq. Micropaleontology, Vol .22, no.2, pp.215-238, pls.1- 

4. 

Kassab, I. I. M., 1978b. Planktonic foraminiferal of the subsurface Lower 

Tertiary of northern Iraq. Journal of Geological Society of Iraq, vol.11, pp. 119- 

159. 7 pls, 5 figs. 

Kassab, I. I. M. Al-Omari, F. S. and Al- Safawee, N. M., 1986. The 

Cretaceous – Tertiary boundary in Iraq (represented by the subsurface section 

of Sasan well No.1, N.W. Iraq) Journal of Geological Society, Iraq, vol.19, 

No.2, pp.129-167. 

Keller, G., 1988. Extinction survivorship and evolution of planktonic 

foraminifera across the Cretaceous/Tertiary boundary at El Kef, Tunisia: 

Marine Micropaleontology. vol. 13, pp. 239-263. 

Keller, G., 1996. The Cretaceous – Tertiary Mass Extinction in planktonic 

foraminifera: Biotic Constraints for catastrophe Theories. Cretaceous – 

Tertiary Mass Extinction: Biotic and Environmental Changes.by Norman 

MacLeod and Gerta Keller, W.W Norton Company, New York- London, pp. 49- 

84. 

Keller, G., 2001. The end-Cretaceous mass extinction in the marine realm: 

year 2000 assessment: Planetary and Space Science, V. 49, pp. 817-830. 

Keller, G., 2002. Guembelitria-dominated Late Maastrichtian planktonic 

foraminiferal assemblage mimics early Danian in central Egypt. Marine 

Micropaleontology.vol. 47, pp.129-167. 



134 




Keller, G., (2004). Low diversity, Late Maastrichtian and Early Danian 

planctonic foraminiferal assemblages of the eastern Tethys. Journal of 

Foraminiferal Research, vol.34, no, 1, p.49-73. 

Keller, G. Li, L. and Maclleod, N., 1995. The Cretaceous/ Tertiary boundary 

stratotype section at El Kef, Tunisia: how catastrophic was the mass 

extiniction? Paleogeography. Paleoclimatology. Paleoecology. 199, pp 221- 

254. 

Khalil H. and Mashaly S., 2004. Stratigraphy and stage boundaries of the 

Upper Cretaceous and Lower Paleogene 

succession in Gabal Musaba 

salama area ,Southwestern Sinai Egypt. Egypt. Jour. Paleont. Vol.4, pp.1-38. 

Kuhnt, W. and Moullade, M., 1991. Quantitative analysis of Upper 

Cretaceous abyssal agglutinated foraminiferal distribution in the north Atlantic 

–paleoceanographic implications. Revue De Micropaleontologie, Vol. 34, no.4, 

pp. 313- 349. 

Kuhnt, W., 1990. Agglutinated foraminifera of western Mediterranean Upper 

Cretaceous pelagic limestones (Umbrian Spennines, Italy, and Betic 

Cordillera, Southern Spain). Micropaleontology. vol. 36, no. 4, pp. 297-330, 6 

pls. 

Kuhnt, W. and Kaminski, M. A., 1997.Cenomanian to Lower Eocene Deep- 

Water agglutinated foraminifera from the Zumaya section, Northern 

Spain.Annales Societatis Geologorum Poloniae, vol. 67, pp. 257-270. 

Lawa, F.A. Al-Karadakhi, A. I, Ismail, K. M., 1998. An interfingering of the 

Upper Cretaceous rocks from Chwarta-Mawat Region (NE-Iraq). Iraqi Geol. 

Journal, vol.31, no.2. 

Li, L. and Keller, G., 1998a. Maastrichtian climate, productivity and faunal 

turnover in planctonic foraminifera in South Atlantic DSDP sites 525A and 21. 

Marine Micropaleontology. vol.33, pp.55-86. 

Li, L. and Keller, G., 1998b. Diversification and extinction in Campanian 

Maastrichtian planktonic foraminifera of northwest Tunisia. Ecol. Geol. 

Helv.,91:pp 75-107. 

Lirer F., 2000 . A new technique for retrieving calcareous microfossils from 

lithified lime deposits. Micropaleontology , Vol. 46, no. 4, pp.365-369. 



135 




Liu, C. and Olsson, R. K., 1992. Evolutionary radiation of microperforate 

planktonic foraminifera following the K/T mass extinction event. Journal of 

foraminiferal research, vol.22, no. 4, pp 328-346. 

Liu, C. and Olsson, R. K., 1994. On the origin of Danian normal perforate 

planktonic foraminifera from Hedbergella. Journal of foraminiferal research, 

vol.24, no. 2, pp 61-74. 

Liu, C. Browning, J. V. Miller, K, G. and Olsson, R. K., 1997. Upper 

Cretaceous to Miocene planktonic foraminiferal Biostratigraphy: Results of leg 

150x, The NewJersey costal plain drilling project. Miller, K, G. and Snyder, S, 

W, (Eds) Proceeding of the Ocean drilling program, Scientific Resylts, 

Vol.150X, pp. 111-127. 

Loeblich, A. R. and Tappan, H., 1988. Foraminiferal genera and their 

Classification.Van Norstrand Reinhold Co., New York, 970 p. with 847 plates. 

Longoria,J. F., 1984. Cretaceous biochronology from the Gulf of Mexico 

region based on planktonic microfossils.Micropaleontology, vol. 30, no.3, 

pp.225-242. 

Longoria, J. F. and VonFeldt, A. E., 1991. Taxonomy, phylogenetics and 

biochronology of single-keeled globotruncanids (Genus Globotruncanita 

Reiss). Micropaleontology, vol. 37, no.2, pp197-243. 

Luger, P., 1988. Campanian to Paleocene agglutinated foraminifera from 

fresh water influenced marginal marine (Deltaic) sediments of southern Egypt. 

Abh. Geol. B.-A. Band 41, pp. 255-263. With 3 figures and 2 plates. 

Luning, S. Kuss, J. Bachmann, M. Marzouk, A. M. and Morsi, A. M., 1998. 

Sedimentary response to basin inversion: Mid Cretaceous- Early Tertiary Preto 

syndeformational deposition at the Areif El Naqa anticline (Sinai, Egypt) 

Institut fur palaontologie der Universitat Erlangen-Nurnberg. Facies. 38, 

pp.103- 136, pl. 35-37, 12 figs. 

Ly, A. and Kuhnt, W., 1994. Late Cretaceous benthonic foraminiferal 

assemblages of the Casamance shelf (Senegal, NW Africa) indication of the 

Late Cretaceous oxygen minimum zone.Revue De Micropaleontologie, vol. 37, 

no. 2, pp. 49-74. 



136 




MacLeod, N., 1996. Nature of the Cretaceous-Tertiary Planktonic 

Foraminiferal record: Stratigraphic Confidence Intervals, Signor-Lipps Effect, 

and Patterns of Survivorship. Cretaceous – Tertiary Mass Extinction: Biotic 

and Environmental Changes.by Norman MacLeod and Gerta Keller, W.W 

Norton Company, New York- London, pp. 85-138. 

Maestas, y. Macleod, K. G. Douglas, R. Self-Trail J. and Ward, P. D., 2003. 

Late Cretaceous Foraminifera, Paleoenvironments, and Paleoceanography of 

the Rosario Formation, San Antonio Del Mar, Baja California, Mexico. Journal 

of Foraminiferal Research, V.33, No. 3, pp. 179-191, 

Mancini, E. A., 1984. Biostratigraphy of Paleocene strta in southwestern 

Alabama. Micropaleontology, Vol. 30, No. 3, pp. 268-291. 

Martines, R. J. I., 1989. Foraminiferal biostratigraphy and paleoenvironments 

of the Maastrichtian Colon mudstone of northern South America. 

Micropaleontology. vol. 35, no. 2 pp.97-113. Pl. 1. 

Masters, B., 1977. Oceanic Micropaleontology. Mesozoic planktonic 

foraminifera. A. T. S. Ramsay (Edit) Academic press. London. Vol.1, pp 301- 

731., 7 Tables. 146 Figs., 58 pls 

Miller, K. Gradstein, F. M. and Berggren, W. A., 1982. Late Cretaceous 

Early Tertiary agglutinated benthonic foraminifera in the Labrdor Sea. 

Micropaleontology, vol. 28, no.1, pp 1-30, pls. 1-3. 

Minas, H. A. A., 1997. Sequence stratigraphic analysis of the Upper 

Cretaceous succession of Central and Northern Iraq. Unpubl. Ph. D. Thesis, 

Univ. Baghdad.188p. 

Molain, E. Algret, L. Arnellas, I. and Arz, J.A., 2005. The Cretaceous / 

Paleocene boundary at the Agost section revisted: Paleoenvironmental 

reconstruction and mass extinction pattern. Journal of Iberian Geology .vol. 

31(1).2005.pp, 135-148. 

Molina, E. Arenillas, I. and Arz, J. A., 1996. The Cretaceous / Tertiary 

boundary mass extinction in planktonic foraminifera at Agost, Spain. Revue de 

Micropaleontologie, vol.39, pp. 225-243. 



137 




Molina, E. Arenillas, I. and Arz, J. A., 1998. Mass extinction in planktonic 

foraminifera at the Cretaceous / Tertiary boundary in subtropical and 

temperate latitudes:Bulletin Societe geologique de France, vol.169, no. 3, pp. 

351-363. 

Morlotti, E., 1988. Late Cretaceous flysch-type agglutinated foraminifera from 

the northern Italian Apennines. Abh. Geol. B.-A. Band 41, pp. 265-285. 

Munim, A. A., 1976 MS. Upper Cretaceous and Lower Tertiary planktonic 

foraminifera of North Iraq, Dohuk area, Ustredni Ustav Geol .Praha. S.O.M. 

Unpubl. Report. Baghdad, 57 pp, 15 pls, 2 figs. 

Munim, A. A., and Said V. K., 1979. Micropaleontology and larger forams of 

the Upper Cretaceous and Tertiary sediments of Arbil-Shaqlawa-Koisinjaq, 

Kaidr area, North Iraq, Direct. General. Geology. Surv. & Mines. 

Invest.Paleont. Dept. Baghdad. Unpublished.Rep.pp.1-109. 

Neagu, TH., 1987. White chalk foraminiferal fauna in southern Dobrogea 

(Romania). Revista Espanola De Micropaleontologia, Vol. XIX, Num. 2, pp. 

281-314. 

Nederbragt, A. J., 1991. Late Cretaceous biostratigraphy and development of 

Heterohelicidae (planktonic foraminifera).Micropaleontology. Vol. 37, No.4, pp. 

329-372. 

Nomura, R., 1995. Paleogene to Neogene deep-sea paleoceanography in the 

eastern Indian Ocean: Benthonic Foraminifera from ODP Site 747,757 

and758.Micropaleontology, vol. 41, no.3, pp. 251-290, text-figures 1-17, plates 

1-4, tables 1-2, appendices 1-4. 

Norris, R. D., 1992. Umbilical structures in Late Cretaceous Planktonic 

foraminifera. Micropaleontology, vol.38, no.2, pp 165-181. 

Obaidalla, N. A., 2005. Complete Cretaceous/Paleogene (K/P) boundary 

section at Wadi Nukhul, southwestern Sinai, Egypt: inference from planktonic 

foraminiferal biostratigraphy. Revue de Paleobiologic, Geneve (2005) Vol. 24. 

(1):pp 201-224. 



138 




Olsson, R. K. Hemleben, C. Berggren, W. A. Huber, B. and Members of 

Paleogene planktonic foraminifera working group., 2000. Atlas of 

Paleocene Planktonic Foraminifera. 

http://services.chronos.org/foramatlas/pages/home.htm. 281p, with 66 plates, 

2 charts.and 29 paleogeographic mapes. 

Olsson, R. K. Hemleben, C. Berggren, W. A. and Liu, C., 1992. Wall texture 

classification of planktonic foraminifera Genera in the Lower Danian. Journal of 

foraminiferal research, vol, 22. no.3, pp, 195-213. 

Olsson, R. K. Wright, J. D. and Miller, K. G., 2001.Paleobiogeography of 

Pseudotextularia elegans during the latest Maastrichtian global warming event. 

Jour.of foram. Research, vol, 31. no.3, pp, 275-282. 

Oszczypko, N. Malata, E. Bak, K. Kedzierski, M. and Oszczypko-Clowes, 

M., 2005. Lithostratigraphy and Biostratigraphy of the Upper Albian – 

Lower/Middle Eocene flysch deposits in the bystrica and Raca subunits of the 

Magura Nappe; Western flysch Carpathians (Beskid Wyspowy and Gorce 

Ranges, Poland). Annales societatis Geologorum Poloniae, vol.75, pp. 27- 

69.with 28 figs. 

Pardo, A. Ortiz, N. and Keller, G., 1996. Latest Maastrichtian and Cretaceous 

–Tertiary Boundary Foraminiferal Turmover and Environmental Changes at 

Agost, Spain. Cretaceous – Tertiary Mass Extinction: Biotic and Environmental 

Changes. 

by Norman MacLeod and Gerta Keller, W.W Norton Company, New York- 

London, pp. 139-171. 

Pearson, P. N., 1998. Evolutionary Concepts in Biostratigraphy. Unlocking the 

stratigraphical record: Advanced in Modern Stratigraphy .Edited by P. Doyle 

and M. R. Bennett, John Wiley & Sons Ltd. 

Petrizzo, M. R., 2002. Paloceanographic and paleoclimatic inferences from 

Late Cretaceous planktonic foraminiferal assemblages from the Exmouth 

Plateau (ODP Site 762 and 763, eastern Indian Ocean) Marine 

Micropaleontology, vol. 45, pp. 117-150. 



139 




Petters, S. W. EL-Nakhal, H. A. and Cifelli, R., 1983. Costellagerina, A new 

Late Cretaceous Globigerina Foraminiferal Genus. Journal of Foraminiferal 

Research, vol.13, no.4, pp. 247-251. 

Poag, C. W. and Commeau, J. A., 1995. Paleocene to Middle Miocene 

planktonic foraminifera of the southwestern Salisbury embayment, Virgenia 

and Maryland: Biostratigraphy, allostratigraphy, and sequence stragraphy. 

Journal of Foraminiferal Research, vol.25, no.2, pp.134-155. 

Postuma. J, A., 1971. Manual of planktonic foraminifera. 5: Mesozoic 

Planktonic Foraminifera. A world-wide review and anlysis. Elsevier Publ. Co., 

Amsterdam. 420p, 24 Figs., 162pls. 

Premoli Silva, I, and Sliter, W, V., 1981. Cretaceous planktonic foraminifera 

from the 

Nauru Basin Leg 61 site 469, Western equatorial Pasific Initial 

reports of the DSDP, LXI, Washington, pp 423-437. 

Premoli Silva, I. and Sliter,W. V., 1995. Cretaceous planktonic foraminiferal 

biostratigraphy and evolutionary trends from the Bottaccione section. Gubbio, 

Italy: Paleontographia Italica.v. 82. pp 1-89. 

Premoli Silva, I. and Sliter, W. V., 1999. Cretaceous Paloceanography: 

Evidence from planktonic foraminiferal evolution, in Barrera, geological society 

of America Special Paper 332, pp 301-328. 

Premoli Silva, I. Spezzaferi. S. and D Angelantonio A., 1998. Cretaceous 

foraminiferal bio-isotope stratigraphy of Hole 967E and Paleogene planktonic 

foraminiferal biostratigraphy of Hole 966E, Eastern Mediterranean. Robertson, 

A, H, F., Emeis, K.C., Richter, C., and Camerlenghi, A. (Eds) Proceedings of 

Ocean Drilling program, Scientific Result, Vol. 160, pp 377-394. 

Quilty, P. G. Shafik, S. Jenkins, C. J. and Keene, J. B., 1997. An Early 

Cenozoic (Paleocene) foraminiferal fauna with Fabiania from offshore eastern 

Australia. Alcheringa, an Australian Journal of Paleontology, Vol.21, no. 3-4, 

pp. 299-315. 

Radoicic, R., 1995. A contribution to the Cretaceous Biostratigraphy of Kaolos 

area, NE Iraq. Ann, Geol, Penins. Balk. 59. 1, pp. 27-52. 

Raffo, S. S. D., 1989. Planktonic foraminifera and biostratigraphy of Aaliji 

Formation and nature of the contact with Shiranish Formation in Mushorah 



140 




well No 1, Northwest Iraq. Unpublished MSc. thesis, University of Mosul, 

Moysl-Iraq.140p.(in Arabic) 

Robaszynski, F., Caron, M., Gonzalez, D. J. M. and Wonders, A. A. H., 

1983-1984. Atlas of Late Cretaceous Globotruncanids Revue de Microp., 26, 

3-4, pp145-305. 

Rodriguez, G. F. Bustamente, S. B. and Fluegeman, Jr. R. H., 1999. 

Paleocene –Eocene planktonic foraminiferal Biostratigraphy of western Cuba. 

Micropaleontology, Vol.45, supplement 2, pp. 27-42. 

Sainta-Marc, P. and Berggren, W. A., 1988. 

Aquantitative analysis of 

Paleocene benthonic foraminiferal assemblages in central Tunisia. Journal of 

foraminiferal Research, vol.18, no.2, pp. 97-113, pl. 1-4. 

Salaj, J., and Solakius, N., 1984. The genus Kassabiana Salaj, 1983 from the 

uppermost Maastrichtian of Tunssia. Con, J, Earth, Sci, Vol. 21, pp.1114-1204. 

Salsj, J.. 1986. The Cretaceous and Paleocene sections of Tunisia proposed 

as the hypostratotypes and their correlation with planktonic zones of Libya. 

Journal of Geological Socity of Iraq, Vol. 18, No. 1mpp. 38 -54. 

Samir, A. M., 2002. Biostratigraphy and paleoenvironmental changes in the 

upper Cretaceous-Early Paleogene deposits of Gabal Samara section, 

Southwestern Sinai, Egypt. Egypt. Jour. Paleontol., Vol. 2, pp. 1-40. 

Shaaban, M. N. A., 1997. Stable isotop stratigraphy across the K/T boundary 

and isotopic investigations of an Ignored Worm Bed, Eastern Desert, 

Egypt.Facies, vol. 37, pp. 137-146. 

Shahin, A., 1992. Contribution to the Foraminiferal biostratigraphy and 

paleobathymetry of the Late Cretaceous and Early Tertiary in the western 

central Sinai, Egypt .Revue de micropaleontology. Vol.35, No.2, pp 157-175. 

Sharbazheri, K. M., 2007a. Aging of Unconformity within Tanjero Formation in 

Chwarta Area 

Science , Vol. 7, No.1, pp. 37-54. 

Northeast of Iraq (Kurdistan Region). Rafidain Journal of 

Sharbazheri, K. M., 2007b. Planktonic foraminiferal biostratigraphy of the 

Upper Cretaceous Reddish to Pale brown succession from Smaquli Area, 

Northeast Iraq (Kurdistan Region) Iraqi Bulletin of Geology and Mining. State 

company of geological survey and mining. In press. 



141 




Sissakian, V. K., 2000. Geological map of Iraq. Sheets No.1, Scale 

1:1000000, State establishment of geological survey and mining. GEOSURV, 

Baghdad, Iraq. 

Sliter, W. V., 1999. Cretaceous foraminiferal Biostratigraphy of the Calera 

Limestone, Northern California, USA. . Journal of Foraminiferal Research, 

vol.29, no.4, pp.318-339. 

Smit, J., 2005. The section of Barranco del Gredero (Caravaca, SE Spain): 

acrucial section for the Cretaceous/Tertiary boundary impact extinction 

hypothesis. Journal of Iberian Geology, vol. 31, pp. 179-191. 

Solakius, N. and Salaj, J., 1986. Anew Kassabiana species from the upper 

most Maastrichtian of northeastern Tunsia. Revista Espanola de 

Micropaleontologia, Vol.XVIII, Num.1, pp.71-77. 

Speijer, R. P. Schmitz, B. and Luger, P., 2000. Stratigraphy of Late 

Paleocene events in the Middle East: implication for low-to middle-latitude 

successions and correlations. Journal of Geological Society, London, Vol. 157, 

pp. 37-47. 

Speijer, R. P., 2003. Systematic and paleoecology of the foraminifer 

Neoeponides duwi (Nakkady) from the Paleocene of Egypt. 

Micropaleontology. Vol. 49, No.2, pp 146-150, text-figures 1, plates. 1. 

Stinnesbeck, W. Keller, G. Adatte, T. Harting, M. Stuben, D. Istrate, G. and 

Kramar, U., 2004: Yaxcopoil-1 and the Chicxulub impact .International Jour.of 

Sciences, GR Geologische Rundschau.10.1007/s00531-004-431-6 

http://www.geo.vu.nl/users.smit/forums, html/fulltext,html. 

Sultan, M. A. and Mohammad, H. M., 1997.The topographic development of 

the Paleocene –Eocene Depositional basin in the Northern and Central part of 

Iraq. Iraqi Geological Journal, Vol.30, no.2, pp.1- 7. ( In Arabic) 

Thomas, F. C., 1988.Taxonomy and stratigraphy of selected Cenozoic 

benthonic foraminifera , Canadian Atlantic margin. Micropaleontology, vol.34, 

no. 1, pp. 67-82.pls.1-2. 

Tibert, N. E. and Leckie, R. M., 2004. High-resolution estuarine sea level 

cycles from the Late Cretaceous: Amplitude constraints using agglutinated 

foraminifera. Journal of foraminiferal research, vol.32, no. 2, pp.130-143. 



142 




Uchman, A. Bubik, M. and Mikulas, R., 2005. The ichnological record across 

the Cretaceous/Tertiary boundary in turbiditic sediments at Uzgrun (Moravia 

Czech Republic). Geologica Carpathica, vol.56, pp. 57-65. 

Van Der Zwaan, g. Jorissen, F., and Stigter, H., 1990. The depth 

dependency of planktonic/Benthonic foraminiferal ratios: Constrains and 

application. Marine Micropaleontology, Vol. 95, pp. 1-16. 

Vergara, L. Rodriguez G. and Martinez, I., 1997. Agglutinated foraminifera 

and sequence stratigraphy from the CHipaque Formation (Upper Cretaceous) 

of El Crucero section, Colombia, South America. Micropaleontology. Vol.43, 

No.2, pp 185-201, text-figures 1-6, plates. 1-2 

Volat, J-L. Hugo, B. and Bignoumba - Ilogue, J., 1996. Arenaceous 

foraminifera from the Late Cretaceous of Gabon. Bulletin, Centres, 

Derecherches. Exploration, Production, Elf Aquitaine. Vol.20, no.1, pp. 230- 

275. 

Widmark, J. G. V. and Malmgren, B., 1992. Benthonic foraminiferal changes 

across the Cretaceous-Tertiary boundary in the deep sea; DSDP Sites 525, 

527, and 465. Journal of foraminiferal research, vol. 22, no. 2, pp. 81-103. 



143 




EXPLANATION OF THE PLATES 

PLATE -1 

Scale bar represents magnification on the specimens 

Figs 1- 3 Globotruncanita stuartiformis. (Dalbiez). 1- spiral view, 2- umbilical view, 

3- side view, Reddish to pale brown succession, Early Maastrichtian, Smaquli, 

Specimen from G, gansseri Zone 

Figs 4-5 Globotruncanita conica. (White). 4- spiral view, 5- umbilical view, 

Reddish to pal brown succession, Early Maastrichtian, Smaquli, 

Specimen from C. contuza Zone 

Figs 6-8 Contusotrancana contusa. (Cushman). 6- spiral view, 7- side view, 

8- umbilical view, reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen from C. contuza Zone 

Fig 9 Racemiguembelina fructicusa. (Egger) .Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from R. fructicusa Zone 

Fig 10 Racemiguembelina powelli. Smith&Pessango, reddish to pal brown succession, 


Fig 11 Gublerina cuvillieri. Kikoine, Reddish to pal brown succession, Early 

Maastrichtian, Smaquli, Specimen from Contusotruncana contusa Zone 

Fig 12 Pseudotextularia elegans. (Rzehak). Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from R. fructicusa Zone

PLATE -2 


Figs. 1-3 Gansserina gansseri (Bolli). 1- spiral view, 2- side view, 

3- umbilical view, Reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen from G., gansseri Zone 

Figs. 4-6 Gansserina wiedenmayeri (Gandolfi). 4- side view , 5- spiral view, 

6- umbilical view. Reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen from G. gansseri Zone 

Figs. 7-8 Contusotrancana plicata (White). 7- umdilical view, 8 spiral view. 


Specimen from G. gansseri Zone 

Fig. 9 Pseudotextularia intermedia De Klasz . Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Sample from P. intermedia Zone 

Figs. 10-12 Globotruncana aegyptiaca Nakkady.10- spiral view, 11- umbilical view, 

12- side view, Reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen from R. fructicusa Zone

PLATE -3 


Figs. 1-3 Contusotruncana fornicata. (Plumer). 1-umdilical view, 2- spiral view, 

3- side view, Reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen from G. gansseri Zone 

Figs. 4-6 Globotruncanita stuarti. (De Lapparent). 4- side view, 5- spiral view, 

6- umdilical view. Reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen from R. fructicusa Zone 

Figs. 7-9 Globotruncana orientalis. El-Naggar. 7- spiral view, 8- side view, 


Smaquli, Specimen from P. hariaensis Zone 

Figs. 10-12 Globotruncanita pettersi. (Gandolfi). 10- umbilical view , 11-side view, 

12- spiral view. Reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen from G. gansseri Zone

PLATE -4 


Figs. 1-3 Globotruncana ventricosa. White. 1- spiral view, 2- umbilical view, 

3- side view. Reddish to pal brown succession, Early Maastrichtian, Smaquli, 

Specimen from G. gansseri Zone 

Figs. 4-5 Globotruncana arca. (Cushman). 4- side view, 5- spiral view, 


Specimen from R. fructicusa Zone 

Fig. 6 Guembelitria dammula. (Voloshina). Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Sample from P. hariaensis Zone 

Figs. 7-9 Globotruncana bulloides. Vohgler . 7- spiral view, 8- umbilical view, 

9- side view. Reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen from Gtr. aegyptiaca Zone 

Figs.10-12 Globotruncanita angulata. Tilev. 10- umbilical view, 11 spiral view, 


Smaquli, Specimen from G. gansseri Zone

PLATE -5 


Figs.1-2 Globotruncana dupeublei. Caron, Gonzalez, Donoso, Robaszynski & 

wonders.1- side view, 2- spiral view,. Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G.gansseri Zone 

Fig. 3 Globotruncana rosetta. (Carsey). umbilical view, Reddish to pal brown 

succession, Early Maastrichtian, Smaquli, Specimen from P. intermedia Zone 

Fig. 4 Abathomphalus intermedius. (Bolli) , umbilical view, reddish to pal brown 

succession, Early Maastrichtian, Smaquli, Specimen from C. contusa Zone 

Fig. 5 Globotruncana falsostuarti. Sigal, side view, Reddish to pal brown 

succession, Early Maastrichtian, Smaquli, Specimen from R. fructicusa Zone 

Fig. 6 Globotruncana insignis. Gandolfi, umbilical view, Reddish to pal brown 

succession, Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone 

Fig.7 Globotruncana mariei. Banner&Blow, umbilical view, Reddish to pal brown 


Figs. 8-9 Globigerinelloides volutes. (White), 8- umbilical view, 9- peripheral view. 

Reddish to pal brown succession, Early Maastrichtian, Smaquli, Specimen 

from G. gansseri Zone 

Figs. 10-12 Rugoglobigerina rugosa. (Plummer), 10- umbilical view, 11- side view, 

12- spiral view. Reddish to pal brown succession, Early Maastrichtian, Smaquli 

, Specimen from R. fructicusa Zone

PLATE -6 


Figs. 1-3 Rugoglobigerina milamensis. Smith & Pessagno.1- umbilical view, 

2- side view, 3- spiral view. Reddish to pal brown succession, 


Figs. 4-6 Rugoglobigerina hexacamerata. Bronnimann. 4- umbilical view, 

5- spiral view, 6- side view, Reddish to pal brown succession, 


Figs.7-9 Rugoglobigerina macrocephala. Bronnimann. 7- umbilical view, 

8- spiral view, 9-. side view, Reddish to pal brown succession, 


Figs. 10-11 Rugoglobigerina rotundata. Bronnimann. 10- umbilical view, 

11- spiral view. Reddish to pal brown succession, Early Maastrichtian, 


Fig. 12 Planoglobulina acervulinoides. (Egger). Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone

PLATE -7 


Fig. 1 Heterohelix globulosa.(Ehrenberg). Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone 

Fig. 2 Heterohelix striata. (Ehrenberg). Reddish to pal brown succession, 


Fig. 3 Heterohelix nauttalli. (Voorwijk). Reddish to pal brown succession, 


Fig. 4 Heterohelix globulosa. (Ehrenberg) reddish to pal brown succession, 


Fig. 5 Heterohelix punctulata. (Cushman), Reddish to pal brown succession, 


Fig. 6 Heterohelix reussi . (Cushman). Reddish to pal brown succession, 


Figs. 7-8 Globotruncanella havanensis. (Voorwijk), 7- spiral view, 

8- umbilical view , Reddish to pal brown succession, Early Maastrichtian, 


Fig. 9 Globotruncanella pschadae. (Keller), spiral view. Reddish to pal brown 

succession, Early Maastrichtian, Smaquli, Specimen from R. fructicusa Zone 

Figs.10-12 Globotruncanella petaloidia. (Gandolfi), 10- side view, 

11- umbilical view, 12- spiral view. Reddish to pal brown succession, 


PLATE -8 


Fig. 1 Pseudotextularia deformis. (Kikoine). Reddish to pal brown succession, 


Fig. 2 Pseudogumbelina costulata. (Cushman). Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from P. intrmidia Zone 

Fig. 3 Pseudotextularia elegans. (Rzehak). Reddish to pal brown succession, 


Figs. 4-6 Rugoglobigerina pennyi. Bronnimann, 4- spiral view, 5- umbilical view, 



Figs.7-9 Rugotruncana subcircumnodifer. (Gandolfi), 7- umbilical view, 

8- spiral view, 9- side view. Reddish to pal brown succession, 


Figs. 10-11 Rugotruncana circumnodifer. Finlay, 10- spiral view, 



Fig. 12 Globotruncanita Sp. Reddish to pal brown succession, Early Maastrichtian, 

Smaquli, Specimen R. fructicusa Zone

PLATE -9 


Fig. 1 Hedbergella monmuthensis (Olsson). Reddish to pal brown succession, 


Fig. 2 Globigerinelloides prairiehillensis Pessango. Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from P. intermedia Zone 

Fig. 3 Globigerinelloides multispinata (Lalicker), Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from C.contusa Zone 

Fig. 4-6 Kuglerina rotundata (Bronnimann). 4- umbilical view, 5- side view, 

6- spiral view. Tanjero Formation, Late Maastrichtian, Smaquli, 

Specimen from P. hariaensis Zone 

Fig. 7 Archaeoglobigerina carteri (Kassab). Tanjero Formation, Late Maastrichtian, 

Smaquli, Specimen from P. intermedia Zone 

Fig. 8-9 Costellagerina cf. bulbosa Belford, 8- spiral view, 9- umbilical view , 

Tanjero Formation, Late Maastrichtian, Smaquli, Specimen from 

P. hariaensis Zone 

Fig. 10-12 Hedbergella monmuthensis (Olsson), 10- umbilical view, 11- Side view, 

12- spiral view, Tanjero Formation, Late Maastrichtian, Smaquli, Specimen 

from P.hariaensis Zone 

.

PLATE -10 


Fig. 1 Lenticulina gunderbookaensis. Crespin. Shiranish Formation, Late Campanian- 

Early Maastrichtian, Smaquli. Specimen from Glt.aegyptiaca Zone. 

Fig. 2 Lenticulina navicula. ( d Orbigny). Shiranish Formation, Late Campanian- 

Early Maastrichtian, Smaquli. Specimen from Glt.aegyptiaca Zone . 

Fig. 3 Gavelinella micra. Reddish to pal brown succession, 


Figs. 4 Oolina apiculata. Reuss, Reddish to pal brown succession, 


. 

Figs. 5 Coryphostomata midwayensis. (Cushman) Shiranish Formation, Late Campanian- 

Early Maastrichtian, Smaquli. Specimen from Glt.aegyptiaca Zone . 

Figs. 6 Dentalinoides sp., Reddish to pal brown succession, 


Figs. 7, 8 Ammodiscus preuvianus. Berry, Reddish to pal brown succession, 


Fig. 9 Spiroplectamina laevis. (Roemer), Shiranish Formation, Late Campanian- 

Early Maastrichtian, Smaquli Specimen from Glt.aegyptiaca Zone . 

Fig.10,11 Bolivina incrassata. Reuss, Reddish to pal brown succession, 


Fig. 12 Cibicidoides excavata. Brotzen, Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone

PLATE -11 


Fig. 1,2 Gyroidina girardana. (Reuss), Reddish to pal brown succession, 


Fig. 3 Dorothia sp. Shiranish Formation, Late Campanian- Early Maastrichtian, 

Smaquli. Specimen from Glt.aegyptiaca Zone. 

Fig. 4 Pullenia quinqueloba ( Reuss). Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Sample from G. gansseri Zone 

Figs. 5 Lenticulina navicula. (d Orbigny). Reddish to pal brown succession, 


Figs. 6,7 Cibicides subcarinatus Cushman&Deaderi. Reddish to pal brown 


Figs. 8,9 Paralabamina hillebrandti. (Fisher) Reddish to pal brown succession, 

Early Maastrichtian, Smaquli. Specimen from G. gansseri Zone 

Fig. 10 Clavulinoides globulifera. Ten Dam & Sigal, Reddish to pal brown 


Fig, 11 Bolivinoides draco. ( Marson). Reddish to pal brown succession, 


Fig. 12 Bolivinoides miliaris . Hilterman & Koch, Reddish to pal brown succession, 


PLATE -12 


Fig. 1 Nodosaria minor. Hantken, Reddish to pal brown succession, 


Fig. 2 Dorothia retusa. Reddish to pal brown succession, 


Fig. 3 Globorotalites sp. Reddish to pal brown succession, 


Figs. 4 Lagena hispida Reuss. Reddish to pal brown succession, 


Figs. 5 Dorothia smokynensis Wall. Reddish to pal brown succession, 


Figs. 6 Lenticulina sp. Reddish to pal brown succession, 


Fig. 7 Dorothia roseta, Reddish to pal brown succession, 


Fig, 8 Palliolatella sp. Reddish to pal brown succession, 

Early Maastrichtian, Smaquli. Specimen from C.contusa Zone 

Fig. 9 Lagena sp, Reddish to pal brown succession, Early Maastrichtian, 

Smaquli. Specimen from C.contusa Zone 

Fig. 10 ,11 Cibicidoides dayi (White) Reddish to pal brown succession, 

Early Maastrichtian, Smaquli. Specimen from P.intermedia Zone 

Fig. 12 Saracenaria navicula (d Orbigny) Reddish to pal brown succession, 

Early Maastrichtian, Smaquli. Specimen from P.intermedia Zone

PLATE -13 


Fig. 1, 2 Praebulimina laevis. (Beissel) , Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from P.intermedia Zone 

Fig. 3 Oolina globosa.(Montagu) Reddish to pal brown succession, 


Fig. 4 Gyroidinoides subangulatus. (Plummer) Reddish to pal brown succession, 


Figs. 5 Nodosaria cf. limbata d , Orbigny. Reddish to pal brown succession, 


Figs. 6 Marsonella oxycona (Reuss). Reddish to pal brown succession, 


Figs. 7 Ammodiscus cretaceus (Reuss). Tanjero Formation, Late Maastrichtian, 

Smaquli. Specimen from R. fructicusa Zone 

Fig. 8 Dentalinoides canulina. Marie, Tanjero Formation, Late Maastrichtian, 


Fig, 9 Oolina apiculata. Reuss, Tanjero Formation, Late Maastrichtian, 


Fig. 10 Dentalina inornata. (d , Orbigny), Tanjero Formation, Late Maastrichtian, 


FIG. 11 Gyroidinoides globosus. (Hagenow) Tanjero Formation, Late Maastrichtian, 


Fig. 12 Praebulimina carseyae (Plummer) Tanjero Formation, Late Maastrichtian, 

Smaquli. Specimen from P.hariaensis Zone

PLATE -14 


Fig. 1, 2 Noneonella insecta. (Schwager), Tanjero Formation, Late Maastrichtian, 


Fig. 3 Gyroidinoides globosus. (Hagenow) ,Tanjero Formation, Late Maastrichtian, 

Smaquli, Specimen from P.hariaensis Zone 

Fig. 4,5 Gaudryna pyramidata. Cushman, Tanjero Formation, Late Maastrichtian, 


Figs. 6 Gaudryna pyramidata. Cushman,., Shiranish/Tanjero 

Smaquli, Specimen from C.contusa Zone 

transition unit, 

Figs. 7 Pullenia jarvisi. Cushman, Tanjero Formation, Late Maastrichtian, 


Figs. 8 Dentalina elegans. d Orbigny, Tanjero Formation, Late Maastrichtian, 


Fig. 9 Textularia astutia. Lalicker ., Tanjero Formation. Smaquli, 

Specimen from P.hariaensis Zone 

Fig, 10 Pleurostomella subnodosa. (Reuss), Reddish to pal brown succession, 

Early Maastrichtian, Smaquli. Specimen from C.contusa Zone 

Fig. 11 Bolivinoides sp. Tanjero Formation, Late Maastrichtian, 

Smaquli,. Specimen from P.hariaensis Zone 

Fig. 12 Ellipsodimorphina sp. Reddish to pal brown succession, 

Early Maastrichtian, Smaquli. Specimen from G. gansseri Zone

PLATE -15 


Fig 1 Lenticulina muennsteri. Tanjero Formation, Late Maastrichtian, Kato, 


Fig 2 Ammosphaeroidina pseudopauciloculata (Mjatliuk) Tanjero Formation, Late 

Maastrichtian, Qishlagh, Specimen from P. hariaensis Zone 

Fig 3 Omphalocyclus macroporus (Lamarck), Tanjero Formation , Late Maastrichtian, 

Kato, Specimen from R. fructicusa Zone 

Fig 4 Orbitoides medius (d archaic), Tanjero Formation , Late Maastrichtian, Kato , 


Figs. 5,6 Cibicides subcarinatus Cushman & deaderi. Tanjero Formation, Late 

Maastrichtian, Kato, Specimen from R. fructicusa Zone 

Figs. 7, 8 Osangularia navarrana (Cushman). Tanjero Formation, Late Maastrichtian 

Kato, Specimen from R. fructicusa Zone 

Fig. 9 Neoflabellina rugosa. (d Orbigny). Tanjero Formation, Late Maastrichtian, 

Dokan, Specimen from R. fructicusa Zone 

Figs. 10 pullenia jarvici Cushman. Tanjero Formation, Late Maastrichtian, Kato, 


Fig. 11 Praebulimina quadrata. Tanjero Formation, Late Maastrichtian, Kato, 


Fig. 12 Ammodiscus cretaceus (Reuss). Tanjero Formation Late Maastrichtian, Kato 

, Specimen from R. fructicusa Zone 

Fig. 13 Spiroplectamina sp. Tanjero Formation, Early Maastrichtian, Kato, Specimen from 

G. gansseri Zone 

Fig. 14 Dorothia crassa, Tanjero Formation, Late Maastrichtian, Kato, Specimen 

from R. fructicusa zone 

Figs. 15, 16 Globotruncanan gagnebini Tilev. Late Maastrichtian, Kato, Specimen 

From P. hariaensis Zone

PLATE -16 


Figs 1-3 Abathomphalus mayaroensis (Bolli) . 1, 2 spiral view, 3 umbilical view, 

Tanjero Formation, Late Maastrichtian. Dokan, Specimen from 

R. fructicosa Zone 

Figs 4, 5 Pseudoguembelina costulata (Cushman), Tanjero Formation, Late Maastrichtian, 

Sirwan, Specimen from P. hariaensis Zone 

Fig 6 Pseudoguembelina hariaensis. Nederbragt. Tanjero Formation, Late Maastrichtian. 

Dokan, Specimen from P. hariaensis Zone 

Figs 7, 8 Pseudoguembelina palpebra. Bronnimann & Brown. . Tanjero Formation, Dokan, 

Specimen from P. palpebra Zone 

Fig 9 Laeviheterohelix glabrans (Cushman) Tanjero Formation, Late Maastrichtian. 

Sirwan, Specimen from P. hariaensis Zone 

Figs 10, 11 Pseudoguembelina excolata (Cushman) Tanjero Formation, Late Maastrichtian. 

Sirwan, Specimen from P. hantkeninoides Zone 

Fig 12 Plummerita hantkeninoides (Bronnimann). Tanjero Formation Late Maastrichtian 

Dokan, Specimen from P. hantkeninoides Zone

PLATE -17 

Figs 1- 3 Globotruncana aegyptiaca Nakkady, 100X, 1- Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone, 2&3 Tanjero 

Formation, Late Maastrichtian, Dokan, Specimen from R. fructicusa Zone 

Figs 4-5 Globotruncana linneiana (d Orbigny), 100X,Shiranish Formation, Late Campanian- 

Early Maastrichtian, Smaquli, Specimen from Globotruncana aegyptiaca Zone. 

Fig 6 Globotruncana ventricosa White. 100X. Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone. 

Figs 7-9 Globotruncana arca. (Cushman). 100X, Reddish to pal brown succession, 


Fig 10-12 Globotruncana bulloides , Vohgler,100X, Reddish to pal brown succession, 


Fig 13-15 Globotruncana orientalis. El-Naggar, 100X, Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone.

PLATE -18 

Figs 1-2 Globotruncana falsostuarti. Sigal, 100X, 1- Tanjero Formation, Late 

Maasrtichtian, Dokan, Specimen from R. fructicusa Zone, 2- Reddish to pal brown 

succession, Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone. 

Fig 3 Globotruncana lapparenti. Brotzen.100X, Shiranish Formation, Late Campanian- 

Early Maastrichtian, Smaquli, Specimen from Globotruncana aegyptiaca Zone. 

Figs. 4-6 Globotruncana dupeublei. Caron, Gonzalez, Donoso, Robaszynski & wonders, 

100X, Tanjero Formation, Late Maastrichtian, 4&5- Smaquli, Specimen from 

R. fructicusa Zone, 6-Sirwan. Specimen from P. hariaensis Zone. 

Figs. 7-8 Globotruncana rosetta (Carsey).100X, Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from P. intermedia Zone . 

Fig. 9-11 Contusotrancana falsocalcarata. Kerdany & Abdelsalam, 100X, Tanjero 

Formation. Late Maastrichtian, 9-Smaquli, 10-Dokan, 11-Serwan, Specimen from 

Plummerita hantkeninoides Zone. 

Figs. 12-14 Gansserina gansseri (Bolli), 100X, Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone . 

Fig 15 Gansserina wiedenmayeri (Gandolfi),100X, Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from G. gansseri Zone.

PLATE -19 

Figs. 1 Gansserina wiedenmayeri (Gandolfi), 100X, Reddish to pal brown succession, 

Early Maastrichtian, Smaquli, Specimen from Contusotrancana contusa Zone. 

Figs. 2-5 Globotruncanita stuarti. (De Lapparent).100X, 2&3- Shiranish Formation, Late 

Campanian- Early Maastrichtian, Smaquli, Specimen from Globotruncana aegyptiaca 

Zone, 4&5- Reddish to pal brown succession, Early Maastrichtian, Smaquli, Specimen 

from G. gansseri Zone. 

Figs. 6-8 Globotruncanita stuartiformis. (Dalbiez).100X, 6-Tanjero Formation, Late 

Maastrichtian, Kato, Specimen from R. fructicusaZone. 7- Tanjero Formation, Late 

Maastrichtian, Dokan, Specimen from R. fructicusaZone. 8- Tanjero Formation, Late 

Maastrichtian, Smaquli, Specimen from R. fructicusaZone. 

Figs 9-13 Globotruncanita conica White, 100X, 9&10 -Tanjero Formation, Late 

Maastrichtian, Dokan, Specimen from R. fructicusaZone.11- Tanjero Formation, Late 

Maastrichtian, Smaquli, Specimen from R. fructicusaZone. 12&13- Tanjero Formation, 

Late Maastrichtian, Qishlagh, Specimen from R. fructicusaZone 

Fig 14 Globotruncanita pettersi, Gandulfi.100X, Tanjero Formation, Late Maastrichtian, 

Sirwan, Specimen from R. fructicusaZone. 

Fig 15 Globotruncanita angulata, Tilev. Tanjero Formation, Late Maastrichtian, 

Smaquli, Specimen from R. fructicusaZone.

PLATE -20 

Figs 1-3 Contusotruncana fornicata (Plumer).100X, Reddish to pal brown succession, 


Figs 4-5 Contusotrancana patelliformis (Gondolfi), 100X, Reddish to pal brown succession, 


Figs 6-9 Contusotrancana contusa (Cushman), 100X, 6&7- Tanjero Formation, Late 

Maastrichtian, Sirwan, Specimen from P. hariaensis Zone. 8- Reddish to pal brown 

succession, Early Maastrichtian, Smaquli, Specimen from Contusotrancana contusa 

Zone. 9-Tanjero Formation, Late Maastrichtian, Dokan, Specimen from P. hariaensis 

Zone. 

Figs 11-12 Contusotrancana walfischensis. Todd, 100X, Tanjero Formation, Late 

Maastrichtian, Smaquli, Specimen from P. hariaensis Zone. 

Figs 10, 13, 14 Contusotrancana sp. 100X, Tanjero Formation, Late Maastrichtian, Smaquli, 

Specimen from P. hariaensis Zone. 

Figs 15 Contusotrancana plicata White.100X, Tanjero Formation, Late Maastrichtian, 

Smaquli, Specimen from P. hariaensis Zone.

PLATE -21 

Figs 1-2 Abathomphalus mayaroensis (Bolli), 100X, 1- Tanjero Formation, late 

Maastrichtian, Smaquli, Specimen from R. fructicusa Zone.2- Tanjero Formation, late 

Maastrichtian, Sirwan, Specimen from P. hariaensis Zone. 

Figs 3-5 Abathomphalus intermedius. (Bolli), 100X, Tanjero Formation, Late 

Maastrichtian, Smaquli Specimen, from R. fructicosa Zone 

Fig 6 Globotruncanella pschadae, (Keller), 100X, Tanjero Formation, Late 

Maastrichtian, Sirwan, Specimen from P. hariaensis zones, 

Figs 7-8 Globotruncanella petaloidea (Gandolfi).100X, Tanjero Formation, Late 

Maastrichtian,7- Smaquli, 8- Sirwan, Specimen from P. hariaensis Zone. 

Fig 9 Globotruncanella havanensis (Voorwijk), 100X, Tanjero Formation, Late 

Maastrichtian, Smaquli, Specimen from R. fructicosa zones, 

Figs10-12 Plummerita hantkeninoides (Bronnimann), 100X, Tanjero Formation, Late 

Maastrichtian, 10-Sirwan,11- Dokan, 12- Smaquli, Specimen from Plummerita 

hantkeninoides Zone., 

Figs 13-14 Archaeoglobigerina cretacea. (d Orbigny)100X, , Reddish to pal brown 


Fig 15 Archaeoglobigerina blowi. Pessango,100X, Reddish to pal brown succession, Early 

Maastrichtian, Smaquli, Specimen from G. gansseri Zone.

PLATE -22 

Fig 1 Archaeoglobigerina blowi. Pessango, 100X, Reddish to pal brown succession, 


Figs 2-5 Rugoglobigerina rugosa. (Plummer), 100X, Tanjero Formation, late 

Maastrichtian, 2&3-Dokan, 4&5-Sirwan, Specimen from P.haiaensis Zone., 

Figs. 6 Rugoglobigerina macrocephala. Bronnimann.100X, Tanjero Formation, Late 


Figs. 7 Rugoglobigerina pennyi Bronnimann, 100X, Tanjero Formation, late Maastrichtian, 

Dokan, Specimen from P.hariaensis Zone 

Fig 8 Rugoglobigerina reicheli .Bronnimann.100X, Tanjero Formation, Late 


Figs. 9-11 Rugoglobigerina hexacamerata. Bronnimann. 100X, Tanjero Formation, Late 

Maastrichtian, 9- Dokan, 10-Qishlagh,11-Smaquli, Specimen from R. fructicusa Zone 

Fig 12 Rugoglobigerina rotundata Bronnimann.100X, Tanjero Formation, Late 


Fig 13 Rugotruncana subcircumnodifer ( Gandolfi), 100X, Reddish to pal brown 


Fig. 14-15 Hedbergella monmuthensis (Olsson), 100X, Tanjero Formation, Late 

Maastrichtian, 14- Sirwan, 15-Dokan, Specimen from Plummerita hantkeninoides 

Zone.

PLATE -23 

Fig. 1 Globigerinelloides multispina .(Lalicker), 100X, Reddish to pal brown succession, 


Fig 2 Globigerinelloides subcarinata.(Bronnimann, 100X, Tanjero Formation, Late 


Fig. 3 Globigerinelloides ultramicra.(Subbotina),100X, Reddish to pal brown succession, 


Fig. 4 Pseudotextularia intermedia (De Klasz). 100X, Tanjero Formation, Late 


Figs 5-6 Pseudotextularia elegans. (Rzehak),100X, Tanjero Formation, Late 

Maastrichtian, Dokan, Specimen from P .hariaensis Zone. 

Figs 7-8 Racemiguembelina fructicosa (Egger) , 100X, Tanjero Formation, Late 

Maastrichtian, Smaquli, Specimen from R. fructicusa Zone 

Fig. 9 Planoglobulina acervulinoides (Egger). 100X, Tanjero Formation, Late 

Maastrichtian, Dokan, Specimen from P. hariaensis Zone. 

Fig. 10 Heterohelix nauttalli (Voorwijk), 100X, Reddish to pal brown succession, Early 

Maastrichtian, Smaquli, Specimen from G gansseri Zone 

Fig. 11 Heterohelix globulosa (Ehrenberg),100X, Tanjero Formation, Late 

Maastrichtian, Dokan, Specimen from P .hariaensis Zone. 

Fig. 12 Heterohelix punctulatus (Cushman),100X, Tanjero Formation, Late 

Maastrichtian, Smaquli, Specimen from R. fructicusa Zone. 

Fig 13 Trinitella scotti. Bronnimann, 100X, Tanjero Formation, late 

Maastrichtian, Smaquli, Specimen from Plummerita hantkeninoides Zone. 

Fig. 14 Kuglerina rotondata (Bronnimann). 100X, Tanjero Formation, Late 

Maastrichtian, Smaquli, Specimen from Plummerita hantkeninoides Zone 

Fig 15 Globotruncanella sp.100X, Tanjero Formation, Late Maastrichtian, Smaquli, 

Specimen from Plummerita hantkeninoides Zone

PLATE -24 


Figs 1-4 Subbotina triloculinoides (Plummer), 1: side view. 2, 4: spiral view. 3: umbilical 

view, Early Paleocene, Kolosh Formation, Dokan, Specimen from (P1b) Subbotina 

triloculinoides-Globanomalina compressa/Praemurica inconstans Zone 

Figs 5-8 Subbotina trivals (Subbotina), 5: umbilical view. 6: side view. 7, 8: spiral view, 

Early Paleocene, Kolosh Formation, Smaquli, Specimen from (Pá) 

Parvularugoglobigirina eugubina Zone 

Figs 9-14 Parvularugoglobigirina eugubina (Luterbacher & Premoli Silva). 9, 10 : spiral 

view, 11, 14 : side view, 12,13 : umbblical view. Early Paleocene, Kolosh Formation, 

Smaquli, Specimen from (Pá) Parvularugoglobigirina eugubina Zone 

Figs 15-17 Woodringina claytonensis Loeblich & Tappan, Early Paleocene, Kolosh 

Formation, Smaquli, Specimen from (Pá) Parvularugoglobigirina eugubina Zone 

Figs 18, 19 Chilogumbelina morsei (Kline) Early Paleocene, Kolosh Formation, Smaquli, 

Specimen from (P1a) Parvularugoglobigirina eugubina- Subbotina triloculinoides 

Zone 

Fig 20 Chilogumbelina midwayensis (Cushman), Early Paleocene, Kolosh Formation, 

Smaquli, Specimen from (P1a) Parvularugoglobigirina eugubina- Subbotina 

triloculinoides Zone

PLATE -25 


Figs 1-6 Parasubbotina aff pseudobulloides (Olsson et al). 1, 4, 5: spiral view, 2: side 

view, 3,6 :umbilical view, Early Paleocene, Kolosh Formation, Smaquli, Specimen 

from (Pá) Parvularugoglobigirina eugubina Zone 

Figs 7-10 Parasubbotina pseudobulloides (Plummer), 7: side view, 8, 10: umbilical view 

9: spiral view, Early Paleocene, Kolosh Formation, Dokan, Specimen from 

(P1a) Parvularugoglobigirina eugubina- Subbotina triloculinoides Zone 

Figs 11-16 Praemurica taurica (Morozova), 11: spiral view. 12, 16: side view. 13-15 

umblical view, Early Paleocene, Kolosh Formation, Smaquli, Specimen from 

(Pá) Parvularugoglobigirina eugubina Zone 

Figs 17-18 Parvularugoglobigirina extensa (Blow), 17: umbilical view. 18: spiral view, 

Early Paleocene, Kolosh Formation, Smaquli, Specimen from(Pá) 

Parvularugoglobigirina eugubina Zone 

Figs 19-20 Globoconusa daubjergensis (Bronnimann), spiral view, Early Paleocene, 

Kolosh Formation, Smaquli, Specimen from (Pá) Parvularugoglobigirina 

eugubina Zone

PLATE -26 


Figs 1-5, 19-20 Eoglobigerina simplicissima Blow, 1, 4, 19: spiral view. 2: side view. 

3, 5, 20: umbilical view, Early Paleocene, Kolosh Formation, Smaquli, Specimen from 


Figs 6-10 Eoglobigerina eobulloides Morozova, 6, 8: side view. 7, 9: umbilical view. 

10: spiral view, Early Paleocene, Kolosh Formation, Smaquli, Specimen from 


Figs 11-15 Eoglobigerina edita (Subbotina), 11: spiral view. 12, 13:umbilical view. 

14-15: side view, Early Paleocene, Kolosh Formation, Smaquli, Specimen from 


Fig 16 Parvularugoglobigirina extensa (Blow), spiral view, Early Paleocene, Kolosh 

Formation, Smaquli, Specimen from (Pá) Parvularugoglobigirina eugubina Zone 

Figs 17-18 Guembelitria cretacea Cushman, Early Paleocene, Kolosh Formation, 

Smaquli, Specimen from (Pá) Parvularugoglobigirina eugubina Zone

PLATE -27 


Figs 1-5 Globanomalina archaeocompressa (Blow), 1, 3: spiral view.2, 4: umbilical 

view. 5: side view, Early Paleocene, Kolosh Formation, Dokan, Specimen from 


Figs 6-11 Globoconusa daubjergensis (Bronnimann), 6, 9: umbilical view. 7, 10 and 11: 

spiral view. 8: side view, Early Paleocene Kolosh Formation, Smaquli, Specimen from, 


Figs 12-13 Hedbergella monmouthensis (Olsson), 12: spiral view. 13: umbilical view, 

Early Paleocene Kolosh Formation, Smaquli, Specimen from, 


Fig 14 Rectoguembelina cretacea Cushman, Early Paleocene, Kolosh Formation, Dokan, 

Specimen from(P1a) Parvularugoglobigirina eugubina- Subbotina triloculinoides Zone 

Fig 15 Ellipsonodosaria plumerae (Cushman). Early Paleocene, Kolosh Formation, Dokan, 

Specimen from(P1a) Parvularugoglobigirina eugubina- Subbotina triloculinoides 

Zone 

Fig 16 Neoflabellina delicatissima (Plummer), Early Paleocene, Kolosh Formation, Dokan, 

Specimen from (P1a) Parvularugoglobigirina eugubina- Subbotina triloculinoides 

Zone 

Fig 17 spiroplectamina dentata (Alth), Early Paleocene, Kolosh Formation, Dokan, 

Specimen from (P1a) Parvularugoglobigirina eugubina- Subbotina triloculinoides Zone 

Fig 18 Pseudonodosaria appressa Loeblich & Tappan, Early Paleocene, Kolosh Formation, 

Dokan, Specimen from (P1a) Parvularugoglobigirina eugubina- Subbotina 

triloculinoides Zone 

Fig 19 Bolivinoides delicates Cushman, Early Paleocene, Kolosh Formation, Dokan, 

Specimen from (P1a) Parvularugoglobigirina eugubina- Subbotina triloculinoides Zone 

Fig 20 Bolivinoides sp. Early Paleocene, Kolosh Formation, Dokan, Specimen from 


Fig 21 pseudonodosaria sp. Early Paleocene, Kolosh Formation, Dokan, Specimen from 

(P1a) Parvularugoglobigirina eugubina- Subbotina triloculinoides Zone

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ϦϴΑϞλΎϔϟΪΤϠϟΔϤϳΪϘϟΔΌϴΒϟϭΔϴΗΎϴΤϟΔϴϗΎΒτϟ 

ϥΎΘγΩέϮ̯ˬΔϴϧΎϤϴϠδϟΔϘτϨϣˬ̶ΛϼΜϟ̶γΎΘϳή̰ϟ 

ϕήόϟϕήηϝΎϤη 

 

 

ΔϟΎγέ 

ΔϴϧΎϤϴϠδϟΔόϣΎΟϡϮϠόϟΔϴϠ̯ΓΩΎϤϋ̶ϟΔϣΪϘϣ 

ΔϔδϠϓϩέϮΘ̯ΩΔΟέΩϞϴϧΕΎΒϠτΘϣϦϣ˯ΰΠ̯ 

̶ϓ 

νέϻϢϠϋ 

 

 

ϞΒϗϦϣ 

 

̵ήϳ̫ΎΑέΎηϞϴϋΎϤγΩϮϤΤϣΪϟΎΧ 

˺̂́˼ϞλϮϣΔόϣΎΟνέϻϢϠϋ̶ϓήϴΘδΟΎϣ 

 

 

ϑήηΖΤΗ 

 

έϮϔϏΩϮϤΤϣΩΎϤϋΩ̶ϤϴόϨϟΪϤΤϣΪϤΣϥΎτΤϗΩ 

ΪϋΎδϣΫΎΘγΪϋΎδϣΫΎΘγ 

 

 

 

˻˹˹̶́ϧΎΜϟϥϮϧΎ̯˺˽˻́ΔΠΤϟϭ 

 

Ϋ

κϠΨΘδϤϟ 

 

ϕΎѧτϧ̶ѧϓϊѧϘΗΔѧγέΪϟϖσΎѧϨϣ̶ѧϓΔϔθѧ̰ϨϤϟϭ̶ѧΛϼΜϟϭ̵ήϴѧηΎΒτϟ̵ήμѧϋϦϴѧΑαΎѧϤΘϟΕΪѧΣϭϥ 

ϥϻϮ̩ΔόϠϗϖσΎϨϣϒΣΰϟϕΎτϧ̶ϓΎϴΰΟϭΐ̯ήΘϟϕΎτϧϭ̶ϟϮϗΎϤδϟϭϥΎ̯ϭΩ̶ΘϘτϨϣΔϴϟΎόϟΕΎϴτϟ 

̵ίϮѧϣϭΐѧϳήϗϖϴѧοςѧΨ̯ϕήѧηΏϮѧϨΟΏήѧϏϝΎϤѧηϩΎѧΠΗΎΑΪѧΘϤΗ̶Θϟϭˬϥϭήϴγ̵ΩϭϭΔΠϧίήΑϭ 

FlyschζϴѧϠϔϟωϮѧϧϦѧϣΕΎѧόΑΎΘΗϦѧϣ̶δѧϴέϞ̰θѧΑϒϟΎѧΘΗΕΪΣϮϟϩάϫϥϭΔϴϧήϳϻΔϴϗήόϟΩϭΪΤϠϟ 

ϭΔ̰ϟϮϗϭ̶Ϡ̳ϊσΎϘϣ̶ϓεϮϟϮ̯ϭϭήΠϧΎΗ̶ϨϳϮ̰ΘϟΔϴΗΎΘϔϟέϮΨμϟϦϣΔ̰ϴϤγΕΎϘΒσϦϣϥϮ̰ΘϤϟϭ 

ΔϠδѧϠγϭϭήΠϧΎѧΗϦϳϮѧ̰ΘϟΓΪѧΎόϟFlysch- MolasseαϻϮѧϤϟ̶ѧϟζϴѧϠϓωϮѧϧϦѧϣϥϮ̰ΘΗϭϥϭήϴγ 

ύϼ 

θϗϭϮΗΎ̶̯ότϘϣ̶ϓβϳϮδϟΔϋϮϤΠϣ˯ήϤΤϟΕΎϘΒτϟ 

ϭˬΔϳέΎΨμѧϟΔѧϴϗΎΒτϟϞΜϣϦϳϭΎ̰ΘϟϩΪϬϟΔϨϴόϤϟήϴϏΕΎϤδϟϞ̯ϞϴϠΤΗ̶ϠϋΔγέΪϟϩάϫΕΰ̯ήΗϭ 

̵ήμѧϋϦϳϭΎѧ̰ΗϦϴѧΑαΎѧϤΘϟΔѧόϴΒσϭˬΔѧϤϳΪϘϟΔѧΌϴΒϟϭΔϤϳΪϘϟΔϴΒϴγήΘϟΔΌϴΒϟ˯ΎϨΑϭΔϴΗΎϴΤϟΔϴϗΎΒτϟ 

˯ήѧѧѧΟϭˬΕΪѧѧѧΣϮϟήѧѧѧϤϋΪѧѧѧϳΪΤΗϭˬ̶ΗΎѧѧѧϴΤϟϭ̵έΎΨμѧѧѧϟ̵ϮѧѧѧΘΤϤϟΚѧѧѧϴΣϦѧѧѧϣ̶ѧѧѧΛϼΜϟϭ̵ήϴѧѧѧηΎΒτϟ 

ϭΙϮѧΤΒϟϝϼѧΧϦѧϣΡήτΗΖϟίΎϣ̶ΘϟϭΔΣϭήτϤϟΔϠΌγϻϦϣήϴΜ̶̯ϠϋΔΑΎΟϼϟΔϴϤϴϠϗϻΕΎϫΎπϤϟ 

ϪΟέΎΧϭϕήόϟϞΧΩϦϣϦϴΜΣΎΑϞΒϗϦϣϦϴϨδϟΕήθϋάϨϣΓΪϳΪόϟΕΎγέΪϟ 

̶ѧѧϠϋϻ̵ήϴѧѧηΎΒτϟΕΎѧѧόΑΎΘΘϟ̵ϮѧѧϠόϟϒθѧѧ̰ϨϤϟ˯ΰѧѧΠϟ̶ѧѧϠϋΔϴϠϴμѧѧϔΗΔѧѧϴϗΎΒσΔϳέΎΨѧѧλΔѧѧγέΩΖѧѧϳήΟ 

ΎπϳΖϠϤηϭˬϥϭήϴγ̵ΩϭϭϮΗΎ̯ϭύϼθϗϭΔ̰ϟϮϗϊσΎϘϣ̶ϓϭήΠϧΎΗϦϳϮ̰ΗϦϣ̵ϮϠόϟ˯ΰΠϟ 

ΕΪѧΣϮϟΖϨϤπѧΗΎѧϤϨϴΑˬ̶ѧΛϼΜϟήѧϤόϟΕΫ˯ήѧϤΤϟΕΎѧϘΒτϟΔϠδϠγϭεϮϟϮ̯ϦϳϮ̰ΗϦϣ̶Ϡϔδϟ˯ΰΠϟ 

ΔѧϴϟΎϘΘϧϻΕΪѧΣϮϟϭζϧήѧηϦϳϮѧ̰Θϟ̵ϮϠόϟ˯ΰΠϟ̶ϟϮϗΎϤδϟΔϘτϨϣ̶Ϡ̳ϊτϘϣ̶ϓΔγϭέΪϤϟΔϴϗΎΒτϟ 

ΔѧγέΩ̶ѧϟϦϳϭΎѧ̰Θϟ ϩάѧϫΖόπѧΧΚѧϴΣˬεϮѧϟϮ̯ϭϭήΠϧΎѧΗ̶ϨϳϮѧ̰ΗϭϭήΠϧΎѧΗϭζϧήѧη̶ϨϳϮ̰ΗϦϴΑ 

ΔγϭέΪϤϟϊσΎϘϤϟ̶ϓϑΩΎϬϟϭϝϮϘόϤϟ̵ϮϧΎΜϟϢϴδϘΘϟϩΎΠΗΎΑΔϔϠΘΨϣϊϗϮϤϟΔϠϣΎηΔϴϠϘΣ 

ϦϳϮѧ̰ΗϦѧϣ̵ϮѧϠόϟ˯ΰѧΠϟϦѧϣΔϴϓΎτϟήϴϔϨϣέϮϔϟΕΎόϤΠΗΰϴϤΗαΎγ̶ϠϋΔϴΗΎϴΣΔϘτϧΔϴϧΎϤΛΖϠΠγ 

ΔѧϘτϨϣ̶ѧϠ̳ϊѧτϘϣ̶ѧϓϭήΠϧΎѧΗϦϳϮѧ̰ΗϭϭήΠϧΎѧΗϭζϧήѧη̶ϨϳϮѧ̰ΗϦϴѧΑΔѧϴϟΎϘΘϧϻΕΪѧΣϮϟϭζϧήη 

ΔѧϘτϧΔѧόΑέΰѧϴϤΗϢѧΗϚϟάѧ̯ϭΔѧγϭέΪϤϟϊσΎѧϘϤϟΔϓΎ̶̯ϓϭήΠϧΎΗϦϳϮ̰ΗϦϣ̵ϮϠόϟ˯ΰΠϟϭ̶ϟϮϗΎϤδϟ 

̶ϟϮϗΎϤδϟϭϥΎ̯ϭΩϭˬϥϭήϴγϖσΎϨϣ̶ϓϞϔγϻϦϴγϮϴϟΎΒϟεϮϟϮ̯ϦϳϮ̰Θϟ̶Ϡϔδϟ˯ΰΠϟϦϣΔϴΗΎϴΣ 

ΕΫΎѧϬϟΔΌϓΎ̰ϤϟΔϘτϧϻϊϣΔγέΪϟϩάϫ̶ϓΕΰϴϣ̶ΘϟΔϴΗΎϴΤϟΔϘτϧϻϦϴΑΔϧέΎϘϣΓΎϫΎπϣΖϳήΟ 

ϕήόϟΝέΎΧϭϞΧΩ̶ϓ̶ΛϼΜϟϭ̵ήϴηΎΒτϟϦϴΑαΎϤΘϟΩϭΪΣϝϮΣϊΎθϟϝΎϤόΘγϻ

̶ѧϟήѧϤΣϻϥϮѧϠϟΕΫ̶ѧϠϋϻ̵ήϴѧηΎΒτϟΕΎѧόΑΎΘΗ̶ѧϠϋΔϴϓΎτϟήϴϔϨϣέϮϔϠϟΔϴΗΎϴΤϟΔϴϗΎΒτϟΔγέΪϟϥ 

ΓΪѧϳΪΟΔѧγϮϤϠϣΔѧϴϗΎΒσΓΪѧΣϭΖѧΣήΘϗ̶ϟϮϗΎϤδѧϟΔѧϘτϨϣΩήѧ̳ϭϞΒΟβσΎϏϊτϘϣ̶ϓΐΣΎθϟ̶ϮϬϘϟ 

ϦϳϭΎѧѧ̰ΘϟϊѧѧϣΓΪѧѧΣϮϟϩάѧѧϬϟΔϴϠϴμѧѧϔΘϟΔѧѧϴϗΎΒτϟΕΎѧϗϼόϟϭΔѧѧϴϠϘΤϟΕΎѧѧψΣϼϤϟΐѧѧΟϮϤΑΔѧѧϘτϨϤϟϩάѧѧϫ̶ѧϓ 

ΔΘѧγΰѧϴϤΗϢΗϭˬϭήΠϧΎΗϦϳϮ̰ΗϭζϧήηϦϳϮ̰ΗϦϴΑ̶ϟΎϘΘϧ̶ϨΤγήϴϐΗΓΪΣϮϟϩάϫϞΜϤΗΚϴΣΓέϭΎΠϤϟ 

ΔϳήΨμϟΓΪΣϮϟϩάϫϞΧΩΔϴϓΎτϟήϴϔϨϣέϮϔϟϦϣΔϴΗΎϴΣΔϘτϧ 

ΔѧϘτϨϣ̶ϓ̶ΛϼΜϟϭ̵ήϴηΎΒτϟ̵ήμϋϦϴΑαΎϤΘϟϦϳϭΎ̰ΗΕΎόΑΎΘΘϟΔϤϳΪϘϟΔϴΒϴγήΘϟΔΌϴΒϟΪϳΪΤΗϢΗ 

̶ѧϟήΧΎѧΘϤϟϥΎϴΘΨϳήΘѧγΎϤϟΓήѧΘϔϟΔѧϴϋΎϘϟϭΔѧϴϓΎτϟήϴϔϨϣέϮѧϔϟϡΪΨΘѧγΎΑϕήόϟϕήηϝΎϤηΔϴϧΎϤϴϠδϟ 

ϭϭήΠϧΎѧΗ̶ϨϳϮѧ̰ΘΑΎϳέΎΨѧλΔѧϠΜϤΘϤϟLate Maastrichtian-Early Danianή̰ΒϤϟϥΎϴϧΪϟΓήΘϓ 

ΔγέΪϟΔϘτϨϣ̶ϓ˯ήϤΤϟΕΎϘΒτϟΔϠδϠγϭϭήΠϧΎΗϦϳϮ̰ΗϭΎϴϤϴϠϗεϮϟϮ̯ 

ϭΔѧϴϓΎτϟήϴϔϨϣέϮѧϔϟϊѧϳίϮΗρΎѧϤϧϝϼѧΧϦѧϣΔѧϤϳΪϘϟϕΎѧϤϋϻϭΔѧΌϴΒϟΪѧϳΪΤΗϞѧϣϮϋΔѧγέΩΖѧϤΗ 

̶ΎμѧΣϻϭ̵έΎθѧΘϧϻϞѧϴϠΤΘϟϭήϴϔϨϣέϮѧϔϟωϮѧϧϻ̶ѧϠ̰ϟΩΪѧόϟϞѧϣϮόϟϩάѧϫΖϨϤπѧΗΚѧϴΣˬΔѧϴϋΎϘϟ 

έΪѧΠϟΕΫήϴϔϨϣέϮѧϔϟΔΒδѧϧϭˬΔѧϴϋΎϘϟ̶ѧϟΔѧϴϓΎτϟήϴϔϨϣέϮѧϔϟΔΒδѧϧϭΔѧϴϋΎϘϟϭΔѧϴϓΎτϟήϴϔϨϣέϮϔϠϟ 

̶ΎϘΘϧϻέΪΠϟΕΫ̶ϟ̶δϠ̰ϟ 

ΐϴѧѧγήΘϟΩϮѧΟϭΔѧѧγέΪϟΔѧϘτϨϣ̶ѧϓΔϓϮѧѧλϮϤϟΔѧϴϓΎτϟήϴϔϨϣέϮѧϔϠϟΔѧѧϴΗΎϴΤϟΔѧϘτϧϻΖδѧ̰ϋϭ 

ϥΎϓϚϟΫ̶ϟΔϓΎοϻΎΑˬωΎτϘϧϻϞϻΩΩϮΟϭϥϭΪΑϭ̶ΛϼΜϟϭ̵ήϴηΎΒτϟϦϴΑαΎϤΘϟΪΣ̶ϠϋήϤΘδϤϟ 

̶ΠϳέΪѧΗΐϴѧγήΗΩϮѧΟϭ̶ѧϠϋΖѧϟΩDanianϥΎѧϴϧΩήѧϤϋΕΫΔѧϴϓΎτϟήϴϔϨϣέϮѧϔϟϦѧϣωϮѧϧΰѧϴϤΗ 

̶ϟϮ ϗΎϤδϟϭϥΎ̯ϭΩϭϥϭήϴγϖσΎϨϣ̶ϓήϤΘδϣ 

ΓΩΎѧѧΘόϤϟΔѧѧϘϳήτϟΖϣΪΨΘѧѧγϭˬΔϓϮѧѧλϮϤϟΔѧѧϴΗΎϴΤϟΔѧѧϘτϧϻΔѧѧϓΎ̰ϟΐϴѧѧγήΘϟϝΪѧѧόϣΩΎѧѧΠϳϢѧѧΗϭ 

Graphic‏‏ΪѧѧόϣςѧѧγϮΘϣϡΪΨΘѧѧγΎΑϚѧѧϟΫϭΔѧѧγέΪϟϩάѧѧϫ̶ѧѧϓ‏‎ΔѧѧϴΗΎϴΤϟΔѧѧϘτϧϻϭΐϴѧѧγήΘϟ method 

ΪΣϝϮΣεϮϟϮ̯ϦϳϮ̰ΗϦϣ̶Ϡϔδϟ˯ΰΠϟϭϭήΠϧΎΗϦϳϮ̰ΗϦϣ̵ϮϠόϟ˯ΰΠϠϟΔϴϗΎΒτϟΕΎόΑΎΘΘϠϟΔϓϮλϮϤϟ 

ΪѧΤϟϝϮѧσ̶ѧϠϋΐϴѧγήΘϟ̶ѧϓΓΩΎѧϳΰϟϭήϤΘδϤϟΐϴγήΘϟΖδ̰ϋ̶Θϟϭ̶ΛϼΜϟϭ̵ήϴηΎΒτϟϦϴΑαΎϤΘϟ 

ΐϴγήΘϟ̶ϓωΎτϘϧ̵ΩϮΟϭϥϭΪΑϭ̶ΛϼΜϟϭ̵ήϴηΎΒτϟ̵ήμϋϦϴΑϞλΎϔϟ

biostratigraphy and paleoecology of cretaceous/tertiary boundary in ...

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