stratigraphy and paleontology of some miocene sediments in ...

Zagazig UniversityFaculty of scinsceDepartment of Geology

STRATIGRAPHY AND PALEONTOLOGY OF SOME MIOCENE SEDIMENTS IN THE

CAIRO-SUEZ DISTRICT, EGYPT.

A Thesis

By

Ahmed Eid Mowafi

( B.Sc. In Geology, 1986 )

Submitted In Partial Fulfillment of the Requirements for the Degree of Master of Science in Geology

( 2006 )

Zagazig UniversityFaculty of scinsceDepartment of Geology

Title:

Author's name: Ahmed Eid Mowafi

Supervisors:1- Prof. Dr. Ezzat Abd-Elshafy

2- Prof. Dr. Abdelbaset El-Sorogy

3- Dr. Mohammed Abd-Elmoneim

STRATIGRAPHY AND PALEONTOLOGY OF SOME MIOCENE SEDIMENTS IN THE CAIRO-SUEZ

DISTRICT, EGYPT.

The present thesis is submitted to Faculty of Science , Zagazig University in partial fulfillment of the requirements for the degree of Master of Scienece in Geology (Stratigraphy and paleontology).

Besides the research work carriedout in this thesis, the author attended 10 postgraduate courses for one academic year in thefollowing subjects:1- Field geology (Stratigraphy and Paleontology)2- Advanced stratigraphy3- Microfossils4- Stratigraphical paleontology5- Foraminifera and methods of correlation6- Geotectonic7- Geology of Egypt and the neighboring areas8- Macrofossils9- Paleoecology10- Palynology and Facies

He has passed successfully the final examination in these courses, besides German language courses, held in November, 1995.

NOTE

Prof. Dr. Ezzat Abd-Elshafi

Head of Geology Department

- I -

Faculty of ScienceZagazig University

In the first place, parise to ALLAH, by whose gase this work has been completed.

I would like to convey my sincere thanks and extreme appreciationto Prof. Dr. E. Abd-Elshafi, Head of Geology Department, Faculty of Science, Zagazig university, Prof. Dr. A. El-Sorogy, Zagazig University, and Dr. M. Abd-Elmoneim, Zagazig University for their supervision, guidance of my research and advises throughout the course of the study.

The author is grateful to Prof. Dr. A. Ziko and Prof. Dr. M.H. Metwally, Zagazig University, Faculty of Science for their great support.

I wish to express my deep gratitude and appreciation to all scientific and technical personnel and workers of the Geology Department, Faculty of Science, Zagazig University for their cooperation.

I would like to express my deep thanks for my family (father, mother, brothers, my wife and my daughter Salwa) for their encouragement and help.

- II -ACKNOLWEDGEMENTS

Ahmed Eid Mowafi

The transgressive-regressive Miocene succession exposed at Gabal Geneifa, Gabal Gharra and Gabal Homeira in the Cairo-Suez District is unconformably underlain and overlain by continental sediments of Oligocene and Post Miocene ( ? ) respectively. It could be differentiated into two rock units, Gharra Formation at the base and Genefe Formation at the top.

Sixty two macrofossil species (40 bivalves, 16 gastropods and 6 echinoids) have been described, identified and photographed. They belong to 34 genera and 26 families. Their paleogeographic and biogeographic distribution of the majority indicated Atlantic-Mediterranean affinity with the Indo-Pacific one in few. The study of 49 thin sections leads to identification of ten microfacies types for limestones and five types for sandstone and shale.

The studied Miocene sequence in the study areas was divided into two sedimentary facies: the lower one is a clastic-dominated facies which represents the Gharra Formation of Burdigalian age, while the upper one is a carbonate-dominated facies which represents the Genefe Formation of Langhian - Serravallian age.

Based on the abundance of the macro-invertebrate fauna especiallybivalves, gastropods and echinoids with some foraminifera, six biozones have been recorded, they are from younger to older : Chlamys(Argopecten) submalvinae zone, Chlamys (Macrochlamis) sardoa zone, Pecten (Pecten) cristato-costatus zone, Pecten (Flabellipecten) flabelliformis zone, Pecten (Pecten) ziziniae zone and Chlamys gentoni zone.

Based on t he microfacies associations, sedimentary structures and fossil content; the studied Miocene succession was deposited in an environment ranged from tidal flat, typical reef flank to shelf lagoon with open circulation.

- III -ABSTRACT

NOTE ………………………… IACKNOLWEDGEMENTS ………………………… IIABSTRACT ………………………… IIICONTENTS ………………………… IVLIST OF FIGURES ………………………… VIIILIST OF TABLES ………………………… IX

Chapter I: Introduction ………………………… 1I.1 Aim of study ………………………… 1I.2 Previous work ………………………… 1

Chapter II: Lithologies of the studied sections 14II.1 Introduction ………………………… 14II.2 Studied sections ………………………… 14

II.2.1 Gabal Geneifa section ………………………… 14II.2.2 Gabal Gharra section ………………………… 24II.2.3 Gabal Homeira section ………………………… 36

Chapter III: Stratigraphy ………………………… 48III.1 Lithostratigraphy ………………………… 48

III.1.1 Introduction ………………………… 48III.1.2 Studied sections ………………………… 49

III.1.2.1 Gharra Formation …………………….. 49III.1.2.2 Genefe Formation …………………….. 53

III.2 Biostratigraphy ………………………… 57III.3 Chronostratigraphy ………………………… 69

Chapter IV: Systematic Paleontology ………………… 74IV.1 Introduction ………………… 74IV.2 Systematic description ………………… 74

IV.2.1 Phylum Mollusca ………………… 74 - Class Bivalvia ………………… 74

- Family Arcidae ………………… 74 - Genus Arca ………………… 74

- IV - CONTENTS

- Family Isognomonidae ………………… 75 - Genus Isognomon ………………… 75

- Family Pectinidae ………………… 76 - Genus Chlamys ………………… 76 - Genus Pecten ………………… 89

- Family Anomiidae ………………… 105 - Genus Anomia ………………… 105

- Family Ostreidae ………………… 107 - Genus Crassostrea ………………… 107 - Genus Alectryonella ………………… 108

- Family Lucinidae ………………… 111 - Genus Lucina ………………… 111 - Genus Linga ………………… 112

- Family Ungulinidae ………………… 113 - Genus Diplodonta ………………… 113

- Family Cardiidae ………………… 113 - Genus Cardium ………………… 113 - Genus Acanthocardia ………………… 114

- Family Mactridae ………………… 115 - Genus Lutraria ………………… 115

- Family Tellinidae ………………… 116 - Genus Gastrana ………………… 116

- Family Psammobiidae ………………… 117 - Genus Gari ………………… 117

- Family Solecurtidae ………………… 118 - Genus Azorinus ………………… 118

- Family Veneridae ………………… 118 - Genus Paphia ………………… 118 - Genus Clementia ………………… 120 - Genus Callista ………………… 120

- Family Clavagellidae ………………… 121 - Genus Clavagella ………………… 121

- Class Gastropoda ………………… 122 - Family Ampullariidae ………………… 122

- Genus Lanistes ………………… 122

- V -

- Family Turritellidae ………………… 123 - Genus Turritella ………………… 123

- Family Cypreadae ………………… 125 - Genus Luria ………………… 125

- Family Naticidae ………………… 126 - Genus Ampullina ………………… 126 - Genus Natica ………………… 127

- Family Bursidae ………………… 129 - Genus Bursa ………………… 129

- Family Ficidae ………………… 129 - Genus Ficus ………………… 129

- Family Olividae ………………… 131 - Genus Oliva ………………… 131

- Family Conidae ………………… 131 - Genus Conus ………………… 132

- Family Planorbidae ………………… 134 - Genus Planorbis ………………… 134

IV.2.2 Phylum Echinodermata ………………… 135 - Class Echinoidea ………………… 135

- Family Clypeasteridae ………………… 135 - Genus Clypeaster ………………… 135

- Family Scutellidae ………………… 137 - Genus Scutella ………………… 137 - Genus Parascutella ………………… 138

- Family Echinolampadidae ………………… 139 - Genus Echinolampas ………………… 139

Chapter V: Microfacies and Depositional Environments 144V.1 Microfacies ……………………………. 144

V.1.1 Limestone group ……………………………. 144V.1.1.1 Wackestone ……………………………. 145

V.1.1.1.1 Sandy dolomitic wackestone ……. 145V.1.1.1.2 Algal wackestone ……………. 147

V.1.1.2 packstone ……………. 149V.1.1.2.1 Sandy bioclasts packstone ……. 149

- VI -

V.1.1.2.2 Sandy foraminiferal bryozoan packstone 151V.1.1.2.3 Sandy echinoidal packstone ……. 154

V.1.1.3 Grainstone ……………. 156V.1.1.3.1 Sandy fossiliferous grainstone ……. 156V.1.1.3.2 Sandy echinoidal foraminiferal grainstone 159V.1.1.3.3 Sandy algal grainstone ………… 161V.1.1.3.4 Sandy molluscan grainstone ……. 163

V.1.1.4 Framestone ………… 165V.1.1.4.1 Coralline framestone ………… 165

V.1.2 Clastic group ………… 168V.1.2.1 Calcareous quartz arenite ………… 168V.1.2.2 Dolomitic calcareous quartz arenite ……. 169V.1.2.3 Calcareous fossiliferous quartz arenite 170V.1.2.4 Calcareous ferrugineous quartz arenite 171V.1.2.5 Sandy-silty shale ……………………. 173

V.2 Depositional environments ……………………. 174V.2.1 Clastic-dominated facies ……………………. 175V.2.2 Carbonate-dominated facies …………………. 176

Chapter VI: Summary and Conclusions ………… 177VI.1 Stratigraphy ………… 177VI.2 Systematic paleontology and biohorizones ………… 178VI.3 Microfacies and depositional environment ………… 179

References ………………………………………… 182PlatesArabic Summary

- VII -

Fig. 1: Location map of the studied sections. 3Fig. 2: Panoramic view of Gabal Geneifa. 15Fig. 3: The succession of shale, gravelly sandstone and

calcareous sandstone of the lowermost part of Gharra Formation, Gabal Geneifa section. 16

Fig. 4: The macrofauna (oysters) embedded in the limestone, middle part of Gharra Formation, Gabal Geneifa section. 17

Fig. 5: General view of the fossiliferous sandy limestone, middle part of Gharra Formation, Gabal Geneifa section. 18

Fig. 6: The highly fossiliferous sandy limestone, lower part of Genefe Formation, Gabal Geneifa section. 19

Fig. 7: Succession of silty calcareous claystone, fossiliferous sandy marl and fossiliferous limestone; middle part of Genefe Formation; Gabal Geneifa section. 21

Fig. 8: The argillaceous limestone of the upper part of Genefe Formation, Gabal Geneifa section. It represents the uppermost part of the Miocene succession in Geneifa area. 22

Fig. 9: Lithostratigraphic succession of the Miocene rocks at Gabal Geneifa section. 23

Fig. 10: Panoramic view of Gabal Gharra. 24Fig. 11: The Oligocene conglomerate band under the Miocene

succession in a mine at the root of Gabal Gharra. 25Fig. 12: The ferruginous sandstone in the lower part of Gharra

Formation, Gabal Gharra section. 26Fig. 13: Broken parts of Scutella ammonis on the surface of

limestone in the middle part of Gharra Formation, Gabal Gharra section. 27

Fig. 14: Band of large-sized pectinides in the limestone of the middle part of Gharra Formation, Gabal Gharra section. 28

Fig. 15: The upper part of Gharra Formation underlying the lower part of Genefe Formation, Gabal Gharra section. 30

Fig. 16: The lower part of Genefe Formation, Gabal Gharra section, (A Bed crowded with fauna specially oysters and pectinids) 31

LIST OF FIGURES- VIII -

Fig. 17: Part of the coral reef band in the lower part of Genefe Formation, Gabal Gharra section. 31

Fig. 18: Oysters and pectinids are embedded in the limestone of the middle part of Genefe Formation. 32

Fig. 19: The chalky limestone of the upper part of Genefe Formation, Gabal Gharra section. 33

Fig. 20: The uppermost part of Genefe Formation which is the uppermost part of the Miocene succession in Gabal Gharra section. 34

Fig. 21: General view of the Genefe Formation, Gabal Gharra section. 34

Fig. 22: Lithostratigraphic succession of the Miocene rocks at Gabal Gharra. 35

Fig. 23: Panoramic view for Gabal Homeira. 36Fig. 24: Clastics of the lowermost part of Gabal Gharra

Formation, Gabal Homeira section. 37Fig. 25: The sandy marl in the lower part of Gharra Formation,

Gabal Homeira section. 38Fig. 26: Pectinids and oysters are embedded in the limestone of

the middle part of Gharra Formation, Gabal Homeira Section. 39

Fig. 27: Limestone of the upper part of the Gharra Formation underlained with clay, Gabal Homeira section. 41

Fig. 28: Oysters are embedded in the limestone of the lowermost part of the Genefe Formation, Gabal Homeira section. 42

Fig. 29: A general view for the marl oyster bank of the middle part of Genefe Formation, Gabal Homeira section. 43

Fig. 30: A close view for the marl oyster bank of the middle part of Genefe Formation, Gabal Homeira section. 45

Fig. 31: The fossiliferous limestone of the uppermost part of the Genefe Formation, Gabal Homeira section which represent the uppermost part of the Homeira Miocene succession. 45

Fig. 32: Lithostratigraphic succession of the Miocene rocks at Gabal Homeira. 46

Fig. 33: Lithostratigraphic correlation chart for the three studied

- IX -

sections at Gabal Geneifa, Gabal Gharra and Gabal Homeira. 47

Fig. 34: Biostratigraphic chart of Gabal Geneifa section 66Fig. 35: Biostratigraphic chart of Gabal Gharra section 67Fig. 36: Biostratigraphic chart of Gabal Homeira section 68Figs. 37a, b: Sandy dolomitic wackestone. 146Figs. 38a, b, c: Algal wackestone. 147-148Figs. 39a, b, c: Sandy bioclasts packstone. 150-151Figs. 40a, b, c, d: Sandy foraminiferal bryozoan packstone. 152-154Figs. 41a, b: Sandy echinoidal packstone. 155Figs. 42a, b, c, d: Sandy fossiliferous grainstone. 157-158Figs. 43a, b: Sandy echinoidal foraminiferal grainstone. 160Figs. 44a, b, c, d: Sandy algal grainstone. 161-163Figs. 45a, b: Sandy molluscan grainstone. 164Figs. 46a, b, c, d: Coralline framestone. 166-167Figs. 47a, b: Calcareous quartz arenite 168-169Fig. 48: Dolomitic calcareous quartz arenite 170Fig. 49: Calcareous fossiliferous quartz arenite. 171Fig. 50a, b: Calcareous ferruginous quartz arenite. 172Fig. 51a, b: Sandy-silty ferruginous shale. 173-174

- X -

Table 1: Different rock units proposed by different authors for the Miocene rocks in the Cairo-Suez District. 13

Table 2: The ages assigned by previous authors to the recrded fauna in some parts of the world. 143

LIST OF TABLES - XI -

1 Chapter I Introduction

CHAPTER I

INTRODUCTION

I.1 Aim of study:

The main objectives of the present work is planned to study the

stratigraphy of the Miocene sediments exposed at the main exposures

lying in the eastren part of Cairo-Suez district to correlate them and

configurate the main lithologic, biostratigraphic and paleoenvironmental

characteristics of the Miocene sequence in this area since the previous

studies had dealt with separate exposures. This study includes the

lithologies, rock units, macrofauna, biostratigraphy, microfacies and

environmental analysis. The material of the study have been collected

from Geneifa, Gharra and Homeira sections (Fig. 1). The studied sections

were carefully examined, sampled and described from the lithologic and

macrofaunistic point of view.

I.2 Previous work:

The Cairo–Suez area lies East of Cairo and extends about 120 km to

the city of Suez. It lies between Latitudes 29 55´ - 30 20´ N and 31 15´

- 32 35´ E (fig. 1). The topography of the area is largely controlled by its

structure and the relief is generally low except for few hills and small

mountains. Topographically, the area is subdivided into three ridges

crossing the district in a more or less E–W alignment; between these

ridges there are two depressions. The Cairo–Suez asphaltic road passes

through the southern one. Gabal Ataqa, Gabal Abou Treifiya, Gabal

Qattamiya, Gabal Anqabiaya, Gabal Nasuri and Gabal Mokattam form an

elongated ridge running parallel to Cairo–Suez high way depression from


East to West and to the South of it (Abou Khadrah et al. 1993). The oldest

exposed rocks in the area are of Early Cretaceous age while the youngest

rocks are of Quaternary age of synrift sedimentary sequence (Bruce and

Hotzl, 1988). The Miocene rocks of the Cairo–Suez area were the subject

of many studies since the last quarter of the 19th century. The majority of

these studies dealt with parts of the district (Table 1).

Fuchs (1883) studied the faunal assemblages of the Miocene

exposures at Gabal Geneifa and Siwa Oasis and found that both localities

belong to the same "horizon" and assigned them to the lower part of the

Middle Miocene.

Depéret and Fourtau (1900) differentiated the Neogene of Lower

Egypt as well as the Isthmus of Suez into the following stages:

- Burdigalian Stage: Consists of sandstones with distinctly Late

Burdigalian fauna similar to those of Rhone Valley, Corsica and Algeria.

- Vindobonian Stage (Helvetian-Tortonian): Consists of marls and

limestones with pectinids and numerous echinoids and one coral bank.

They attributed the marls to the "Schlier" of Austria and the coral bank to

the Helvetian of Barcelona and Algeria. Contrary to this opinion,

Blanckenhorn (1901) regarded all the Egyptian Miocene occurrences as

Middle Miocene sediments including those studied by Depéret and

Fourtau (1900). But Lower Miocene rocks were recorded at the base of

Gabal Geneifa followed by a Middle Miocene sequence by Barron

(1907a).


THIS PAGE FOR THE LOCATION MAP.


Fourtau (1916 and 1920) referred to the presence of two Neogene

depositional basins during the Miocene: the more littoral "Marmarica

Gulf" comprising the Western Desert; and the "Egyptian Gulf" including

the Cairo–Suez district and the Gulf of Suez to the latitude 27 N. He

correlated the Neogene echinoids of Egypt with those of other localities in

the Western Mediterranean and found that the half of these species are

restricted to Egypt while the others are known in France, Italy, Sardinia,

Malta, Algeria and Corsica. In addition, he recorded four species of Indo-

Pacific affinity from the passage beds between the Burdigalian and

Vindobonian of the "Egyptian Gulf".

Shukri and Akmal (1953) divided the Miocene succession of Gabal

Nasuri-Gabal Anqabia area into a lower marine unit followed by a non-

marine unit. The later replaces the unfossiliferous sands and gravels of

doubtful age of Barron (1907a), while the marine unit consists of highly

fossiliferous sandstones clays and limestones. The same succession was

described by Shukri and Ayouti (1956) at Gabal Iweibid where they

recorded silicified wood of small size with chips of Scutella spp. in the

sands and gravels of the non-marine unit.

Sadek (1959) mentioned that the Miocene rocks outcrop at several

points in the central part of the area between the Suez Canal and Gabal

Ataqa and Geneifa. He assigned the basal beds of Gabal Geneifa to the

Late Burdigalian and the overlying limestone beds with Lithothamnium

and Heterostegina to the Vindobonian, and correlated these beds with the

Heterostegina beds of Malta and the Tortonian Leithakalk of Vienna

Basin. Also, he mentioned that Gabal Geneifa itself is a plateau of Eocene

Limestone rising to 260m above sea level and ending by vertical scarp to


the East, at the foot of which there are ridges of Miocene limestones

which with the exposures of Miocene rocks at Kabrit and Shalluffa, form

an important succession. The strata extend as a band, averaging two

kilometers wide, reaching from Wadi Abu Hassa South of Gabal Geneifa

for about 8 kilometers northwards along the foot of the Geneifa Eocene

scarp. They are mainly composed of light-colored limestones, forming a

line of low scarps averaging 30 to 60m above the plain to the East, which

faulted against the Eocene Limestones which forming the main Geneifa

cliff. Below these light-colored limestones, there are soft marls and shales

which extend to the East for a short distance before they are covered by

the alluvial deposits of the plain.

Said (1962a) followed Shukri and Akmal (1953) and Shukri and

Ayouti (1956) in dividing the Miocene rocks of the Cairo–Suez district

into marine and non-marine units. He divided the former into a more

sandy part followed by another calcareous one, and correlated them with

the Moghra and Marmarica formations in the North Western Desert,

respectively. Also, he correlated the non-marine unit with the evaporites

of the Gulf of Suez region. (Table 1).

Said and Metwalli (1963) identified 65 Miocene foraminiferal

species from Wadi El-Ful, El-Gafra, Dar El-Beida and El-Rebeiki in the

Cairo–Suez district. Metwalli (1963) divided the marine Miocene of the

Cairo–Suez district into two informal units:

- Unit I comprises the lower sandy part with rich assemblage of macro-

and microfauna of Burdigalian age.

- Unit II represents the calcareous part containing a faunal assemblage of

Middle Miocene (Helvetian) age.


The first formal classification of Miocene rocks of Cairo–Sukhna

area was proposed by Ghorab and Marzouk (1965). They subdivided these

rocks into the marine Gharra Formation which represents the marine

Lower Miocene unit, and includes the Sukhna, Reishi, Abbasia, Gafra and

Genefe members; and the Upper Miocene unit, Iweibid Formation, which

represents the non-marine sediments and includes El-Hamza and El-

Bahhara members.

Hamam (1966) divided the Miocene deposits of the Agrud area,

northwest of Suez, into three informal units (Table 1):

- The Burdigalian rock units I & II.

- The Helvetian rock unit III.

This author correlated these units with the other Burdigalian and

Helvetian units in the Cairo–Suez district and North Western Desert, and

concluded that the Miocene transgression was from the East (from the

Gulf of Suez). He recognized the Burdigalian Operculina complanata

zone and the Helvetian Heterostegina costata costata zone and correlated

them with those established in Gabal Gharra by Souaya (1963).

Farag and Sadek (1966) subdivided the Miocene rocks in Gabal

Homeira area into marine and non-marine units. The former includes the

Burdigalian and Helvetian fossiliferous sediments, while the non-marine

unit consists of unfossiliferous fluviatile sediments of Late Miocene age.

They correlated the marine Miocene with the Lower and Middle Series of

Gabal Ataqa, and non-marine sediments with the upper Series South of

Gabal Ataqa as well as the non-marine units of Gabal Iweibid and Gabal

Nasuri – Gabal Anqabia area.


Abdallah and Abd El-Hady (1966) subdivided the Miocene rocks in

the Sadat area into three formal units:

1- The Sadat Formation (Late Burdigalian), represents the Lower

Miocene sediments.

2- The Hommath Formation (Vindobonian), represents the Middle

Miocene, unconformably overlies the Sadat Formation.

3- The Hagul Formation (Late Miocene), unconformably overlies the

Hommath Formation.

They mentioned that the Sadat Formation was deposited under

shallow marine, warm water conditions, while the presence of salt and

gypsum within the Hommath Formation led them to consider more or less

sheltered lagoonal conditions were favourable for depositing this

formation, and they proposed that the Hagul Formation was deposited in a

shallow marine environment.

Barakat and Aboul Ela (1970) analyzed the microfacies of the

Miocene rocks exposed at Gabal Geneifa area and found that the Lower

Miocene (Burdigalian) is represented by shallow marine sediments with

reefal forms (inner neritic to reefal environment) while shallow agitated

marine of reefal environment prevailed during the Middle Miocene

(Vindobonian). They mentioned that the continental conditions prevailed

during the Late Miocene led to the deposition of fluviatile sediments.

Said (1971) used the term Gharra Formation to replace the unit I of

Metwalli (1963). It unconformably overlies the Abu Zabaal basalt and

unconformably underlies solid marine limestone (unit II of Metwally).

The Stratigraphic Sub-Committee (1974) modified the classification

of Abdallah and Abd El-Hady (1966) for the Miocene rocks at the Sadat


area and applied it for the whole Cairo-Sukhna area, where the marine

Miocene was represented by the Lower Miocene Sadat Formation

followed unconformably by the Middle Miocene Hommath and Genefe

formations. On the other hand, the non-marine sediments were represented

by the Upper Miocene Hagul Formation. The Hommath Formation was

subdivided into three informal units which are in ascending order: Reishi,

Abbasia and Gafra members.

In his monograph on the marine gastropods in the Cairo – Suez

district, Abbass (1977) identified 97 new species. He utilized the

following classification for Gharra Formation:

4- Genefe Chalky Limestone Member (Vindobonian).

3- Hommath Sandy Limestone Member (Upper Burdigalian-Karpatian).

2- Sadat Reefal Limestone Member (Burdigalian-Helvetian).

1- Agrud Sandstone Member (Aquitanian-Burdigalian).

El-Heiny (1982) referred the Sadat Formation to the Burdigalian

due to the presence of Miogypsina globulina, M. intermedia and

Heterostegina heterostegina and suggested a Late Burdigalian age to the

lower part of the Hommath-Genefe sequence as it yields Miogypsina

cushmani. On the other hand, he referred the upper part of this sequence

with Neoalveolina melo to the Vindobonian and proposed a Messinian age

to the Hagul Formation.

Abd El-Wahab and El-Belassy (1987) recorded Lower and Middle

Miocene rocks in the area of Gabal El-Hamza–Gabal Um Qamar, Cairo–

Suez district. They suggested a Burdigalian age to the former as it

contains Operculina complanata and correlated it with those of Gabal

Homeira and Gabal Gharra. They referred the Middle Miocene rocks in


these areas to the Vindobonian and correlated them with those of Gabal

Geneifa and Gabal Um Raqm.

Szczechurar and Abd-Elshafy (1988) presented the first study

concerning the Miocene ostracods of the area between Gabal Ataqa and

Northern Galala plateau. Also, they studied the foraminiferal association

for the age assignment and paleoecologic interpretation. The study was

carried out on two sections to the North of Bir Bada both belong to the

Hommath Formation. They referred the formation to the Middle Miocene,

but with histation, and did not accept the Tortonian age proposed by

Youssef et al. (1971) for this formation. Among the foraminiferal

assemblages, they recorded Mississippina neagui Popescu which seems to

be restricted (at least outside Egypt) to the Middle Miocene. They

mentioned that the two sections were laid down in shallow water,

pericostal but normal marine environment.

Said (1990) utilized the Gharra Formation to represent the Lower

Miocene deposits in the Cairo – Suez district. He referred it to the

Aquitanian-Burdigalian age and referred the unconformably overlying

Genefe Formation to the Middle Miocene (Langhian). On the other hand,

this author suggested the Late Pliocene age for the Hagul Formation and

the overlying Hamzi Formation.

Abd-Elshafy and Abd-Elmoneim (1992) differentiated the Miocene

rocks exposed in the area between Gabal Ataqa and Northern Galala

Plateau into four formations; The Sadat, Hommath, Hagul and Ghweibba

formations. They followed the opinion of Abdallah and Abd El-Hady

(1966) for the Sadat and Hommath formations. They restricted the name

Hagul Formation to the lower clastic rocks exposed in its type section


under the uppermost limestone bed, and they introduced Ghweibba

Formation to represent the limestone succession overlying the clastics of

the Hagul Formation. These authors assigned the Sadat Formation to the

Upper Burdigalian–Langhian, the Hommath Formation to the Serravalian

and the Hagul and Ghweibba Formations to the Tortonian.

Abd-Elmoneim (1992) studied the stratigraphy of the Miocene

rocks in the area between Gabal Ataqa and Northern Galala plateau and

followed the classification of Abd-Elshafy and Abd-Elmoneim (1992), he

recorded 93 species and subspecies belonging to the Rhodophycophyta,

Foraminifera, Chilostomata, Bivalvia, Gastropoda and Echinodermata.

Depending on this fossil association, this author presented the first

biostratigraphical study for the Miocene rocks of that area. He recognized

10 biozones, the lower five biozones are recorded in the Sadat Formation,

they run from top to base as follows:

5- Lithothamnium sp acme zone.

4- Pecten (Amussiopecten) burdigalensis – Psammechinus aegyptiacus

assemblage zone.

3- Pecten (Flabellipecten) schweinfurthi range zone.

2- Pecten (Pecten) fraasi range zone.

1- Pecten (Pecten) ziziniae range zone.

The upper five biozones are recorded in the Hommath Formation,

they run from top to base as follows:

5- Turritella (Eichwaldiella) fouadi zone.

4- Chlamys (Argopecten) submalvinae zone.

3- Placuna (Indoplacuna) miocenica zone.

2- Crassostrea crassissima zone.


1- Amphiope arcuata fuchsi zone.

Hamza (1992) introduced a biostratigraphical study of the Neogene

in the eastren part of Egypt and defined four biohorizones. This auther

followed the classification of Abdallah and Abd El-Hady (1966) which

was modified by the Stratigraphic Sub-Committee (1974) for the Miocene

of Cairo-Suhkna District. From top to base these biozones are:

4- Chlamys submalvinae – Pycnodonte virleti biohorizon.

3- Pecten josslingi biohorizon.

2- Flabellipecten burdigalensis – Pecten ziziniae biohorizon.

1- Crassostrea duvergieri – Cubitostrea digitalina biohorizon.

Abou Khadrah et al. (1993) studied the facies development and the

sedimentary structures of synrift sediments in the Cairo–Suez district by

means of six stratigraphic sections (Tower-3, El-Hamza, 10th of Ramadan,

El-Gafra, Homeira and Geneifa). They concluded that the Oligocene and

Miocene sequences comprise the Gabal Ahmar and Qatrani formations

(Oligocene sequences) followed by Sadat and Hagul formations (Miocene

sequences). They defined four distinctive facies recognized as:

4- Non-Marine Miocene facies.

3- Marine Middle Miocene facies.

2- Marine Lower Miocene facies.

1- Sand and gravel facies (Oligocene).

El-Sorogy and Ziko (1999) referred that the marine Miocene

sequence in Wadi Hagul is classified into two rock units, from base to top

as follows:


1-Sadat Formation (Abdallah and Abd El-Hady, 1966): It is of Late

Burdigalian to Early Langhian age, mainly composed of white, pale

yellow, coralline limestone, part siliceous at the base, with few marl

interbeds. The Sadat Formation unconformably overlies the coarse clastics

of the Upper Eocene and represents the oldest Miocene unit in the area.

2-Hommath Formation (Abdallah and Abd El-Hady, 1966): It is of Late

Langhian-Serravalian age, overlies conformably the Sadat Formation, and

is mainly composed of limestone, yellow friable sandstone, yellowish

brown sandy marl, with interbeds of calcareous grits in the lower part.

El Safori and El-Sorogy (1999) identified 26 bryozoan species from

the Miocene of Gabal Gharra. They used Gharra Formation of Ghourab

and Marzouk (1965) and gave it an Early Miocene age.

El Shazly and Saber (1999) studied the facies and

macropaleontology of the Marine Miocene sediments at Gabal Homeira

and divided it into two formations, the lower Gharra Formation represents

the Lower Miocene and the upper Genefe Formation represents the

Middle Miocene.

Elattar (2003) studied the echinoids of the Sadat Formation. This

auther followed the classification of Abdallah and Abd El-Hady (1966)

and assigned the Sadat Formation to Burdigalian – Langhian age.


THIS PAGE FOR THE TABLE OF THE PREVIOUS WORK

Chapter II Lithologies of the studied Miocene sections

14

CHAPTER II

LITHOLOGIES OF THE STUDIED MIOCENE SECTIONS

II.1 INTRODUCTION:

Three stratigraphic sections have been chosen to fullfill the aim of

the present study. These are Gabal Geneifa, Gabal Gharra and Gabal

Homeira sections (Fig. 1). They are measured and sampled carefully and

the collected samples were described in detail in the field and subjected

to different laboratory techniques according to their lithological nature.

Among these, the insoluble residue for the main clastic/non-clastic

nature and microfacies examinations through thin sections for the

lithologic constituents were carried out. The fossil contents were

compiled from collecting the macrofossils and picking of the

microfossils in both field and laboratory.

II.2 STUDIED SECTIONS:

II.2.1 Gabal Geneifa section:

This section is encountered between the Eocene limestone of

Gabal Geneifa to the West and Suez - Port Said asphaltic road to the

East (Fig. 2). It extends between longitudes 32 20 30 and 32 22 30

E, and latitudes 30 12 20 and 30 13 20 N. The base of the

succession is unexposed. The scarp of Geneifa gets gradually lower and

lower southwards, finally going to the earth at a point where a wadi is

draining in the area between Geneifa and Ataqa breaks. To the South of

Geneifa succession, the surface of this un-named wadi is a flat plain,

covered by alluvial gravels which extends to the foot of the high

escarpment of Gabal Ataqa. At the foot of Gabal Ataqa escarpment, the

Miocene rocks are seen occupying small patches exposed in the sides of

some of the deep wadis. The lowermost rock samples of this section are


15

available to be collected from a mine near the asphaltic road, South of

Geneifa town. The succession measures a total thickness of 97.1m and

runs from base to top as follow :

Fig. 2: Panoramic view for Gabal Geneifa from the eastern side.

1- Shale: Gray, brownish gray to yellowish gray; moderately compact;

thinly laminated, jointed, unfossiliferous, ferruginous, gypsiferous, with

gypsum bands and veins (thickness up to 2cm); very slightly calcareous;

dipping to the West (20-30 deg.); silty, its base is unexposed and the

exposed part measures 25m.

2- Conglomeratic sandstone: Yellow to yellowish brown; medium to

coarse quartz grains, occasionally very coarse grained, sometimes fine

grained; subangular to subrounded; poorly sorted; semi-friable to

moderately compact; unfossiliferous. Pebbles and cobbles constitute

about 20-30% of the sample. This bed represents period of unconformity

between the underlying and the overlying beds. Its thickness is 0.5m.

3- Calcareous sandstone: Yellowish brown; fine to medium quartz

grains; subrounded to subangular; moderately sorted; semi-friable to

moderately compact; with few fresh feldspar minerals (plagioclase);

fossiliferous with shell fragments of bivalvia. The calcareous matter is

Part of the Miocene deposits in Geneifa area


16

calcite, represents the cement among the quartz grains. Its thickness is

1.6m.

Fig. 3: Sandstone of the lowermost part of Gharra Formation, Gabal

Geneifa section. The succession of the three beds: upper part of bed no.

1, bed no. 2 and bed no. 3.

4- Calcareous sandstone: Brown to yellowish brown, occasionally

brownish gray; fine to coarse quartz grains; subrounded to subangular;

poorly to ill-sorted; moderately compact to semi-friable; rarely

fossiliferous; ferruginous. The calcareous matter is calcite, represents the

cement among the quartz grains. The macrofauna are represented by

shell fragments of bivalvia. Its thickness is 12m.

5- Fossiliferous sandy limestone: Brownish white to white, occasionally

yellowish white; compact; massive; jointed; slightly argillaceous. Sand

grains are fine to medium quartz grains and angular to subrounded. It is

Bed no. 3

Bed no. 2

Bed no. 1


17

highly fossiliferous yielding many fossil species, including bivalvia as

Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs, Alectryonella

plicatula (Gmelin) subsp virleti Deshayes, Azorinus sp., Isognomon sp.,

Chlamys gentoni Fontannes; gastropod molds; echinoids as

Echinolampas amplus Fuchs, Clypeaster sp., Scutella sp. and others;

numerous Balanus concavus (Bronn.); red algae as Lithothamnium sp.;

Holoporella sp.; corals (small heads, sometimes dissolved and leaving

only their molds). The main foraminiferal species in this bed are

Operculina sp., Amphistegina sp. and Heterostegina sp. Its thickness is

7.5m.

Fig. 4: The macrofauna (oysters ) are embedded in the limestone and not

easy to be collected, middle part of Gharra Formation, Gabal Geneifa

section, bed no. 5.


18

Fig. 5: General view of the fossiliferous sandy limestone, middle part of

Gharra Formation, Gabal Geneifa section, bed no. 5.

6- Fossiliferous limestone: Brownish white to yellowish white; highly

compact; fractured; dolomitic. The limestone is composed of

cryptocrystalline calcite, and the dolomite is composed of micro to fine

euhedral crystals. It yields Holoporella sp.; foraminifers as Operculina

complanata (Defrance), Amphistegina sp., Miogypsinids and other

foraminifers; echinoid fragments (plates and spines); molluscan

fragments. Its thickness is 1.5m.

7- Silty claystone: Brown to dark brown and yellowish brown;

moderately compact; laminated; gypsiferous; ferruginous;

unfossiliferous; very slightly calcareous. Silt represents 30-40% and

composed of quartz grains. Its thickness is 14.5m.


19

8- Dolomitic argillaceous sandstone: Yellowish white to white and

yellow; compact; fine to medium quartz grains; subangular to rounded;

moderately sorted; with dolostone lenses of micro to fine subhedral

crystals, sometimes associated with grains of ferruginous materials;

poorly fossiliferous, represented by some molluscan fragments. Its

thickness is 3.5m.

Fig. 6: The highly fossiliferous sandy limestone, lower part of Genefe

Formation, Gabal Geneifa section, bed no. 9.

9- Highly fossiliferous sandy limestone: Grayish white to yellowish

white, brownish gray in parts; moderately compact; slightly argillaceous.

The calcareous matter is composed of cryptocrystalline calcite. The sand

content is made up of fine to medium quartz grains, subrounded to

subangular. It yields bivalvia as Chlamys radians (Nyst), Chlamys

(Chlamys) costai (Fontannes), Chlamys (Argopecten) macrotis

(Sowerby), Pecten (Pecten) cristato-costatus Sacco, Pecten (Pecten)

fraasi Fuchs, Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs;


20

gastropods as Natica sp. Abbass, Ampullina (Pseudamaura) macfaydeni

Abbass; regular echinoids; bryozoans as Retepora sp., Holoporella sp.;

foraminifers as Amphistegina sp., Miogypsina intermedia Drooger,

Operculina sp. and other foraminifers. Its thickness is 5m.

10- Silty calcareous claystone: Greenish gray to brownish gray; soft to

moderately compact; highly gypsiferous; ferruginous; unfossiliferous.

Silt is composed of medium quartz grains. The calcareous matter are

composed of crypto to micro crystalline calcite. Its thickness is 1.5m.

11- Fossiliferous sandy marl: Brownish white to yellowish white; soft to

moderately compact; calcareous matter are composed of crypto to micro

crystalline calcite; sand grains are fine to medium quartz grains,

subrounded to subangular. It bears bivalvia as Pecten (Pecten) cristato-

costatus Sacco, Pecten (Pecten) fraasi Fuchs, Chlamys (Argopecten)

macrotis (Sowerby), Chlamys (Chlamys) costai (Fontannes), Chlamys

radians (Nyst); echinoidal and molluscan fragments; Holoporella sp.

The microfossils are represented by Operculina complanata (Defrance),

Miogypsina intermedia Drooger. Also, it yields algae as Lithothamnium

sp. and Lithophyllum sp. Its thickness is 1m.

12- Fossiliferous Limestone: Yellowish brown to brown; compact;

massive; argillaceous; fossiliferous; calcareous matter are micro to

cryptocrystalline calcite; slightly ferruginous in the upper part. It

contains Chlamys (Macrochlamis) sardoa Ugolini, Clypeaster

intermedius Desmoulins; echinoidal, molluscan and bryozoans

fragments. The microfossils include algal fragments as Lithothamnium

sp. and Lithophyllum sp.; foraminifers as Operculina complanata

(Defrance), Miogypsina intermedia Drooger, Amphistegina sp. and other

foraminifers. Its thickness is 1.5m.


21

Fig. 7: Succession of silty calcareous claystone, fossiliferous sandy marl

and fossiliferous limestone; middle part of Genefe Formation; Gabal

Geneifa section. The succession of the four beds: 10, 11, 12 and 13.

13- Fossiliferous limestone: White to yellowish white grading upwards

into yellow; moderately compact to compact; massive; calcareous matter

are crypto to microcrystalline calcite; slightly argillaceous; with some

gypsum veins; fossiliferous to highly fossiliferous at the upper part,

sandy in the lower part. Sand grains are medium to fine quartz grains;

subrounded to subangular. It bears bivalvia as large sized oysters, single

and double-valved, not easy to be collected as Alectryonella plicatula

(Gmelin) subsp. virleti Deshayes, Crassostrea frondosa (Deserres)

subsp. rohlfsi Fuchs and others; large sized pectinids as Pecten

(Oppenheimopecten) convexo-costatus, Abich, Chlamys (Macrochlamis)

Bed no. 13

Bed no. 12

Bed no. 10

Bed no. 11


22

sardoa Ugolini; other bivalves as Gastrana sp. Schumacher; gastropods

as Conus (Lithoconus) mercati Brocchi, Ampullina (Pseudamaura)

maedai Abbass; echinoids as Echinolampas amplus Fuchs, Clypeaster

marginatus Lamarck and others which are turned upside down in many

cases, embedded in the rock, not easy to be collected; bryozoans such as

Holoprella sp. Also, it contains algae as Lithothamnium sp. and

Lithophyllum sp; foraminifers as Operculina complanata (Defrance),

Miogypsina intermedia Drooger, Amphistegina sp., and other

foraminifrs. Its thickness is 17m.

14- Argillaceous fossiliferous limestone: Yellow to yellowish brown;

moderately compact; fossiliferous. The calcareous matter are micro to

cryptocrystalline calcite. It yields bivalvia as Crassostrea frondosa (De

Serres) subsp. rohlfsi, Fuchs, and Alectryonella plicatula (Gmelin)

subsp. virleti Deshayes; foraminifers as Miogypsina intermedia Drooger.

Its thickness is 5m.

Fig. 8: The argillaceous limestone of the upper part of Genefe

Formation, Gabal Geneifa section, bed no. 14. It represents the

uppermost part of the Miocene succession in Geneifa area.


23

For fig. 9 (Lithostratigraphic succession of the Miocene rocks at Gabal

Geneifa).


24

II.2.2 Gabal Gharra section:

Gabal Gharra lies about 13 km to the West of Gabal Geneifa and

about 13 km to the northeast of Gabal Iweibed (Fig. 10). It extends

between longitudes 32 17 00 and 32 18 00 E, and latitudes 30 10

30 and 30 12 00 N. The base of the Miocene succession is exposed

where it unconformably overlies the Oligocene sands and gravels, this is

clearly obvious in a mine lies to the South of the succession (Fig. 11).

As the previous section, the lower part of this Miocene succession is

represented mainly by clastic deposits, but its upper part is represented

by non-clastic deposits. The studied section measures a total thickness of

141.7m and runs from base to top as follow:

Fig. 10: Panoramic view from the southern side of Gabal Gharra.

1- Sandstone: Yellowish brown to reddish brown; moderately compact

to semi-friable; fine to medium quartz grains; subangular to subrounded;

moderately sorted; unfossiliferous. It unconformably overlies the

Oligocene sands, gravels and boulders. Its thickness is 3.4m.

2- Shale: Reddish brown at the base, gray upwards; soft at bottom, firm

upwards; sandy; silty; very slightly calcareous, unfossiliferous,


25

overlianed by a ferruginous hard sandstone band of 5 cm thickness. Sand

grains in shale are fine to medium quartz grains; subrounded to

subangular. Sand grains in the ferruginous band are medium to coarse

quartz grains; subangular to subrounded. Its thickness is 7m.

Fig. 11: The Oligocene conglomeratic bed under the Miocene succession

in a mine at the root of Gabal Gharra.

3- Ferruginous sandstone: Yellowish brown; fine to medium quartz

grains; subangular to subrounded; moderately sorted; argillaceous; very

slightly calcareous; unfossiliferous. It is encountered between two hard

ferruginous sandstone bands 5 cm thick for each (fig 12). Its thickness is

1.5m.

4- Shale: Light to dark gray; moderately compact; sandy; silty; slightly

calcareous; underliened by ferruginous hard sandstone band of 5 cm

thick. Its thickness is 6.1m.


26

Fig. 12: The ferruginous sandstone in the lower part of Gharra

Formation, Gabal Gharra section, bed no. 3.

5- Calcareous sandstone: Dark yellowish brown; moderately compact;

fine to medium quartz grains; subangular to subrounded; moderately

sorted; unfossiliferous; ferruginous in parts. The calcareous matter is

composed of cryptocrystalline calcite. Its thickness is 2m.

6- Fossiliferous sandy limestone: Yellow to yellowish white; moderately

compact; slightly argillaceous; calcareous matter are crypto to

microcrystalline calcite (fig. 13). Sand grains are fine to medium quartz

grains; subangular to subrounded. Fossils are represented by


plicatula (Gmelin) subsp virleti Deshayes, Chlamys gentoni Fontannes;

Lucina sp.; gastropods as Natica cf. millepunctata Lamarck; many chips

of Scutella ammonis Fuchs, Parascutella stefaninii (Desio),

Prionocidaris cf. avenionensis (Desmoulins), Echinolampas sp.,

Clypeaster sp. and echinoid spines; bryozoa. Its thickness is 7.7m.


27

Fig. 13: Broken parts of Scutella ammonis on the surface of limestone of

the middle part of Gharra Formation, Gabal Gharra section, the surface

of bed no. 6.

7- Sandy limestone: Yellow to yellowish brown; moderately compact;

slightly argillaceous; calcareous matter are cryptocrystalline calcite.

Sand grains are fine to medium quartz grains; subangular to subrounded.

It is poorly fossiliferous yielding foraminifers as Amphistegina sp,

Operculina complanata (Defrance) and Miogypsina intermedia Drooger.

Its thickness is 6m.

8- Argillaceous limestone: Yellowish brown; moderately compact;

slightly sandy; poorly fossiliferous with Chlamys gentoni Fontannes and

other broken fragments. Its thickness is 0.5m.

9- Calcareous shale: Dark gray to gray; moderately compact; fractured;

unfossiliferous; very slightly sandy; silty. Sand grains are fine to very

fine quartz grains, subrounded to subangular. Its thickness is 5m.


28

Fig. 14: Band of large-sized pectinids in the limestone of the middle part

of Gharra Formation, Gabal Gharra section. The band represents the

upper 0.5m of bed no. 10.

10- Fossiliferous argillaceous limestone: Brownish yellow to yellow;

soft (fig. 14). It yields Alectryonella plicatula (Gmelin) subsp virleti

Deshayes. A pectinids band occurs at the upper 0.5m, yields large-sized

pectinids as Pecten (Pecten) fraasi Fuchs, Pecten (Pecten) ziziniae

Blanckenhorn, Pecten (Oppenheimopecten) benedictus (Lamarck), very

crowded with Pecten beudanti Basterot, Pecten (Amussiopecten)

burdigalensis Lamarck. This bed also yields Gastrana sp.; gastropods as

Conus (Lithoconus) mercati Brocchi, Ficus sp. Abbass; crustacea as

Balanus; bryozoa and few coral heads; algae as Lithothamnium sp. and

Lithophyllum sp; foraminifers as Operculina complanata (Defrance),

Miogypsina intermedia and Heterostegina sp. Its thickness is 3.2m.

11- Sandy shale: Dark gray to gray; soft to moderately compact;

gypsiferous; unfossiliferous; more sandy upwards; interbedded with

ferruginous bands of 5 cm thick for each, these bands increase in


29

number upwards. Sand grains are fine to very fine quartz grains;

subrounded. Its thickness is 19.5m.

12- Fossiliferous calcareous sandstone: Yellow to yellowish white,

occasionally yellowish brown; moderately compact, occasionally semi-

friable to friable; fine to medium quartz grains; subangular to

subrounded; moderately sorted; pebbly at base. It yields bivalvia as


plicatula (Gmelin) subsp virleti Deshayes; Chlamys scabrella Lamarck,

Pecten (Flabellipecten) flabelliformis (Brocchi), Anomia burdigalensis

Defrance, Clementia sp. Also it yields echinoderms as Scutella

ammonis Fuchs, Parascutella stefaninii (Desio) and other echinoderms.

Its thickness is 4.9m.

13- Fossiliferous limestone: Yellow to yellowish white; compact;

massive; slightly argillaceous; slightly sandy. It is croweded with

bivalvia as Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs,

Alectryonella plicatula (Gmelin) subsp virleti Deshayes, Pecten (Pecten)

cristato-costatus Sacco, Chlamys scabrella Lamarck, Chlamys

(Argopecten) macrotis (Sowerby), Chlamys senatoria (Gmelin);

Cardium sp.; rich in molds of Callista (Costacallista) erycina (Linné),

Paphia (Callistotapes) vetula (Bastrot), Clementia sp., Diplodonta sp.,

Gari sp. Also it contains Lutraria sp., Gastrana laminosa (Sowerby);

gastropods as Turritella (Turritella) terebralis Lamarck; echinoderms as

Echinolampas amplus Fuchs, Clypeaster marginatus Lamarck, Scutella

ammonis Fuchs; crustacea as Balanus concavus (Bronn); coral reefs as

Leptastrea sp. The lower 0.5m of this bed represents a pectinids and

oysters bank, whereas the upper (20-125cm) represents a sclaractenian

coral reef which is monospecific (Leptastrea sp.), and it is replaced in

parts with an algal limestone band. Algae are represented by

Lithothamnium sp. and Lithophyllum sp. Its thickness is 16.4m.


30

Fig. 15: Upper part of Gharra Formation underlies the lower part of

Genefe Formation, Gabal Gharra section. The succession represents the

three beds (upper part of bed 11, bed 12 and lower part of bed 13).

Bed no. 13

Bed no. 12

Bed no. 11

Lower part of Genefe Fm.

Upper part of Gharra Fm.


31

Fig. 16: The lower part of Genefe Formation, Gabal Gharra section, bed

no. 13. The bed is crowded with fauna specially oysters and pectinids

forming a bank in the lower part of this bed.

Fig. 17: Part of the coral reef bank in the lower part of Genefe

Formation, Gabal Gharra section, the upper part of bed no. 13.


32

14- Fossiliferous limestone: White to yellowish white, occasionally

milky white; moderately compact; bioturbated in the upper part with a

yellowish brown color; calcareous matter is composed of

cryptocrystalline calcite. It is rich with Crassostrea frondosa (De Serres)

subsp. rohlfsi Fuchs, Alectryonella plicatula (Gmelin) subsp virleti

Deshayes, embryonic stages of oysters are found. Also, it contains

Chlamys (Macrochlamis) sardoa Ugolini, and other pectinid fragments;

Echinolampas amplus Fuchs, Clypeaster intermedius Desmoulins,

echinoid spines and corals; algae as Lithothamnium sp. and

Lithophyllum sp. Its thickness is 24.5m.

Fig. 18: Oysters and pectinids are embedded in the limestone of the

middle part of Genefe Formation, Gabal Gharra section, bed no. 14.

15- Fossiliferous sandy chalky limestone: Yellow to yellowish white;

moderately compact; chalky; algal in parts; calcareous matter is

represented by cryptocrystalline calcite. Sand grains are fine to medium

quartz grains; subangular to subrounded. It bears Crassostrea frondosa


33

(De Serres) subsp. rohlfsi Fuchs, Alectryonella plicatula (Gmelin) subsp

virleti Deshayes, Chlamys (Argopecten) submalvinae (Blanckenhorn),

Chlamys (Argopecten) macrotis (Sowerby), Chlamys malvinae (Dubois),

Chlamys senatoria (Gmelin); broken parts of echinoids; bryozoa and

few corals; foraminifers as Miogypsina intermedia Drooger. Its

thickness is 30m.

Fig. 19: The chalky limestone of the upper part of Genefe Formation,

Gabal Gharra section, bed no. 15.

16- Chalky limestone: Yellowish white to white, occasionally yellow;

moderately compact; chalky. It yields some shell fragments, echinoid

plates and undefined foraminifera. Also, it yields algae as

Lithothamnium sp. and Lithophyllum sp. Its thickness is 4m.


34

Fig. 20: The uppermost part of Genefe Formation which forms the

uppermost part of the Miocene succession in Gabal Gharra section. This

photo represents the upper part of bed no. 15 and the bed no. 16.

Fig. 21: General view of Genefe Formation from the eastern side, Gabal

Gharra section.


35


Gharra).


36

II.2.3 Gabal Homeira section:

Gabal Homeira lies to the North of Gabal Ataqa and to the

southeast of Gabal Iweibid (fig. 10). It extends between longitudes 32°

11 00 and 32° 13 20 E, and latitudes 30° 02 12 and 30° 03 18" N.

The basal part of Homeira Miocene succession is represented mainly by

clastic deposits, unconformably overling the Oligocene sands and

gravels, then an alternation between clastic and non-clastic beds

throughout the lower part, while the upper part is represented mainly by

non-clastic deposits. This succession measures a total thickness of 110.9

m and runs from base to top as follow:

Fig. 23: Panoramic view for Gabal Homeira from the southern side.

1- Shale: Varicolored, yellow, brown; moderately compact; fractured;

unfossiliferous; slightly calcareous; slightly sandy; slightly silty. This

bed unconformably overlies Oligocene made up of alternating sands and

gravel. Its thickness is 2.7m.

A part of the Miocene succession


37

2- Sandy dolostone: Yellowish brown; compact to highly compact;

fractured; calcareous matter is represented by euhedral microcrystalline

dolomite rhombs (fig. 34). The sand grains are fine to medium quartz

grains; subangular to subrounded. Poorly fossiliferous, the fossil content

is represented by echinoid fragments and undefined foraminiferal tests.

Its thickness is 0.5m.

Fig. 24: Clastics of the lowermost part of Gharra Formation, Gabal

Homeira section. Succession of the three beds 1, 2, and 3.

3- Calcareous sandstone: Yellowish brown to yellowish white;

moderately compact; fine to medium grained; subrounded to rounded;

moderately sorted; cement is represented by calcareous matter of

cryptocrystalline calcite; poorly fossiliferous. Its thickness is 2.9m.

4- Sandy limestone: Yellowish white to yellowish brown; moderately

compact; slightly argillaceous; calcareous matter is represented by

crypto to microcrystalline calcite. Sand grains are medium to coarse

quartz grains; subrounded to subangular. It is poorly fossiliferous. Its

thickness is 1.4m.

Bed no. 3

Bed no. 2

Bed no. 1


38

5- Sandy marl: Yellowish white; moderately compact. Sand grains are

fine to medium quartz grains; subrounded to subangular. It is

fossiliferous with sclaractenian corals, echinoid plates and spines. Its

thickness is 5m.

Fig. 25: The sandy marl of the lower part of Gharra Formation, Gabal

Homeira section, bed no. 5.

6- Sandy limestone: Yellowish white; moderately compact; slightly

argillaceous; calcareous matter is represented by cryptocrystalline

calcite. Sand grains are fine to coarse quartz grains; angular to

subrounded; with eroded periphery; pebbly in parts. It contains oysters

and pectinids which are embedded in the rock and not easy to be

collected. Also, it bears Heterostegina sp. Its thickness is 3m.

7- Calcareous sandstone: Yellowish white to yellowish brown;

moderately compact; fine to coarse quartz grains; angular to

subrounded; poorly sorted; with eroded periphery; slightly argillaceous;


39

calcareous matter is represented by cryptocrystalline calcite; poorly

fossiliferous with bad preserved oysters and pectinids. Its thickness is

1.5m.

Fig. 26: The pectinids and oysters are embedded in the limestone of the

middle part of Gharra Formation, Gabal Homeira section, bed no. 8.

8- Sandy limestone: Yellowish white; slightly to moderately compact;

calcareous matter represented by cryptocrystalline calcite. Sand grains

are fine to coarse quartz grains; angular to subrounded; with eroded

periphery; pebbly in parts. It is rich with oysters and pectinids which are

embedded in the rock and not easy to be collected. Also, it bears

Heterostegina sp. Its thickness is 3m.

9- Shale: Greenish gray to yellowish green, occasionally stained with

yellow color; moderately compact; highly fractured and jointed; soapy;

gypsiferous; unfossiliferous; slightly calcareous; slightly sandy; slightly

silty. Its thickness is 4.3m.


40

10- Sandy limestone: Yellowish white to yellowish brown; moderately

compact; calcareous matter is represented by micro to cryptocrystalline

calcite. Sand grains are fine to medium quartz grains; subangular to

subrounded; with eroded periphery; pebbly at its lower part. It is poorly

fossiliferous, contain some bad preserved bivalvia, Balanus concavus

(Bronn.) and echinoid fragments. Its thickness is 1.5m.

11- Fossiliferous sandy limestone: Yellowish brown to light brown; soft

to moderately compact; slightly argillaceous; calcareous matter

represented by cryptocrystalline calcite. Sand grains are fine to medium

quartz grains; subangular to subrounded. It is rich with bivalvia as


plicatula (Gmelin) subsp. virleti Deshayes, Pecten fuchsi Fontannes,

Pecten (Pecten) ziziniae Blanckenhorn, Chlamys malvinae (Dubois),

Chlamys (Aequipecten) scabriscula (Matheron); Paphia (Callistotapes)

vetula (Bastrot), Acanthocardia (Acanthocardia) paucicostata

(Sowerby), Cardium sp., Anomia sp.; gastropods as Ficus sp. Abbass,

Turritell (Turritella) cleevelyi Abbass, Turritella (Eichwaldiella) fouadi

Abbass, Turritella (Turritella) terebralis Lamarck; Bursa faizae Abbass,

echinoderms as Echinolampas amplus Fuchs, Echinolampas

plagiosomus Agassiz, Clypeaster marginatus Lamarck; bryozoa as

Holoporella polythele (Russ); algae as Lithothamnium sp and

Lithophyllum sp.; foraminifers as Operculina complanata (Defrance),

Miogypsina intermedia Drooger and other foraminifers. Its thickness is 5m.

12- Claystone: Gray to light gray, occasionally dark gray; soft;

gypsiferous; unfossiliferous; slightly calcareous; slightly silty. Its

thickness is 4.2m.

13- Fossiliferous sandy limestone: Yellowish white to brownish white;

moderately compact; fractured; slightly argillaceous; calcareous matter

is represented by cryptocrystalline calcite. Sand grains are fine to coarse


41

quartz grains; subrounded to rounded and stained with iron oxides on

periphery. It yields bivalvia as Crassostrea frondosa (De Serres) subsp.

rohlfsi Fuchs, Alectryonella plicatula (Gmelin) subsp. virleti Deshayes.

It is rich in pectinids as Pecten (Pecten) ziziniae Blanckenhorn, Pecten

fuchsi Fontannes, Pecten (Oppenheimopecten) benedictus (Lamarck),

Pecten erythraensis Sowerby, Pecten beudanti Basterot, Pecten

(Flabellipecten) flabelliformis (Brocchi), other bivalves as Linga (Linga)

columbella (Lamarck), Cardium sp., Anomia burdigalensis Defrance,

Anomia (Anomia) ephippium Linné subsp. rogulosostriata Brocchi;

gastropods as Conus (Lithoconus) mercati Brocchi, Conus (Conolithus)

melficus Desio, Ficus reticulatus Lamarck; broken echinoids as

Clypeaster sp. ; and Balanus concavus (Bronn); algae as Lithothamnium

sp. and Lithophyllum sp. Its thickness is 2.5m.

Fig. 27: Limestone of the upper part of the Gharra Formation

underlained with clay, Gabal Homeira section. Succession of the two

beds no. 12 and 13.

Bed no. 12

Bed no. 13


42

14- Claystone: Gray, greenish gray to light green, occasionally

yellowish green; moderately compact; fractured; jointed; fissile; no

macrofossils have been encountered; slightly calcareous; very slightly

sandy; slightly silty. Its thickness is 4.6m.

15- Argillaceous calcareous sandstone: Yellow to yellowish brown;

moderately compact; fine to medium quartz grains; angular to

subrounded; moderately sorted; with altered plagioclase, microcline and

biotite. Its thickness is 6.1m.

Fig. 28: Large oysters are embedded in the limestone of the lowermost

part of Genefe Formation, Gabal Homeira section, bed no. 16.

16- Fossiliferous limestone: Yellowish white to yellow, yellowish brown

to brown in the upper two meters; moderately compact; calcareous

matter is composed of cryptocrystalline calcite. It is rich in large-sized

oysters as Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs,

Alectryonella plicatula (Gmelin) subsp virleti Deshayes. Also, it yields

Pecten (Pecten) cristato-costatus Sacco, Cardium sp.; broken parts of


43

echinoids as Scutella ammonis Fuchs, Parascutella stefaninii (Desio)

and echinoid spines; algae as Lithothamnium sp. and Lithophyllum sp.;

foraminifera as Amphistegina sp. Its thickness is 25.5m.

17- Fossiliferous sandy limestone: Yellow to yellowish white;

moderately compact; calcareous matter is composed of fine to

cryptocrystalline calcite; argillaceous. Sand grains are fine to medium

quartz grains; rounded to subrounded; stained with iron oxides on

periphery. It is rich with Scutella ammonis Fuchs, Parascutella

stefaninii (Desio) and broken parts of other echinoid species. Also, it

yields Pecten (Pecten) cristato-costatus Sacco, some fragments of other

pectinids and other bivalves and foraminifers as Miogypsina intermedia

Drooger. Its thickness is 3.9m.

Fig. 29: A general view for the marl oyster bank of the middle part of

Genefe Formation, Gabal Homeira section, bed no. 18.


44

18- Marl: (Oyster bank) Brownish yellow; soft to moderately compact;

clayey at base, gradually become more calcareous at top. The sediments

represent the matrix between the fauna which are mainly represented by


plicatula (Gmelin) subsp virleti Deshayes. Also, it yields Pecten

(Pecten) cristato-costatus Sacco; broken parts of Scutella ammonis

Fuchs and Parascutella stefaninii (Desio). Its thickness is 3.3m.

19- Fossiliferous sandy limestone: Yellowish white to light brownish

white; moderately compact to compact; massive; fractured in parts;

calcareous matter is composed of fine to cryptocrystalline calcite;

argillaceous. Sand grains are fine to medium quartz grains; subrounded

to subangular. It yields oysters embedded in the rock and can not be

collected; Chlamys (Macrochlamis) sardoa Ugolini and other small-

sized pectinids; molds of other bivalves as Cardium sp., Clavagella sp.,

Gastrana sp., Gastrana laminosa (Sowerby), Arca (Anadara) grondica

Mayer; gastropods as Turritella (Turritella) terebralis Lamarck, Ficus

sp. Abbass, Lanistes (Lanistes) mahmoudi Abbass, Luria (Luria) salwae

Abbass, Oliva (Neocyclindrus) wagihi Abbass, Planorbis (Planorbis)

nakanoi Abbass; worm tubes; sclarctenian corals and bryozoans. Also it

yields foraminifers as Heterostegina sp., Amphistegina sp. and other

foraminifers; algae as Lithothamnium sp. and Lithophyllum sp. Its

thickness is 30m.


45

Fig. 30: A close view for the marl oyster bank of the middle part of

Genefe Formation, Gabal Homeira section, bed no. 18.

Fig. 31: The fossiliferous limestone of the uppermost part of Genefe

Formation, Gabal Homeira section, bed no. 19 which represents the

uppermost part of the Homeira Miocene succession.


46


Homeira).


47

For fig. 33 (Correlation chart for the three studied sections at Gabal

Geneifa, Gabal Homeira and Gabal Gharra).

Chapter III Stratigraphy

48

CHAPTER III

STRATIGRAPHY

III.1 LITHOSTRATIGRAPHY

III.1.1 Introduction:

The Miocene sediments of the study area were the subject of many

publications such as that of Fuchs (1883) who studied the faunal

assemblages of the exposures at Gabal Geneifa and found that they

belong to the lower part of the Middle Miocene. Barron (1907) studied

the rocks at the roots of Gabal Geneifa and related them to the Lower

Miocene followed by the Middle Miocene sequence while Sadek (1959)

assigned the basal beds of Gabal Geneifa to the Late Burdigalian and the

overlying limestone beds with Lithothamnium and Heterostegina to the

Vindobonian. In 1963, Metwalli divided the marine Miocene of the

Cairo-Suez District into two informal units, the lower one is sandy and

rich in assemblage of macro- and microfauna of Burdigalian age while

the upper one is calcareous containing faunal assemblage of Middle

Miocene. Farag and Sadek (1966) subdivided the Miocene rocks in Gabal

Homeira into two units: the lower one is the marine unit which includes

the Burdigalian and Helvetian fossiliferous sediments, the upper one is

the non-marine unit which consists of unfossiliferous fluviatile sediments

of Late Miocene age; Barakat ane Aboul Ela (1970) studied the

microfacies types of the Miocene rocks exposed at Gabal Geneifa area

and found that the Lower Miocene (Burdigalian) is represented by

shallow marine sediments with reefal forms (inner neritic to reefal

environment), the Middle Miocene (Vindobonian) is represented by

shallow agitated marine of reefal environment; Said (1990) referred that

the Gharra Formation represents the Lower Miocene deposits of the

Cairo-Suez District and related it to the Aquitanian-Burdigalian age and


49

considered the overlying Genefe Formation to represent the Middle

Miocene (Langhian); El-Shazly and Saber (1999) studied the facies and

macropaleontology of the marine Miocene sediments at Gabal Homeira

and divided the succession into two formations: the lower one is Gharra

Formation representing the Lower Miocene, and the upper one is Genefe

Formation representing the Middle Miocene.

In the present study, there are three stratigraphical sections have

been measured and sampled from Gabal Geneifa, Gabal Gharra and

Gabal Homeira in order to study in detail the main Miocene successions

in the eastern part of Cairo-Suez area; this to detect the lateral geographic,

stratigraphic and lithologic continuity and its changes in this area which

was close to the Miocene transgression from the East and not isolated

completely from the North. According to the detected lithologies, fossil

content and microfacies types the sedimentary succession in these

sections represent the Lower-Middle Miocene sequence. In the study

area, this sequence is divided into two lithostratigraphic units namely, in

asending order, the Gharra Formation and the Genefe Formation. The

lithologies of the beds constituting the recorded formations are shown in

figures (2 – 33). The diagnosis and description of these formations are

here under.

III.1.2 Studied sections:

III.1.2.1 Gharra Formation:

Author : Ghorab and Marzouk (1965).

Etmology : After Gabal Gharra.

Type locality: Gharra section.

Thickness : 66.8 m at Gabal Gharra (fig. 22)

Limits : The Gharra Formation rests unconformably on sediments of

Oligocene age (sands and gravels) with silicified woods in both


50

Gabal Gharra and Gabal Homeira sections, while in Gabal Geneifa

section the base of the formation is unexposed (figs. 9, 22, 32). In

all the three studied sections, the Gharra Formation is conformably

overlained by the Genefe Formation.

In Geneifa section, this formation measures 66.1m, its base is not

exposed while its top is conformably followed by the Genefe Formation.

In Gharra section, it measures 66.8m where it unconformably overlies the

Oligocene sediments and conformably overlies the Genefe Formation

(fig. 15). In Homeira section, this formation measures 48.2m since it

unconformably overlies the Oligocene sediments and underlies the

Genefe Formation.

Lithology: The Gharra Formation consists mainly of clastics (shale,

claystone, marl and sandstone) with sandy limestone interbeds. The

limestones are fossiliferous to highly fossiliferous, containing rich

assemblages of macrofossils.

Fossil content: The Gharra formation contains varity of fauna like

bivalves, gastropods, echinoderms and coralline red algae. The most

interesting fauna can be summarized in the following:

The fossiliferous sandy limestone of the beds no. 5 in Gabal

Geneifa section and no. 6 in Gabal Gharra section nearly contain the same

faunal content of common oysters and pectinids, pectinides, many other

bivalves, gastropod molds, echinoderms, algae and bryozoans. These

beds can be considered as a horizon of correlation for the middle part of

the Gharra Formation in the study area. The collected samples of

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes from bed no. 5

in Gabal Geneifa section are of large sizes and moderate valve thickness


51

which mean that the prevailing conditions was favourable for their

growth better than the another locality. The presence and abundance of

the embryonic stages of Crassostrea frondosa (De Serres) subsp. rohlfsi

Fuchs in Gharra section mean that the environmental changes were very

rapid which did not left a chance for migration to another suitable

environment.

The fossiliferous argillaceous limestone of bed no. 10 in Gabal

Gharra section and the fossiliferous sandy limestone of bed no. 13 in

Gabal Homeira section, are closely similar in their faunal content which

is mostly of oysters, pectinids, many other bivalves, gastropod molds,

Balanus sp. and algae. This can be considered a good horizon of

correlation for the upper part of the Gharra Formation in the area of the

recorded two sections in the studied area. The abundance of Pecten

(Pecten) zizinia Blanchenhorn, Pecten beudanti Basterot, Pecten

(Oppenheimpecten) benedictus (Lamarck) and Ficus sp Abbass in these

two beds in the two sections can be considered as a special marker. The

collected samples of Alectryonella plicatula (Gmelin) subsp. virleti

Deshayes from these two beds in the two mentioned sections are of large

sizes and moderate valve thickness which mean that the prevailing

environment was favourable for their growth. Through these two beds in

the two sections, there is a pectinid band (clearly recorded in the upper

0.5m of bed no. 10 in Gabal Gharra section) yielding large-sized pectinids

of Pecten beudanti Basterot and Pecten (Oppenheimpecten) benedictus

(Lamarck).

The dolomitic argillaceous sandstone of bed no. 8 in Gabal Geneifa

section, in addition to the fossiliferous calcareous sandstone of bed no. 12

in Gabal Gharra section and the argillaceous calcareous sandstone of bed

no. 15 in Gabal Homeira section represent the uppermost part of the

Gharra Formation in the area of the three studied sections. The above


52

mentioned two sandstone beds in Gabal Geneifa and Gabal Homeira

sections are poorly fossiliferous, but the above mentioned sandstone bed

in Gabal Gharra section is fossiliferous yielding oysters, pectinids; it is

very crowded with molds of Cardium sp. and molds of other bivalvia;

also, it yields Scutella ammonis Fuchs and Parascutella stefaninii (Desio)

which means a moderate energy environment favourable for the

deposition of the sandstone and the growth of the contained fauna.

Microfacies types: The microfacies types of the Gharra Formation are

mainly clastic-dominated facies. The lower part is characterized by an

erosional base, followed by cross-bedded sandstones and topped by thin

laminated mudstone. The upper part of this facies is intercalated with

sandy limestones, oyster banks, mudstones and sandstones.

This formation is mainly characterized by the following

microfacies associations: calcareous quartz arenite, dolomitic calcareous

quartz arenite, calcareous fossiliferous quartz arenite, calcareous

ferrugineous quartz arenite, sandy echinoidal foraminiferal grainstone,

sandy dolomitic wackestone, sandy fossiliferous grainstone, sandy

echinoidal packstone, sandy algal grainstone, sandy bioclasts packstone,

and sandy foraminiferal bryozoan packstone.

Environment: Based on microfacies associations, sedimentary structures

and fossil content, the Gharra Formation was probably deposited in an

environment ranging from tidal flat for the lower part to typical reef flank

for coral and algal reefs and high energy on shoals for the grain-supported

fabrics (grainstone and packstone), (figs. 39-45).

Age: In the previous works, Sadek (1959); Farag and Sadek (1966)

assigned this formation to be of Early Miocene age (Aquitanian?-


53

Burdigalian) while Metwalli (1963); Souaya (1963); Barakat and Aboul

Ela (1970); Said (1990); Hamza (1992); El-Shazly and Saber (1999)

assigned this formation to be of (Burdigalian) age.

In the present work, based on the lithology, fossil content,

microfacies types, environment and the assignment with the previous

works; this formation is assigned to the Early Miocene age (Burdigalian).

III.1.2.2 Genefe Formation:

Author : Ghorab and Marzouk (1965).

Etmology : Gabal Geneifa.

Type locality: Geneifa section.

Thickness : 31 m at Gabal Geneifa (fig. 9)

Limits : In the three studied sections, the Genefe Formation rests

conformably on the sediments of Gharra Formation and its top is

not covered in the three sections.

Genefe Formation in Geneifa section measures 31m, it is overlying

the dolomitic argillaceous sandstone of the top of Gharra Formation; in

Gharra section, it measures 74.9m where it is overlying the fossiliferous

calcareous sandstone of the top of Gharra Formation while in Homeira

section, it measures 48.2m since it is overlying the argillaceous

calcareous sandstone of the top of Gharra Formation.

Lithology: The Genefe Formation consists mainly of algal, reefal and

chalky limestones with oyster banks, mudstone and marl intercalations.

The limestones and marls are fossiliferous to highly fossiliferous

containing rich assemblagaes of macrofossils.


54

Fossil content: The Gharra formation contains varity of fauna like

bivalvia, gastropods, echinoderms and coralline red algae. The most

interesting fauna can be summarized in the following:

The coralline red algae (Lithothamnium sp. and Lithophyllum sp.)

are more dominant in the lower part of the Genefe Formation.

The fossiliferous sandy marl of the bed no. 11 in Gabal Geneifa

section with its high abundance of pectinids (pectinid band) is

correlatable with the lowermost part (0.5m) of bed no. 13 in Gabal Gharra

section with its high abundance of pectinids and oysters (pectinid-oyster

band), it can be considered a horizon for correlation in the area of the two

mentioned sections for the lower part of the Genefe Formation. The

abundance of Pecten (Pecten) cristato-costatus Sacco and Chlamys

(Argopecten) macrotis (Sowerby) in the above mentioned two occurances

represents a specific horizon for correlation in the area of the above

mentioned two sections for the lower part of the Genefe Formation.

In the same time, the above mentioned fossiliferous limestone of

the bed no. 13 in Gabal Gharra section correlatable with the fossiliferous

limestone of the bed no. 16 in Gabal Homeira section with its abundance

of fauna (specially oysters) which is considered a horizon of correlation

in the area of the above mentioned two sections for the lower part of the

Genefe Formation. The abundance of Alectryonella plicatula (Gmelin)

subsp. virleti Deshayes and Crassostrea frondosa (De Serres) subsp.

rohlfsi Fuchs in the above mentioned two occurances is also a specific

horizon for correlation in the area of the above mentioned two sections

for the lower part of the Genefe Formation. The fauna (specially

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes) are

characterized by large sizes and thick valves which indicate that the

prevailing environment was favourable for their growth. The gradiation

of fauna from abundant pectinid band (in bed no. 11, Gabal Geneifa


55

section) to an oyster-pectinid band (in the lower 0.5m of bed no. 13,

Gabal Gharra section) to the high abundant of oysters band (in bed no. 16,

Gabal Homeira section), means the gradiation of the environment.

The fossiliferous limestone of the bed no. 13 in Gabal Geneifa

section, the fossiliferous limestone of bed no. 14 in Gabal Gharra section

and the marl of bed no. 18 in Gabal Homeira section are characterized by

the abundance of the main prevailing fauna in the three occurances of

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes and Crassostrea

frondosa (De Serres) subsp. rohlfsi Fuchs which can be considered a

horizon for correlation in the area of the above mentioned three sections.

These last fauna in Gabal Gharra section are characterized by large sizes

and thick valves, in addition to resonable presence of embryonic stages

from these fauna. The marl bed no. 18 in Gabal Homeira section is very

crowded with these above mentioned fauna assembly, where the

sediments represent the matrix among the fauna.

Microfacies types: The microfacies types of the Genefe Formation are

mainly carbonate-dominated facies.

This formation is mainly characterized by the following

microfacies associations: Sandy bioclasts packstone, sandy foraminiferal

bryozoan packstone, sandy molluscan grainstone, foraminiferal algal

wackestone, sandy bioclasts packstone, sandy echinoidal foraminiferal

grainstone, sandy algal grainstone, algal coralline framestone and

coralline framestone.

Environment: The microfacies associations, fossil content and

sedimentary structures stated that the environment of deposition was

reefal for the lower part, due to the presence of abundant coralline red

algae, oysters, Amphistigena sp, Miogypsina sp. to shelf lagoons with


56

open circulation and an intertidal environment with low energy conditions

for the deposition of mudstones in the top most part of Genefe Formation.

Age: In the previous works, Souya (1963); Metwalli (1963); Sadek

(1959); Souaya (1963); Farag and Sadek (1966); Barakat and Aboul Ela

(1970); Said (1990); Hamza (1992); El-Shazly and Saber (1999) assigned

the Genefe Formation to the Middle Miocene age (Langhian-

Serravallian).

In the present work, this formation is assigned to the Middle

Miocene age (Langhian-Serravallian).


57

III.2 BIOSTRATIGRAPHY

Few biostratigraphic studies were carried out on the Miocene rocks

of the study area. They were mostly based on the larger foraminifera.

Hamam (1966) studied the Miocene rocks in the Agrud area and

defined the following biozones:

2- Heterostegina costata costata zone (Helvetian)

1- Operculina complanata zone (Burdigalian)

Cherif (1966) recognized the following biozones in the Sadat area:

4- Ostrea crassissima aegyptiaca zone (Tortonian)

3- Heterostegina costata politesta zone (Tortonian)

2- Heterostegina costata costata zone (Helvetian)

1- Heterostegina heterostegina heterostegina zone (Burdigalian)

The classification of Abdallah and Abd El-Hady (1966) for the

Cairo-Sukhna District have been modified by Stratigraphic Sub-

Committee (1974) and introduced the following biozones:

4- Chlamys submalvinae-Pycnodonte virleti biohorizon. (Middle Miocene)

3- Pecten josslingi biohorizon. (Middle Miocene)

2- Flabellipecten burdigalensis-Pecten ziziniae biohorizon. (Burdigalian)

1- Crassostrea duvergieri-Cubitostrea digitalina biohorizon. (Burdigalian)

Abd-Elmoneim (1992) studied the stratigraphy of the Miocene

rocks in the area between Gabal Ataqa and Northern Galala Plateau, and

established the following ten biozones:

The lower five biozones (in Sadat Formation / Late Burdigalian-

Langhian) are:

5- Lithothamnium sp acme zone.


58

4- Pecten (Amussiopecten) burdigalensis – Psammechinus aegyptiacus

assemblage zone.

3- Pecten (Flabellipecten) schweinfurthi range zone.

2- Pecten (Pecten) fraasi range zone.

1- Pecten (Pecten) ziziniae range zone.

The upper five biozones (in Hommath Formation / Serravalian) are:

5- Turritella (Eichwaldiella) fouadi zone.


3- Placuna (Indoplacuna) miocenica zone.

2- Crassostrea crassissima zone.

1- Amphiope arcuata fuchsi zone.

Hamza (1992) in his biostratigraphical study of the Neogene in the

eastern part of Egypt defined four biohorizones:

4- Chlamys submalvinae-Pycnodonte virleti biohorizon (Middle Miocene).

3- Pecten josslingi biohorizon (Middle Miocene).

2- Flabellipecten burdigalensis-Pecten ziziniae biohorizon (Burdigalian).

1- Crassosterea duvergieri-Cubitostrea digitalina biohorizon (Burdigalian).

In the present study, as mentioned before, Gharra Formation

consists mainly of clastic rocks with few beds of sandy and clayey

limestones. On the other hand, Genefe Formation consists entirly of

limestones with little clay and marl interbeds. The limestone beds are rich

in macro-invertebrate fauna especially bivalves, gastropods and echinoids

with some foraminifers as Operculina. According to the abundance of

these fauna and their good preservation, especially the pectinids, the

recorded macrofauna of pectinids are found enough and reliable for

biostratigraphic differentiation in Gharra and Genefe Formations where

six biozones have been established. The vertical distribution and lateral


59

extension of all identified species have been recorded and represented in

the distribution faunal charts (figs. 34-36). Investigation of these charts

with the actual impression from the field led to the establishment of very

distinctive six macro-biozones characterized by good feasibility in

practical application. From younger to older, these biozones are:


5- Chlamys (Macrochlamis) sardoa zone.

4- Pecten (Pecten) cristato-costatus zone.

3- Pecten (Flabellipecten) flabelliformis zone.

2- Pecten (Pecten) ziziniae zone.

1- Chlamys gentoni zone.

1- Chlamys gentoni zone:

Zone type : Range zone.

Type section : Gabal Gharra.

Thickness : 14.2m in its type section.

Limits : This zone overlies a barren zone extending from the base of

Gharra section to the first appearance of the fauna of the biozone.

It underlies the Chlamys gentoni - Pecten (Pecten) ziziniae barren

interzone.

Fauna : In addition to the zonal species, this biozone is

characterized by the presence of Crassostrea frondosa (De Serres)

subsp. rohlfsi Fuchs, Alectryonella plicatula (Gmelin) subsp.

virleti Deshayes, Lucina sp., Natica cf. millepunctata Lamarck,

Scutella ammonis Fuchs and Parascutella stefaninii (Desio).

Boundaries : The lower boundary of Chlamys gentoni zone is defined by

the first appearance of the zonal species in addition to Crassostrea

frondosa (De Serres) subsp. rohlfsi Fuchs, Alectryonella plicatula

(Gmelin) subsp. virleti Deshayes, Lucina sp., Natica cf.


60

millepunctata Lamarck, Scutella ammonis Fuchs and Parascutella

stefaninii (Desio). The upper boundary of this zone is marked by

the disappearance of the zonal species with Lucina sp. and Natica

cf. millepunctata Lamarck.

Remarks : Chlamys gentoni zone represents the lowermost bio-unit in

the Miocene rocks of the study area. It is well developed in Gabal

Gharra and Gabal Geneifa sections but not recognized in Homeira

section. The interval of this zone is made up of fossiliferous sandy

limestone beds. The thickness of the biozone is reduced at Gabal

Geneifa succession reaching 7.5m.

Age : Burdigalian.

2- Pecten (Pecten) ziziniae zone:


Type section : Gabal Homeira.

Thickness : 11.7m at its type section.

Limits : Pecten (Pecten) ziziniae zone overlies a barren zone

extending from the base of Gabal Homeira section to the first

appearance of the fauna of this zone. It underlies Pecten (Pecten)

ziziniae - Pecten (Pecten) cristato-costatus barren interzone.


characterized by the presence of Chlamys malvinae (Dubois),

Chlamys (Aequipecten) scabriuscula (Matheron), Pecten fuchsi

Fontannes, Pecten (Pecten) ziziniae Blanckenhorn, Pecten

beudanti Basterot, Pecten erythraensis Sowerby, Pecten

(Flabellipecten) flabelliformis (Brocchi), Pecten

(Oppenheimopecten) benedictus Lamarck, Anomia burdigalensis

Defrance, Anomia (Anomia) ephippium Linné subsp.

rugulosostriata Brocchi, Crassostrea frondosa (De Serres)


61


virleti Deshayes, Acanthocardia (Acanthocardia) paucicostata

(Sowerby), Paphia (Callistotapes) vetula (Bastrot), Cardium sp.,

Linga (Linga) columbella (Lamarck), Turritella (Turritella)

cleevelyi Abbass, Turritella (Turritella) terebralis Lamarck,

Turritella (Eichwaldiella) fouadi Abbass, Ficus reticulatus

(Lamarck), Ficus sp., Conus (Lithoconus) mercati Brocchi,

Conus (Conolithus) melficus Desio, Bursa faizae Abbass,

Clypeaster marginatus Lamarck, Echinolampas amplus Fuchs,

Echinolampas plagiosomus Agassiz.

Boundaries : The lower boundary of Pecten (Pecten) ziziniae zone is

defined by the first appearance of the above mentioned fauna

while its upper boundary is characterized by the disappearance of

the zonal species and the disappearance of Chlamys malvinae

(Dubois), Chlamys (Aequipecten) scabriuscula (Matheron),

Pecten fuchsi Fontannes, Pecten (Pecten) ziziniae Blanckenhorn,

Pecten beudanti Basterot, Pecten erythraensis Sowerby, Pecten

(Flabellipecten) flabelliformis (Brocchi), Pecten

(Oppenheimopecten) benedictus Lamarck, Anomia burdigalensis

Defrance, Anomia (Anomia) ephippium Linné subsp.

rugulosostriata Brocchi, Acanthocardia (Acanthocardia)

paucicostata (Sowerby), Paphia (Callistotapes) vetula (Bastrot),

Linga (Linga) columbella (Lamarck), Turritella (Turritella)

cleevelyi Abbass, Turritella (Eichwaldiella) fouadi Abbass, Ficus

reticulatus (Lamarck), Conus (Lithoconus) mercati Brocchi,

Conus (Conolithus) melficus Desio, Bursa faizae Abbass,

Clypeaster marginatus Lamarck, Echinolampas amplus Fuchs,

Echinolampas plagiosomus Agassiz.


62

Remarks : This biozone represents the lowermost bio-unit in the

Miocene rocks in Gabal Homeira section. The interval of this

biozone is made up of fossiliferous sandy limestone. Its thickness

is reduced from 11.7m at its type section (Gabal Homeira) to 3.2m

at Gabal Gharra.

Age : Burdigalian.

3- Pecten (Flabellipecten) flabelliformis zone:




Limits : This biozone rests on Pecten (Pecten) ziziniae - Pecten

(Flabellipecten) flabelliformis barren interzone and underlies

Pecten (Pecten) cristato-costatus zone.

Fauna : In addition to the zonal species, this biounit contains

Parascutella stefaninii (Desio), Scutella ammonis Fuchs,

Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs,

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes, Anomia

burdigalensis Defrance, Chlamys scabrella Lamarck and

Clementia sp.

Boundaries : The lower boundary of this zone is defined by the first

appearance of the zonal species in addition to Anomia

burdigalensis Defrance, Chlamys scabrella Lamarck and

Clementia sp. The upper boundary is marked by the

disappearance of the zonal species, Anomia burdigalensis

Defrance and Parascutella stefaninii (Desio), .

Remarks : Pecten (Flabellipecten) flabelliformis zone is the youngest

zone in Gharra Formation, it ends the Lower Miocene succession

in Gabal Gharra and made up of calcareous sandstone.


63

Age : Burdigalian.

4- Pecten (Pecten) cristato-costatus zone:




Limits : Pecten (Pecten) cristato-costatus zone overlies Pecten

(Pecten) ziziniae - Pecten (Pecten) cristato-costatus barren

interzone and underlies Chlamys (Macrochlamis) sardoa zone.


characterized by the presence of Crassostrea frondosa (De Serres)


virleti Deshayes, Scutella ammonis Fuchs and Parascutella

stefaninii (Desio).

Boundaries : The lower boundary of this biozone is marked by the first

appearance of the zonal species and the first appearance of both ,

Scutella ammonis Fuchs and Parascutella stefaninii (Desio). The

upper boundary is defined by the disappearance of the previous

species in addition to the disappearance of Crassostrea frondosa

(De Serres) subsp. rohlfsi Fuchs, Alectryonella plicatula (Gmelin)

subsp. virleti Deshayes.

Remarks : Pecten (Pecten) cristato-costatus zone represents the

lowermost bio-unit in the Middle Miocene rocks in the study area.

The interval of the zone is made up of limestone and marl in its

type section while in Geneifa section there are a sandy shale bed

and another marl one while in Gharra section the interval is made

up entirly of limestones. The thickness of the zone changes from

32.7m in its type section at Gabal Homeira (the extreme West of


64

the study area) to 16.4m at Gabal Gharra and to 7.5m at Gabal

Geneifa (the extreme East of the study area).

Age : Langhian – Serravallian.

5- Chlamys (Macrochlamis) sardoa zone:



Thickness : 30m at its type section.

Limits : This biozone rests on Pecten (Pecten) cristato-costatus zone and

underlies Chlamys (Argopecten) submalvinae zone.

Fauna : In addition to the zonal species, the zone is characterized

by the presence of Arca (Anadara) grondica Mayer, Cardium sp.,

Gastrana laminosa (Sowerby), Gastrana sp., Clavagella sp.,

Lanistes (Lanistes) mahmoudi Abbass, Turritella (Turritella)

terebralis Lamarck, Ficus sp., Luria (Luria) salwae Abbass,

Oliva (Neocylindrus) wagihi Abbass, Oliva (Neocylindrus)

wagihi Abbass and Planorbis (Planorbis) nakanoi Abbass.

Boundaries : The lower boundary of this zone is characterized by the

first appearance of Arca (Anadara) grondica Mayer, Gastrana

laminosa (Sowerby), Gastrana sp., Clavagella sp., Lanistes

(Lanistes) mahmoudi Abbass, Luria (Luria) salwae Abbass,

Oliva (Neocylindrus) wagihi Abbass, Oliva (Neocylindrus)

wagihi Abbass and Planorbis (Planorbis) nakanoi Abbass, while

its upper boundary is marked by the first appearance of the zonal

species of the overlying zone, i.e. Chlamys (Argopecten)

submalvinae zone.

Remarks : Chlamys (Macrochlamis) sardoa biozone ends the

Miocene succession in Gabal Homeira and Gabal Geneifa while

it underlies the Chlamys (Argopecten) submalvinae zone in Gabal


65

Gharra section. The interval of this zone is made up of sandy

limestone, its thickness is reduced eastwards from 30m and

24.5m at Gabal Homeira and Gabal Gharra respectively to 18.5m

at Gabal Geneifa.


6- Chlamys (Argopecten) submalvinae zone:



Thickness : 30m at its type section.

Limits : This biozone ends the Miocene rocks in the study sections.

It overlies the Chlamys (Macrochlamis) sardoa zone

Fauna : In addition to the zonal species, this biozone characterized

by the presence of Chlamys senatoria Gmelin, Chlamys malvinae

(Dubois), Chlamys (Argopecten) macrotis (Sowerby),

Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs,

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes.

Boundaries : The lower boundary of this biounit is defined by the first

appearance of Chlamys (Argopecten) submalvinae

(Blanckenhorn) and Chlamys malvinae (Dubois).

Remarks : Chlamys (Argopecten) submalvinae biozone represents the

youngest zone in the Miocene rocks of the study area. It is well

defined in Gabal Gharra only and made up entirely of ckalk.



66

This page for fig. 34 ( Biostratigraphic chart of Gabal Geneifa section )


67

This page for fig. 35 ( Biostratigraphic chart of Gabal Gharra section )


68

This page for fig. 36 ( Biostratigraphic chart of Gabal Homeira section )


69

III.3 CHRONOSTRATIGRAPHY

The Miocene rocks in the Cairo-Suez area have been differentiated

into the Lower, Middle and Upper Miocene stages. This differentiation of

the Miocene series was accepted by the majority of authors who had dealt

with the Miocene in this part of the country as Sadek (1926 and 1959),

Said (1962), Abdalla and Abd El-Hady (1966 and 1971), Cherif and

Yehia (1977), El-Heiny (1982) and Abdel-Moneim (1992).

In this study, the characters and age assignment of these

chronostratigraphic units are discussed in the following:

III.3.1 The Early Miocene

It is represented by the Gharra Formation which is attributed to the

Burdigalian according to the presence of macro-invertebrate fossils with

Early Miocene affinity. Abd-Elmoneim (1992) mentioned that Pecten

(Pecten) fraasi Fuchs, Pecten (Pecten) ziziniae Blanckenhorn, Pecten

(Amussiopecten) burdigalensis Lamarck, Pecten (Flabellipecten)

flabelliformis (Brocchi) and Anomia burdigalensis Defrance are of Lower

Miocene affinity (Burdigalian). Ali (1973) assigned the age Burdigalian

depending on the presence of Echinolampus amplus Fuchs. Also, Hamza

(1992) assigned the same age (Burdigalian) insured by the presence of

Pecten (Pecten) ziziniae Blanckenhor.

In the present study, the sediments which are assigned to the Lower

Miocene measures 66.1m, 66.8m and 48.2m in Geneifa section, Gharra

section and Homeira section respectively. They consist mainly of clastic

beds (sandstone, shale, clay and marl) with frequent interbeds of

carbonate (limestones). The carbonates are fossiliferous to highly

fossiliferous containing bivalves, gastropods, echinoids, algae and

foraminifera. It overlies unconformably the Oligocene sands, gravels and


70

conglomerates. The upper limit of the Lower Miocene is marked with a

bed of sandstone which is unfossiliferous (in Gabal Geneifa and Gabal

Homeira) to fossiliferous (in Gabal Gharra).

The studied intervals which belong to the Early Miocene bear the

following fauna:

a- Geneifa section contains: Chlamys gentoni Fontannes, Crassostrea


(Gmelin) subsp. virleti Deshayes, Isognomon sp., Azorinus sp. and

Echinolampus amplus Fuchs.

b- Gharra section contains: Chlamys gentoni Fontannes, Pecten (Pecten)

fraasi Fuchs, Pecten (Pecten) ziziniae Blanckenhorn, Pecten

beudanti Basterot, Pecten (Oppenheimopecten) benedictus

(Lamarck), Pecten (Amussiopecten) burdigalensis Lamarck, Pecten

(Flabellipecten) flabelliformis (Brocchi), Anomia burdigalensis

Defrance, Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs,

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes, Cardium

sp., Lucina sp., Gastrana sp., Natica cf. millepunctata Lamarck,

Conus (Lithoconus) mercati Brocchi, Scutella ammonis Fuchs and

Parascutella stefaninii (Desio).

c- Homeira section contains: Chlamys malvinae (Dubois), Chlamys

(Aequipecten) scabriuscula (Matheron), Pecten fuchsi Fontannes,

Pecten beudanti Basterot, Pecten erythraensis Sowerby, Pecten

(Pecten) ziziniae Blanckenhorn, Pecten (Flabellipecten)

flabelliformis (Brocchi), Pecten (Oppenheimopecten) benedictus

(Lamarck), Anomia burdigalensis Defrance, Anomia (Anomia)

ephippium Linne, subsp. rugulosostriata Brocchi, Crassostrea


(Gmelin) subsp. virleti Deshayes, Cardium sp., Acanthocardia

(Acanthocardia) paucicostata (Sowerby), Linga (Linga)


71

columbella (Lamarck), Paphia (Callistotapes) vetula (Bastrot),

Turritella (Turritella) cleevelyi Abbass, Turritella (Eichwaldiella)

fouadi Abbass, Turritella (Turritella) terebralis Lamarck, Ficus

reticulatus Lamarck, Ficus sp., Bursa faizae Abbass, Conus

(Lithoconus) mercati Brocchi, Conus (Conolithus) melficus Desio,

Clypeaster marginatus Lamarck, Echinolampus amplus Fuchs and

Echinolampus plagiosomus Agassiz.

III.3.2 The Middle Miocene

According to Harland et al. (1982), the earlier part of the Langhian

belongs to the Early Miocene. Recently, the boundary between the Early

and Middle Miocene is placed at the base of the Langhian (Boggs, 1987;

Haq et al., 1987 and Abdel-Moneim, 1992). Butterlin (1988) and Sartorio

and Venturini (1988) mentioned that the extinction of the Lepidocyclinids

indicates the boundary between the Lower and the Middle Miocene. More

than one century ago, Deperet and Roman (1902) correlated the Middle

Miocene rocks with Pecten cristatocostatus Sacco which he had

recognized in the Cairo-Suez District with the Middle Miocene of

Austria.

Abd-Elmonein (1992) assigned the age Serravallian for some

Miocene exposures in the Cairo-Sukhna area depending on the presence

of a definite Middle Miocene (Serravallian) fauna which he had recorded

because they characterize this age in other African and European

countaries. Such fauna include: Chlamys (Argopecten) submalvinae

(Blanckenhorn), Pecten (Pecten) cristato-costatus Sacco, Anomia

(Anomia) ephippium Linne, subsp. rugulosostriata Brocchi,

Acanthocardia (Acanthocardia) paucicostata (Sowerby), Turritella

(Eichwaldiella) fouadi Abbass.


72

In the present study, the sedimentary intervals which are attributed

to the Middle Miocene measures 31m in Geneifa section, 74.5m in

Gharra section and 61.8m in Homeira section. They consist mainly of

limestones and chalky limestones with few interbeds of clay and marl.

The limestones and marls are fossiliferous to highly fossiliferous

containing bivalves, gastropods, echinoids, algae and foraminifera.

a- These intervals which are attributed to the Middle Miocene contain:

Chlamys radians (Nyst), Chlamys (Chlamys) costai (Fontannes),

Chlamys (Argopecten) macrotis (Sowerby), Chlamys

(Macrochlamis) sardoa Ugolini, Pecten (Pecten) cristato-costatus

Sacco, Pecten (Pecten) fraasi Fuchs, Pecten (Oppenheimopecten)

convexo-costatus Abich, Crassostrea frondosa (De Serres) subsp.

rohlfsi Fuchs, Alectryonella plicatula (Gmelin) subsp. virleti

Deshayes, Gastrana sp., Ampullina (Pseudamaura) macfaydeni

Abbass, Ampullina (Pseudamaura) maedai Abbass, Natica sp.,

Conus (Lithoconus) mercati Brocchi, Clypeaster intermedius

Desmoulins, Clypeaster marginatus Lamarck and Echinolampus

amplus Fuchs in Geneifa section.

b- Chlamys senatoria (Gmelin), Chlamys malvinae (Dubois), Chlamys

(Argopecten) macrotis (Sowerby), Chlamys (Argopecten)

submalvinae (Blanckenhorn), Chlamys (Macrochlamis) sardoa

Ugolini, Pecten (Pecten) cristato-costatus Sacco, Crassostrea


(Gmelin) subsp. virleti Deshayes, Cardium sp., Paphia

(Callistotapes) vetula (Bastrot), Gastrana laminosa (Sowerby),

Callista (Costacallista) erycina (Linne), Diplodonta sp., Gari sp.,

Lutraria sp., Turritella (Turritella) terebralis Lamarck, Clypeaster

marginatus Lamarck, Clypeaster intermedius Desmoulins, Scutella

ammonis Fuchs and Echinolampus amplus Fuchs in Gharra section.


73

c- Arca (Anadara) grondica Mayer, Chlamys (Macrochlamis) sardoa

Ugolini, Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs,

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes, Cardium

sp., Lucina sp., Gastrana sp., Gastrana laminosa (Sowerby),

Clavagella sp., Lanistes (Lanistes) mahmoudai Abbass, Turritella

(Turritella) terebralis Lamarck, Luria (Luria) salwae Abbass,

Ficus sp., Oliva (Neocyclindrus) wagihi Abbass, Planorbis

(Planorbis) nakanoi Abbass, Scutella ammonis Fuchs and

Parascutella stefaninii (Desio) in Homeira section.

74 Chapter IV Systematic paleontology

CHAPTER IV

SYSTEMATIC PALEONTOLOGY

IV.1 Introduction:

The studied macrofossils include Bivalvia, Gastropoda and

Echinodermata. This chapter deals with the taxonomy, illustration and

description of the collected fauna from the studied sections.

The terminology and systematic classification of 62 species

belonging to 34 genera and 26 families were followed according to the

general criteria of the identification of macrofauna after many authors,

among them Deperet and Roman (1902-1912), Cossmann and Peyrot

(1909-1924), Roger (1939), Moore (1969), Davies (1971), Cox (1927),

Ali (1975), Abbass (1977), and Murray (1985). Table 2 illustrates the

ages assigned by previous authors to the recorded fauna in some parts of

the world. All the collected materials are deposited at the Geology

Department, Faculty of Science, Zagazig University.

IV.2 Systematic Description:

IV.2.1 Phylum Mollusca:

Phylum: Mollusca Cuvier, 1795

Class: Bivalvia Linne, 1758

Subclass: Pteriomorphia Beurlen, 1944

Order: Arcoida Stoliczka, 1871

Superfamily: Arcacea Lamarck, 1809

Family: Arcidae Lamarck, 1809

Subfamily: Arcinae Lamarck, 1809

Genus: Arca Linne, 1758

Type species: Arca noae; subsequent designation Schmidt, 1818.


Arca (Anadara) grondica Mayer

(pl. 1, fig. 1)

1914 Arca (Anadara) grondica Mayer.; Cossmann and Peyrot, p. 158, pl.

7, figs. 34-37; pl. 8, figs. 1-2.

1994 Arca (Anadara) grondica Mayer.; El-Safori, pl. 6, figs. 8-9.

Material: One moderately preserved internal mold.

Dimensions: Mold : Length (1) 11mm.

: Height (1) 7mm.

Description: Small size, equivalve, inequilateral, elongate,

subtrapezoidal to subrectangular, longer than high, truncated; cardinal

area broad, straight; peak prosogyrate.

Occurrence: This species appears in Gabal Homeira section, bed no. 19.

Distribution: This species was recorded from the Neogene of Aquitan

Province (Cossmann and Peyrot, 1914) and from the Miocene of the

western side of the Gulf of Suez (El Safori, 1994).

Age: Langhian - Serravallian.

Order: Pterioida Newell, 1965

Suborder: Pteriina Newell, 1965

Superfamily: Pteriacea Gray, 1847

Family: Isognomonidae Wooding, 1925

Genus: Isognomon Lightfoot, 1786

Type species: Ostreab perna; Linné, 1767

Isognomon sp.

(Pl. 1, fig. 2)

Material: Moderately preserved one internal mold.


Dimensions: Mold : Length (1) 61mm.

: Height (1) 111mm.

Description: Internal mold of moderate size, dorso-ventrally elongated,

rhomboidal or rectangular in shape; anterior and posterior margins nearly

straight, ventral margin subrounded; subequivalve; inequilateral;

ligamental area broad, flate, with numerous and regular arranged

ligamental grooves showing deep furrows between ligamental grooves;

each valve have two accessory muscle scars at the dorsal part.

Occurrence: This species occurs in Gabal Geneifa section, bed no. 5.

Age: Burdigalian.

Superfamily: Pectinacea Rafinesque, 1815

Family: Pectinidae Rafinesque, 1815

Genus: Chlamys Röding, 1798 (non Koch, 1801)

Type species: Pecten islandicus Müller, 1776; subsequent designation

Herrmannsen, 1847

Chlamys gentoni Fontannes

(pl. 1, figs. 3a, b)

1939 Chlamys gentoni Fontannes; Roger, p. 142, pl. 16, figs. 17a, b.

1976 Chlamys gentoni Fontannes; Metwally, p. 139, pl. 5, figs. 5a, b.

Material: Six left valves.

Dimensions: LV: L (6) 11.5mm, (10-13mm)

: H (6) 12.3mm, (10.5-14mm)

Description: Shell of small size, moderately convex, ovally triangular,

subequilateral; orthogyrate; umbonal region feebly convex; lateral sides

relatively long, anterior one slightly shorter, posterior one feebly


concave; crenulated, subrounded ventral margin, auricles of left valve

are triangular with 5-6 fine scaly costules of which the first four are

more prominent; valve ornamented with 18-20 rounded costae, separated

by equally concave interspaces; costae ornamented with 2-3 very fine

regularly spaced scaly costules more developed near margin.

Occurrence: Members of this species have been recorded in Gabal

Geneifa section, beds no. 5; Gabal Gharra section, in beds no. 6 and 8.

Distribution: This species was known from the Neogene of Europe

(Roger, 1939); in Egypt, it was recorded by Metwally (1976) from

Salum area, Wadi Umm Ashtan section.

Age: Burdigalian.

Chlamys malvinae (Dubois)


1883 Pecten malvinae (Dubois); Fuchs, p. 59, pl. 21, fig. 3.

1939 Chlamys malvinae (Dubois); Roger, p. 145, pl. 18, figs. 3, 4.

1968 Chlamys malvinae (Dubois); El-Gamal, p. 148, pl, 14, fig. 3.

1976 Chlamys malvinae (Dubois); Metwally, p. 147, pl. 6, fig. 4.

Material: Two right valves.

Dimensions: RV: L (2) 32mm, (32mm).

: H (2) 31.5mm, (31-32mm).

Description: Right valve of moderate size, convex, ovally triangular,

inequilateral; orthogyrate, umbonal region convex; ventral margin

rounded; lateral sides short, posterior one slightly longer and inclined

with relatively wide angle, anterior one short, slightly concave; auricles

unequal, anterior one wing-shapped, with acute, deep byssal notch,


ornamented with 6 costules; posterior one triangular with 7-8 fine

costules; cardinal line straight; surface ornamented with 22-24 costae,

subrounded in cross section, separated by slightly narrow, flat concave

interspaces; costae with 4-5 scaley costules; interspaces with 2-3 fine

scaley costules.

Occurrence: This species is recorded here in Gabal Gharra section, bed

no. 15; Gabal Homeira section, bed no. 11.

Distribution: This species was recoded from the Neogene of Europe

(Roger, 1939); in Egypt, it was recorded by El-Gamal (1968) and

Metwally (1976).

Age: Early - Middle Miocene.

Chlamys radians (Nyst)


1939 Chlamys radians (Nyst); Roger, p. 134, pl. 16, figs. 8-12; pl. 17,

fig. 9.

1976 Chlamys radians (Nyst); Metwally, p. 153, pl. 7, fig. 4.

Material: Four right valves.

Dimensions: RV: L (4) 26.6mm, (22-36mm)

: H (4) 26.1mm, (21.5-35mm)

Description: Right valve of small to moderate size, ovally triangular,

feebly convex, unequilateral; lateral sides incurved, anterior one shorter;

undulating interal margin; auricles subequal, anterior one more

developed, wing-shapped with 6 fine radial scaley costules, posterior one

triangular with 8 fine costules; surface crossed by concentric lamellae,

ornamented with 17-19 high costae, radiated, rounded, separated by


rather narrow, flat intercostal spaces which occupied by 1-2 fine

costules; inner side show rectangular costae corresponding to that on

the outer surface, separated by short, rounded interspaces disappearing

toward the umbonal region; the muscle scar is subrounded, deep.

Occurrence: Individuals of this species are recorded only in Gabal

Geneifa section from beds no. 9 and 11.

Distribution: This species was described from the Neogene of Europe

(Roger, 1939); in Egypt, Metwally (1976) recorded it from Salum area.

Age: Langhian – Serravallian.

Chlamys scabrella Lamarck

(pl. 1, fig. 6)

1939 Chlamys scabrella Lamarck; Roger, p. 104, pl. 12, figs. 8, 9, 9a,

10, 10a; pl. 13, figs. 3-13.

1972 Chlamys scabrella Lamarck; Hamza, p. 93, pl. 2, figs. 5, 5a, 5b;

pl. 3, figs. 1, 1a, 1b.

1976 Chlamys scabrella Lamarck; Metwally, p. 157, pl. 7, fig. 6; pl. 8,

fig. 1.

Material: One complete shell.

Dimensions: RV: L (1) 37mm.

: H (1) 38mm.

LV: L (1) 37mm.

: H (1) 38mm.

Description: Shell of moderate size, suborbicular to subtriangular;

equivalve, equally convex, subequilateral; lateral sides nearly equally

inclined, anterior side shorter, straight, posterior side longer, slightly


incurved, concave; subrounded ventral margin; orthogyrate, slightly

incurved; umbonal region feebly convex; auricles unequal, almost flat;

anterior one of the right valve longer than posterior one, wing-shapped,

ornamented with 5 slightly strong costules; posterior one of the right

valve is triangular, with 8 fine radial costules; the two auricles of the left

valve are nearly equal, triangular, ornamented with 8 fine costules;

cardinal line straight; surface ornamented with 16-18 costae, equal,

rounded in cross section, separated by equally wide, concave, intercostal

spaces; costae with 3 secondary costules; the intercostal spaces with 2

fine costules.

Occurrence: Occurs in Gabal Gharra section, beds no. 12 and 13.

Distribution: Chlamys scabrella was recoded from the Neogene of

Europe (Roger, 1939) In Egypt, it is known in the Pliocene (Hamza,

1972) and in the Neogene of Salum area (Metwally, 1976).

Age: Early – Middle Miocene.

Chlamys senatoria Gmelin


1927 Chlamys senatoria Gmelin; Cox, p. 45, pl. 7, figs. 1-3.

1974 Chlamys senatoria Gmelin; Ghonima, p. 166, pl. 12, figs. 7, 8.

1976 Chlamys senatoria Gmelin; Metwally, p. 162, pl. 8, figs. 3a, b.

Material: Two left valves.

Dimensions: LV: L (2) 28.2mm, (24.5-32mm).

: H (2) 27mm, (25-29mm).

Description: Left valve of moderate size, convex, suborbicular, with

remarkably truncated posterior margin; inequilateral, posterior longer;


auricles unequal, posterior one longer; ventral margin nearly rounded;

cardinal line straight; costae 19-21, rounded with 3-4 threads-like

costules separated by rather narrow, flate interspaces with 2-3 threads-

like costules.

Occurrence: Specimens of this species have encountered only from

beds no. 13 and 15 in Gabal Gharra section.

Distribution: Cox (1927) mentioned that Chlamys senatoria is common

in the Lower Miocene of Zinzibar. In Egypt, it was recrded from Salum

area (Ghonima, 1974), and described by Metwally (1976) from Matruh

area as Karpatian (uppermost of Lower Miocene) and who recorded it

also from Wadi Umm Ashtan section in Salum area.


Subgenus: C. Chlamys Röding, 1798

Chlamys (Chlamys) costai (Fontannes, 1884)


1939 Chlamys costai (Fontannes); Roger, p. 160, pl. 22, fig. 8; pl. 23,

fig. 6.

1966 Chlamys costai (Fontannes); Cherif, pl. 11, fig. 2.

1972 Chlamys costai (Fontannes); Cherif, p. 100, pl. 5, fig. 12.

1976 Chlamys costai (Fontannes); Metwally, p. 134, pl. 5, fig. 2.

1992 Chlamys (Chlamys) costai (Fontannes); Abdel-Moneim, p. 101, pl.

2, fig. 2.

Material: Three right valves.

Dimensions: RV: L (3) 24.3mm, (17-30mm).

: H (3) 25.3mm, (19-29.5mm).


Description: Specimen of medium size, convex, suborbicular to

subtriangular, subequilateral, orthogyrate; umbonal region slightly

convex; ventral margin rounded, crenulated; lateral sides nearly straight,

posterior one slightly longer; auricles relatively large, anterior auricle of

right valve is wing-shaped, with 6 fine costules; cardinal line straight;

triangular resilial pit; surface ornamented with 19-21 costae which are

rounded, divided to 2 fine scaly costules in the umbonal area increase to

3-4 near the ventral margin; costae are separated by slightly smaller

interspaces, divided by 2 scaly costules.

Occurrence: This species is recorded in Gabal Geneifa section, beds no.

9 and 11.

Distribution: Roger (1939) mentioned that the Chlamys costai

(Fontannes) is present abundantly in the Burdigalian of Portugal and

rarely in the same stage in the Vienna Basin. Also, he reported the

presence of this species in the Helvetian or Tortonian of France. In

Egypt, Cherif (1966 and 1972) recorded it from the Miocene of the Sadat

area; Metwally (1976) recorded it from the Vindobonian of Salum area;

while Abdel-Moneim (1992) recorded it from the Sadat Formation (Late

Burdigalian) in the Sadat area.


Subgenus: Chlamys (Aequipecten) Fischer, 1886

Ttype species: Ostrea opercularis Linné, 1758

Chlamys (Aequipecten) scabriuscula (Matheron, 1842)

(pl. 2, fig. 1)

1939 Chlamys scabriuscula (Matheron); Roger, p. 58, pl. 6.

1976 Chlamys scabriuscula (Matheron); Metwally, p. 160, pl. 8, fig. 2.


1992 Chlamys (Aequipecten) scabriuscula (Matheron); Abdel-Moneim,

p. 102, pl. 2, fig. 4a, b.

Material: One right valve.


: H (1) 58mm.

Description: Right valve of moderate size, suborbicular to orbicular,

subequilateral, highly convex; orthogyrate, incurved; umbonal region

highly convex; lateral sides concave, posterior one slightly longer;

ventral margin rounded, undulating; auricles equal, anterior one wing-

shapped, with 4 well developed costules, posterior one triangular with 6

fine costules; cardinal line straight; byssal notch acute, deep below

anterior auricle; surface ornamented with 21 rounded costae, sharp near

umbonal region, separated by rather narrow concave interspaces, costae

with 6 fine radial costules, interspaces with 3 fine costules; surface

crossed by regularly spaced concentric lamellae increasing in number

near ventral margin.

Occurrence: The collected specimenof this species was found in bed no.

11, in Gabal Homeira section.

Distribution: Roger (1939) reported that Chlamys scabriuscula is a

Helvetian and Tortonian form, being recorded from France, North and

Central Italy and Sardinia. In Egypt, Metwally (1976) recorded it from

the Vindobonian of Matruh area, while Abdel-Moneim (1992) recorded

it in the Serravallian of Sadat area, commonly in the Hommath

Formation.

Age: Burdigalian.

Subgenus: Chlamys (Argopecten) Monterosato, 1890

Ttype species: Pecten solidulus Reeve, 1853; original designation


Chlamys (Argopecten) macrotis (Sowerby, 1847)


1939 Chlamys macrotis (Sowerby); Roger, p. 114, pl. 14, figs. 7-10; pl.

15, figs. 7, 8.

1968 Chlamys macrotis (Sowerby); El-Gamal, p. 143, pl. 14, fig. 13.

1976 Chlamys macrotis (Sowerby); Metwally, p. 145, pl. 6, figs. 2a-d.

1992 Chlamys (Argopecten) macrotis (Sowerby); Abdel-Moneim, p.

103, pl. 2, fig. 5.

1999 Chlamys macrotis (Sowerby); El-Shazly and Saber, p. 325, pl. 2,

fig. 3.

Material: Three left valves.

Dimensions: LV: L (3) 20.3mm, (14-29mm).

: H (3) 21.3mm, (15.5-29mm).

Description: Shell of moderate size, subequivalve, inequilateral,

suborbicular, extended posteriorly; left valve more convex; orthogyrate,

incurved; umbonal region feebly convex; lateral sides unequal, slightly

concave, anterior one shorter, straight, posterior one longer, highly

curved; undulating, subrounded ventral margin; auricles unequal,

relatively large, the two auricles of left valve subtriangular, with

numerus fine radial costules; surface ornamented with 19-21 equally

salinet subrounded costae with 2-3 scaley costules (the main one more

strong), separated by rather narrow concave interspaces; interspaces with

the same number of costules.

Occurrence: This species is recorded here in Gabal Geneifa section,

beds no. 9 and 11; Gabal Gharra section, beds no. 13 and 15.


Distribution: Chlamys macrotis is present in the Tortonian of the

Vienna Basin and other European localitis and in the Atlantic Province

as in Portugal (Roger, 1939). In Egypt, it was recorded from the Salum

and Matruh areas by El-Gamal (1968) and Metwally (1976); from the

Sadat and Hommath Formations (Late Burdigalian and Serravallian) in

the south eastern part of the Cairo-Suez area (Suez-Sukhna) by Abdel-

Moneim (1992); and from the Marine Miocene sediments of Gabal

Homeira, Cairo-Suez District by El-Shazly and Saber (1999).


Chlamys (Argopecten) submalvinae (Blanckenhorn, 1901)


1901 Pecten sub-malvinae Blanckenhorn, p. 120, pl. 2, fig. 5.

1921 Chlamys sub-malvinae Blanckenhorn; Stefanini, p. 137

1929 Chlamys sub-malvinae (Blanckenhorn); Desio, p. 219, pl. 32, fig. 8.

1939 Chlamys sub-malvinae Blanckenhorn; Roger, p. 118, pl. 15, figs. 5,

6; pl. 16, figs. 13-16.

1955 Chlamys sub-malvinae (Blanckenhorn); Said and Yallouze, p. 68,

pl. 3, fig. 12.

1966 Chlamys sub-malvinae (Blanckenhorn); Cherif, pl. 5, fig. 4.

1966 Chlamys sub-malvinae (Blanckenhorn); Hamam, pl. 9, fig. 12.

1968 Chlamys sub-malvinae (Blanckenhorn); El-Gamal, p. 132, pl. 15,

figs. 2, 3, 10.

1972 Chlamys sub-malvinae (Blanckenhorn); Cherif, p. 99, pl. 5, fig. 14.

1976 Chlamys sub-malvinae (Blanckenhorn); Metwally, p. 163, pl. 8,

figs. 4a-c.


1980 Chlamys (Aequipecten) sub-malvinae (Blanckenhorn); Abed and

Metwally, p. 307, pl. 4, figs. 4a-c.

1987 Chlamys sub-malvinae (Blanckenhorn); El-Shazly, p. 184, pl. 1,

figs. 5a-c.

1989 Chlamys (Aequipecten) sub-malvinae (Blanckenhorn); El-Bedewy,

p. 197, pl. 8, fig. 6.

1992 Chlamys (Argopecten) submalvinae (Blanckenhorn); Abdel-

Moneim, p. 104, pl. 2, fig. 6.

1999 Chlamys sub-malvinae (Blanckenhorn); El-Shazly and Saber, p.

325, pl. 2, figs. 2, 7.

Material: Ten right valves and eleven left valves.

Dimensions: RV: L (10) 30.9mm, (13-48mm).

: H (10) 30.5mm, (14.5-45mm).

LV: L (11) 36.1mm, (11-47mm).

: H (11) 37mm, (18-49mm).

Description: Shell of small to medium size, equivalve, inequilateral,

valves moderately convex; right valve more convex and ovally

triangular; orthogyrate; umbonal region convex; lateral sides unequal,

anterior one nearly straight, shorter; ventral margin subrounded; auricles

unequal, feebly descending along the lateral margin; anterior auricle of

the right valve wing-shapped, with 6 costules; posterior one of the right

valve is rectangular, with 5-6 fine threads-like costules; right valve with

acute byssal notch, deep below the anterior auricle; auricles of the left

valve triangular with 5-6 fine costules, the anterior one with rounded

margin; cardinal line straight; with large, triangular resilial pit; one pair

of cardinal crura; surface ornamented with 19 rounded costae, the

median is dominant, separated by rather narrow concave interspaces,


costae acute near the umbo then become low and wider near the ventral

margin, costae with fine radial scaley costules increase by intercalation

near the ventral margin; interspaces between the costae are with 2 scaley

costules.

Occurrence: This species is recorded in Gabal Gharra section, bed no. 15.

Remarks: Chlamys sub-malvinae (Blanckenhorn) differs from Chlamys

malvinae (Dubois) in having less convexity and less number of ribs. On

the other hand, it has more ribs and more dense ornamentation than

Chlamys scabrella (Lamarck).

Distribution: This species was recrded from the Miocene of Italy

(Stefanini, 1921); from many Mediterranean regions such as Egypt,

Syria and Cyprus (Roger, 1939). In Egypt, it was recorded from the

Miocene by Blanckenhorn (1901); From the Miocene of the Western

Desert by (Desio, 1929), (El-Gamal, 1968), (Metwally, 1976) and (Abed

and Metwally, 1980); from the Cairo–Suez district by Said and Yallouze

(1955), Hamam (1966), El-Bedewy (1989) and El-Shazly and Saber

(1999); from Sinai by El-Shazly (1987) and from the Sadat area by

Cherif (1966 and 1972) and Abdel-Moneim (1992).


Subgenus: Chlamys (Macrochlamis) Sacco, 1897

Ttype species: Ostrea latissima Brocchi, 1814, original designation

Chlamys (Macrochlamis) sardoa Ugolini, 1906


1906 Chlamys (Flaxopecten) sardous Ugolini, p. 86, Pl. 10, fig. 5; pl. 12,

fig. 1.

1939 Chlamys sardoa Ugolini; Roger, p. 46, pl. 19, fig. 3a.


1976 Chlamys sardoa Ugolini; Metwally, p. 155, pl. 7, figs. 5a, b.

Material: One double-valved shell, one right valve and one mold for a

right valve.


: H (1) 50mm.

LV: L (1) 63mm.

: H (1) 50mm.

Description: Shell of medium size, subtriangular, length is slightly

larger than height, subequilateral, valves moderately convex, subequal

lateral sides, posterior one longer, slightly curved, feebly concave;

orthogyrate, umbonal region convex; hinge line straight; anterior auricle

subtriangular to wing-shapped, ornamented by fine lamellae which

condensed and become larger at the margin of the auricle and show well

formed radial costulations; posterior auricle is right angled triangle,

ornamented by fine lamellae which condensed and become larger at the

margin of the auricle and show well formed radial costulations. Right

valve convex, with 9 ribs, 5 of which are promainant, rectangular in

cross-section, interspaces between ribs slightly less than the rib width,

ribs ornamented with 3-4 riblets. Left valve convex, contain 8 ribs, 4 of

which are promainant, ribs and riblets are with nodes which forming 4

concentric arcs, interspaces are slightly less than the rib width.

Occurrence: Members of this species have been recorded in Gabal

Geneifa section, beds no. 12 and 13; Gabal Homeira section, bed no. 19;


Remarks: Ugolini (1906) referred this species to the subgenus Chlamys

(Flexopecten), but this subgenus is characterized by larger right valve

than left one which is not the case of Chlamys sardoa. Also, Chlamys


(Flexopecten) is characterized by several plicate ribs, but in Chlamys

sardoa the plicate ribs are few (about 4-5). In the present study, the

recorded specimens are referred to Chlamys (Macrochlamis) as this

subgenus is characterized by more convex left valve and entire surface

covered with radial striae.

Distribution: Roger (1939) mentioned that this species was found by

Ugolini (1906) in the Upper Miocene of Sardenia and in the Upper

Burdigalian to Langhian of Gabal Geneifa of Egypt by Blanckenhorn

(1901). As this species is an Indo-Pacific one, so Roger (op. cit.)

considered the form of Gabal Geneifa as an intermediate one. Metwally

(1976) recorded it in Salum area, Wadi Umm Ashtan section to indicate

Upper Burdigalian.


Genus: Pecten Müller, 1776

Type species: Ostrea maximal Linné, 1758; subsequent designation

Schmidt, 1818

Pecten beudanti Basterot


1902 Pecten beudanti Basterot; Depéret and Roman, p. 19, pl. 2, figs. 1,

1a, 2.

1914 Pecten beudanti Basterot; Cossmann and Peyrot, p. 274, pl. 13,

figs. 8-11

Material: Five right valve and four left valves.

Dimentions: RV: L (5) 69mm, (61-75mm).

: H (5) 65.5mm, (58-73mm.


LV: L (4) 76mm, (60-88mm).

: H (4) 72mm, (57-86mm).

Dscription: Shell of medium to large size, ovally triangular in shape,

subequilateral; right valve convex; umbonal region inflatted; ventral

margin rounded, forming half circle; very slightly incurved lateral sides;

auricles incurved, subequal; anterior one very slightly smaller, wing-

shapped, with 5-7 low radial costules; posterior one right angle triangle,

with 5-7 low radial costules; the two auricles crossed by very fine closed

space concentric lamellae; costae 15 radial, trapizoidal, 12 of them

strong, equal, become broad and slightly flatened near the ventral

margin; the lateral costae feebly and narrow; costae separated by slightly

narrow, flaty, rounded interspaces; surface crossed by fine regular closed

space concentric lamellae; inner side characterized by rectangular costae

running to about half valve; shallow subrounded muscle scar; two pair of

cardinal crura; resilial pit subtriangular, moderate size; cardinal line

slightly curved. Left valve fan-shaped, slightly convex; lateral sides

concave, feebly incurved, have radial costulation; auricles internally

curved, triangular in shape, having 4-5 radial costules crossed by very

fine concentric lamellae; costae 11 slightly weak at the umbonal region,

become strong at the ventral margin, trapizoidal in shape, nearly equal;

surface crossed by very fine concentric lamellae; inner surface with

crenulated margin extends nearly to the lower half of the valve;

subrounded muscle scar; cardinal region rectangular; cardinal line nearly

straight; subtriangular resilial pit; have two pair of cardinal crura.

Occurrence: This species is present in Gabal Homeira section, bed no.

13; Gabal Gharra section, bed no. 10 which is mostly crowded by its

specimens.


Distribution: Pecten beudanti was recrded from the Miocene of the

Mediterranean Basin by Depéret and Roman (1902) and Cossmann and

Peyrot (1914).

Age: Burdigalian.

Pecten erythraensis Sowerby


1902 Pecten erythraensis Sowerby; Depéret and Roman, p. 36, pl. 4,

figs. 6, 7.

1972 Pecten erythraensis Sowerby; Hamza, p. 89, pl. 2, figs. 3, 3a.

1976 Pecten erythraensis Sowerby; Metwally, p. 112, pl. 2, fig. 2.

Material: Two left valves.

Dimentions: LV: L (2) 49.5mm, (48-51mm).

: H (2) 47mm, (46-48mm).

Description: Left valve of medium size, semi-circular in outline,

equilateral, fan-shaped, slightly concave especially at the umbonal

region; lateral sides concave, feebly incurved; auricles internally curved,

right angled triangular in shape with 4-5 radial costules crossed by very

fine concentric lamellae; 11 costae, very weak at the umbonal region,

strong near the ventral margin; two less dominant costules on each

lateral side; surface crossed by very fine concentric lamellae; crenulated

internal margin; well formed subrounded muscle scar; cardinal line

straight; cardinal region rectangular; small triangular resilial pit.

Occurrence: This species is recorded in Gabal Homeira section, bed

no. 13.


Remarks: Pecten erythraensis Sowerby, can be easily differentiated

from Pecten benedictus (Lamarck) by its highly convex umbonal

region, also the costae are more strong and well formed at the ventral

margin.

Distribution: Depéret and Roman (1902) recrded this species from the

Neogene of Europe. In Egypt, it was recorded from the Pliocene (Hamza,

1972) and from the Neogene of Salum-Matruh areas (Metwally, 1976).

Age: Burdigalian.

Pecten fuchsi Fontannes


1902 Pecten fuchsi Fontannes; Depéret and Roman, p. 13, pl. 1, figs. 6-7.

1939 Pecten fuchsi Fontannes; Roger, p. 238.

1976 Pecten fuchsi Fontannes; Metwally, p. 115, pl. 2, figs. 3a, 3b.

Material: Three left valves.

Dimentions: LV: L (3) 36.3mm, (35-37mm).

: H (3) 35.1mm, (34.5-36mm).

Description: Left valve of moderate size, orbicular to suborbicular,

nearly flat; umbonal region slightly concave; lateral sides slightly

curved; auricles inequal, anterior longer, each ornamented with 5

concentric lamellae; cardinal line straight; resilial pit triangular; surface

ornamented with 18 well developed radial ribs as well as about four

small ones on the anterior and posterior lateral sides.

Occurrence: This species is recorded only in Gabal Homeira section,

beds no. 11, 13.


Distribution: Pecten fuchsi Fontannes was recorded from the Miocene

of the Mediterranean Basin (Depéret and Roman, 1902). It is a frequent

Miocene species in the area of West Mediterranean Basin, the Lower

Miocene of Italy, Helvatian of Spain, Burdigalian of Tunisia and Austria,

and the Vindobonian of Syria (Roger, 1939). In Egypt, it was recorded

from the Miocene of Gabal Tanka (Sinai) by Roger (1939) and the

Burdigalian of the Salum area by Metwally (1976).

Age: Burdigalian.

Subgenus: Pcten (Pecten) Müller, 1776

Pecten (Pecten) cristato-costatus Sacco, 1897


1902 Pecten cristato-costatus Sacco; Depért and Roman, p. 14, pl. 1,

figs. 11, 12.

1908 Pecten cristato-costatus Sacco; Ugolini, p. 72, pl. 24, figs. 6, 7

1929 Pecten cristato-costatus Sacco; Desio, p. 228, pl. 33, fig. 8.

1955 Pecten cristato-costatus Sacco; Said and Yellouze, p. 68, pl. 3,

figs. 4, 7.

1966 Pecten cristato-costatus Sacco; Cherif, pl. 11, figs. 7, 9.

1966 Pecten cristato-costatus Sacco; Hamam, pl. 9, fig. 11.

1972 Pecten cristato-costatus Sacco; Cherif, p. 98, pl. 6, figs. 22, 24.

1976 Pecten cristatocostatus Sacco; Metwally, p. 111, pl. 2, figs. 1a, b, c.

1989 Pecten (Pecten) cristatocostatus Sacco; El-Bedewy, p. 205, pl. 9,

fig. 4.

1992 Pecten (Pecten) cristato-costatus Sacco; Abdel-Moneim, p. 108, pl.

3, fig. 2.


Material: Two right valves and four left valves.

Dimensions: RV: L (2) 43mm, (42-44mm).

: H (2) 41mm, (40-42mm).

LV: L (4) 22.6mm, (20.5-25mm).

: H (4) 23.1mm, (19-27mm).

Description: Right valve of medium size, suborbicular, convex,

subequilateral; hinge line straight; umbo orthogyrate, overlaps the hinge;

umbonal region strongly convex; lateral sides curved; auricles equal,

triangular; with 5-7 weak radial costules, crossed by concentric lamellae;

surface ornamented by 19-20 strong radial costae, triangular in cross-

section, separated by interspaces lesser than their width, flat base;

concentric lamellae appear on the ribs as well as on the interspaces. Left

valve orbicular to suborbicular, nearly flat; umbonal region slightly

concave; lateral sides slightly curved; auricles unequal, anterior longer;

auricles ornamented with 5 concentric lamellae; surface onamented by

18-20 costae, median ones of which are more prominent, separated by

rather narrow, flat intervals; cardinal line straight; resilial pit triangular.

Occurrence: This species occurs in Gabal Geneifa section , beds no. 9

and 11; Gabal Gharra section, bed no. 13; Gabal Homeira section, beds

no. 16, 17 and 18.

Remarks: According to Depéret and Roman (1902, p. 14-15), the name

Pecten acuticostatus had been occupied by a Jurassic species prior to the

Miocene species. Thus, Pecten cristato-costatus replaces this name for

the Miocene species. But till now, many authors use the specific part of

the name (acuticostatus) which is absolutely wrong. Here, the

synonomys of both names are included in the systematic table of the

species but the perfect name is followed.


Distribution: The present species was recrded from the Neogene of

Europe by Depéret and Roman (1902) and from the Miocene of Europe

by Ugolini (1906). Regarding the Egyptian localities, it was recorded

from the Miocene rocks at many locations, For example: North Western

Desert (Desio, 1929) and (Metwally, 1976), Cairo–Suez district (Said

and Yellouze, 1955), (Hamam, 1966) and (El-Bedewy, 1989), Sadat area

(Cherif, 1966, 1972) and (Abdel-Moneim, 1992).


Pecten (Pecten) fraasi Fuchs, 1883


1883 Pecten Fraasi Fuchs; p. 41, pl (21) 16, figs. 7, 8.

1902 Pecten Fraasi Fuchs; Depéret and Roman, p. 26, pl. 2, figs. 7-9.

1992 Pecten Fraasi Fuchs; Abdel-Moneim, p. 110, pl. 3, fig. 3.

Material: Two right valves and four left valves.

Dimensions: RV: L (2) 54mm, (48-60mm).

: H (2) 52mm, (47-57mm).

LV: L (4) 53.2mm, (47-60mm).

: H (4) 50.5mm, (44-58mm).

Description: Shell of medium size, semi circular in shape,

subequilateral, umbo orthogyral, nearly median. Right valve convex;

umbonal region inflated, convex; very slightly incurved lateral sides;

auricles incurved, subequal, anterior one very slightly smaller, wing-

shapped, with 4-5 low radial costules; posterior one right angled triangle,

with 4-5 low radial costules; cardinal line very slightly incurved; costae

15-16 radial, larger than interspaces, 12 of them are strong and equal,


separated by rounded interspaces; surface crossed by fine regular closed

space concentric lamellae. Left valve fan-shapped, flate to very slightly

concave; lateral sides concave, feebly incurved; rectangular cardinal

region, cardinal line nearly straight; subtriangular resilial pit; having two

pairs of cardinal crura; auricles triangular in shape, having 4-5 radial

costules, crossed by fine concentric lamellae; costae 11 slightly weak at

the umbonal region, become strong near the ventral margin, trapizoidal

in shape; surface crossed with very fine concentric lamellae; inner

surface with crenulated margin extends nearly to the lower half of the

valve; subrounded muscle scar; cardinal region rectangular, cardinal line

nearly straight; subtriangular resilial pit; with two pairs of cardinal crura.

Occurrence: This species appears in Gabal Geneifa section, beds no. 9

and 11; Gabal Gharra section, bed no. 10.

Distribution: Fuchs (1883) described Pecten Fraasi Fuchs from the

Miocene rocks of Gabal Geneifa. Also, it was recorded from the

Helvetian rocks (Middle Miocene) of France by Depéret and Roman

(1902), these two authers mentioned that this species occurs in the

terminal part of the Egyptian Burdigalian. In Egypt, Abdel-Moneim

(1992) recorded this species from the Upper Burdigalian of Sadat

Formation in the Sadat area.

Age: Early - Middle Miocene

Pecten (Pecten) ziziniae Blanckenhorn, 1901


1901 Pecten ziziniae Blanckenhorn; p. 132.

1902 Pecten ziziniae Blanckenhorn; Depért and Roman, p. 80, pl. 9,

figs. 3-5.


1955 Pecten ziziniae Blanckenhorn; Said and Yellouze, p. 69, pl. 3, fig. 9.

1966 Pecten ziziniae Blanckenhorn; Cherif, p. 162, pl. 2, figs. 1a, 1b, 8.

1966 Pecten ziziniae Blanckenhorn; Hamam, pl. 9, figs. 8, 10.

1972 Pecten ziziniae Blanckenhorn; Cherif, p. 97, pl. 5, fig. 11; pl. G,

fig. 23.

1976 Pecten ziziniae Blanckenhorn; Metwally, p. 120, pl. 3, figs. 3a, b, c.

1987 Pecten ziziniae Blanckenhorn; El-Shazly, p. 180, pl. 1, fig. 7.

1989 Pecten (Flabellipecten) ziziniae Blanckenhorn; El-Bewedy, p. 215,

pl. 11, fig. 3.

1992 Pecten (Pecten) ziziniae Blanckenhorn; Abdel-Moneim, p. 111, pl.

3, fig. 5.

1999 Pecten ziziniae Blanckenhorn; El-Shazly and Saber, p. 323, pl. 2,

figs. 4, 10.

Material: One right valve and eight left valves.

Dimentions: RV: L (1) 33mm.

: H (1) 28.5mm.

LV: L (8) 60.5mm, (41-77mm).

: H (8) 53.0mm, (38.5-68mm).

Description: Left valve of medium to large size, triangly oval,

inequilateral, almost flat, with slightly convex near the ventral margin,

with marked umbonal depression; hinge line straight; auricles triangular,

posterior one slightly larger than anterior, ornamented with 2-3 feebly

radial costules and crossed by concentric lamellae, auricles occupy

nearly half length of the lateral margins; triangular resilial pit; one pair

of cardinal crura at each auricle, the lower one more dominant; rounded,

relatively large adductor muscle scar; surface with 9 prominent costae

and one lateral costae less prominent and occupy the folded lateral


margins, anterior costal space are wider, flat; the prominent costae

occupy a longitudinal depressed area extended from the umbonal region

to the ventral margin; crenulated margin; the lateral costae running to

about the center of the valve. Right valve of moderate size, triangly

oval, subequilateral, moderately convex; orthogyral, incurved; umbonal

region convex; cardinal line straight; resilifer small, triangular pit; one

pair of crura on both sides of resilifer pit; lateral sides very slightly

concave, posterior one slightly longer; auricles unequal, posterior one

larger, flate; ventral margin subrounded, crenulated in the lower third of

the valve; surface ornamented with 10 principle costae and 2 less

prominent costae on both anterior and posterior margins; the principle

costae are rounded, separated by narrow concave subrounded

interspaces, all crossed by concentric striae; semi-circular , deep

adductor muscle scar.

Occurrence: Some specimens of this species have been recorded in

Gabal Gharra section, bed no. 10; Gabal Homeira section, beds no. 11

and 13.

Remarks: This present species differs from Pecten blanckenhorni

Depéret and Roman in having less number of ribs and wider interspaces.

Distribution: Pecten ziziniae Blanckenhorn is known only from the

Miocene of Egypt (Depéret and Roman, 1902). It was recorded from

Gabal Gafra by Blanckenhorn (1901); after half century, it was recorded

from the Cairo-Suez disrict, Sadat area and Central Sinai by Said and

Yellouze (1955), (Hamam, 1966), (Cherif, 1966 and 1972), (El-Shazly,

1987), (El-Bedewy, 1989), (Abdel-Moneim, 1992) and (El-Shazly and

Saber, 1999); and from the Western Desert by Metwally (1976).

According to the most previous authors, Pecten ziziniae

(Blanckenhorn) ranges in its age from the Burdigalian to the Tortonian;


this is wider than that by Depéret and Roman (1902) who reported that

this species is related to the first Mediterranian stage (i.e. Burdigalian).

Age: Burdigalian.

Subgenus: Pecten (Amussiopecten) Sacco, 1897.

Type species: Pecten burdigalensis Lamarck, 1809

Pecten (Amussiopecten) burdigalensis Lamarck, 1809


1914 Pecten (Amussiopecten) burdigalensis Lamarck; Cossman and

Peyrot, p. 290, pl. 14, fig. 21.

1976 Pecten (Amussiopecten) burdigalensis Lamarck; Metwally, p. 126,

pl. 4, fig. 3.

1989 Pecten (Amussiopecten) burdigalensis Lamarck; El-Bedewy, p.

217, pl. 11, fig. 4.

1992 Pecten (Amussiopecten) burdigalensis Lamarck; Abdel-Moneim, p.

113, pl. 3, fig. 6.

Material: One right valve and one left valve.


: H (1) 75mm.

LV: L (1) 80mm.

: H (1) 80mm.

Description: Specimen of moderately large size, orbicular,

subequilateral. Right valve nearly flate; umbo orthogyrate, umbonal

region very slightly convex; cardinal line slightly concave; auricles

slightly equal, nearly smooth; anterior one subtriangular, rounded

anteriorly; posterior one truncated; anterio-dorsal and posterio-dorsal


sides nearly straight; ventral margin rounded forming half-circle; outer

surface ornamented with 11-12 weak, low, broad costae, separated by

rather narrow intercostal spaces; surface crossed with fine closed

concentric lamellae, more developed in the lower half of the valve. Left

valve nearly flate, umbo orthogyrate, umbonal region very slightly

convex; cardinal line straight; auricles slightly equal; anterio-dorsal and

posterio-dorsal sides nearly straight; ventral margin rounded forming

half-circle; outer surface ornamented with 11-12 weak , low, broad

costae, separated by rather narrow intercostal spaces; surface crossed

with fine closed concentric lamellae, more developed in the lower half of

the valve.

Occurrence: This species occurs only in Gabal Gharra section, bed no. 10.

Remarks: According to Moore (1969), the subgenus Amussiopecten

Sacco characterizes entirely the Lower Miocene of East Africa.

Distribution: This species is known in many localities in Europe and

characterizes mainly the Burdigalian of the Mediterranean Basin as

mentioned by Cossman and Peyrot (1914). In Egypt, it was recorded

from Matruh area by Metwally (1976); from the Middle Miocene of the

Cairo-Suez district by El-Bedewy (1989); and from the Sadat Formation

(Late Burdigalian) in the Sadat area by Abdel-Moneim (1992).

Age: Burdigalian.

Subgenus: Pecten (Flabellipecten) Sacco, 1897.

Type species: Ostrea flabelliformis Brocchi, 1814

Pecten (Flabellipecten) flabelliformis (Brocchi, 1809)



1912 Flabellipecten flabelliformis Brocchi; Depéret and Roman, p. 139,

pl. 18, figs. 1, 2.

1914 Pecten (Flabellipecten) flabelliformis (Brocchi); Cossman and

Peyrot, p. 285, pl. 12, fig. 29.

1976 Flabellipecten flabelliformis (Brocchi); Metwally, p. 123, pl. 3, fig. 5.

1992 Pecten (Flabellipecten) flabelliformis (Brocchi); Abdel-Moneim, p.

114, pl. 3, fig. 7.

Material: One mold for a complete shell, two right valves and one left

valve.

Dimensions: RV: L (3) 90mm, 88-92mm.

: H (3) 81.6mm, 78-84mm.

LV: L (2) 98.5mm, 88-109mm.

: H (2) 92mm, 78-106mm.

Description: Specimen of large size, orbicular, subequilateral. Right

valve slightly convex; umbo orthogyrate; umbonal region slightly

convex; cardinal line long, very slightly curved; auricles subequal,

anterior one slightly larger; antero-dorsal and postero-dorsal sides nearly

straight; ventral margin rounded forming half-circle; outer surface

ornamented with 20-22 costae, separated by narrow intervals. Left valve

slightly convex; umbo orthogyrate; umbonal region very slightly convex

to flate; auricles equal, triangular in shape, with very fine radial costules,

crossed with very fine closed concentric lamellae; cardinal line straight,

cardinal area long; antero-dorsal and postero-dorsal sides nearly straight;

ventral margin rounded forming half-circle; outer surface ornamented

with 20-22 costae, separated by narrow concave interspaces.

Occurrence: Few specimens of this species have been encountered from

Gabal Gharra section, bed no. 12; Gabal Homeira section, bed no. 13.


Distribution: Depéret and Roman (1902) mentioned that this species

was recorded in the Tortonian and Pliocene of Italy, Tunisia and

Algeria while Cossmann and Peyrot (1914) recorded it from the Miocene

of the Aquitanian Basin (France). In Egypt, Metwally (1976) mentioned

the presence of Pecten (Flabellipecten) flabelliformis (Brocchi) in the

Burdigalian of Matruh area; also, it was recorded from the Late

Burdigalian (Sadat Formation) in the Sadat area by Abdel-Moneim

(1992).

Age: Burdigalian.

Subgenus: Pecten (Oppenheimopecten) von Teppner, 1922.

Type species: Pecten subbenedictus Fontannes, 1878

Pecten (Oppenheimopecten) benedictus Lamarck, 1819


1883 Pecten benedictus Lamarck; Fuchs, p. 35, pl. 20 (15), figs. 3-6.

1902 Pecten benedictus Lamarck; Depéret and Roman, p. 33, pl. 4,

figs. 1-5.

1972 Pecten benedictus Lamarck; Hamza, p. 87, pl. 2, figs. 1, 2.

1976 Pecten benedictus Lamarck; Metwally, p. 106, pl. 1, figs. 4a-d.

1989 Pecten (Oppenheimopecten) benedictus Lamarck; El-Bedewy, p.

221, pl. 12, fig. 5

1992 Pecten (Oppenheimopecten) benedictus Lamarck; Abdel-Moneim,

p. 115, pl. 3, fig. 9.

Material: Four right valves.

Dimentions: RV: L (4) 60.2mm, (38-77mm).

: H (4) 41.2mm, (34-69mm).


Description: Right valve of medium to large-sized, semi-circular,

subequilateral, moderately convex; ventral margin forming almost half

circle with slightly incurved lateral sides; auricles subequal, anterior one

triangular, slightly smaller, with rounded outline, with 6-8 feebly radial

costules; posterior auricle slightly larger, crossed by concentric lamellae;

cardinal line straight; triangular resilial pit; two pairs of cardinal crura;

12 most prominent radial costae, wide, beecome low and broad near the

ventral margin, subrounded, separated by rather narrow flatten

interspaces; surface crossed by closed space fine concentric lamellae;

crenulated internal margin.

Occurrence: This species is recorded in Gabal Gharra section, bed no.

10; Gabal Homeira section, bed no. 13.

Distribution: According to Depéret and Roman (1902), Pecten

(Oppenheimopecten) benedictus Lamarck appears in the Burdigalian of

the Rhone Valley with small-sized individuals and becomes abundant in

the Upper Miocene with large-sized examples and it reaches its

maximum abundance in the Pliocene of Italy, Spain and Algeria. In

Egypt, it was recorded from the Pliocene by Fuchs (1883), Hamza

(1972), Metwally (1976), El-Bedewy (1989). Abdel-Moneim (1992)

recorded this species in the Sadat area from the Sadat and Hommath

formations (Late Burdigalian and Serravallian).

Age: Burdigalian.

Pecten (Oppenheimopecten) convexo-costatus Abich, 1857

(pl. 4, fig. 3)

1883 Pecten convexo-costatus Abich; Fuchs, p. 40, pl. 21 (16), figs. 1, 2.

1902 Pecten convexo-costatus Abich; Depéret and Roman, p. 55, pl. 6,

fig. 7.


1976 Pecten convexo-costatus Abich; Metwally, p. 109, pl. 1, fig. 6.

1992 Pecten convexo-costatus Abich; Abdel-Moneim, p. 116, pl. 3, fig. 1.

Material: Five right valves.

Dimentions: RV: L (5) 53.5mm, (43-60mm).

: H (5) 48.7mm, (40-55mm).

Description: Right valve of medium to large size, subtriangular to

suborbicular, umbo orthogyral, incurved; umbonal area strongly convex;

lateral sides slightly curved; auricles equal, triangular, with smooth

concentric growth lines; cardinal line straight; surface ornamented with

13-14 primary ribs in addition to 3-4 less prominent ribs at the anterior

and posterior margins, ribs are semi-circular in cross-section; primary

ribs separated by slightly narrow concave interspaces.

Occurrence: This species occurs only in Gabal Geneifa section, bed

no. 13.

Distribution: Depéret and Roman (1902) recorded this species from the

Burdigalian of Arminia and Azrabigan. In Egypt, Fuchs (1883) recorded

it from the Middle Miocene of Geneifa; Metwally (1976) recorded it

from the Burdigalian rocks of the Salum and Matruh areas; Abdel-

Moneim (1992) recorded this specis from Sadat Formation (Late

Burdigalian) in the Sadat Quarry.


Superfamily: Anomiace Rafinesque, 1815

Family: Anomiidae Rafinesque, 1815

Genus: Anomia Linné, 1758

Type species: Anomia ephippium; SD Schmidt, 1818

Anomia burdigalensis Defrance

(Pl. 4, figs. 4a, b)


1914 Anomia burdigalensis Defrance; Cossman and Peyrot, p. 402, pl.

22, figs. 10, 11, 18, 19.

Material: Well preserved two left valves.

Dimensions: LV: Length (2) 28mm, 26-30mm

: Height (2) 32mm, 27-37mm.

Description: Left valve of small to moderate size, suborbicular, nearl

convex, curved anterior margin, truncatd posterior margin, irregular

outline; hinge short; short ligamental area, monomyarian; subcentral

adductor muscle scar; surface ornamented with radial striae.

Occurrence: This species appears in Gabal Gharra section, bed no. 12;

Gabal Homeira section, bed no. 13.

Distribution: It was recorded from the Neogene of the Aquitan Province

by Cossman and Peyrot (1914).

Age: Burdigalian.

Subgenus: Anomia (Anomia) Linné, 1758

Type species: Anomia (A.) ephippium Linné, 1758

Anomia (Anomia) ephippium Linné, 1758 subsp. rugulosostriata

Brocchi, 1814

(Pl. 4, fig. 5)

1910 Anomia ephippium Linné var. rugulosostriata Brocchi; Schaffer,

pl. 12, figs. 5-7.

1914 Anomia ephippium Linné var. rugulosostriata Brocchi; Cossmann

and Peyrot, p.407, pl. 22, figs. 16, 17.

1920 Anomia ephippium Linné var. rugulosostriata Brocchi; Dollfus and

Dautzenberg, pl. 47, figs. 11-19.


1992 Anomia ephippium Linné var. rugulosostriata Brocchi; Abdel-

Moneim, p. 118, pl. 4, fig. 1.

Material: Well preserved one left valve.

Dimensions: LV: Length (1) 32mm.

: Height (1) 28mm.

Description: Left valve of small size, suborbicular, nearl cup-shapped,

curved anterior margin, truncated posterior margin, irregular outline;

hinge short; short ligamental area, monomyarian; subcentral adductor

muscle scar; surface ornamented with radial striae.

Occurrence: Only one specimen of this subspecies has been recorded in


Remarks: The subspecies Anomia (Anomia) ephippium Linné var.

rugulosostriata Brocchi differs from Anomia burdigalensis Defrance, by

its slightly arched hinge and more extended posterior margin.

Distribution: This species recorded by Schaffer (1910) from the

Miocene of Eggenberg and the Helvetian of Algeria; from the Neogene

of the Aquitan Province by Cossman and Peyrot (1914) and from the

Miocene of France by Dollfus and Dautzenberg (1920). In Egypt, it was

recorded from the Miocene of the Sadat area by Abdel-Moneim (1992).

Age: Burdigalian.

Suborder: Ostreina Ferussac, 1822

Superfamily: Ostreacea Rafinesque, 1815

Family: Ostreidae Rafinesque, 1815

Subfamily: Ostreinae Rafinesque, 1815

Genus: Crassostrea Sacco, 1897

Type species: Ostrea (Crassostrea) virginica (Gmelin, 1791)


Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs, 1883


1955 Ostrea (Cubitostrea) frondosa De Serres var. Rohlfsi; Said and

Yallouze, p. 65, pl. 1, figs. 6-10

1966 Ostrea frondosa var. rohlfsi Fuchs; Cherif, pl. 8, fig. 5; pl. 6, figs.

1, 3.

1966 Ostrea frondosa var. rohlfsi Fuchs; Hamam, pl. 9, fig. 3.

1968 Ostrea frondosa De Serres var. rohlfsi Fuchs; El-Gamal, p. 161,

pl. 16, figs. 1-3, 6, 7

1972 Ostrea frondosa rohlfsi Fuchs; Cherif, p. 105, pl. 2, figs. 4, 8, 10;

pl. 3, fig. 5

1992 Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs; Abdel-

Moneim, p. 122, pl. 4, fig. 7

Material: Eight double-valved shells, 58 right valves and 35 left valves.

Dimensions: RV: L (66) 44.5mm, 24-67mm.

: H (66) 53.5mm, 40-88mm.

LV: L (43) 50.9mm, 21-90mm.

: H (43) 62.5mm, 22-102mm.

Description: Shell of medium size, slightly posteriorly incurved, slightly

dorsally-ventrally elongated, valves of medium thickness; subtriangular

ligamental area, with shallow, posteriorly incurved reselium pit;

opithogyrate; dysodont; monomyarian, moderate size, semi-circular,

shallow adductor muscle scar. Right valve with smooth internal margin;

outer surface ornamented with concentric growth lines. Left valve with

crenulated internal margin; outer surface ornamented with 19-20

crenulated radial ribs radiating from the umbonal area. Generally, the left


valve is slightly thicker than the right valve. In some cases, some

individuals characterized by incrusting Balanus perforatus.

Occurrence: Common members of this species have been found in

Gabal Geneifa section, beds no. 5, 9, 13 and 14; Gabal Gharra section in

beds no. 6, 12, 13, 14 and 15; Gabal Homeira section, beds no. 11, 13, 16

and 18.

Remarks: This form occurs abundantly in Gabal Geneifa section, bed

no. 5; in Gabal Homeira section, beds 11, 16 and, 18; and Gabal Gharra

section, bed no. 14. It is worth to mention that it present in its

embryonic stages in Gabal Homeira section, bed no. 11; and Gabal

Gharra section, bed no. 6.

Distribution: This subspecies was recorded by many authors from

different Egyptian Miocene localities as the Miocene of the North

Western Desert (El-Gamal, 1968); from the Miocene of the Cairo–Suez

district (Said and Yallouze, 1955) and (Hamam, 1966); and from the

Miocene of the Sadat area by Cherif (1966 and 1972) and Abdel-

Moneim (1992). The last author recorded it from the Sadat and

Hommath formations (Late Burdigalian and Serravallian).


Genus: Alectryonella Sacco in Bellardi and Sacco, 1897

Type species: Ostrea plicatula Gmelin, 1791

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes, 1833


1883 Ostrea virleti Deshayes; Fuchs, p. 43, pl. 9(4), figs. 1-6; pl. 10(5),

figs. 1-4.

1927 Ostrea virleti Deshayes; Cox, p. 66, pl. 11, figs. 1, 2; pl. 16, fig. 1.


1929 Ostrea plicatula Gmelin var. virleti Deshayes; Desio, pl. 36, fig. 4.

1955 Ostrea (Alectryonia) plicatula Gmelin var. virleti Deshayes; Said

and Yallouze, p. 67, pl. 2, figs. 5,6.

1962 Ostrea virleti Deshayes; Said, pl. 9, fig. 1.

1966 Ostrea (Lopha) plicatula var. virleti Deshayes; Cherif, pl. 8, figs.

1, 3; pl. 10, figs. 1, 3, 7

1966 Ostrea plicatula var. virleti Deshayes; Hamam, pl. 9, figs. 1, 4.

1968 Ostrea (Lopha) plicatula var. virleti Deshayes; El-Gamal, p. 166,

pl. 16, fig. 4.

1972 Ostrea (Lopha) plicatula var. virleti Deshayes; Cherif, p. 108,

pl. 2, figs. 1, 3, 7; pl. 3, figs. 1, 3.

1992 Alectryonella plicatula (Gmelin) subsp. virleti Dshayes; Abdel-

Moneim, p. 124, pl. 5, figs. 2a, b.

1999 Ostrea virleti Deshayes; El-Shazly and Saber, p. 327, pl. 3, fig. 3.

Material: Nine double-valved shells, 56 right valves and 41 left valves.

Dimensions: RV: L (65) 67.6mm, 45-105mm.

: H (65) 78.5mm, 52-107mm.

LV: L (50) 76.7mm, 46-117mm.

: H (50) 92mm, 55-123mm.

Description: Shell of medium to large size, slightly dorsally-ventrally

elongated, truncated posterior margin; opithogyrate; dysodont;

subtriangular ligamental area; posteriorly incurved reselium pit; shallow

to moderate umbonal cavity; deep, semi-circular, medium to large size

adductor muscle scar. Right and left valves are of moderate thickness to

thick. Both valves with smooth internal surface; outer surface of each

ornamented with 10-12 crenulated radial ribs radiating from the umbonal

area.


Occurrence: Members of this species occur in Gabal Geneifa section in

beds 5, 13 and 14; Gabal Gharra section in beds 6, 10, 12, 13, 14 and

15; Gabal Homeira section in beds 11, 13, 16 and 18.

Remarks: El-Shazly (1987) related the type virleti to the genus

Flemingostrea, this is not correct from two openions. Firstly, the genus

Flemingostrea is characterized by adductor muscle scar with the

following features: concave to straight upper surface, near to the ventral

and posterior margins. These features are not found in the type virleti

whose adductor muscle scar with convex upper surface, near to the

dorsal side than the ventral margin. Secondly, the genus Flemingostrea,

there is no attitude from the organisms to develop over each others. But

in this study, we found that some organisms developed their left valve

over the right valve of other organisms. The above mentioned made the

author to relate the type virleti to Alectryonella and not to the genus

Flemingostrea as mentioned by El-Shazly (1987).

In the present study, this subspecies is abundant in Gabal Geneifa

section, beds no. 5 and 13; Gabal Homeira section, beds 11, 13, 16 and

18; Gabal Gharra section, beds no. 10, 13 and 14. The collected

individuals from bed no. 16 (Homeira section) and beds no. 13 and 14

(Gharra section) are characterized by large sizes and thick valves. While

those which were collected from bed no. 5 (Geneifa section), bed no. 13

(Homeira section) and bed no. 10 (Gharra section) are characterized by

large sizes and moderate valve thickness.

Distribution: Many authors recorded this subspecies from many

Egyptian Miocene localities. Fuchs (1883) recorded it from the Middle

Miocene of Siwa Oasis and Gabal Geneifa. It was recorded from the

Miocene of the North Western Desert by Desio (1929), Said (1962) and

El-Gamal (1968). From the Cairo–Suez district, it was recorded by Said


and Yallouze (1955) and Hamam (1966). From the Sadat area,

Alectryonella plicatula (Gmelin) subsp. virleti Deshayes was recorded

by Cherif (1966 and 1972) and Abdel-Moneim (1992). These authors

referred the rocks bearing this speices to the Burdigalian–Tortonian.


Subclass: Heterodonta Neumayr, 1884

Order: Veneroida H. Adams & A. Adams, 1856

Superfamily: Lucinacea Fleming, 1828

Family: Lucinidae Fleming, 1828

Subfamily: Lucininae Fleming, 1828

Genus: Lucina Bruguiére, 1797

Type species: Venus jamaicensis Spengler, 1784; subsequent

designation, Gray, 1874.

Lucina sp.

(Pl. 5, fig. 2)

Material: Three moderately preserved internal molds.

Dimensions: Mold : Length (3) 61mm, 58-65mm.

: Height (3) 51mm, 48-55mm.

Descriptin: Internal mold of medium size, equivalve, slightly

inequilateral, oval to subtrapezoidal, slightly flattened; hinge with two

cardinals, hinge line large, slightly curved, more curved in its posterior

part; prosogyrate; smooth internal surface.

Occurrence: This species occurs in Gabal Gharra section, bed no. 6.

Age: Burdigalian.

Genus: Linga De Gregorio, 1884


Type species: Lucina columbella Lamarck, 1819; subsequent

designation, Sacco, 1889.

Subgenus: Linga (Linga) De Gregorio, 1884

Linga (Linga) columbella (Lamarck, 1819)

(Pl. 5, fig. 3)

1870 Lucina columbella Lamarck; Hornes, pl. 33, fig. 4.

1909 Lucina (Linga) columbella (Lamarck); Dollfus and Dautzenberg, p.

251, pl. 17, figs. 12-15.

1992 Linga (Linga) columbella (Lamarck); Abdel-Moneim, p. 128, pl. 6,

fig. 3.


Dimensions: Mold: Length (1) 50mm.

: Height (1) 44mm.

Descriptin: Internal mold of medium size, subrounded to oval,

equivalve; inequilateral; hinge line slightly curved, with two cardinals;

peak prosogyrate; valves ornamented by concentric growth lines.


Distribution: Linga (Linga) columbella (Lamarck) was recorded from

the Miocene of Vienna Basin (Hornes, 1870), and from the Middle

Miocene of France (Dollfus and Dautzenberg, 1909). In Egypt, it was

recorded from the Serravallian of Hommath Formation in the Sadat area

by Abdel-Moneim (1992).

Age: Burdigalian.

Family: Ungulinidae Adams & Adams, 1857

Genus: Diplodonta Bronn, 1831


Type species: Venus lupinus Brocchi, 1814 (non Linné, 1758)

Diplodonta sp.

(Pl. 5, fig. 4)

Material: Two moderately preserved internal molds.


: Height (2) 22mm, 20-24mm.

Description: Internal mold of medium size, subtrigonal to oblong in

outline, equivalve, inequilateral; hinge line slightly curved, with two

developed oblique cardinals; peak prosogyrate.

Occurrence: This species appear only in Gabal Gharra section, bed no. 13.


Superfamily: Cardiacea Lamarck, 1809

Family: Cardiidae Lamarck, 1809

Subfamily: Cardiinae Lamarck, 1809

Genus: Cardium Linne′, 1758

Cardium sp.

(Pl. 5, fig. 5)

Material: Twelve moderately preserved internal mold.


: Height (12) 48mm, 36-51mm.

Descriptin: Internal molds of medium size, subrounded to subquadrate,

shell gaping at posterior margin; hinge line long, straight to moderately

curved; peak nearly central; orthogyrate; molds with faint print for radial

ribs which reflect the inner surface of the valves.


Occurrence: Specimens of this species have been recorded in Gabal

Gharra section, bed no. 13; Gabal Homeira section, beds no. 11, 13, 16

and 19.


Genus: Acanthocardia Gray, 1851

Type species: Cardium aculeatum Linné, 1758; subsequent designation,

Stoliczka, 1870.

Subgenus: Acanthocardia (Acanthocardia) Gray, 1851

Acanthocardia (Acanthocardia) paucicostata (Sowerby, 1839)

(Pl. 5, fig. 6)

1912 Cardium paucicostatum Sowerby; Cossmann and Peyrot, p. 478,

pl. 20, fig. 30.

1986 Acanthocardia (Acanthocardia) paucicostata (Sowerby);

Studencka, p. 65, pl. 10, figs. 1-2.

1992 Acanthocardia (Acanthocardia) paucicostata (Sowerby); Abdel-

moneim, p. 130, pl. 10, fig. 6.



: Height (1) 44mm.

Descriptin: Internal mold of medium size, semicircular to oval,

elongated, higher than long, equivalve, subequilateral, anterodorsal

margin shorter than the posterodorsal margin; umbo median,

prosogyrate; hinge line nearly straight; mold reflects very convex valves,

very convex umbonal area, mold have print for 14-16 radial ribs in its

lower half which reflec the inner ornamentation of the valves.


Occurrence: This subspecies is recorded only in Gabal Homeira

section, bed no. 11.

Distribution: The form in question is known from the Middle Miocene

of France (Cossmann and Peyrot, 1912) and from the Middle Miocene of

South Poland (Studencka, 1986). In Egypt, it was recorded from

Serravallian of the Hommath Formation in the Sadat area by Abdel-

Moneim (1992).

Age: Burdigalian.

Superfamily: Mactracea Lamarck, 1908

Family: Mactridae Lamarck, 1908

Subfamily: Lutrariinae Adams & Adams, 1856

Genus: Lutraria Lamarck, 1799

Type species: Mya lutraria Linne, 1758

Lutraria sp.

(Pl. 5, fig. 7)

Material: Nine moderately preserved internal molds.


: Height (9) 33mm, 30-37mm.

Description: Molds of medium size, anteriorly-posteriorly elongated,

inequilateral, subequivalves; valves slightly gaping; prosogyrate; hinge

line slightly curved.

Occurrence: Members of this species are present only in Gabal Gharra



Superfamily: Tellinacea de Blainville, 1814


Family: Tellinidae de Blainville, 1814

Subfamily: Macominae Olsson, 1961

Genus: Gastrana Schumacher, 1817

Type species: Gastrana donacina = Tellina obildgaardiana Spengler,

1798; subsequent designation Bucquoy, Dautzenberg and Dollfus, 1898.

Gastrana sp.

(Pl. 5, fig. 8)

Material: Three moderately preserved internal mold.


: Height (3) 32mm, 29-34mm.

Description: Mold of moderate size, oblique, ovate to subrounded,

inequilateral; peak prosogyrate.

Occurrence: This species is recorded in Gabal Geneifa section, bed no.



Gastrana laminosa (Sowerby)

(Pl. 5, fig. 9)

1914 Gastrana laminosa (Sowerby); Cossmann and Peyrot, p. 445, pl.

24, figs. 13-14.

1992 Gastrana laminosa (Sowerby); Abdel-Moneim, p. 134, pl. 6, fig. 12.


Dimensions: Mold: Length (2) 35.5mm, 30-41mm.

: Height (2) 27.5mm, 24-31mm.


Description: Mold of small to medium size, elongate; inequilateral,

slightly inequivalve, left valve is little larger; peaks a little anterior to

midline, opisthogyrate.

Occurrence: This species occurs in Gabal Gharra section, bed no. 13;


Distribution: Cossmann and Peyrot (1914) recorded this species from

the Miocene (Helvetian) of the Aquitaine Province, France; Abdel-

Moneim (1992) recorded it from the Hommath Formation (Serravallian)

in the Sadat area.


Family: Psammobiidae Fleming, 1828

Subfamily: psammobiinae Fleming, 1828

Genus: Gari Schumacher, 1817

Type species: Gari vulgaris = solen amethystus Wood, 1815

Gari sp.

(Pl. 6, fig. 1)



: Height (1) 37mm.

Description: Mold of moderate size, inequilateral, valves more or less

equal, ovate, anteriorly-posteriorly elongated; peak prosogyrate.

Occurrence: This species appears only in Gabal Gharra section, bed

no. 13.



Family: Solecurtidae d’Orbigny, 1846

Subfamily: Solecurtinae d’Orbigny, 1846

Genus: Azorinus Recluz, 1869

Type species: Solen coarctatus Gmelin, 1791

Azorinus sp.

(Pl. 6, fig. 2)



: Height (1) 18mm.

Description: Mold of moderate size, elongated; peak subcentral, ventral

margin straight; dorsal margin slightly curved at peak region.

Occurrence: This species is recorded only in Gabal Geneifa section, bed

no. 5.

Age: Burdigalian.

Superfamily: Veneracea Rafinesque, 1815

Family: Veneridae Rafinesque, 1815

Subfamily: Tapetinae Adams & Adams, 1857

Genus: Paphia Röding, 1798

Type species: Paphia alapapiliomis (= Venus rotundata Linné, 1758);

subsequent designation Dall, 1902.

Subgenus: Paphia (Callistotapes) Sacco, 1900

Type species: Venus vetula Bastrot, 1825; original designation

Paphia (Callistotapes) vetula (Bastrot, 1825)

(Pl. 6, fig. 3)

1870 Tapes vetula Bastrot; Hornes, pl. 11, fig. 1.


1906 Tapes vetula Bastrot; Dollfus and Dautzenberg, p. 176, pl. 12,

figs. 1-6.

1910 Tapes vetula Bastrot; Schaffer, pl. 41, figs. 1-4.

1912 Tapes (Callistotapes) vetula (Bastrot); Cossmann and Peyrot, p.

306, pl. 11, figs. 34-36.

1992 Pahia (Callistotapes)vetula (Bastrot); Abdel-Moneim, p. 136, pl.

7, fig. 3.


Dimensions: Mold: Length (2) 67.5mm, 65-70mm

: Height (2) 46.5mm, 44-49mm.

Description: Mold of moderate size, ovally-elliptical, equivalve,

strongly inequilateral, anteriorly-posteriorly elongated; peak anterior,

prosogyrate.

Occurrence: This subspecies is present in Gabal Gharra section, bed no.


Distribution: This species occurs in the Miocene of many areas in the

Mediterranean region and in Europe. Hornes (1870) recorded it from

Vienna basin; Dollfus and Dautzenberg (1906) mentioned that it is

present in the Miocene of France, Swiss, Bavaria, Austria, Transylvania,

Portugal, Egypt as well as in the Tortonian of Rhone Valley and Italy.

Also, it was recorded from the Eggenburg by Schaffer (1910) and from

the Aquitaine Basin by Cossmann and Peyrot (1912). In Egypt, it was

recorded from the Hommath Formation (Serravallian) in the Sadat area

by Abdel-Moneim (1992).


Subfamily: Clementiinae Frizzel, 1936


Genus: Clementia Gray, 1842

Type species: Venus papyracea Gray, 1825; SD Gray, 1847.

Clementia sp.

(Pl. 6, fig. 4)



: Height (1) 43mm.

Descriptin: Mold of medium size, equivalve, strongly inequilateral,

ovate; peak anterior (prosogyrate); anterio-lateral side shorter and more

stepper than the posterio-lateral side; surface ornamented with concentric

growth lines.

Occurrence: Occurs only in Gabal Gharra section, beds no. 12 and 13.

Age: Early Miocene

Subfamily: Pitarinae Stewart, 1930

Genus: Callista Poli, 1791

Type species: Venus choine Linne, 1758; SD Meek, 1876.

Subgenus: C. (Costacallista) Palmer, 1927

Type species: Venus erycina Linne, 1758; OD

Callista (Costacallista) erycina (Linne, 1758).

(Pl. 6, fig. 5)

1870 Cytherea erycina Lamarck; Hornes, p. 137, pl. 19, figs. 1,2.

1883 Cytherea erycina Lamarck; Fuchs, p. 39.

1910 Callista erycina Linné; Schaffer, pl. 36, figs. 6-9.

1992 Callista (Costacallista) erycina (Linne); Abdel-Moneim, p. 135,

pl. 7, fig. 2.



Dimension: Mold: Length (2) 57mm, 54-60mm

: Height (2) 39.5mm, 39-40mm.

Description: Mold of medium size, equivalve, strongly inequilateral,

ovate to trigonal, slightly elongated; peak anterior, prosogyrate; anterio-

lateral side is shorter & more steo than the posterio lateral side.

Occurrence: This form is recorded only in Gabal Gharra section, bed

no. 13.

Distribution: This species was recorded from the Miocene of Vienna

Basin (Hornes, 1870) and from the Miocene of Eggenburg (Schaffer,

1910. In Egypt, it was recorded from the Miocene of Siwa Oasis (Fuchs,

1883) and from the Miocene of Sadat area (Abdel-Moneim, 1992).


Subclass: Anomalodesmata Dall, 1889

Order: Pholadomyoida Newell, 1965

Superfamily: Clavagellacea d’Orbigny, 1844

Family: Clavagellidae d’Orbigny, 1843

Genus: Clavagella Lamarck, 1818

Type species: Clavagella echinata; SD Children, 1823.

Subgenus: C. (Stirpulina) Stoliczka, 1870

Type species: C. coronata Deshayes, 1824; OD

Clavagella sp.

(Pl. 6, fig. 6)

Material: Three moderately preserved internal molds.


Description: Moderately preserved mold reflects a left valve fixed to

siphonal tube with extended end, right valve free, anterior end with

tubules formed only in terminal corona.

Occurrence: This species recorded in Gabal Homeira section, bed no. 19.


Class: Gastropoda Cuvier, 1797

Subclass: Prosobranchia Milne-Edwards, 1848

Order: Mesogastropoda

Superfamily: Cyclophoracea

Family: Ampullariidae

Genus: Lanistes Montfort, 1810

Type species: Lanistes (Lanistes) carinatus (Oliver)

Subgenus: Lanistes

Lanistes (Lanistes) mahmoudi Abbass, 1977

(pl. 6, fig. 7)

1977 Lanistes (Lanistes) mahmoudi Abbass, p. 113, pl. 3, figs. 12, 13.

Description: Mold of small size, planispiral, sinistrally coiled with

slightly raised spire; whorl outline convex, separated by deep sutures;

last whorl large with rounded sides; umbilicus wide, aperture not

complete.


no. 19.

Distribution: This form recorded in Egypt as a new one by Abbass

(1977) from the Helvetian-Tortonian (Upper Hommath Member) in

Sadat area.



Superfamily: Cerithiacea Fleming, 1822

Family: Turritellidae Clark, 1851

Genus: Turritella Lamarck, 1799

Type species: Turritella terebra (Linné), 1758

Subgenus: Turritella Turritella Lamarck, 1799

Turritella (Turritella) cleevelyi Abbass, 1977

(pl. 6, fig. 8)

1977 Turritella (Turritella) cleevelyi Abbass; p. 114, pl. 2, figs. 7-9.

Description: Mold of small size, turriculate; spire high, narrow,

consisting of numerous whorls; whorl outline strongly convex with deep

sutures.

Occurrence: This species recorded in Gabal Homeira section, bed no. 11.

Distribution: Abbass (1977) described this species from the

Vindobonian in Geneifa area (Lower Genefe Member).

Age: Burdigalian.

Turritella (Turritella) terebralis Lamarck, 1799

(pl. 6, fig. 9)

1955 Turritella terebralis Lamarck; Said and Yallouze, p. 57, pl. 4,

fig. 15.

1966 Turritella terebralis Lamarck; Cherif, pl. 13, fig. 14.

1966 Turritella terebralis Lamarck; Hamam, pl. 10, figs. 1, 3, 7.

1968 Turritella terebralis Lamarck; El-Gamal, p. 168, pl. 20, figs. 5-7.


1972 Turritella terebralis Lamarck; Cherif, p. 112, pl. 6, fig. 14.

1992 Turritella (Turritella) terebralis Lamarck; Abdel-Moneim, p. 139,

pl. 7, fig. 8.

Description: Mold of small to medium size, turriform, moderate spire,

body whorl medium, subrounded basal aperture.

Occurrence: This species is recorded in Gabal Gharra section, bed no.

13; Gabal Homeira section, beds no. 11 and 19.

Distribution: Turritella terebralis Lamarck was recorded from the

Miocene rocks of many Egyptian localitis. It was recorded from the

North Western Desert by El-Gamal (1968); from Agrud area by Hamam

(1966); from the Middle Miocene of Gabal Oweibid by Said and

Yallouze (1955); and from the Sadat area by Cherif (1966 and 1972),

and Abdel-Moneim (1992). The last author recorded it from the

Hommath Formation.


Subgenus: Eichwaldiella Friedberg, 1933

Type species: Turritella (Eichwaldiella) bicarinata Eichwald

Turritella (Eichwaldiella) fouadi Abbass, 1977

(pl. 7, fig. 1)

1977 Turritella (Eichwaldiella) fouadi Abbass; p. 115, pl. 2, figs. 6, 12, 13.

1992 Turritella (Eichwaldiella) fouadi Abbass; Abdel-Moneim, p. 141,

pl. 7, fig. 10.

Description: Mold of medium size, turriculate; spire narrow, consists of

many whorls; whorl outline convex with two carina, separated by wider

interspaces; suture linear, deep.


Occurrence: This species occurs only in Gabal Homeira section, bed

no. 11.

Distribution: Turritella (Eichwaldiella) fouadi Abbass was recorded in

Egypt as a new species by Abbass (1977) from the Helvetian in Ramlyia

in Sadat area from the Lower Hommath Member. Also, it recorded by

Abdel-Moneim (1992) from the Hommath Formation in the Sadat area

from the Serravallian.

Age: Burdigalian.

Superfamily: Cypraecea

Family: Cypreaadae

Genus: Luria Jousseaume, 1884

Type species: Luria (Luria) lurida (Linné)

Subgenus: Luria

Luria (Luria) salwae Abbass, 1977

(pl. 6, fig. 10)

1977 Luria (Luria) salwae Abbass; p. 129, pl. 5, fig. 14.

Description: Mold of small size, cypraeaform, convolute external cast,

with shallow apical umbilicus; whorl inflated posteriorly; outer lip forms

even curve; aperture long and narrow.


Distribution: Abbass (1977) described this species from the Helvetian

in Ramlyia in Sadat area from the Upper Sadat Member.



Superfamily: Naticacea

Family: Naticidae

Subfamily: Globularinae

Genus: Ampullina Bowditch, 1822

Type species: Ampullina depressa (Lamarck)

Subgenus: Pseudamaura P. Fischer, 1885

Type species: Ampullina (Pseudamaura) bulbiformis (Sowerby)

Ampullina (Pseudamaura) maedai Abbass, 1977

(pl. 6, fig. 11)

1977 Ampullina (Pseudamaura) maedai Abbass; p. 129, pl. 5, fig. 9.

Description: Mold of small size, subglobular with short pointed,

gradately conical spire; whorl convex with deep concave shoulder;

suture deep; body whorl large, globular, with deeply concave posterior

shoulder, strongly convex sides and base; aperture narrow rounded

posteriorly, wide anteriorly.

Occurrence: This species is recorded only in Gabal Geneifa section, bed

no. 13.

Distribution: Ampullina (Pseudamaura) maedai Abbass was recorded

in Egypt as a new one by Abbass (1977) from the Helvetian in Ramlyia

in Sadat area from the Lower Hommath Member.


Ampullina (Pseudamaura) macfaydeni Abbass, 1977

(pl. 6, fig. 12)

1977 Ampullina (Pseudamaura) macfaydeni Abbass; p. 130, pl. 5, fig. 8.


Description: Mold of small size, globular; spire low, slightly raised

above body whorl; whorl slightly convex with moderately deep suture;

body whorl large, forming the greater part of the shell with strongly

convex sides, with subrounded base; aperture crescentic, angular

posteriorly, widely rounded anteriorly.

Occurrence: Only one mold of this form have been encountered from

Geneifa section, bed no. 9.

Distribution: This species recorded in Egypt as a new one by Abbass

(1977) from the Helvetian in Ramlyia in Sadat area from the Lower

Hommath Member.


Subfamily: Naticininae

Genus: Natica Scopoli, 1777

Type species: Natica (Natica) citellus Linné, 1758

Natica sp.

(pl. 7, fig. 2)

Description: Mold of small size, naticoid, naticoid, spire with 2-3

whorls, large and inflated body whorl.

Occurrence: This species recorded in Gabal Geneifa section, bed no. 9.


Natica cf. millepunctata Lamarck, 1822

(pl. 7, fig. 3)

1856 Natica Millepunctata Lamarck; Hornes, pl. 47, figs. 1, 2.


1883 Natica sp. cf. Millepunctata Lamarck; Fuchs, p. 19 (37).

1966 Natica Millepunctata Lamarck; Cherif, pl. 13, figs. 3, 6.

1966 Natica Millepunctata Lamarck; Hamam, pl. 10, fig. 21.

1972 Natica Millepunctata Lamarck; Cherif, p. 112, pl. 6, figs. 3, 6.

1992 Natica cf. Millepunctata Lamarck; Abdel-Moneim, p. 144, pl. 7,

fig. 15.

Description: Internal mold of small size, naticoid, trochoid, spire with 2-

3 whorls, sutures depressed.

Occurrence: The specimen belonging to this species is recorded in



Basin by Hornes (1856). It was recorded from many Egyptian Miocene

localities such as the Middle Miocene of Siwa Oasis by Fuchs (1883);

the Burdigalian of Agrud area by Hamam (1966); from the Tortonian of

the Sadat area by Cherif (1966) who recorded it again (1972) from the

Serravallian of the Sadat area; and later Abdel-Moneim (1992) recorded

it from the Hommath Formation in the Sadat area (Serravallian).

Age: Burdigalian.

Superfamily: Tonnacea

Family: Bursidae

Genus: Bursa (Bolten) Röding, 1798

Type species: Bursa bufonia (Gmelin)

Bursa faizae Abbass, 1977

(pl. 7, fig. 4)

1977 Bursa faizae Abbass; p. 132, pl. 6, figs. 12, 13.


Description: Mold of medium size, fusiform external cast; spire short,

small, consisting of three whorls; whorl outline convex, strongly curved

posteriorly; suture deep; body whorl large, strongly inflated posteriorly

with side curving anteriorly into short peak; aperture not preserved.

Occurrence: This species occurs in Gabal Homeira section, bed no. 11.

Distribution: Abbass (1977) recorded this species in Egypt as a new

species from the Burdigalian of Agrud area in the Cairo-Suez area.

Age: Burdigalian.

Family: Ficidae

Genus: Ficus Bolten, 1798

Type species: Ficus communis Bolten, 1798

Ficus reticulatus (Lamarck, 1799)

(pl. 7, fig. 5)

1856 Pyrula reticulata Lamarck; Hornes, pl. 28, figs. 1-3.

1966 Ficus reticulata (Lamarck); Hamam, pl. 10, figs. 14-25.

1966 Ficus reticulatum (Lamarck); Cherif, pl. 13, fig. 8.

1972 Ficus reticulatum (Lamarck); Cherif, p. 114, pl. 6, fig. 8.

1992 Ficus reticulatus (Lamarck); Abdel-Moneim, p. 145, pl. 8, fig. 1.

Description: Internal mold of medium size; trochoidal, very low spire,

body whorl large, consistig the greater part of specimen, highly inflated

posteriorly; aperture longitudinal; outer lip slightly curved.

Occurrence: This species appears only in Gabal Homeira section, bed

no. 13.


Destribution: Ficus reticulatus (Lamarck) was recorded from the

Miocene of Vienna Basin by Hornes (1856). In Egypt, it was recorded

from the Middle Miocene of Agrud area Hamam (1966); from the Sadat

area Cherif (1966 and 1972) and Abdel-Moneim (1992). The last author

recorded it from the Serravallian from the Hommath Formation.

Age: Burdigalian.

Subgenus: Trophosycon Cooper

Type species: Ficus (Trophosycon) kenianus (Cooper)

Ficus sp.

(pl. 7, fig. 6)

Description: Mold of small to medium size; trochoidal, naticoid; spire

very low, slightly raised above posterior side of last whorl; last whorl

large, consisting the greater part of specimen, highly inflated posteriorly,

contracted anteriorly into long narrow beak.

Occurrence: This species occur in Gabal Homeira section, beds no. 11

and 19.


Order: Neogastropoda Thiele, 1925

Superfamily: Volutacea

Family: Olividae

Subfamily: Olivinae

Genus: Oliva Martyn, 1786

Type species: Oliva (Oliva) corticata Martyn

Subgenus: Neocylindrus P. Fischer, 1883

Type species: Oliva (Neocylindrus) tessellata Lamarck


Oliva (Neocylindrus) wagihi Abbass, 1977

(pl. 7, fig. 7)

1977 Oliva (Neocylindrus) wagihi Abbass; p. 143, pl. 7, figs. 7, 8.

Description: Mold of small size; convolute; spire short, conical,

consisting of three whorls; whorls low with nearly straight sides; sutures

almost superficial; body whorl consisting the greater part of the shell;

aperture long, narrow, angular posteriorly, wide anteriorly, thickened at

the margin.

Occurrence: This subspecies has been recorded only in Gabal Homeira


Distribution: Abbass (1977) recorded this subspecies in Egypt as a new

one from the Helvetian in the Geneifa area from the Lower Genefe

Member.


Superfamily: Conacea

Family: Conidae

Subfamily: Coninae

Genus: Conus Linné 1758

Type species: Conus (Conus) marmoreus Linne', 1758

Subgenus: Conus (Lithoconus) Morch, 1852

Type species: Conus (Lithoconus) millepunctatus Linne', 1758

Conus (Lithoconus) mercati Brocchi, 1841

(pl. 7, fig. 8)

1856 Conus Mercati Brocchi; Hornes, pl. 2, figs. 1-3.


1883 Conus sp. cf. Mercati Brocchi; Fuchs, p. 36.

1910 Conus (Lithoconus) Mercati Brocchi; Cerilli- Irelli, P. 48, PL. 4,

fig. 47.

1966 Conus mercati Brochhi; Cherif, pl. 13, figs. 4, 10.

1966 Conus cf. C. mercati Brochhi; Hamam, pl. 10, fig. 2.

1972 Conus mercati Brocchi; Cherif, p.116, pl.6, figs. 4, 10.

1977 Conus mercati Brocchi; El-Bedewy, p.143, pl. 13, figs. 2, 4, 6.

1992 Conus (Lithoconus) mercati Brocchi, Abdel-Moneim, p. 148, pl .

8, fig. 5.

Description: Mold of medium to large size, biconical; spire low,

conical, consisting of numerous whorls; suture nearly superficial; body

whorl large, consisting the greater part of shell; aperture narrow, long;

outerlip almost straight; innerlip straight, parallel to outerlip.

Occurrence: This species is recorded in Gabal Geneifa section, bed no. 13;

Gabal Gharra section, bed no. 10; Gabal Homeira section, bed no. 13.

Remarks: Conus (Lithoconus) mercati Brocchi is well known from the

Miocene of many Egyptian localities. Recently, it is accepted that Conus

is a Pliocene to Recent genus (Davies, 1971). However the previous

authors with few exceptions as Cerilli-Irelli (1910), didn't use the

subgenera of this genus. Here, the subgenus Lithoconus which is

characterized by a flat to low-coeloconid spire is used.


Basin by Hornes (1856) and from the Miocene of Italy by Cerilli-Irelli

(1910). In Egypt, Fuchs (1883) recorded this species from the Miocene

of Siwa Oasis and the Pliocene of Giza; Hamam (1966) recorded it from

the Burdigalian of the Agrud area; Cherif (1966 and 1972) recorded it

from the Middle and Upper Miocene of the Sadat area; El-Bedewy


(1977) recorded it from the Middle Miocene of Gabal El-Rusas in

Qosseir-Marsa Alam area; and Abdel-Moneim (1992) recorded it from

the Hommath Formation in the Sadat area.


Subgenus: Conus (Conolithus) Herrmannsen, 1847

Type species: Conus (Conolithus) antedilucianus Bruguiere

Conus (Conolithus) melficus Desio, 1929

(pl. 7, fig. 9)

1929 Conus (Dendroconus) melficus Desio, p. 279, pl. 37, fig. 4.

1966 Conus melficus Desio; Hamam, pl. 10, fig. 9.

1992 Conus (Conolithus) melficus Desio; Abdel-Moneim, p. 149, pl. 8,

fig. 6.

Description: Mold of small size, biconical; spire conical with concave

sides, numerous low whorls; suture subcardinal; body whorl high,

conical, with narrow concave posterior shoulder; aperture narrow, long;

parallel inner and outer lips.


no. 13.

Remarks: Conus (Conolithus) melficus Desio is more cylindrical than

C. mercati, Brocchi and has a prominent conical spire.

Distribution: Desio (1929) recorded this species from the Miocene of

the North Westren Desert; Hamam (1966) recorded it from from the

Burdigalian of Agrud area; and Abdel-Moneim (1992) recorded it from

the Sadat and Hommath Formations in the Sadat area.

Age: Burdigalian.


Order: Pulmonata

Suborder: Basomatophora

Superfamily: Hygrophilacea

Family: Planorbidae

Genus: Planorbis Muller, 1774

Type species: Planorbis (Planorbis) corneus (Linne')

Subgenus: Planorbis

Planorbis (Planorbis) nakanoi Abbass, 1977

(pl. 7, fig. 10)

1977 Planorbis (Planorbis) nakanoi Abbass; p. 152, pl. 3, figs. 9-11.

Description: Mold of small size, planispiral; sinistrally coiled; with

shallow apical umbilicus, deeper basal umbilicus, basal umbilicus wider

than apical one; 3-4 whorls with convex dorsal sides; suture deep; last

whorl subcircular in cross section with concave inner side; aperture

nearly parallel to shell axis.

Occurrence: This species occurs in Gabal Homeira section, bed no. 19.

Distribution: Abbass (1977) recorded this species in Egypt as a new

species from the Helvetian-Tortonian in Ramlyia in Sadat area from the

Upper Hommath Member.


IV.2.2 Phylum Echinodermata:


Phylum: Echinodermata

Class: Echinoidea Leske, 1778

Subclass: Euechinoidea Bronn, 1860

Superorder: Echinacea Claus, 1876

Order: Clypeasteroida Agassiz, 1872

Suborder: Clypeasterina Agassiz, 1872

Family: Clypeasteridae Agassiz, 1835

Genus: Clypeaster Lamarck, 1801

Type species: Echinus rocaceus Linné, 1758

Clypeaster intermedius Desmoulins, 1837

(pl. 7, fig. 11)

1920 Clypeaster intermedius Desmoulins; Fourtau, p. 50.

1966 Clypeaster intermedius Desmoulins; Cherif, pl. 14, fig. 7.

1972 Clypeaster intermedius Desmoulins; Cherif, p. 118, pl. 1, fig. 11.

1992 Clypeaster intermedius Desmoulins; Abdel-Moneim, p. 152, pl. 9,

figs. 1a, 1b.

Description: Test of medium size, elongated, pentagonal outline; aboral

surface slightly convex; oral surface flate, highly depressed toward

peristome; apical system central, pentagonal, with rounded genetal

pores; ambulacral areas are short, wide, swollen at petal areas, nearly

equal, not reach the margin; poriferous zones contain two raws of

uniserial pores, internal pores are rounded and the external ones are slit-

like shapped, pore pairs are conjugated with slit-like grooves; peristome

central, pentagonal; periproct submarginal and rounded.

Occurrence: This species appears in Gabal Geneifa section, bed no. 12;


Distribution: Fourtau (1920) recorded this species from the


Vindobonian of Gabal Geneifa and referred to its presence in the

Miocene of France, Algeria, Spain, Italy, Sardinia and many other

countries; Cherif (1966 and 1972) recorded it from the Sadat area, and

mentioned that this species is found only in the Burdigalian of Egypt;

Abdel-Moneim (1992) recorded it from the Late Burdigalian (Sadat

Formation) in Sadat area.


Clypeaster marginatus Lamarck, 1816

(pl. 8, fig. 1)

1920 Clypeaster marginatus Lamarck; Fourtau, p. 51, pl. 8, fig. 1.

1975 Clypeaster marginatus Lamarck; Ali, p. 210, pl. 5, figs. 1-4.

1987 Clypeaster marginatus Lamarck; El-Shazly, p. 196, pl. 5, fig. 2.

1992 Clypeaster marginatus Lamarck; Abdel-Moneim, p. 153, pl. 9,

fig. 3a, b.

Occurrence: This species appears in Gabal Geneifa section, bed no.

13; Gabal Gharra section, in bed no. 13; Gabal Homeira section, bed

no. 11.

Remarks: Clypeaster marginatus Lamarck, 1816 differs from

Clypeaster intermedius Desmoulins, 1837 in that the former is

characterized by large size, more broad width, slightly swollen petals

and the interporiferous zones are less swollen and wider.

Distribution: Fourtau (1920) recorded this species from the

Vindobonian of West Sinai. He mentioned that it is present in the

Miocene of France, Portugal, Malta, Sicile, Italy and other countries. In

Egypt, it was recorded from the Helvetian of Matruh area by Ali (1975);


from the Middle Miocene of Marout El-Khoshera in West Sinai by El-

Shazly (1987); and from the Late Burdigalian (Sadat Formation) in the

Sadat area by Abdel-Moneim (1992).


Suborder: Scutellina Haeckel, 1896

Family: Scutellidae Gray, 1825

Genus: Scutella Lamarck, 1816

Type species: Echinodiscus subrotundus Leske, 1778

Scutella ammonis Fuchs, 1883

(pl. 8, fig. 2)

1883 Scutella Ammonis Fuchs; p. 48, pl. 14 (9), figs. 1-4.

1955 Scutella ammonis Fuchs; Said and Yallouze, p. 76.

1962 Scutella ammonis Fuchs; Said, pl. 9, fig. 5.

1966 Scutella ammonis Fuchs; Hamam, pl. 10, fig. 18.

1968 Scutella ammonis Fuchs; El-Gamal, p. 232, pl. 22, fig. 1.

1975 Scutella ammonis Fuchs; Ali, p. 246, pl. 14, fig. 4-9.

1989 Scutella ammonis Fuchs; El-Bedewy, p. 154, pl, 4, fig. 1.

1992 Scutella ammonis Fuchs; Abdel-Moneim, p. 154, pl. 9, fig. 4.

Description: Test of medium to large size, subrounded, thin aboral

surface, nearly flate; oral surface slightly depressed toward peristome;

apical system central; ambulacral areas pateloid, medium, wide;

poriferous zones contain two rows uniserial pores, each pair are

connected with slit-like grooves; peristome submarginal, rounded;

periproct central, rounded.

Occurrence: This species is recorded in Gabal Gharra section, beds no.

6, 12 and 13; Gabal Homeira section, bed no. 16, 17 and 18 (broken


parts).

Distribution: Fuchs (1883) identified this specis from the Middle

Miocene of Siwa Oasis. After that, it was recorded by many authors from

sevaral Egyptian Miocene localities such as Said and Yallouze (1955)

from the Middle Miocene of Gabal Oweibid; Said (1962) from the

Middle Miocene of the North Western Desert and the Cairo-Suez

district; Hamam (1966) from the Burdigalian of Agrud area; El-Gamal

(1968) from the Helvetian of the Salum area; Ali (1975) from the

Helvetian of Siwa Oasis; El-Bedewy (1989) from the Miocene of the

Cairo-Suez area and Abdel-Moneim (1992) recorded few complete

specimens as well as many chips of this species from the Serravallian

(Hommath Formation) in the Sadat area.


Genus: Parascutella

Parascutella stefaninii (Desio, 1929)

(pl. 8, fig. 3)

1929 Scutella stefaninii Desio; pl. 40, fig. 3.

1968 Parascutella stefaninii (Desio); El-Gamal, p. 238, pl. 23, figs. 4, 5.

1975 Scutella stefaninii Desio; Ali, p. 252, pl. 16, fig. 7.

1992 Parascutella stefaninii (Desio); Abdel-Moneim, p. 155, pl. 9, fig. 5.

Description: Test of medium to large size, subrounded, thin; aboral

surface nearly flate; oral surface flate; apical system central; ambulacral

areas petaloid, wide, extending to ¾ of the half length; poriferous zones

contain two rows of uniserial pores, conjugated; peristome central.

Occurrence: This species occur in Gabal Gharra section, beds no. 6 and

12; Gabal Homeira section, bed no. 16, 17 and 18.


Distribution: Parascutella stefaninii (Desio) was described by its

author from the Miocene of the Western Desert. It was recorded later by

El-Gamal (1968) from the Burdigalian of the Salum area; Ali (1975)

recorded it from the same stage in Matruh area; while Abdel-Moneim

(1992) recorded it from the Serravallian (Hommath Form ation) in the

Sadat area.


Superorder: Atelostomata Zettel, 1879

Order: Cassiduloida Claus, 1880

Family: Echinolampadidae Gray, 1825

Genus: Echinolampas Gray, 1825

Type species: Echinus oviformis Gmelin, 1789

Echinolampas amplus Fuchs, 1883


1883 Echinolampas amplus Fuchs; p. 27, pl. 14 (9), figs. 5-8.

1920 Echinolampas amplus Fuchs; Fourtau, p. 65.

1955 Echinolampas amplus Fuchs; Said and Yallouze, p. 77, pl. 5, fig. 2.

1962 Echinolampas amplus Fuchs; Said, pl. 9, figs. 6a, b.

1966 Echinolampas amplus Fuchs; Cherif, pl. 14, fig. 1.

1966 Echinolampas amplus Fuchs; Hamam, pl. 10, fig. 20.

1968 Echinolampas amplus Fuchs; El-Gamal, pl. 24, fig. 7; pl. 25,

figs. 3, 4.

1972 Echinolampas amplus Fuchs; Cherif, p. 117, pl. 7, fig. 10.

1973 Echinolampas amplus Fuchs; Ali, p. 174, pl. 13, figs. 1, 2.

1989 Echinolampas amplus Fuchs; El-Bedewy, p. 160, pl. 5, fig. 2.

1992 Echinolampas amplus Fuchs; Abdel-Moneim, p. 156, pl. 10,


figs. 2a, b.

Description: Test of medium to large size, ovoidal to discoidal, very

slightly elongated; aboral surface slightly depressed, uniformally

convex; oral surface almost flate, slightly depressed around peristome;

apical system relatively small, pentagonal, with large genital pores;

ambulacral areas are flush; petals long, more or less narrow; anterior and

antero-lateral petals reach margin; anterior petal the shortest and

narrowest; postero-lateral petals the longest, broadest; poriferous zones

slightly depressed, with narrow pore pairs, uniserial, the internal pores

are rounded, the external ones are slit-like shapped; interporiferous zones

almost flate, broad, nearly 3.5 times as poriferous zone; peristome

relatively large, pentagonal, excentric anteriorly; periproct elliptical,

large submarginal, anterior margin more rounded.

Occurrence: This species is recorded in Gabal Geneifa section, beds no.

5 and 13; Gabal Gharra section, beds no. 13 and 14; Gabal Homeira


Distribution: Echinolampas amplus is well known from the Miocene of

Egypt since it is first recorded by Fuchs (1883) from the Middle

Miocene rocks of Siwa Oasis and Gabal Geneifa. Later, it was recorded

by many authors from several localities such as Said and Yallouze

(1955) from Gabal Oweibid; Said (1962) from the Cairo-Suez district

and the Middle Miocene of the North Westren Desert; Hamam (1966)

from the Burdigalian of Agrud area; Cherif (1966 and 1972) from the

Sadat area; El-Gamal (1968) from the Helvetian of the Salum area; Ali

(1973) from the Burdigalian of the North Western Desert and from the

Vindobonian of Gabal Shabrawet; El-Bedewy (1989) from the Miocene

in the Cairo-Suez area from the Genefe Formation; and Abdel-Moneim


(1992) from the Serravallian (Hommath Formation) in the Sadat area.

According to Fourtau (1920) Echinolampas amplus Fuchs is the most

typical species of the Egyptian Vindobonian.


Echinolampas plagiosomus Agassiz, 1840


1920 Echinolampas plagiosomus Agassiz; Fourtau, p. 71.

1966 Echinolampas plagiosomus Agassiz; Cherif, pl. 14, fig. 3.

1972 Echinolampas plagiosomus Agassiz; Cherif, p. 117, pl. 7, fig. 12.

1973 Echinolampas plagiosomus Agassiz; Ali, p. 184, pl. 17, fig. 1.

1975 Echinolampas plagiosomus Agassiz; Ali, p. 282, pl. 24, fig. 1, 2.

1992 Echinolampas plagiosomus Agassiz; Abdel-Moneim, p. 157, pl.

10, fig. 3.

Description: Test medium, almost subpentagonal, with maximum

breadth posteriorly; aboral surface slightly depressed, irregularly inflated

along anterior-posterior plane; oral surface strongly depressed toward

peristome, convex near margin; apical system moderate in size, excentric

anteriorly with conspicuous genital pores; ambulacral areas weakly

depressed especially near apex; petals long, moderate in width, not

reaching the margin, anterior petal shortest and narrowest; postero-lateral

petals broadest; poriferous zones broad, with pore pairs; interporiferous

zones flat, nearly 3.5 times as one poriferous zone; peristome large,

subpentagonal, excentric anteriorly; periproct large, subelliptical,

submarginal.

Occurrence: This species appaers only in Gabal Homeira section, bed


no. 11.

Distribution: Fourtau (1920) mentioned that this species occurs in the

Miocene of France, Italy, Malta, Hongeria, Sardinia as well as the

Vindobonian of the Western Desert of Egypt. Ali (1973 and 1975)

recorded it from the Vindobonian of Matruh area and North Westren

Desert; Cherif (1966 and 1972) recorded it from the Serravallian of the

Sadat area; and Abdel-Moneim (1992) recorded it also from the

Serravallian (Hommath Formation) in the Sadat area.

Age: Burdigalian.


This page for Table # 2: ( The ages assigned by previous authors to the

recorded fauna in some parts of the world ).

Chapter V Microfacies and depositional environments

144

CHAPTER V

MICROFACIES AND DEPOSITIONAL ENVIRONMENTS

V.1 MICROFACIES

The present study deals with the petrographic examination and

description, as well as microfacies analysis and depositional environment

of the Lower – Middle Miocene sediments in the study area. 49 thin

sections (from the total collected samples) were subjected to the

microfacies investigation. The limestone study have been carried out in

accordance with the procedure by Flugel (1982) especially the “Chick

List” suggested by him. The nomenclature of the studied carbonate

samples are based on the classification of Dunham (1962) and Embry and

Klovan (1972), as well as the energy index classification of Plumley et al.

(1962). With respect to the sandstone, they are described and subdivided

following the classification of Folk (1959 and 1962) and Pettijohn

(1975). The examined thin sections have been categorized within the

following two groups:

V.1.1 Limestone group.

V.1.2 Clastic group.

V.1.1 LIMESTONE GROUP

This group represents 55 % of the total examined thin sections,

most of them are characterized by the presence of considerable amounts

of quartz grains, and differentiated into the following microfacies

associations:

V.1.1.1 Wackestone.

V.1.1.2 Packstone.

V.1.1.3 Grainstone.

V.1.1.4 Framestone.


145

The following is a detailed description and discussion of these

assocciations:

V.1.1.1 Wackestone:

This microfacies association is characterized by the presence of

carbonate and non-carbonate particles in lime-mud supporting types, and

represents 6 % of the total examined carbonate thin sections. According

to the predominant allochemes, this association can be subdivided into

the following microfacies types:

V.1.1.1.1 Sandy dolomitic wackestone (figs. 34a, b):

This micofacies type represents 50 % of the total examined

wackestones. The groundmass is represented by microsparite with little

amount of fine rhombs of dolomite. Fossils are micritized and

recrystallized, of sparite size; represented by bioclastic of shell

fragments, foraminiferes (Miliolidae), and dominant echinoid fragments.

The quartz grains (20 %) are fine to medium, subangular to subrounded,

moderately sorted.

In comparison with the standard microfacies types of Wilson

(1975) and Flugel (1982), this microfacies type is correlatable with the

standard microfacies type (19) and facies zone (8). This means that the

environment of deposition was probably restricted bays or cut-off

lagoons or costal ponds with restricted circulation. This microfacies type

is recorded in Gabal Homeira section, in bed no. 2.


146

Fig. 37a: Sandy dolomitic wackestone with rhombic zoned, idiotypic

dolomite crystals and fine to medium quartz grains. Gabal Homeira,

lower part of Gharra Formation, bed 2, X 44, C.N.

Fig. 37b: Sandy bioclastic dolomitic wackestone with micritized

foraminiferal tests and subangular to subrounded quartz grains embdded

in micrite matrix. Gabal Homeira, lower part of Gharra Formation, bed 2,

X 22, P.P.L.


147

V.1.1.1.2 Algal wackestone (figs. 35a, b, c):

This microfacies type represents 50 % of the total examined

wackestones. The cement is represented by neomorphic sparite filling the

cavities among the main constituents. Fossils are biomorpha; represented

by red algae (Lithothamnium sp. and Lithophyllum sp.); frequent forms of

bryozoans, mollusks, echinoidal fragments, and sclaractenian corals.

Some of the algal parts are recrystallized and micritized and act as

sediment binder for the other constituents.


(1975) and Flugel (1982), this micrfacies type is correlatable with the

standard microfacies type (8) and facies zone (2) and/or (7). This means

that the environment of deposition was shelf lagoons with open

circulation and quiet water below normal wave base. This microfacies

type is recorded in Gabal Homeira section, in bed no. 19.

Fig. 38a: Algal wackestone with well preserved red algae

(Lithothamnium sp.). Gabal Homeira, upper part of Genefe Formation,

top part of bed 19, X 44, P.P.L.


148

Fig. 38b: Algal wackestone with well preserved red algal (Lithothphyllum

sp.), Gabal Homeira, upper part of Genefe Formation, top part of bed 19,

X 44, P.P.L.

Fig. 38c: Foraminiferal algal wackestone with complete amphistiginid

test and red algal fragments embdded in micrite matrix. Gabal Homeira,

upper part of Genefe Formation, top part of bed 19, X 22, P.P.L.


149

V.1.1.2 Packstone:

This microfacies association is characterized by the presence of

different carbonate and non-carbonate particles supported in a muddy and

sparitic background and represents 36 % of the total examined carbonate

thin sections. According to the predominant particles, this association can

be subdivided into the following microfacies types:

V.1.1.2.1 Sandy bioclastic packstone (figs. 36a, b, c):

This microfacies type represents 36.5 % of the total examined

packstones. The cement is represented by microsparite grading to micrite

in parts. The skeletal grains are polymictic bryozoans, algae, molluscan

fragments, echinoids, and foraminifera (Operculina complanata,

Amphistegina sp., Miogypsina sp. and others). These skeletal particles

act as rock forming constituents. The non-carbonate particles (25-30 %)

are represented by fine to medium quartz grains, subangular to rounded,

moderately sorted.




that the environment of deposition was deep shelf margin or basin margin

or foreslope (clinothem). This microfacies type is recorded in Gabal

Geneifa section, in the lower and middle parts of bed no. 13; in Gabal

Homeira section, in bed no. 17; and in Gabal Gharra section, in bed no. 7.


150

Fig. 39a: Sandy bioclastic packstone with foraminiferal biomorpha and

bioclastic (Amphistignids and operculinids), echinoid fragments and fine

to medium quartz grains, all embdded in microsparite. Gabal Gharra,

middle part of Gharra Formation, bed 7, X 22, C.N.

Fig. 39b: Sandy bioclastic packstone with large Operculina in the lower

left corner. Gabal Geneifa, middle part of Genefe Formation, bottom part

of bed 13, X 22, P.P.L.


151

Fig. 39c: Sandy bioclastic packstone with echinoid spine and

foraminiferal test. Gabal Geneifa, middle part of Genefe Formation,

bottom part of bed 13, X 22, P.P.L.

V.1.1.2.2 Sandy foraminiferal bryozoan packstone (figs. 37a, b, c, d):


packstones. The cement is represented by microsparite. The skeletal

grains are polymictic of different types of foraminifera (Operculina

complanata, Amphistegina sp., Miogypsina sp., miliolidae and others),

algae, bryozoans, molluscan fragments and echinoids. Some molluscan

fragments show silicification. The bryozoan chambers are filled with

neomorphic sparite (dog teeth cement). The skeletal grains act as rock

forming constituents. Algal oncoids are found. The non-carbonate

particles (20-40 %) are represented by medium to fine, subangular to

subrounded, moderately sorted quartz grains. In comparison with the

standard microfacies types of Wilson (1975) and Flugel (1982), this

micrfacies type is correlatable with the standard microfacies type (5) and

facies zone (4). This means that the environment of deposition was of a


152

typical reef flank facies accompanied by non-uniform sedimentation of

debris. This microfacies type is recorded in Gabal Geneifa section, in

beds 11, 12 and the upper part of bed no. 13; and in Gabal Gharra

section, in bed no. 10.

Fig. 40a: Sandy foraminiferal bryozoan packstone with ideoniform

bryozoans, foraminiferal and molluscan shell fragments and subrounded

quartz grains. Gabal Geneifa, lower part of Genefe Formation, bed 11, X

22, P.P.L.


153

Fig. 40b: Sandy foraminiferal bryozoan packstone with red algal

fragments (lithophyllum sp), foraminiferal, molluscan, bryozoan

fragments and fine quartz grains, all embedded in microsparite cement.

Gabal Geneifa, top part of Genefe Formation, top part of bed 13, X 22,

C.N.

Fig. 40c: Sandy foraminiferal bryozoan packstone, with biomorpha of

Operculina and Heterostegina tests, molluscan and bryozoan fragments.

All embdded in microsparite cement. Gabal Gharra, middle part of

Gharra Formation, bed 10, X 22, P.P.L.


154

Fig. 40d: Sandy foraminiferal bryozoan packstone as above, with

biomorpha of Miogypsina, Operculina and Heterostegina tests. All

embdded in microsparite cement. Gabal Geneifa, middle part of Genefe

Formation, bed 12, X 22, P.P.L.

V.1.1.2.3 Sandy echinoidal packstone (figs. 38a, b):

This microfacies type represents 27 % of the total packstones. The

matrix is represented by microsparite to micrite in patrs. The skeletal

grains are represented by very little foraminifera, algae, bryozoa and shell

fragments of echinoidal plates and spines. The skeletal grains are

considered as essential rock building constituents. The non-carbonate

particles (5-30 %) are represented by fine to coarse, angular to

subrounded, poorly sorted quartz grains.




that the environment of deposition was a high energy environment on

shoals and had moved down by local sloping to be under quiet water.


155

This microfacies type is recorded in Gabal Homeira section, in bed 10

and in Gabal Gharra section, in beds no. 6 and 8.

Fig. 41a: Sandy echinoidal packstone with echinoidal, molluscan

fragments and few quartz grains, embedded in micrite matrix. Gabal

Gharra, middle part of Gharra Formation, bed 8, X 22, P.P.L.

Fig. 41b: Sandy echinoidal packstone with echinoidal plates and

subangular to rounded quartz grains, all embedded in micrite matrix.

Gabal Gharra, middle part of Gharra Formation, bed 6, X 22, P.P.L.


156

V.1.1.3 Grainstone:

This microfacies association is characterrized by the presence of

different carbonate and non-carbonate particles (grain supported) in

sparitic background and represents 47 % of the total examined carbonate

thin sections. According to the predominant particles, this association can

be subdivided into the following microfacies types:

V.1.1.3.1 Sandy fossiliferous grainstone (figs. 39a, b, c, d):

This microfacies type represents 43 % of the total grainstones thin

sections. The cement is represented by sparite, and in parts represented

by microsparite. The skeletal grains are shell fragments (recrystallized in

parts), represented by foraminifera (Heterostegina sp.), algae, pelecypod

fragments, and echinoidal plates and spines. The skeletal grains form

essential rock building constituents. The non-carbonate particles (20-40

%) are represented by fine to coarse, subangular to rounded, poorly

sorted quartz grains, stained with iron oxides in parts and associated with

feldspasic minerals in other parts.




environment of deposition was mostly on slopes and shelf edges. This

microfacies type occurs in Gabal Homeira section, in beds no. 4, 5, 6, 8.


157

Fig. 42a: Sandy fossiliferous grainstone with molluscan shell fragments,

echinoids and polycrystalline quartz grains, all cemented by sparite.

Gabal Homeira, middle part of Gharra Formation, bed 8, X 22, P.P.L.

Fig. 42b: Sandy fossiliferous grainstone. Gabal Homeira, lower part of



158

Fig. 42c: Sandy fossiliferous grainstone with Miogypsina sp. and fine to

medium quartz grains in sparitic cement. Gabal Homeira, middle part of


Fig. 42d: Sandy fossiliferous grainstone. Gabal Homeira, lower part of



159

V.1.1.3.2 Sandy echinoidal foraminiferal grainstone (figs. 40a, b):


grainstones. The matrix is represented by sparite filling the cavities

between the essential rock constituents and in some parts fill the internal

cavities of the constituents. The skeletal grains are fossils and shell

fragments, biomorpha in parts, some of them are recrystallized,

represented by foraminifera (Operculina complanata, Amphistegina sp.,

Heterostegina sp. and other miogypsenoids ), some serpulids, algae

(Lithothamnium sp.), ostracods, bryozoa (Holoporella sp.), molluscan

fragments (pelecypods and gastropods), echinoidal fragments (plates and

spines). Sometimes, the foraminifera are larger and monospicific. The

skeletal particles act as essential rock building constituents. The non-

carbonate particles (10-20 %) are represented by fine to coarse, angular

to subrounded, poorly sorted quartz grains, the coarser ones are cracked.




that the environment of deposition was mostly in tidal bars and channels

of lagoons. This microfacies type is recorded in Gabal Geneifa section, in

beds no. 5 and 6; and in Gabal Homeira section, in the lower part of bed

no. 19.


160

Fig. 43a: Sandy echinoidal foraminiferal grainstone with echinoid

fragments, complete operculinid foraminifera and subrounded to

subangular quartz grains, all cemented by sparite. Gabal Geneifa, middle

part of Gharra Formation, bed 5, X 22, C.N.

Fig. 43b: Sandy echinoidal foraminiferal grainstone. Gabal Geneifa,

middle part of Gharra Formation, bed 6, X 22, P.P.L.


161

V.1.1.3.3 Sandy algal grainstone (figs. 41a, b, c, d):


grainstones. The matrix is represented by sparite to microsparite in parts.

The skeletal grains are micritized bioclastic of broken shell fragments of

foraminifera (Miogypsina sp., Amphistegina sp., miliolides and others),

algae (Lithothamnium sp.), ostracods, pectinides, oysters, gastropods, and

echinoidal plates and spines. The skeletal particles act as rock building

constituents. Pellets are also present. The non-carbonate particles (10 %)

are represented by fine to medium, subrounded to subangular, moderately

sorted quartz grains. Little amount of pellets are present. In comparison

with the standard microfacies types of Wilson (1975) and Flugel (1982),

this micrfacies type is correlatable with the standard microfacies type

(16) and facies zone (7) and/or (8). This means that the environment of

deposition was of warm, shallow water with only moderate water

circulation. This microfacies type is recorded in Gabal Homeira section,

in beds no. 11 and 16; and in Gabal Gharra section, in beds no. 15 & 16.

Fig. 44a: Sandy algal grainstone with red algal and molluscan fragments,

cemented by sparite. Gabal Homeira, lower part of Genefe Formation,

bed 16, X 22, P.P.L.


162

Fig. 44b: Sandy algal grainstone with Lithophyllum sp. and fine to

medium, subrounded to subangular quartz grains, all cemented by sparite.

Gabal Homeira, lower part of Genefe Formation, bed 16, X 22, p.p.l.

Fig. 44c: Sandy algal grainstone with ostracod and red algal fragments.

Gabal Gharra, uppermost part of Genefe Formation, bed 16, X 22, P.P.L.


163

Fig. 44d: Sandy algal grainstone with micritized red algae

(Lithothamnium sp.) and fine to medium quartz grains in sparitic cement.

Gabal Gharra, middle-upper part of Genefe Formation, bed 15, X 22,

P.P.L.

V.1.1.3.4 Sandy molluscan grainstone (figs. 42a, b):

This microfacies type represents 14 % of the total grainstones. The

matrix is represented by sparitic materials. The skeletal grains are

represented by shell fragments of foraminifera (Amphistegina sp.,

Miogypsina sp., Operculina sp. and others), ostracods, algae, bryozoans,

pelecypods, and gastropods. The skeletal particles act as essential rock

building constituents. The non-carbonate particles (10-20 %) are fine to

medium, subrounded to subangular, moderately sorted quartz grains.




that the environment of deposition was shelf with restricted water

circulation or tidal flats. This microfacies type is recorded in Gabal

Geneifa section, in beds no. 9 and 14.


164

Fig. 45a: Sandy molluscan grainstone with molluscan shell fragments and

fine to medium quartz grains, all cemented with sparite. The molluscan

shells show their original microstructure. Gabal Geneifa, lowermost part

of Genefe Formation, bed 9, X 22, P.P.L.

Fig. 45b: Sandy molluscan grainstone. Gabal Geneifa, lowermost part of

Genefe Formation, bed 9, X 22, P.P.L.


165

V.1.1.4 Framestone:

This microfacies association includes those sediments in which the

original components were bound together during deposition and

represents 11 % of the total carbonates. According to the predominant

particles, the following microfacies type have been distinguished:

V.1.1.4.1 Coralline framestone (figs. 43a, b, c, d):

This microfacies type is wholly composed of organic reef

(scleractenian corals and/or algae) with frequent amounts of foraminifera,

shell fragments, and echinoidal plates. These skeletal particles act as

essential rock building constituents. Algal oncoids are found. The matrix

is represented by micritic to sparitic materials. The non-carbonate

particles are represented by few fine, occasionally medium, subrounded

to subangular, moderately sorted quartz grains.




environment of deposition was rich in organic reef, often found on

platform margins. This microfacies type is recorded in Gabal Gharra

section, in beds no. 13 and 14.


166

Fig. 46a: Coralline framestone. The coral skeleton are recrystallized. The

coral spaces are filled with micrite matrex. Gabal Gharra, lowermost part

of Genefe Formation, bed 13, X 22, P.P.L.

Fig. 46b: Coralline framestone. The coral skeleton are highly

recrystallized and silisified. The coral cavities are filled with micritic

matrix. Gabal Gharra, lowermost part of Genefe Formation, bed 13, X

44, P.P.L.


167

Fig. 46c: Coralline framestone. The coral skeleton are highly

recrystallized and silisified. The coral cavities are filled with micritic

matrix. Gabal Gharra, lowermost part of Genefe Formation, bed 13, X

22, P.P.L.

Fig. 46d: Coralline framestone with well preserved algae (Lithophyllum

sp. And Lithothamnium sp.), Gabal Gharra, lowermost part of Genefe

Formation, bed 13, X 22, P.P.L.


168

V.1.2 CLASTIC GROUP

This group represents 45 % of the total examined thin sections,

represented by sandstones and shales, and include the following

microfacies types:

V.1.2.1 Calcareous quartz arenite (figs. 44a, b):

This micofacies type represents 25 % of the total clastics. This

microfacies type is characterized by fine to medium quartz grains,

occasionally coarse, subrounded to subangular, occasionally rounded,

moderately to poorly sorted, some quartz grains are cracked. Few

feldespar grains (plagioclase and microcline), with iron oxides in parts.

Some remains of molluscan shell fragments are present. All of these

grains are cemented by sparite. This microfacies type is recorded in

Gabal Geneifa section, in beds no. 3, and 4; in Gabal Homeira section, in

beds no. 3, 7 and 15.

Fig. 47a: Calcareous quartz arenite with fine to medium, subangular to

subrounded quartz grains, cemented with calcareous materials. Gabal

Geneifa, lower-middle part of Gharra Formation, bed 3, X 22, C.N.


169

Fig. 47b: Calcareous quartz arenite. Gabal Homeira, lower-middle part of

Gharra Formation, bed 7, X 22, C.N.

V.1.2.2 Dolomitic calcareous quartz arenite (fig. 45):

This micofacies type represents 4 % of the total clastics. This

microfacies type is characterized by fine to medium quartz grains which

are subangular to subrounded, moderately sorted, with ferrigenous

materials, and euhedral and zoned dolomite rhombs. All of these grains

are cemented by sparitic material and dolomite mineral. This microfacies

type is recorded in Gabal Geneifa section, in bed no. 8.


170

Fig. 48: Dolomitic calcareous quartz arenite with fine to medium,

subrounded to subangular quartz grains. The quartz grains are cemented

by sparite & dolomite rhombs, notice the upper right corner. Gabal

Geneifa, uppermost part of Gharra Formation, bed 8, X 22, C.N.

V.1.2.3 Calcareous fossiliferous quartz arenite (fig. 46):

This micofacies type represents 8 % of the total clastics, it is

characterized by fine to medium quartz grains which are subangular to

subrounded, moderately to poorly sorted. Some grains are stained with

iron oxides on periphery, other grains have eroded peripheries and

occasionally some of the coarser graines are cracked. Few foraminifera,

echinoids (plates and spines) and fragments of bivalvia are found, most

of them are recrystallized with blocky calcite. All of these grains are

cemented by sparitic carbonate matter. This microfacies type is recorded

in Gabal Gharra section, in bed no. 12.


171

Fig. 49: Calcareous fossiliferous quartz arenite. Gabal Gharra, uppermost

part of Gharra Formation, bed 12, X 22, P.P.L.

V.1.2.4 Calcareous ferruginous quartz arenite (figs. 47a, b):

This micofacies type represents 12 % of the total clastics. The

main characteristics of this type are fine to coarse, subangular to

subrounded, moderately to poorly sorted quartz grains. Some grains have

eroded peripheries and occasionally cracked. Some grains of feldspar

minerals (plagioclase) occur. All of these grains are cemented with

sparitic calcareous matter. This microfacies type is recorded in Gabal

Gharra section, in beds no. 1, 3 and 5.


172

Fig. 50a: Calcareous ferruginous quartz arenite with fine to coarse,

subangular to subrounded quartz grains. All components are cemented

with sparitic calcareous matter. Gabal Gharra, lower-middle part of the

Gharra Formation, bed 5, X 22, C.N

Fig. 50b: Calcareous ferruginous quartz arenite. Gabal Gharra, lower part

of the Gharra Formation, bed 3, X 22, C.N.


173

V.1.2.5 Sandy – silty shale (figs. 48a, b):

This micofacies type represents 51 % of the total clastics. The sand

grains which are floating in the clay minerals are fine to very fine

grained, occasionally grading to silt size, subrounded to subangular,

poorly sorted. The sand and silt grains increase and localize in form of

thin laminae or very thin intercalations in some part toseparate the shale

in form of sheets. Iron oxides occasionally occur. This microfacies type

is recorded in Gabal Geneifa section, in beds no. 1, 7 & 10; in Gabal

Homeira section, in beds no. 1, 9, 12 and 14 and in Gabal Gharra section,

in beds no. 2, 4, 9 & 11.

Fig. 51a: Sandy–silty ferruginous shale with sand and silt grains which

icrease and localize in form of lamina or may thin intercalation in some

part to separate the shale in form of sheets. Gabal Geneifa, upper part of

the Gharra Formation, bed 7, X 22, C.N.


174

Fig. 51b: Sandy – silty ferruginous shale. Gabal Gharra, middle part of

the Gharra Formation, bed 9, X 22, C.N.

V.2 DEPOSITIONAL ENVIRONMENTS

Selley (1978) defined the sedimentary facies as “a mass of

sedimentary rocks“, which can be defined and distinguished from others

by its geometry, lithology, sedimentary structures, paleocurrent pattern

and fossils.

The recognition and interpretation of the recorded sedimentary

facies are based on a number of megascopic and microscopic features and

guided with the facies model of Wilson (1975) as well as the

environmental criteria and case histories described by Flugel (1982).

The marine Miocene sequence in the study areas can be divided

into two sedimentary facies: The lower one is a clastic-dominated facies

representing the Gharra Formation. The upper facies is carbonate-

dominated and represents the Genefe Formation.


175

V.2.1 Clastic-dominated facies:

The lower part of this facies is an erosional base with extra-and

intraformational clasts, followed upward by cross-bedded sandstones and

topped by thinly laminated mudstone; while its upper part is mainly

intercalated with sandy limestone, oyster banks, mudstone and sandstone.

The sandstone is mainly of fine to coarse grained, subrounded to

subangular, calcareous, fossiliferous with molluscan fragements (mainly

pectinids and other bivalves), echinoids (Scutella sp. and Clypeaster sp.)

and molds of gastropods. The mudstones are of medium to thick bedded,

non-fossiliferous, moderately compact, jointed, and ferrugineous,

The limestones are mainly thin to medium bedded, compact,

massive, jointed, rich in macrofossils mainly of molluscs (especially

pelecypods), gastropod molds, badly preserved echinoderms. Oysters are

common and of large size,

This main sedimentary facies is characterized by the following

varaties of microfacies associations: calcareous quartz arenite, dolomitic

calcareous quartz arenite, calcareous fossiliferous quartz arenite,

calcareous ferrugineous quartz arenite, sandy echinoidal foraminiferal

grainstone, sandy dolomitic wackestone, sandy fossiliferous grainstone,

sandy echinoidal packstone, sandy algal grainstone, sandy bioclastic

packstone, and sandy foraminiferal bryozoan packstone.

Based on these microfacies associations, sedimentary structures

and fossil content, the Gharra Formation was probably deposited in an

environment ranging from tidal flat for the lower part to typical reef flank

for coral and algal reefs and high energy on shoals for the grain

supported fabrics (grainstone and packstone).


176

V.2.2 Carbonate-dominated facies:

This main sedimentary facies consists essentially of limestones,

sandstones and mudstones. The limestones are thick-bedded, compact,

massive, chalky, jointed, fractured, bioturbated and highly fossiliferous

with coralline red algae, Amphistigina sp., Miogypsina sp. and oysters.

The sandstone is characterized by abundance of Scutella sp. and large

pectens. The mudstone is thinly laminated, moderately compact,

nonfossiliferous, with lenticular beds of fine sandstone.

In the study area the carbonate-dominated facies is characterized

by the following microfacies associations: sandy bioclastic packstone,

sandy foraminiferal bryozoan packstone, sandy molluscan grainstone,

foraminiferal algal wackestone, sandy bioclastic packstone, sandy

echinoidal foraminiferal grainstone, sandy algal grainstone, algal

coralline framestone and coralline framestone.

The microfacies associations, fossil content and sedimentary

structures stated that the environment of deposition of this type was

probably reefal environment for the lower part, due to the presence of

abundant coralline red algae, oysters, Amphistigena sp, Miogypsina sp.

And moved to shelf lagoons with open circulation and an intertidal

environment with low energy conditions for the deposition of mudstones

in the top most part of Genefe Formation.

Chapter VI Summary and conclusions

177

CHAPTER VI

SUMMARY AND CONCLUSIONS

The present work deals with the study of stratigraphy, systematic

paleontology, microfacies analysis and depositional environments of

some Miocene sediments, Cairo-Suez District, Egypt.

VI.1 Stratigraphy:

The marine Miocene sequence exposed at gabals Geneife (97.1 m

thick), Homeira (110.9 m thick) and Gharra (141.7 m thick) in Cairo-

Suez District is a transgressive-regressive sequence lying unconformably

between continental sediments of Oligocene and post Middle Miocene.

The Lower Miocene deposits in the studied sections consist of

sandstones and mudstones with minor intercalations of sandy limestone.

They differ from the Lower Miocene algal limestone of the Sadat

Formation (Abdallah and Abdel-Hady 1966). Thus the name Gharra

Formation of Said (1971) is feasible to these Lower Miocene deposits.

On the other hand, the Middle Miocene rocks consists mainly of

algal, reefal, and chalky limestones with oyster banks, and minor

mudstone and sandstone intercalations. These facies differ from the

clastic facies of the Hommath Formation (Abdallah and Abdel-Hady

1966). Thus, the auhor follows the rock unit Genefe Formation (Said,

1990) for the Middle Miocene rocks exposed in the studied areas.

Based on the abundance of macro-invertebrate fauna especially

bivalves, gastropods and echinoids with some foraminifera, six

biohorizones have been recorded, they are from younger to older:

Chlamys (Argopecten) submalvinae zone, Chlamys (Macrochlamis)

sardoa zone, Pecten (Pecten) cristato-costatus zone, Pecten


178

(Flabellipecten) flabelliformis zone, Pecten (Pecten) ziziniae zone and

Chlamys gentoni zone.

VI.2 Systematic paleontology and biohorizons:

Sixty two macrofossil species (40 bivaves, 16 gastropods, 6

echinoids) have been identified, described and illustrated. They belong to

34 genus and 26 families. Their Paleogeographic and biogeographic

distribution indicated Atlantic-Mediterranean affinity as well as the Indo-

Pacific one in few.

The fossiliferous sandy limestones (beds 5 in Gabal Geneifa , 11

in Gabal Homeira and 6 in Gabal Gharra) nearly contain a common

content of fauna (oysters, pectinids and many other bivalves, gastropods,

echinods, algae and bryozoans) which can be considered a horizon for

correlation of the middle part of Gharra Formation in the study area. In

addition to the abundance of Alectryonella plicatula (Gmelin) subsp.

virleti Deshayes and Crassostrea frondosa (De Serres) subsp. rohlfsi

Fuchs in these beds in the three sections can be considered a biohorizon

for correlation.

The fossiliferous sandy limestones (bed no. 13 in Gabal Homeira

and bedno. 10 in Gabal Gharra) nearly contain a common content of

fauna (oysters, pectinids and many other bivalves, gastropod molds,

barnacles and algae) can be considered a horizon for correlation of the

upper part of Gharra Formation. In addition to the abundance of Pecten

(Pecten) ziziniae Blankenhorn, Pecten beudanti Basterot, Pecten

(Oppenheimpecten) benedictus (Lamarck) in the two sections can be

considered a biohorizon for correlation.

The fossiliferous sandy marl (bed 11 in Gabal Geneifa and the

lowermost part of bed 13 in Gabal Gharra) with their high abundance of

pectens are correletable. The abundance of Chlamys (Argopecten)


179

macrotis (Sowerby), Pecten (Pecten) cristato-costatus Sacco, Pecten

beudanti Basterot, Pecten (Oppenheimpecten) benedictus (Lamarck) and

Chlamys gentoni (Fontannes) in the two sections can be considered a

biohorizon for correlation for the lower part of Genefe Formation.

The fossiliferous sandy limestone (beds 16 in Gabal Homeira and

13 in Gabal Gharra) nearly contain a common content of fauna (oysters

and pectinids) can be considered a horizon for correlation of for the lower

part of Genefe Formation in the study area. In addition to the abundance

of Alectryonella plicatula (Gmelin) subsp. Virleti Deshayes and

Crassostrea frondosa (De Serres) subsp. Rohlfsi Fuchs in these beds

considered a biohorizon for correlation.

VI.3 Micofacies and depositional environments:

49 thin sections from the total collected samples were subjected to

microfacies investigation. The examined thin sections have been

categorized into two main groups:

1- Limestone group, which represents 55 % of the studied thin sections.

They differentiated into four main microfacies types: wackestone (sandy

dolomitic and algal), packstone (sandy bioclastic, sandy foraminiferal

bryozoan and sandy echinoidal), grainstone (sandy fossiliferous,sandy

echinoidal foraminiferal, sandy algal and sandy molluscan) and

framestone (coralline).

2- Clastic group, which represents 45 % and includes the following

microfacies types: quartz arenite (calcareous, dolomitic calcareous,

calcareous fossiliferous and calcareous ferrugineus) and sandy-silty shale.

The marine Miocene sequence in the study areas could be divided

into two sedimentary facies: the lower one is a clastic-dominated facies,

which represents the Gharra Formation, while the upper facies is

caarbonate-dominated and represents the Genefe Formation.


180

VI.3.1 Clastic-dominated facies:

The lower part of this facies is an erosional base with extra-and

intraformational clasts, followed upward by cross-bedded sandstones and

topped by thinly laminated mudstone, while its upper is mainly

intercalated with sandy limestone, oyster banks, mudstone and sandstone.

This sedimentary facies is characterized by the following

microfacies associations: calcareous quartz arenite, dolomitic calcareous

quartz arenite, calcareous fossiliferous quartz arenite, calcareous

ferrugineous quartz arenite, sandy echinoidal foraminiferal grainstone,

sandy dolomitic wackestone, sandy fossiliferous grainstone, sandy

echinoidal packstone, sandy algal grainstone, sandy bioclasts packstone,

and sandy foraminiferal bryozoan packstone.

Based on microfacies associations, sedimentary structures and

fossil content, the Gharra Formation is deposited in an environment

ranging from tidal flat for the lower part to typical reef flank for coral and

algal reefs and high energy on shoals for the grain-supported fabrics

(grainstone and packstone).

VI.3.2 Carbonate-dominated facies:

This sedimentary facies consists essentially of limestones and

mudstones. The limestones are thick-bedded, compact, massive, chalky,

jointed, fractured, bioturbated and highly fossiliferous with coralline red

algae, Amphistigina sp., Miogypsina sp. and oysters. Mudstone is thinly

laminated, moderately compact, nonfossiliferous, with lenticular beds of

fine sandstone.

In the study area the carbonate-dominated facies is characterized

by the following microfacies associations: Sandy bioclasts packstone,

sandy foraminiferal bryozoan packstone, sandy molluscan grainstone,

foraminiferal algal wackestone, sandy bioclasts packstone, sandy


181

echinoidal foraminiferal grainstone, sandy algal grainstone, algal

coralline framestone and coralline framestone.

The microfacies associations, fossil content and sedimentary

structures stated that the environment of deposition was reefal

environment for the lower part, due to the presence of abundance of

coralline red algae, oysters, Amphistigena sp, Miogypsina sp. to shelf

lagoons with open circulation and an intertidal environment with low

energy conditions for the deposition of mudstones in the top most part of

Genefe Formation.

References

182

REFERENCES

Abbass, H. L. (1977): A Monograph on the new Miocene gastropod species

in the Cairo-Suez district, Egypt. J. Univ. Kuwait ( Sci.) 4, 157 p.

Abdallah, M. A. and Abd El-Hady, F. M. (1966): Geology of Sadat area,

Gulf of Suez. J. Geol. U.A.R., 10/1, 1-24.

Abdallah, M.A. and Abd El-Hady, F. M. (1971) : Microfacies of Eocene

and Miocene rocks at the southeastern corner of Gabel Ataqa, Gulf

of Suez, A.R.E. Bull. Fac. Sci., Cairo Univ., Vol. 43, pp. 345-358.

Abd-Elmoniem, M. (1992): Stratigraphy of the Miocene rocks in the area

between Gabal Ataqa and Northern Galala, Gulf of Suez, Egypt.

Ph.D Thesis, Fac. Sci., Zagazig Univ., 252p.

Abd-Elshafy, E. and Abd-Elmoneim, M. (1992): Lithostratigraphy of the

Miocene rocks in the area between Gabal Ataqa and the Northern

Galala, Eastern Desert, Egypt. Bull. Fac. Sci., Zagazig Univ.,

14/2, 290-302.

Abdel Wahab, S. and El-Belassy, M. (1987): Sedimentology of the

Lower-Middle Miocene sequence in Gebel Hamza-Gebel Um

Qamar. Bull. Fac. Sci., Cairo Univ., 55/2, 445-480.

Abed, M. M. and Metwally, M. H. M. (1980): Distribution of pectinides

in some Miocene sections in Egypt. Mansoura Fac. Sci. Bull., 8,

233-256.

Abou Khadrah, A. M., Wali, A. M. A., Müller, A. M. A., and El Shazly,

A. M. (1993): Facies development and sedimentary structures of

synrift sediments, Cairo-Suez District, Egypt, Bull Fac. Sci.,

Zagazig Univ., 15/2, 355-373

Adams, C. G. (1973): Some Tertiary foraminifera. In: Atlas of

Palaeobiogeography (Hallam, A., ed.). Elsevier Scient. Publ.

Comp., Amsterdam, London, New York, 453-468.

References

183

Ali, M. S. M. (1973): A study of the genus Echinolampas in the Tertiary

rocks of Egypt. M.Sc. Thesis, Fac. Sci., Ain Shams Univ., 237 p.

Ali, M. S. M. (1975): A study on some Tertairy Echinoids of Egypt.

Ph.D. Thesis, Fac. Sci., Ain Shams Univ., 371 p.

Barakat, M. G. and Aboul Ela, N. M. (1970): Microfacies and

Paleontology of Middle Eocene and younger sediments in Geneifa

area, Cairo-Suez District. U.A.R. J. Geol., 14/1, 23-35.

Barron, T. (1907a): The topography and geology of the district between

Cairo and Suez. Egypt. Surv. Dept., Cairo. 133 p.

Barron, T. (1907b): The topography and geology of the Peninsula of Sinai

(western portion). Geol. Surv. And Mini Res. Dept., Cairo, 241 p.

Blanckenhorn, M. (1901): Neues Zur Geologie und Palaeontologie

d’egyptens. III- Das Miocan. Zeitschr. deutsch. Geol. Ges. 53/1,

52-132.

Boggs, S. Jr. (1987) : Principles of sedimentology and stratigraphy.

Merrill Publish. Comp., London, 784 p.

Bruce, H. and Hotzl, H. (1988): The sedimentary evolution of the Red

Sea rift: a comparison of the northwest (Egyptian) and northeast

(Saudi Arabia) margins. Tectonophysics, 153, 193-208.

Butterlin, J. (1988) : Origine et evolution des Lepidocyclines da la region

des Caraibes. Comparaison et relations avec les Lepidocyclines

autres regions du Monde. Revue de Paleobiologie, Vol. Spec. No.

2, Benthos's 86, ISSN 0253-6730, pp. 623-629, Geneva.

Cerilli-Irelli, S. (1907-1912) : Fauna Milacologica Mariana. Palaeontol.

Italica, parts prima-sesta, 13-18.

Cherif, O. H. (1966): Geology of Sadat area, south-west of Suez. M.Sc.

Thesis, Fac. Sci., Ain Shams Univ., Cairo.

Cherif, O. H. (1972): Tertiary fauna from the Sadat area (south-west of

Suez). Bull. l'Instit. D'Egypte, 22, 91-123.

References

184

Cherif, O.H. and Yehia, M.A. (1977) : Stratigraphy of the area between

Wadi Gimal and Wadi Hommath, Gulf of Suez, Egypt. Egypt. J.

Geol., 21, No. 2, pp. 185-203.

Cossmann, M. and Peyrot, A. (1909-1924) : Conchologie Neogenique de

l'Aquitaine, 4 Vols. : Act. Soc. Linn. De Bordeaux.

Cox, L. R. (1927): Neogene and Quaternary Mollusca from the Zanzibar

Protectorate. In: Report of the Palaeontology of the Zanzibar

Protectorate. Authority of the Government of Zanzibar, 13 – 102.

Davies, A. M. (1971): Tertiary faunas. 2 vols., George Allen & Unwin

Ltd., London.

Depéret, Ch. and Fourtau, R. (1900): Sur les Terrains Neogene de la

Basse-Egypte et de l'Isthme de Suez. C.R. Acad. Sci., Paris, 131,

401-403.

Depéret, C. and Roman, F. (1902-1912): Monographie des Pectinides

neogenes de l'Europe et des regions voisines. Mem. Soc. Geol. de

France, Mem. 26.

Desio, A. (1929): Resultati Scientifici della Missione alla Oasi Di

Giarabub. III: La Paleontologia. R. Soc. Geogr. Italiana, Rome, 4.

Dollfus, G. F. and Dautzenberg, Ph. (1902-1920): Conchyliologie du

Miocene moyen du Bassin de la Loire. Mem. Soc. Geolog. France,

Paleont., No. 27

Dunham, R. J. (1962): Classification of carbonate rocks according to

depositional texture. Mem. Amer. Ass. Petrol. Geol. 1, 108-121.

Elattar, A. A. A. A., (2003): Early-Middle Miocene Echinoids of Sadat

Formation, Sadat area, South Gabal Ataqa, NW Gulf of Suez,

Egypt, Egpt. Jour. Paleontol., 3, 209-241.

El-Bedewy, F. M. (1977): Paleontological studies on some Neogene fauna

of the area between Qosseir and Mersa Alam, Red Sea Coast, Egypt.

M.Sc. Thesis, Fac. Sci., Al-Azhar Univ., Egypt, 202 p.

References

185

El-Bedewy, F. M. (1989): Paleontological studies on some Neogene

Macrofossils of Egypt. Ph.D. Thesis, Fac. Sci., Mansoura Univ.,

Egypt, 413 p.

El-Gamal, M. (1968): Geology of Salum area (W.D.). M.Sc. Thesis, Fac.

Sci., Ain Shams Univ., Cairo.

El-Heiny, I. (1982): Neogene stratigraphy of Egypt. Newsl. Stratigr.,

11/2, 41-54.

El Safori, Y. A. (1994): Stratigraphy and paleontology of some Miocene

exposures on the westren side of the Gulf of Suez, Egypt, Ph.D.

Thesis, Ain Shams Univ., 278 p.

El Safori, Y. A. and El-Sorogy, A. S. (1999): Early Miocene bryozoa of

Gabal Gharra northwest Gulf of Suez, Egypt. Egyptian Journal of

Geology, 43/2, 353-375.

El-Shazly, S. H. (1987): Stratigraphy and microfacies of the Miocene

sediments at Sudr-Gharandal, West Sinai, Egypt. Ph.D. Thesis,

Fac. Sci., Ain Shams Univ., 274 p.

El-Shazly, S. H. and Saber, S. G. (1999): Facies and

macropaleontological studies of the Marine Miocene sediments of

Gabal Homeira, Cairo-Suez District, Egypt, Egyptian Journal of

Geology, 43/2, 317-341.

El-Sorogy, A. S. and Ziko, A. (1999): Facies development and

environments of Miocene reefal limestone, Wadi Hagul, Cairo-

Suez District, Egypt. N. Jb. Geol. Paläont. Mh, 4, 213-226.

Embry, A. F. and Klovan, E. J. (1972): Absolute water depths limits of

Late Devonian Paleoecological zones. Geol. Rdsch. 61/2.

Farag, I.M. and Sadek, A. (1966): Stratigraphy of Gebel Homeira area,

Cairo-Suez district. J. Geol. U.A.R. 10/2, 107-123.

Flugel, E. (1982): Microfacies Analysis of Limestone: Berlin, Springer-

Verlag, 633 p.

References

186

Folk, R. L. (1959): Practical petrographic classification of limestones.

Bull. Amer. Assoc. Petro., Geol., 43/1, 1-38.

Folk, R. L. (1962): Spectral subdivision of limestone types. In:

Classification of carbonate rocks. Bull. Amer. Assoc. Petro. Geol.,

46/1, 62-84.

Fourtau, R. (1916): The Echinoid fauna of the Neogene formations. Geol.

Mag., London, dec. 6, 3, 355-366.

Fourtau, R. (1920): Echinoderms neogenes de l’Egypte; catalogue des

invertebres fossiles de l'Egypte. Terrains Tertiares, Pt. 2. Geol.

Survey Egypt, Cairo, 100 p.

Fuchs, T. H. (1883): Beitrage zur kenntnis der Miocanfauna l’egyptens

und der Lybischen Wüste. Paleontographica, Stuttgart, 30, 18-66.

Ghonima, S.A., 1974 : Biostratigraphy of Mersa Matruh area ( North-

Western Desert, Egypt ). Ph.D. Thesis, Fac. Sci., Ain Shams Univ.

Ghorab, M. A. and Marzouk, I. M. (1965): A summary report on the

rock-stratigraphic classification of the Miocene in the Cairo-

Sukhna area. Internal Report, General Petroleum Co., Cairo, 600.

Hamam, K. A. (1966): Stratigraphy and paleontology of the area northwest

of Suez. M.Sc. Thesis, Fac. Sci., Ain Shams Univ., Cairo.

Hamza, F. H. (1972): Study on some Pliocene fauna from Egypt. M.Sc.

Thesis, Fac. Sci., Ain Shams Univ., Cairo, 228 p.

Hamza, F. H. (1992): Contribution to the Neogene biostratigraphy in the

eastern patr pf Egypt. M.E.R.C. Ain Shams Univ., Earth Sci. Ser.,

6, 151-166.

Haq, B.U., Hardenbal, J. and Vail, P.R. (1987) : Chronology of

fluctuating sea levels since the Triassic. Science, Vol. 235, pp.

1156-1166.

References

187

Harland, W. B.; Cox, A. V.; Llewellyn, P. G.; Pickton, C. A. G.; Smith,

A. G. and Walters, R. (1982) : A geologic time scale. Cambridge

Univ. Press, 140 p.

Hornes, M. (1856-1870): Die Fossilen Mollusken des Tertiaer. Beckens

von Wien.

Metwalli, H. M. (1963): The study of some Miocene sediments in Cairo

Suez district. M.Sc. Thesis, Fac. Sci., Cairo Univ.

Metwally, M. H. M. (1976) : Paleontological studies on some Neogene

pectinids from Egypt. M.Sc. Thesis, Fac. Sci., Ain Shams Univ.,

Cairo. 180 p.

Moore, R. C. (1969): Treatise on Invertebrate Paleontology. Geolo. Soc.

Amer., part N. Bivalvia, Univ. Kansas Press.

Murray, J. W. (1985): Atlas of invertebrate macrofossils. Longman, 241 p.

Pettijohn, F. J. (1975): Sedimentary Rocks. Harper & Row. New York,

628 pp.

Plumley, W. J., Risley, G. A., Graves, R. W., Kaley, M. E. (1962):

Energy index for limestone interpretation and classification. Mem.

Amer. Ass. Petrol., Geol., Tulsa, 1, 85-107.

Roger, J. (1939): Le genre Chlamys dans les Formations Neogene de

L'Europe. Ph.D. Theses, Faculty Des Science, Universite De Lyon,

286 p.

Sadek, H. (1926): The geography and geology of the district between

Gebel Ataqa and El-Galala El-Bahariya (Gulf of Suez). Geol. Surv.

of Egypt, 40, 120 p.

Sadek, H. (1959): The Miocene in the Gulf of Suez region (Egypt). Geol.

Surv. & Min. Research Dept., U.A.R., 118 p.

Said, R. (1962): Uber das Miozan in der westlichen Wuste Agypten.

Geol. Jb, 80, 349-366.

References

188

Said, R. (1971): Exploratory notes to accompany the geological map of

Egypt. Geol. Surv. Egypt, paper No. 56, 123 p.

Said, R. (1990): The Geology of Egypt. Balkema, Rotterdam, Brookfield,

734 p.

Said, R. and Metwalli, H. (1963): Foraminifera of some Miocene

sediments of the Cairo-Suez District. J. Geol. U.A.R., 7/1, 29-65.

Said, R. and Yellouze, M. (1955): Miocene fauna from Gebel Oweibed,

Egypt. Bull. Fac. Sci., Cairo Univ., 33, 61-81.

Sartorio, D. and Venturini, S. (1988) : Southern Tethys Biofacies. Agip.

Milan, Italy, 235 p.

Schaffer (1910): Zur kenntins der Miocanbildungen von Eggenburg. I.

Die Bivalvenfauna. Sitz. d. k. Akad. Wissensch. CXIX/1, Wien.

Selley, R. C. (1978): Ancient sedimentary environments (2nd edition).

Cornell Univ. Press, New York, 287 p.

Shukri, N. M. and Akmal, G. (1953): The geology of Gebel El Nasuri and

Gebel Anqabiya district. Bull. Soc. Geogr. Egypte, 26, 243-276.

Shukri, N. M. and Ayouti, M. K. (1956): The geology of Gebel Iweibid-

Gafra area, Cairo-Suez district. Bull. Soc. Geogr. Egypte, 29, 67-109.

Souaya, F. J. (1963): On the foraminifera of Gebel Gharra (Cairo-Suez

Road) and some Miocene samples. J. Paleont., 37/3, 433-457.

Stefanini, G. (1921): Fossili Terziari dell Cirenaica-Paleont. Ital., Vol. 27.

Stratigraphic Sub-Committee of the National Committee of Geological

Sciences (1974): Miocene Rock Stratigraphy of Egypt, (El-Gezeery,

M. N. and Marzouk I. M. eds.). Egypt. J. Geol., 18/1, 59 p.

Studencka, B. (1986): Bivalves from the Badenian (Middle Miocene)

marine sandy facies of Southern Poland.-Palaeotologia Polonica,

47, 1-128.

References

189

Szczechura, J. and Abd-Elshafy, E. (1988): Ostracodes and Foraminifera

from the Middle Miocene of the western coast of the Gulf of Suez,

Egypt. Acta Palaeont. Polonica, 33/4, 273-342.

Ugolini, R. (1906): Monographia dei pectinidi della Sadegena, 1st partie:

Generi Chlamys, Hinnites, Inequipecten. Paleont. Ital., 12.

Ugolini, R. (1908): Monographia dei pectinidi neogenic della Sadegena,

partie terza: Generi Amussipecten (Conti), Flabellipecten, Pecten,

Paleont. Ital., 14.

Wilson, J. L. (1975): Carbonate Facies in Geologic History : New York,

Springer-Verlag, 471 p.

Youssef, M. I., Bassiouni, M. A. and Cherif, O. H. (1971): Some

stratigraphic and tectonic aspects of the Miocene in the north

eastern part of the Eastern Desert. Bull. Inst. Desert. Egypte, 43,

109- 115.

Plates

Plate 1 Page Fig. 1: Arca (Anadara) grondica Mayer. 75 internal mold, right valve Fig. 2: Isognomon sp. 75 internal mold Fig. 3: Chlamys gentoni (Fontannes 1882) 76 a: external view of left valve b: internal view of left valve Fig. 4: Chlamys malvinae (Dubois) 77 a: external view of right valve b: internal view of right valve Fig. 5: Chlamys radians (Nyst) 78 a: external view of right valve b: internal view of right valve Fig. 6: Chlamys scabrella Lamarck 79 external view of left valve Fig. 7: Chlamys senatoria Gmelin 80 a: external view of right valve b: external view of left valve Fig. 8: Chlamys (Chlamys) costai (Fontannes, 1884) 81 a: external view of right valve b: internal view of right valve

Bar scale = 1cm

Plates

Plate 2 Page Fig. 1: Chlamys (Aequipecten) scabriuscula

(Matheron, 1842) 82 external view of right valve Fig. 2: Chlamys (Argopecten) macrotis (Sowerby, 1847) 84 a: external view of left valve b: internal view of left valve Fig. 3: Chlamys (Argopecten) submalvinae

(Blanckenhorn, 1901) 85 a: external view of right valve b: internal view of right valve Fig. 4: Chlamys (Macroclamis) sardoa Ugolini, 1906 87 a: external view of right valve b: external view of left valve Fig. 5: Pecten beudanti Basterot 89 a: external view of right valve b: internal view of left valve

Bar scale = 1cm

Plates

Plate 3 Page Fig. 1: Pecten erythraensis Sowerby 91 a: external view of left valve b: internal view of left valve Fig. 2: Pecten fuchsi Fontannes 92 a: external view of left valve b: internal view of left valve Fig. 3: Pecten (Pecten) cristato-costatus Sacco, 1897 93 a: external view of left valve b: internal view of left valve Fig. 4: Pecten (Pecten) fraasi Fuchs, 1883 95 a: external view of left valve b: internal view of left valve Fig. 5: Pecten (Pecten) ziziniae Blanckenhorn, 1901 96 a: external view of right valve b: internal view of right valve Fig. 6: Pecten (Amussiopecten) burdigalensis

Lamarck, 1819 99 a: internal mold b: internal mold

Bar scale = 1cm

Plates

Plate 4 Page Fig. 1: Pecten (Flabellipecten) flabelliformis

(Brocchi, 1809) 101 a: internal mold b: internal mold Fig. 2: Pecten (Oppenheimopecten) benedictus

Lamarck, 1819 102 a: external view of right valve b: internal view of right valve Fig. 3: Pecten (Oppenheimopecten) convexo-costatus

Abich, 1857 104 external view of right valve Fig. 4: Anomia burdigalensis Defrance 105 a: external view of right valve b: internal view of right valve Fig. 5: Anomia (Anomia) ephippium Linne, 1758 subsp.

rugulosostriata Brocchi, 1814 105 internal view of left valve Fig. 6: Crassostrea frondosa (De Serres) subsp. rohlfsi

Fuchs, 1883 107 a: external view of left valve b: internal view of left valve

Bar scale = 1cm

Plates

Plate 5 Page Fig. 1: Alectryonella plicatula (Gmelin) subsp. virleti

Deshayes, 1833 109 a: external view of left valve b: internal view of left valve Fig. 2: Lucina sp. 111 internal mold Fig. 3: Linga (Linga) columbella (Lamarck, 1819) 112 internal mold Fig. 4: Diplodonta sp. 113 internal mold Fig. 5: Cardium sp. 113 internal mold Fig. 6: Acanthocardia (Acanthocardia) paucicostata

(Sowerby, 1839) 114 internal mold Fig. 7: Lutraria sp. 115 internal mold Fig. 8: Gastrana sp. 116 internal mold, dorsal view Fig. 9: Gastrana laminosa (Sowerby) 116 internal mold

Bar scale = 1cm

Plates

Plate 6 Page Fig. 1: Gari sp. 117 internal mold Fig. 2: Azorinus sp. 118 internal mold Fig. 3: Paphia (Callistotapes)vetula (Bastrot, 1825) 119 internal mold Fig. 4: Clementia sp. 120 internal mold Fig. 5: Callista (Costacallista) erycina (Linne, 1758) 121 internal mold Fig. 6: Clavagella sp. 122 internal mold Fig. 7: Lanistes (Lanistes) mahmoudi Abbass, 1977 122 internal mold Fig. 8: Turritella (Turritella) cleevelyi Abbass, 1977 123 internal mold Fig. 9: Turritella (Turritella) terebralis Lamarck, 1799 124 internal mold Fig. 10: Luria (Luria) salwae Abbass, 1977 125 internal mold Fig. 11: Ampullina (Pseudamaura) maedai Abbass, 1977 126 internal mold Fig. 12: Ampullina (Pseudamaura) macfaydeni

Abbass, 1977 127 internal mold

Bar scale = 1cm

Plates

Plate 7 Page Fig. 1: Turritella (Eichwaldiella) fouadi Abbass, 1977 124 internal mold Fig. 2: Natica sp. 127 internal mold Fig. 3: Natica cf. millepunctata Lamarck, 1822 128 internal mold Fig. 4: Bursa faizae Abbass, 1977 129 internal mold Fig. 5: Ficus reticulatus (Lamarck, 1799) 129 internal mold Fig. 6: Ficus sp. 130 internal mold Fig. 7: Oliva (Neocylindrus) wagihi Abbass, 1977 131 internal mold Fig. 8: Conus (Lithoconus) mercati Brocchi, 1841 132 internal mold Fig. 9: Conus (Conolithus) melficus Desio, 1929 133 internal mold Fig. 10: Planorbis (Planorbis) nakanoi Abbass, 1977 134 internal mold Fig. 11: Clypeaster intermedius Desmoulins, 1837 135 aboral view

Bar scale = 1cm

Plates

Plate 8 Page Fig. 1: Clypeaster marginatus Lamarck, 1816 136 aboral view Fig. 2: Scutella ammonis Fuchs, 1883 137 view of a fragment Fig. 3: Parascutella stefaninii (Desio, 1929) 138 aboral view Fig. 4: Echinolampas amplus Fuchs, 1883 139 a: aboral view b: aboral view Fig. 5: Echinolampas plagiosomus Agassiz, 1840 141 a: aboral view b: oral view

Bar scale = 1cm

Plates

1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60 61 62 63 64 65 66 67 68 69 70 71 72 73 74 75 76 77 78 79 80 81 82 83 84 85 86 87 88 89 90 91 92 93 94 95 96 97 98 99 100 101 102 103 104 105 106 107 108 109 110 111 112 113 114 115 116 117 118 119 120 121 122 123 124 125 126 127 128 129 130 131 132 133 134 135 136 137 138 139 140 141 142 143 144 145 146 147 148 149 150 151 152 153 154 155 156 157 158 159 160 161 162 163 164 165 166 167 168 169 170 171 172 173 174 175 176 177 178 179 180 181 182 183 184 185 186 187 188 189 190 191 192 193 194 195 196 197 198 199 200 201 202 203 204 205 206 207 208 209 210 211 212 213 214 215 216 217 218 219 220 221 222 223 224 225 226 227 228 229 230 231 232 233 234 235 236 237 238 239 240 241 242 243 244 245 246 247 248 249 250 251 252 253 254 255 256 257 258 259 260 261 262 263 264 265 266 267 268 269 270 271 272 273 274 275 276 277 278 279 280 281 282 283 284 285 286 287 288 289 290 291 292 293 294 295 296 297 298 299 300

Plates

1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55 56 57 58 59 60 61 62 63 64 65 66 67 68 69 70 71 72 73 74 75 76 77 78 79 80 81 82 83 84 85 86 87 88 89 90 91 92 93 94 95 96 97 98 99 100 0 0 0 0 0 0 0 0 0 0 1a 2a 3a 4a 5a 6a 7a 8a 9a 10a 11a 12a 13a 14a 15a 16a 17a 18a 19a 20a 21a 22a 23a 24a 25a 26a 27a 28a 29a 30a 31a 32a 33a 34a 35a 36a 37a 38a 39a 40a 41a 42a 43a 44a 45a 46a 47a 48a 49a 50a 51a 52a 53a 54a 55a 56a 57a 58a 59a 60a 61a 62a 63a 64a 65a 66a 67a 68a 69a 70a 71a 72a 73a 74a 75a 76a 77a 78a 79a 80a 81a 82a 83a 84a 85a 86a 87a 88a 89a 90a 91a 92a 93a 94a 95a 96a 97a 98a 99a 100a 0a 0a 0a 0a 0a 0a 0a 0a 0a 0a 1b 2b 3b 4b 5b 6b 7b 8b 9b 10b 11b 12b 13b 14b 15b 16b 17b 18b 19b 20b 21b 22b 23b 24b 25b 26b 27b 28b 29b 30b 31b 32b 33b 34b 35b 36b 37b 38b 39b 40b 41b 42b 43b 44b 45b 46b 47b 48b 49b 50b 51b 52b 53b 54b 55b 56b 57b 58b 59b 60b 61b 62b 63b 64b 65b 66b 67b 68b 69b 70b 71b 72b 73b 74b 75b 76b 77b 78b 79b 80b 81b 82b 83b 84b 85b 86b 87b 88b 89b 90b 91b 92b 93b 94b 95b 96b 97b 98b 99b 100b 0b 0b 0b 0b 0b 0b 0b 0b 0b 0b a b c a b c a b c a b c d e f g h i j k l m n o p q r s t u v w x y z i ii iii iv v vi vii viii ix x xi xii xiii xiv xv xvi xvii xviii xix xx A B C A B C A B C A B C D E F G H I J K L M N O P Q R S T U V W X Y Z I II III IV V VI VII VIII IX X XI XII XIII XIV XV XVI XVII XVIII XIX XX

Plates

+++++++++++

2 0.5

xxxxxxxxxxxxx

Gabal Geneifa section.

BE

D N

O.

TH

ICK

. (

m )

LIT

HO

LO

GY

BIO

ST

RA

TIG

RA

PH

IC

U

NIT

S

M

i

o

c

e

n

e

M i

d d

l e

M i

o c

e n

e

L a

n g

h i

a n

-

---

S

e r

r a

v a

l i

a n

(

? )

G e

n e

f e

F o

r m

a t

i o

n

14 5

13

TIM

E

UN

IT

RO

CK

UN

IT

17

Chl

amys

(Mac

roch

lam

is)

sard

oa

zone

12 1.511 1

Pec

ten

(Pec

ten)

cr

ista

to-

cost

atus

zon

e

10 1.5

9 5

E a

r l

y

M

i o

c e

n e

B

u

r

d

i

g

a

l i

a

n

G h

a r

r a

F o

r m

a t

i o

n

8

5

3

Chl

amys

ge

nton

i zo

ne

4 12

3.5

7 14.5

6 1.5

1.6

1 25

7.5

0

1

2

3 m

++++++++++++

8 0.5

Gabal Gharra section.

B

IOS

TR

AT

IGR

AP

HIC

U

NIT

S

4

15 30

M

i

o

c

e

n

eM

i

d

d

l

e

M

i

o

c e

n

e

L a

n g

h i

a n

----

S e

r r

a v

a l

i a

n

( ?

)G

e n

e f

e

F

o r

m a

t i

o n

Chl

amys

(Arg

opec

ten)

su

bmal

vina

e z

one

14 24.5

Chl

amys

(Mac

roch

lam

is)

sard

oa z

one

16.4

Pec

ten

(Pec

ten)

cr

ista

to-c

osta

tus

zo

ne

E

a r

l

y

M

i

o

c e

n

e

B

u

r

d

i

g

a

l i

a

n

G h

a r

r a

F o

r m

a t

i o

n

12 4.9Pecten

(Flabellipecten) flabelliformis zone

11 19.5

Pec

ten

(P.)

ziz

inia

e -

Pec

ten

(Fla

belli

pect

en)

flab

ellif

orm

is

bar

ren

inte

rzon

e

10 3.2 Pecten (P.) ziziniae zone

6.1

9 5

Chl

amys

ge

nton

i zo

ne

7 6

6 7.7

3.4

TH

ICK

. ( m

)

LIT

HO

LO

GY

3 1.5

2 7

5 2

4

Oligocene

TIM

E U

NIT

RO

CK

UN

IT

BE

D N

O.

1

13

16

3 m

012

++++++++

2 0.5

Gabal Homeira section.

19 30

Chl

amys

(M

acro

chla

mis

) sa

rdoa

zon

e

18

M

i

o

c

e

n

e

M

i

d

d

l

e

M

i o

c

e

n

e

L a

n g

h i

a n

----

S e

r r

a v

a l

i a

n

(

? )

G e

n e

f e

F o

r m

a t

i o

n

3.3

Pec

ten

(P

ecte

n) c

rist

ato-

cost

atus

zon

e

17 3.9

16 25.5

13 2.5

E

a r

l

y

M

i

o

c e

n

e

B

u

r

d

i

g

a

l i

a

n

G h

a r

r a

F o

r m

a t

i o

n

15

10

7

4

B

IOS

TR

AT

IGR

AP

HIC

UN

ITS

1.5

6 3

1.5

9 4.3

8 3

Pec

ten

(Pec

ten)

zi

zini

ae z

one

2.7

TH

ICK

. ( m

)

LIT

HO

LO

GY

1.4

2.9

5

4.2

5

6.1

4.6

Oligocene

TIM

E U

NIT

RO

CK

UN

IT

BE

D N

O.

1

3

5

12

11

14

3 m

0

1

2

Congl.

BE

D N

O.

TH

ICK

.

LITHO

LOGY

SstClayShale

LITHO

LOGY

BE

D N

O.

TH

ICK

.

LITHO

LOGY

Marl16 4 +++++++

Time Rock Unit

Ro

ck U

nit

BE

D N

O.

TH

ICK

.

e unexposedp uncovered

LITHO

LOGY

Marl16 4 +++++++

Lst

15 30

Time Rock Unit

Ro

ck U

nit

BE

D N

O.

TH

ICK

.

Chalky Lst

Dolom.xxxxxxx

M

i

o

c

e

n

e

M i

d d

l e

M

i o

c e

n e

L a

n g

h I

a n

-

--

S e

r r

a v

a l

I a

n

(

? )

G e

n e

f e

F o

r m

a t

I o

n 19 30

+++++++ ++++++

BE

D N

O.

TH

ICK

.

LITHO

LOGY

4.2

13 16.4

4.9

15 30

M

i

o

c

e

n

e

M i

d d

l e

M

i o

c e

n e

L a

n g

h I

a n

-

--

S e

r r

a v

a l

I a

n

(

? )

G e

n e

f e

F o

r m

a t

I o

n 19 30

BE

D N

O.

TH

ICK

.

LITHO

LOGY

14 24.5 5

17

18 3.314

17 3.9

13

16 25.5

12 1.510 & 11 2.5

9 5

L o

w e

r

M

i o

c e

n e

B

u

r

d

i

g

a

l

i a

n

G h

a r

r a

F o

r m

a t

i o

n

15 6.1 12 8 3.5

7 14.5

11 19.5

14 4.6

13 2.5

126 1.5

11 55 7.510 1.5 10 3.2

9 4.39 5

128 3

7 & 8 6.57 1.56 3

5 56 7.7 2 & 3

4

2.14 1.4

1 25

2 & 3 3.4 5 2

4 6.11 2.7

O l i g o c e n e 3 1.5

2 7

xxxxxxx1 3.4

Oligoc.Geneifa section

( 97.1m )

Homeira section( 110.9m )

8 m

0 m

4 m

Gharra section( 141.7m )

Fig. 2 : Lithostratigraphic correlation chart for the three studied Miocene sections in the Cairo-Suez District.

( 97.1m )Gharra section( 141.7m )

Shukry & Akmal

( 1953 )

Shukri & Ayouti

( 1956 )

Plioc.Hamzi

Fm

Genefe Member

Genefe Fm

Gafra Member

Reishi Member

Un

it

II Sadat Reefal LST

Member

Un

it

I

Agrud Sandstone

Member

PresentWork

Eoc

ene

Oligoce

ne

Oligoce

ne

Oligoce

ne

Upper Eocene

Mid

dle

Mio

cen

e

Gen

efe

Fo

rmat

ion

Ear

ly M

ioce

ne

Gh

arr

a F

orm

ati

on

Olig

ocen

e

Elattar(2003)

Gh

arr

a F

orm

ati

on

Mid

dle

M

ioce

ne

Sad

at

Fo

rmat

ion

Ear

ly M

ioce

ne

( ? )

Mid

dle

Mio

cen

e

Gen

efe

Fo

rmat

ion

Ear

ly M

ioce

ne

&Saber

Late

Miocene

Mid

dle

M

ioce

ne

Ear

ly M

ioce

ne

Upper Eocene

Sad

at

Fo

rmat

ion

Ho

mm

ath

F

m

Moneim( 1992 )

Lat

e M

ioce

ne

Abdel-

Ha

gu

l F

mG

hew

eib

ba

Fm

Oligoce

ne

Oligoce

ne

Olig

ocen

e

Olig

ocen

e

Oligocene

Oligoce

ne

Oligocene

Bu

rdig

ali

an

Sad

at

Fo

rmat

ion

Aq

uit

ania

n-

Bu

rdig

ali

an

Gh

arra

F

orm

atio

n

Genefe Chalky

LST Member

Mid

dle

Mio

cen

e

Lan

gh

ian

Gen

efe

Fo

rmat

ion

Ho

mm

ath

Fo

rmat

ion

Ho

mm

ath

San

dy

Lim

esto

ne

Mem

ber

Mar

ine

Mio

cen

e

Mid

dle

Mio

cen

e

Genefe Formation

Gh

arra

F

orm

atio

n

Ho

mm

ath

Fo

rmat

ion

Abbasia Member

Reishi Member

Lo

wer

Mio

cen

e

Sadat Formation

Un

it

I

II

Hel

veti

an

Mar

ine

Mio

cen

eV

ind

ob

on

ian

Bu

rdig

ali

an

Bu

rdig

ali

an

Hel

veti

an

Un

it

I

I

Gh

arra

F

orm

atio

n

Hel

veti

an

Gafra Member

Abbasia Member

Bu

rdig

ali

an

Un

it

I

Sukhna Member

Bu

rdig

ali

anM

arin

e M

ioce

ne

Mid

dle

Mio

cen

eM

arin

e M

ioce

ne

Cal

care

ou

s U

nit

Lo

wer

Mio

cen

e

San

dy

Un

it

Hagul Formation

Lat

e P

lioce

ne

Hamzi Fm

Mes

sin

ian

Hagul Fm Hagul

FmNo

n M

arin

e M

ioce

ne

Up

per

Mio

cen

e

No

n M

arin

e M

ioce

ne

Up

per

Mio

cen

e

Iwei

bid

Fm El-Bahhara

Member

Up

per

Mio

cen

e

El-Hamza Member

Non Marine Miocene

Up

per

Mio

cen

eN

on

Mar

ine

Mio

cen

e

( 1990 )( 1965 ) ( 1966 ) ( 1970 ) ( 1974 )

El-Heiny Said(1962b) ( 1963 ) Marzouk ( 1966 ) Sadek Aboul Ela ( 1977 ) ( 1982 )

Said Metwalli & HamamEl Shazly

( 1999 )

PO

ST

M

IDD

LE

M

IOC

EN

E

Ghorab Farag BarakatStratigraphic

Sub-Committee& & Abbass

Oligocene

Eoc

ene

Oligoce

ne

Oligoce

ne

Oligoce

ne

Upper Eocene

Olig

ocen

e

Upper Eocene

Oligoce

ne

Oligoce

ne

Olig

ocen

e

Olig

ocen

e

Oligocene

Oligoce

ne

Oligocene

Table 1: Different rock units proposed by different authors for the Miocene rocks in the Cairo-Suez District.

Egy

pt

Syr

ia

Alg

eria

Ital

y

Mal

ta

Rho

ne

Val

ley

Vie

nna

Bas

in

Fra

nce

Esp

ain

Por

tuga

l

Pol

and

Hon

gari

a

Arm

enia

Zan

zib

ar

Present Work

1- Arca (Anadara) grondica Mayer (M) M

2- Isognomon sp. E

3- Chlamys gentoni Fontannes (M) E

4- Chlamys malvinae (Dubois) (M) L E-M

5- Chlamys radians (Nyst) L M

6- Chlamys scabrella Lamarck L E E-M

7- Chlamys senatoria Gmelin E E M

8- Chlamys (Chlamys) costai (Fontannes) E-M E-L E M

9- Chlamys (Aequipecten) scabriuscula (Matheron) M M-L M, L E

10- Chlamys (Argopecten) macrotis (Sowerby) M M E-L E E-L M

11- Chlamys (Argopecten) submalvinae (Blanckenhorn) M M M

12- Chlamys (Macrochlamis) sardoa Ugolini E L M

13- Pecten beudanti Basterot (M) E

14- Pecten erythraensis Sowerby (M) E

15- Pecten fuchsi Fontannes M L E

16- Pecten (Pecten) cristato-costatus Sacco E (M) M

17- Pecten (Pecten) fraasi Fuchs E M E-M

18- Pecten (Pecten) ziziniae Blanckenhorn E E

19- Pecten (Amussiopecten) burdigalensis Lamarck E E E

20- Pecten (Flabellipecten) flabelliformis (Brocchi) L L (M) E

21- Pecten (Oppenheimopecten) benedictus Lamarck E-M E-L E

22- Pecten (Oppenheimopecten) convexo-costatus Abich E M

23- Anomia burdigalensis Defrance M (M) E

24- Anomia (Anomia) ephippium subsp. rugulosostriata Brocchi M L (M) (M) E

25- Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs (M) (M) E-M

LocalitiesSpesies

26- Alectryonella plicatula (Gmelin) subsp. virleti Deshayes E-L E-M

27- Lucina sp. (M) (M) (M) E

28- Linga (Linga) columbella Lamarck M (M) M E

29- Diplodonta sp. (M) (M) (M) M

30- Cardium sp. E-M

31- Acanthocardia (Acanthocardia) paucicostata (Sowerby) M M M E

32- Lutraria sp. M

33- Gastrana sp. (M) E-M

34- Gastrana laminosa (Sowerby) M M

35- Gari sp. (M) M

36- Azorinus sp. E

37- Paphia (Callistotapes) vetula (Bastrot) M (M) L L (M) M (M) E-M

38- Clementia sp. E-M

39- Callista (Costacallista) erycina (Linne) M (M) M

40- Clavagella sp. (M) M

41- Lanistes (Lanistes) mahmoudi Abbass L M

42- Turritella (Turritella) cleevelyi Abbass (M) E

43- Turritella (Turritella) terebralis Lamarck E-M E-M

44- Turritella (Eichwaldiella) fouadi Abbass L E

45- Luria (Luria) salwae Abbass L M

46- Ampullina (Pseudamaura) maedai Abbass L M

47- Ampullina (Pseudamaura) macafaydeni Abbass L M

48- Natica sp. Abbass (M) (M) M

49- Natica cf. millepunctata Lamarck E-M (M) E

50- Bursa faizae Abbass E E

51- Ficus reticulatus (Lamarck) M (M) E

52- Ficus sp. (M) (M) E-M

53- Oliva (Neocylindrus) wagihi Abbass L M

54- Conus (Lithoconus) mercati Brocchi E-L (M) (M) E-M

55- Conus (Conolithus) melficus Desio E-M E

56- Planorbis (Planorbis) nakanoi Abbass L M

57- Clypeaster intermedius Desmoulins E-M (M) (M) (M) (M) (M) M

58- Clypeaster marginatus Lamarck M (M) (M) (M) (M) E-M

59- Scutella ammonis Fuchs E-M E-M

60- Parascutella stefaninii (Desio) E- M E-M

61- Echinolampas amplus Fuchs E-M E-M

62- Echinolampas plagiosomus Agassiz M (M) (M) (M) (M) E

E = Early Miocene M = Middle Miocene L = Late Miocene (M) = MioceneTable 2: The ages assigned by previous authors to the recorded fauna in some parts of the world.

Ro

ck U

nit

Bed No.

Th

ick

.

(

m )

Lit

ho

log

y

+++++

Silty calcareous claystone : Greenish gray to brownish gray; soft to moderately compact; highly gypsiferous; ferruginous; unfossiliferous. Silt composes of medium quartz grains.

Highly fossiliferous sandy limestone : Grayish white to yellowish white, brownish gray in parts; moderately compact; slightly argillaceous. It yields bivalvia as Chlamys radians, Chlamys (Chlamys)

17

Argillaceous limestone : Yellow to yellowish brown; moderately compact; fossiliferous, with Crassostrea frondosa subsp. rohlfsi, and Alectryonella plicatula subsp. virleti and foraminifers as Miogypsina intermedia.

Fossiliferous limestone : white to yellowish white grading upwards into yellow; moderately compact to compact; massive; slightly argillaceous; with some gypsum veins; fossiliferous to highly fossiliferous at the upper part, sandy in the lower part. Sand grains are medium to fine quartz grains; subrounded to subangular.

It yields bivalvia as large sized oysters, single and double-valved as Alectryonella plicatula subsp. virleti , Crassostrea frondosa (De Serres) subsp. rohlfsi Fuchs and others; large sized pectinids as Pecten (Oppenheimopecten) convexo-costatus, Chlamys (Macrochlamis) sardoa, Gastrana sp.; gastropods as Conus (Lithoconus) mercati, Ampullina (Pseudamaura) maedai; echinoids as Echinolampas amplus, Clypeaster marginatus; bryozoans such as holoporella sp. also, it yields algae as Lithothamnium sp. and Lithophyllum sp; foraminifers as Operculina complanata, Miogypsina intermedia, Amphistegina sp., and other foraminifers.

Fossiliferous sandy marl : Brownish white to yellowish white; soft to moderately compact. It yields bivalvia as Pecten (Pecten) cristato-costatus, Pecten (Pecten) fraasi, Chlamys (Argopecten) macrotis, Chlamys (Chlamys) costai, Chlamys radians; echinoidal, molluscan and foraminiferal fragments; Holoporella sp. The microfossils are represented by Operculina complanata, Miogypsina intermedia. Also, it yields algae as Lithothamnium sp. and Lithophyllum sp.

Fossiliferous limestone : Yellowish brown to brown; compact; massive; slightly ferruginous; argillaceous; fossiliferous. It yields Chlamys (Macrochlamis) sardoa, Clypeaster intermedius; echinoidal, molluscan and bryozoans fragments. The microfossils such as algal fragments as Lithothamnium sp. and Lithophyllum sp.; foraminifers as Operculina complanata, Miogypsina intermedia, Amphistegina sp. and other foraminifers.

1.5

Time Rock UnitInsoluble Residue % Lithologic Description

14 5

n

e

M i

d d

l e

M i

o c

e n

eL

a n

g h

i a

n

--

--

S

e r

r a

v a

l i

a n

( ?

)

G e

n e

f e

F o

r m

a t

i o

n

13

11 1

12

10 1.5

9 5

0 50 1000 50

Fossiliferous sandy limestone :Brownish white to white, occasionally yellowish white; compact; massive; jointed; slightly argillaceous. It is highly fossiliferous yielding Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp virleti , Azorinus sp., Isognomon sp., Chlamys gentoni; gastropod molds; echinoids as Echinolampas amplus, Clypeaster sp., Scutella sp. and others; numerous Balanus concavus; red algae as Lithothamnium sp.; Holoporella sp.; corals (small heads, sometimes dissolved and leaving only their molds). The main foraminiferal species in this bed are Operculina sp., Amphistegina sp. and Heterostegina sp.

Silty claystone : Brown to dark brown and yellowish brown; moderately compact; laminated; gypsiferous; ferruginous; unfossiliferous; very slightly calcareous. Silt represents 30-40% and composed of quartz grains.

Fossiliferous limestone : Brownish white to yellowish white; highly compact; fractured; dolomitic. Limestone composed of crypto crystalline calcite. Dolomite composed of micro to fine euhedral crystals. It yields Holoporella sp.; Operculina complanata, Amphistegina sp., Miogypsinids; echinoid fragments (plates and spines); molluscan fragments.

Dolomitic argillaceous sandstone : Yellowish white to white and yellow; compact; fine to medium quartz grains; with dolostone lenses of micro to fine subhedral crystals, sometimes associated with grains of ferruginous materials; poorly fossiliferous represented by some molluscan fragments.

y g y g y y y ( y )costai , Chlamys (Argopecten) macrotis, Pecten (Pecten) cristato-costatus, Pecten (Pecten) fraasi , Crassostrea frondosa subsp. rohlfsi, gastropods as Natica sp., Ampullina (Pseudamaura) macfaydeni ; regular echinoids; bryozoans as Retepora sp., Holoporella sp.; foraminifers as Amphistegina sp., Miogypsina intermedia , Operculina sp. and other foraminifers.

M

i

o

c

e

8 3.5

4 12

7 14.5

6 1.5

5 7.5

M

i o

c e

n e

g

a

l

i

a

n

F o

r m

a t

i o

n

Calcareous sandstone : Brown to yellowish brown, occasionally brownish gray; fine to coarse quartz grains; subrounded to subangular; poorly to ill-sorted; moderately compact to semi-friable; rarely fossiliferous; ferruginous. The calcareous matter is calcite, represents the cement between the quartz grains. The fauna are represented by shell fragments of bivalvia.

2 0.5

xxxxx

Fig. 9: Lithostratigraphic succession of the Miocene sediments at Gabal Geneifa.

Base unexposed

Top uncovered

Conglomerate

xxxxxxxx

+++++++

Sandstone

Clay

Shale

Marl

Limestone

Chalky Limestone

Dolomite

1.6L o

w e

r

B

u

r

d

i

G h

a r

r a

Shale : Gray, brownish gray to yellowish gray, moderately compact, thinly laminated, jointed, unfossiliferous, ferrugineous, gypsiferous, with gypsum bands and veins (Thick up to 2 cm), very slightly calcareous, dipping to the west ( 20-30 deg ), silty, its base unexposed.

1 25

Calcareous sandstone : Yellowish brown; fine to medium quartz grains; moderately sorted; semi-friable to moderately compact; with few fresh feldspar minerals (plagioclase); fossiliferous with shell fragments of bivalvia.

Conglomeratic sandstone : Yellow to yellowish brown, medium to coarse quartz grains, occasionally very coarse grained, occasionally fine grained, subangular to subrounded, poorly sorted, semi- friable to moderately compact, unfossiliferous.

3

0

1

2

3 m

RO

CK

UN

IT

BE

D N

O.

TH

ICK

.( m

)

LIT

HO

LO

GY

+++++

Chalky Limestone

Dolomite

Top uncovered

Oligocene

+++++++

Olig.

Clay

Shale

Marl

Limestone

? )

Time Rock Unit

INSOLUBLE RESIDUE %

15 30

LITHOLOGIC DESCRIPTION

16 4

Chalky Limestone : Yellowish white to white, occasionally yellow; moderately compact. It yields some shell fragments, echinoid plates and undefined foraminifera. Also, it yields algae as Lithothamnium sp. and Lithophyllum sp.

Conglomerate

Sandstone

Fossiliferous sandy chalky limestone : Yellow to yellowish white; moderately compact; algal in parts. Sand grains are fine to medium quartz grains; subangular to subrounded. It yields Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp virleti, Chlamys (Argopecten) submalvinae, Chlamys (Argopecten) macrotis, Chlamys malvinae, Chlamys senatoria; broken parts of echinoids; bryozoa and few corals; foraminifers as Miogypsina intermedia .

0 50 100

n

eM

i

d

d

l

e

M

i o

c

e

n

e

L a

n g

h i

a n

----

S e

r r

a v

a l

i a

n

(

G e

n e

f e

F o

r m

a t

i o

n

14 24.5

Fossiliferous limestone : White to yellowish white, occasionally milky white; moderately compact; bioturbated in the upper part with a yellowish brown color. It yields Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp virleti , embryonic stages of oysters are found. Also, it yields Chlamys (Macrochlamis) sardoa, and other pectinidae fragments; Echinolampas amplus, Clypeaster intermedius , echinoid spines and corals; algae as Lithothamnium sp. and Lithophyllum sp.

Fossiliferous limestone: Yellow to yellowish white; compact; massive; slightly argillaceous; slightly sandy. It yields bivalvia as Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp virleti , Pecten (Pecten) cristato-costatus, Chlamys (Argopecten) macrotis, Chlamys scabrella, Chlamys senatoria ; Cardium sp.; rich in molds of Callista (Costacallista) erycina, Paphia (Callistotapes) vetula, Clementia sp., Diplodonta sp., Gari sp. Also it yields Lutraria sp., Gastrana laminosa; gastropods as Turritella (Turritella) terebralis ; echinoderms as Echinolampas amplus, Clypeaster marginatus,

M

i

o

c

e

13 16.4

11 19.5

Scutella ammonis; crustacea as Balanus concavus; coral reefs as Leptastrea sp. The lower 0.5m of this bed represents a pectinids and oyster bank, whereas the upper (20-125 cm) represents a sclaractenian coral reef which is monospecific (Leptastrea sp.), and it is replaced in parts with an algal limestone band. Algae represented by Lithothamnium sp. and Lithophyllum sp.

12 4.9

Fossiliferous calcareous sandstone : Yellow to yellowish white, occasionally yellowish brown; moderately compact, occasionally semi-friable to friable; fine to medium quartz grains; pebbly at base. It yields bivalvia as Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp virleti ; Chlamys scabrella, Pecten (Flabellipecten) flabelliformis, Anomia burdigalensis, Clementia sp. Also it yields echinoderms as Scutella ammonis , Parascutella stefaninii and other echinoderms.

Sandy shale : Dark gray to gray; soft to moderately compact; gypsiferous; unfossiliferous; more sandy upwards; interbedded with ferruginous bands of 5 cm thick for each, these bands increase in number upwards. Sand grains are fine to very fine quartz grains; subrounded.

8 0.5

Calcareous shale : Dark gray to gray; moderately compact; fractured; unfossiliferous; very slightly sandy; silty. Sand grains are fine to very fine quartz grains, subrounded to subangular, moerately sorted.

L

o

w

e

r

M

i o

c

e

n

e

B

u

r

d

i

g

a

l

i a

n

G h

a r

r a

F o

r m

a t

i o

n

Fossiliferous argillaceous limestone : Brownish yellow to yellow; soft. It yields Alectryonella plicatula subsp virleti. A pectinids band occurs at the upper 0.5m, it yields large-sized pectinids as Pecten (Pecten) fraasi, Pecten (Pecten) ziziniae, Pecten (Oppenheimopecten) benedictus, very crowded with Pecten beudanti, Pecten (Amussiopecten) burdigalensis. This bed also yields Gastrana sp.; gastropods as Conus (Lithoconus) mercati, Ficus sp.; crustacea as Balanus; bryozoa and few coral heads; algae as Lithothamnium sp. and Lithophyllum sp; foraminifers as Operculina complanata, Miogypsina intermedia and Heterostegina sp.

10 3.2

9 5

Argillaceous limestone : Yellowish brown; moderately compact; slightly sandy; poorly fossiliferous with Chlamys gentoni and other broken fragments.

7 6 Sandy limestone : Yellow to yellowish brown; moderately compact; slightly argillaceous. Sand grains are fine to medium quartz grains; subangular to subrounded. It is poorly fossiliferous yielding foraminifers as Amphistegina sp, Operculina complanata and Miogypsina intermedia .

6 7.7

Fossiliferous sandy limestone : Yellow to yellowish white; moderately compact; slightly argillaceous. Sand grains are fine to medium quartz grains; subangular to subrounded. Fossils are represented by Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp virleti , Chlamys gentoni ; Lucina sp.; gastropods as Natica cf. millepunctata ; many chips of Scutella ammonis , Parascutella stefaninii , Prionocidaris cf. avenionensis , Echinolampas sp., Clypeaster sp. and echinoid spines; bryozoa.

5 2Calcareous sandstone : Dark yellowish brown; moderately compact; fine to medium quartz grains; subangular to subrounded; moderately sorted; ferruginous in parts.

4 6.1

Shale : Light to dark gray; moderately compact; sandy; silty; slightly calcareous; underlianed by ferruginous hard sandstone band of 5 cm thick.

Ferruginous sandstone : Yellowish brown; fine to medium quartz grains; subangular to subrounded; moderately sorted; argillaceous; very slightly calcareous, unfossiliferous. It is encountered between 3 1.5

Fig. 22: Lithostratigraphic succession of the Miocene sediments at Gabal Gharra.

Olig.

two hard ferruginous sandstone bands 5 cm thick for each.

2 7Shale : Reddish brown at the base, gray upwards; soft at bottom, firm upwards; sandy; silty; very slightly calcareous, unfossiliferous, unfossiliferous. Sand grains in shale are fine to medium quartz grains; subrounded to subangular. Sand grains in the ferruginous band are medium to coarse quartz grains; subangular to subrounded.

The uppermost part of the Oligocene sediments are composed mainly of sands, gravels, boulders and silicified woods.

1 3.4Sandstone : Yellowish brown to reddish brown; moderately compact to semi-friable; fine to medium quartz grains; subangular to subrounded; moderately sorted; unfossiliferous. It unconformably overlies the Oligocene sands, gravels and boulders.

3 m

0

1

2

Ro

ck

Un

it

Bed

No

.

Th

ick

. (

m )

Lit

ho

log

y

++++

Time Rock Unit

Insoluble Residue % Lithologic Description

Fossiliferous sandy limestone : Yellowish white to light brownish white; moderately compact to compact; massive; fractured in parts; argillaceous. Sand grains are fine to medium quartz grains; subrounded to subangular. It yields Chlamys (Macrochlamis) sardoa and other small-sized pectinids; molds of other bivalves as Cardium sp., Clavagella sp., Gastrana sp., Gastrana laminosa, Arca (Anadara) grondica; gastropods as Turritella (Turritella) terebralis , Ficus sp., Lanistes (Lanistes) mahmoudi , Luria (Luria) salwae , Oliva (Neocyclindrus) wagihi , Planorbis (Planorbis) nakanoi; worm tubes; sclarctenian corals and bryozoans. Also it yields foraminifers as Heterostegina sp., Amphistegina sp. and other foraminifers; algae as Lithothamnium sp. and Lithophyllum sp.

19 30

e

n

ei

a n

( ?

) i

o n

Marl

Limestone

Chalhy Limestone

Dolomite

ConglomerateSandstone

Clay

Shale

Top uncovered +++++++

0 50 100

Marl : ( Oyster bank ): Brownish yellow; soft to moderately compact; clayey at base, gradually become more calcareous at top. The sediments represent the matrix between the fauna which are mainly represented by Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp virleti . It yields Pecten (Pecten) cristato-costatus; broken parts of Scutella ammonis and Parascutella stefaninii.

Fossiliferous limestone : Yellowish white to yellow, yellowish brown to brown in the upper two meters; moderately compact. It is rich in large-sized oysters as Pecten (Pecten) cristato-costatus, Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp virleti . Also, it yields Cardium sp.; broken parts of echinoids as Scutella ammonis, Parascutella stefaninii and echinoid spines; algae as Lithothamnium sp. and Lithophyllum sp.; foraminifera as Amphistegina sp.

18 3.3

17 3.9

16 25.5

c

e

n

eM

i

d

d

l

e

M

i o

c

L

a n

g h

i a

n

--

--

S

e r

r a

v a

l i

G e

n e

f e

F o

r m

a t

Fossiliferous sandy limestone : Yellow to yellowish white; moderately compact; argillaceous. Sand grains are fine to medium quartz grains; rounded to subrounded. It yields Pecten (Pecten) cristato-costatus . It is rich in Scutella ammonis , Parascutella stefaninii and broken parts of other echinoid species. Also, it yields some fragments of pectinids and other bivalves nd foraminifers as Miogypsina intermedia .

Shale : Greenish gray to yellowish green, occasionally stained with yellow color; moderately compact; highly fractured and jointed; soapy; gypsiferous; unfossiliferous; slightly calcareous; slightly sandy; slightly silty.

Sandy limestone : Yellowish white to yellowish brown; moderately compact. Sand grains are fine to medium quartz grains; subangular to subrounded; moderately sorted; with eroded periphery; pebbly at its lower part. It is poorly fossiliferous with bad preserved bivalvia, Balanus concavus and echinoid fragments.

Claystone : Gray, greenish gray to light green, occasionally yellowish green; moderately compact; fractured; jointed; fissile; unfossiliferous; slightly calcareous; very slightly sandy; slightly silty.

Argillaceous calcareous sandstone : Yellow to yellowish brown; fine to medium quartz grains; angular to subrounded; moderately sorted; moderately compact; with altered plagioclase, microcline and biotite.

Fossiliferous sandy limestone : Yellowish brown to light brown; soft to moderately compact; slightly argillaceous. Sand grains are fine to medium quartz grains; subangular to subrounded; moderately sorted.

Claystone : Gray to light gray, occasionally dark gray; soft; gypsiferous; unfossiliferous; slightly calcareous; silty.

Calcareous sandstone : Yellowish white to yellowish brown; fine to coarse quartz grains; angular to subrounded; poorly sorted; moderately compact; slightly argillaceous; poorly fossiliferous with bad preserved oysters and pectinids.

It yields bivalvia as Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp. virleti. It is rich in pectinids as Pecten (Pecten) ziziniae , Pecten fuchsi , Pecten (Oppenheimopecten) benedictus, Pecten erythraensis, Pecten beudanti , Pecten (Flabellipecten) flabelliformis, other bivalves as Linga (Linga) columbella , Cardium sp., Anomia burdigalensis, Anomia (Anomia) ephippium subsp. rogulosostriata ; gastropods as Conus (Lithoconus) mercati , Conus (Conolithus) melficus, Ficus reticulatus ; broken echinoids as Clypeaster sp. ; and Balanus concavus; algae as Lithothamnium sp. and Lithophyllum sp.

Fossiliferous sandy limestone : Yellowish white to brownish white; moderately compact; fractured; slightly argillaceous; calcareous matter represented by cryptocrystalline calcite. Sand grains are fine to coarse quartz grains; subrounded to rounded; poorly sorted and stained with iron oxides on periphery.

It yields Crassostrea frondosa subsp. rohlfsi , Alectryonella plicatula subsp. virleti , Pecten fuchsi , Pecten (Pecten) ziziniae , Chlamys malvinae, Chlamys (Aequipecten) scabriscula; Paphia (Callistotapes) vetula , Acanthocardia (Acanthocardia) paucicostata, Cardium sp., Anomia sp.; Ficus sp., Turritell (Turritella) cleevelyi , Turritella (Eichwaldiella) fouadi , Turritella (Turritella) terebralis ; Bursa faizae , Echinolampas amplus, Echinolampas plagiosomus, Clypeaster marginatus; bryozoa as Holoporella polythele; algae as Lithothamnium sp and Lithophyllum sp.; Operculina complanata, Miogypsina intermedia .

Sandy limestone : Yellowish white; slightly to moderately compact; slightly compact. Sand grains are fine to coarse quartz grains; angular to subrounded; poorly sorted; with eroded periphery; pebbly in

parts. It yields oysters and pectinids. Also, it yields Heterostegina sp.

4.6

13 2.5

15 6.1

4.2

11 5

10 1.5

9 4.3

3

1.5

B

u

r

d

i

g

a

l

i a

n

G h

a r

r a

F o

r m

a t

i o

n

8

12

14

7

M

i

o

L

o

w

e

r

M

i

o

c

e

n

e

2 0.5

Fig. 32: Lithostratigraphic succession of the Miocene sediments at Gabal Homeira.

Sandy limestone : Yellowish white; moderately compact; slightly argillaceous. Sand grains are fine to coarse quartz grains; angular to subrounded; poorly sorted. It yields oysters and pectinids which are embedded in the rock and not easy to be collected. Also, it yields Heterostegina sp.

Sandy marl : Yellowish white; moderately compact. Sand grains are fine to medium quartz grains; subrounded to subangular, moderately sorted. It is fossiliferous with sclaractenian corals, echinoid plates and spines.

6 3

4

5 5

3

Olig.

1 2.7

2.9

1.4

The uppermost part of the Oligocene sediments are composed mainly of sands, gravels, boulders and silicified woods.

Shale : Varicolored, yellow, brown; moderately compact; fractured; unfossiliferous; slightly calcareous; slightly sandy; slightly silty. This bed unconformably overlies sands and gravels bed of Oligocene age.

Sandy dolostone : Yellowish brown; compact to highly compact; fractured; calcareous matter represent by euhedral microcrystalline dolomite rhombs. The sand grains are fine to medium quartz grains. Poorly fossiliferous, with echinoid fragments and undefined foraminiferal tests.

Sandy limestone : Yellowish white to yellowish brown; moderately compact; slightly argillaceous. Sand grains are medium to coarse quartz grains; subrounded to subangular; moderately sorted. It is poorly fossiliferous with echinoid plates.

Calcareous sandstone : Yellowish brown to yellowish white; fine to medium grained; subrounded to rounded; moderately sorted; moderately compact; cement represented by calcareous matter of cryptocrystalline calcite; poorly fossiliferous.

3 m

0

1

2

BED NO.

TH

ICK

.

(m)

LITHOLOGY

+++++

+++++

Marl

Limestone

Chalky LST

Dolomite

Conglomerate

Sandstone

Clay

Shale

INSOLUBLE RESIDUE %

16 4

15 30

BE

D N

O.

TH

ICK

. (m

)

LITH

OLO

GY INSOLUBLE

RESIDUE %

3019

xxxxx

+++++

Base unexposed

Top uncovered

Oligo.Oligocene

Time Rock Unit

Ro

ck U

nit

( ?

)

0 50 1000 50 100

0 50 100

Cairo

Suez

26 30 34

24

27

30

14 24.5

3.3

3.9

25.5

18

17

16

14 5

LITH

OLO

GY INSOLUBLE

RESIDUE %

BE

D N

O.

TH

ICK

.

(m)

13 17M

i

d

d

l

e

M

i

o

c

e

n

e

L

a

n

g

h

i

a

n

--

--

S

e

r

r

a

v

a

l

i

a

n

G

e

n

e

f

e

F

o

r

m

a

t

i

o

n

n

e

. 0 50 100

13 16.4

12 4.915 6.1

11 19.5

14 4.6

13 2.5

12 4.2

11 5

10 1.5

F

o

r

m

a

t

i

o

n

12 1.5

11 1

10 1.5

9 5

8 3.5

7 14.5

6 1.5

5 7.5

M

i

o

c

e

M

i

o

c

e

n

e

g

a

l

i

a

n

8 0.5

2 0.5

2 0.5

9 4.3

1.4

7 6

7 1.5

9 58 3

6

5 5

3

10 3.2

2

4 6.1

6 7.7

1 2.7

Homeira section ( 110.9 m )

3

5

O l i g o.

G

h

a

r

r

a

3 2.9

4

1.5

2 7

4 12

3 1.6

1 25

L

o

w

e

r

B

u

r

d

i

3 m

0

1

2

xxxxx

Geneifa section ( 97.1 m )

Gharra section ( 141.7 m )

Fig. 33 : Lithostratigraphic correlation chart for the three studied Miocene sections.

1 3.4

Oligo.

0

لملخص العربى ا

1

العربيالملخص

الةتهدف ى الرس ات دراسة إل ات والحفري رة الطبق سحالكبي ة ن وال ات الترسيب الدقيق وبيئ

سفلى ين ال خور الميوس بعض ص طل شفة واألوس شرقي المنك زء ال ي الج اطق ف ي بعض المن ف

ة م ومقارنته بمصر السويس -القاهرة بمنطقه لوضع تصورعن الطبقية الصخرية والطبقية الحيوي

ة الزم ذة المنطق ة له يب القديم ات الترس ة وبيئ ة الزمني ة والطبقي د . ني رت وق ة اختي ة للدراس ثالث

. وجبل حميره هه وجبل غرفقطاعات إستراتجرافيه بمناطق جبل جني

:الطبقات

ل غر مناطق جبل جنيفه في المنكشف البحرييمثل التتابع االستراتجرافى للميوسين ه وجب

وق الرواسب تراجعي - يتقدمميره بتتابع حوجبل ة ويرسو ف ة القاري االوليجوسين زمن ل التابع

. بعدم توافق بينهما

12́ ˝20 وخطى عرض ˚30 22́ ˝30 ، ˚32 20́ ˝30يقع بين خطى طول : جبل جنيفه -1

ابع لعصر االي ˚30 13́ ˝20 ، ˚30 رى الت ر الجي ين الحج ق وينحصر ب ين وطري وس

. متر97.1 بورسعيد االسفلتى ، ويمثل فى قطاع الدراسة بسمك –السويس

10́ ˝30 وخطى عرض ˚32 18́ ˝00 ، ˚32 17́ ˝00يقع بين خطى طول : جبل غره -2

د ˚30 12́ ˝00 ، ˚30 ى بع ع عل و يق د 13 وه ى بع ه وعل ل حنيف ر غرب جب و مت آيل

شمالية 13 ة ال ى الجه ر ف و مت د ، ويم آيل ل عويب ن جب شرقية م ة ث ال اع الدراس ى قط ل ف

. متر141.7بسمك

ره -3 ل حمي ين خطى طول : جب ع ب ˝12 وخطى عرض ˚32 13́ ˝20 ، ˚32 11́ ˝00يق

ه وهو يقع إلى الشمال من جبل ˚30 03́ ˝18 ، ˚30 02́ شرقى عناق وب ال ى الجن وال

. متر110.9 من جبل عويبد ، ويمثل فى قطاع الدراسة بسمك

اطق في وتتكون رواسب الميوسين السفلى ي من حجر الدراسة من ي رمل مع و حجر طين

سفلى . الرملي الجيريالقليل من الحجر الحجر ( وهذه الرواسب تختلف عن رواسب الميوسين ال

س ) 1966 وعبدا لهادى عبد اهللا ( ون السادات تك بم الممثلة ) الطحلبي الجيري اع ت ميه ولهذا تم إتب

.الدراسة منطقه فيلرواسب الميوسين السفلى ) 1971سعيد ( همتكون غر

ه أحجار جيريه من األوسط تتكون رواسب الميوسين أخرى ناحيةومن طباشيرية وشعا بي

صخورالرمليه ة وال صخور الطيني ن ال ل م ستر والقلي ض االوي ع بع ه م ضًا . وطحلبي ذه وأي ه


2

س في الرواسب تختلف ه لمتكون حماص ته الفتا نح سحنتها عن ال دالهادى ( ي داهللا وعب )1966عب

جنيفه بمتكون األوسط للميوسين التابعة الرواسب تسميه تم ولهذا السادات منطقه فى

).1990سعيد ( إتباعًا

:الحفريات

رة الالفقارية من الحفريات ًا نوع 62 تم وصف وتعريف ات ، محا 40 ( الكبي ع 16ري قواق

ذه تنتمي) قنفذيات 6، واع ه ة األن ى المعرف ه 26 ، جنس 34( إل م . )عائل د ت ع دراسة وق التوزي

ذه الجغرافي واع القديم والحديث له ة الدراسة وأوضحت األن . البحر المتوسط – االطلنطى هوي

. للقليل منهاالهندي – الهادي هوية إلىهذا باالضافه

: الزمنية ية الحيويةالطبق

ظ خاصة د الحف رى جي وى الحف ى المحت ادًا عل ة اعتم ات حيوي تة نطاق ى س م التعرف عل ت

Pctininds النطاقات من االحدث إلى االقدم والمتواجدة بأعداد وفيرة وهذه :


5- Chlamys(Macrochlamis) sardoa zone.

4- Pecten (Pecten) cristato-costatus zone.

3- Pecten (Flabellipecten) flabelliformis zone.

2- Pecten(Pecten) ziziniae zone.

1- Chlamys gentoni zone.

وى سفليه والمحت ه وال سمك والحدود العلوي وقد تم دراسة نوع النطاق وقطاع الدراسة وال

الحفرى واالسطح الفاصلة والعمر لكل من النطاقات الستة

:الطبقية الزمنية

:لدراسة الى مرحلتين زمنيتين هما سيم صخور الميوسين بمنطقة اقتم ت

ر -1 ين المبك ره :الميوس ون غ ل بمتك ى الثالث( ممث ةةف ات المدروس ر ) قطاع ذات العم

ر ين المبك ة الميوس رة ذات هوي ات الكبي ن الحفري وى م ى المحت ادًا عل الى إعتم البردج

Pectinids وخصوصًا ال


3

ى –ممثل بمتكون جنيفه ذات العمر الالنغي : الميوسين االوسط -2 ادًا عل سيرافالى إعتم ال

ات والقواق رى من المحاري وى الحف ى المحت ورامينفرا ف ة والطحالب والف ذ البحري ع والقناف

القطاعات الثالثة المدروسة

:ات الترسيبئالسحن الدقيقه وبي

م عمل ًاًا قطاع49ت ات رقيق ثال للعين ة الصخرية ومم ة من القطاعات المجمع محل الثالث

ة سيمات الدراس دت تق د اعتم م وق ان 1962 دنه رى وآلوف افه 1972 وام ىباالض وإل ملى بل

رين د 1982 فلوجلو 1962 وآخ ة فق ار الرملي ا األحج ة، أم ار الجيري صنيف سحن األحج ى ت ف

ة ومن خالل فحص القطاعات . 1975وبيتجون 1962 ، 1959أتبعت أعمال فولك م الرقيق د ت فق

: سحنيًا إلىالمدروسةتقسيم الصخور

ر -1 ات الحج ريقطاع ل الجي ات % 55 وتمث ن القطاع ةم ضم المدروس هأ وت حنات ربع س

سيه ه رئي والتي (wackestone, packstone , grainstone and framestone) هي رقيق

قيقه فرعيه ر عشرة سحن إلىتنقسم بدورها

ل -2 ه وتمث ات الفتاتي ات % 45القطاع ن القطاع ةم الحجر المدروس ه ب ي وممثل ر الرمل والحج

.قيقه رالطفلى وتم تصنيفها فى خمس سحنات

ة الدراسات أدتد وق سحنيه الحقلي ة وال ابع المدروس والحفري سيم التت ى فى تق سحنتين إل ال

:ينتالرسوبيتين التالي

: السحنة الفتاتية -1

ه مكون غره وتوجد في أسفل التتابع ممثله بمتكون سطح تعري ل ب سفلى يمث حيث حدها ال

م حجر طيني متطبق من حجر رملي آونجلوميراتى يليه لألعلى أحجار رملية معكوس ة التطبق ث

ة ى األحجار روالجزء العلوي منها يحتوى على أحجار جيري ستر باإلضافة إل ة وشعاب األوي ملي

ة وا ة الطيني ل .لرملي ة مث ات الالفقاري ن الحفري ر م ى الكثي سحنة عل ذه ال خور ه وى ص وتحت

0والقواقع متوسطه إلى رديئة الحفظ البحرية المحاريات والقنافذ

ري وعلى وى حف أساس ما تحتويه هذه السحنة الرسوبية الفتاتية من تراآيب رسوبية ومحت

راوح من تقد ه رغقيق فأن متكون ر وسحني ى م رسب في بيئة تت سفلى إل د في الجزء ال سطح الم

.بيئة شعابية ذات طاقة أمواج عالية في الجزء العلوي


4

: السحنة الجيرية -2

ه ب ابع ممثل ى التت ي أعل د ف ى صخور وتوج ة عل و متوافق ث ترس ه حي ون جنيف . هرغمتك

ن أ ا م ون أساس ن حجوتتك ر م ة والكثي ب الحيوي ن التراآي ر م ا الكثي ق به ميكة التطب ة س ار جيري

رة يالحفريات خصوصا األويستر والطحالب المرجانية والفورام داخل مع األحجار . نفرا الكبي ويت

0الجيرية األحجار الطينية رقيقة التطبق

ة وسحن وعل ة الرسوبية من تراآيب رسوبية أولي سحنة الجيري ذه ال ه ه ى أساس ما تحتوي

ات ى ال قيقة وحفريات أمكن التعرف على بيئة ترسيب متكون جنيفة وه ر ات رصيفيه جون مع بيئ

.ني في الجزء العلوي من المتكون قليلة األمواج تناسب ترسيب الحجر الطي مديهتحت

الزقازيقةجامع العلومة آلي

قسم الجيولوجيا

ة وحفرية لبعض رواسب الميوسين بمنطقطباقية السويس بمصر–القاهرة

منةرسالة مقدم

أحمد عيد موافي

الجيولوجيا فيم العلوماجستير ةلحصول على درج الستكمال متطلبات ا

اقسم الجيولوجي

العلومةآلي

الزقازيقةجامع

2006

الزقازيقةجامع العلومة آلي

قسم الجيولوجيا

: العنوان ـــــــــــــــ

السويس بمصر- القاهرةة وحفرية لبعض رواسب الميوسين بمنطقاقيةطب

: أسم الطالب ــــــــــــــــــــ

د أحمد موافى أحمد عي

:ة المؤهالت العلمي ـــــــــــــــــــــــــــــ

1986 بكالوريوس علوم فى الجيولوجيا عام

:اإلشراف ة لجن ــــــــــــــــــــــــ

ستاذ الطبقات والحفريات ورئيس قسم أ: د عزت عبدالشافى محمد . أ الزقازيق جامعة - الجيولوجيا

قسمأستاذ الطبقات والحفريات : السروجي صبريد عبدالباسط .أ الزقازيق جامعة– الجيولوجيا

قسم –مدرس الطبقات والحفريات : محمد عبدالمنعم محمد يوسف . د الزقازيقجامعة – الجيولوجيا

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