SEDIMENTLOGICAL STUDIES ON

THE PALEOGENE-EARLY MIOCENE

SEDIMENTS ALONG EL-QATTAMIYA

EL-SOKHNA ROAD

An Essay Submitted to

The Geology Department,

Faculty of Science,

Port-Said University

By

Ethar Galal Abd El-Samea Gebril

Yassmeen El-Sayed Gomaa Abu Warda

(4th

Geology Level)

In partial fulfillments of the

B.Sc. Degree in Geology

(Geology of Petroleum and Natural Gas)

(2016)

CHAPTER ONE

INTRODUCTION

1.1 PRELUDE:

The Paleogene is a geologic time incorporating Paleocene, Eocene and

Oligocene (Fig. 1.1). It ranges from 66.2 to 25.2 my (Polarity chronozone from

C29 to middle of C13 of early Tertiary (Haq&VanEysinga, 1998). In Europe the

Paleocene Epoch is subdivided into a Danian (lower carbonate unit) and Thanetian

(clastic unit). The Eocene Epoch on the other hand includes three

Chronostratigraphic subdivisions, the Early Eocene (Ypresian), the Middle Eocene

containing Lutetian and Bartonian ages and the Upper Eocene (Priabonian), Table

(1.1). This subdivision will be adopted in this work.

Fig. (1): The Cenozoic subdivisions

Table (1.1): Subdivisions of the Paleocene and Eocene

Period System Subdivisions P

AL

EO

GE

NE

Eocene

Upper Priabonian

Middle Bartonian

Lutetian

Lower Yepresian

Paleocene Upper Thanetian

Lower Danian

1.2. PREVIOUS WORK:

The Paleogene rocks of Egypt were widely reported and discussed from different

topics by many workers from the beginnings of the last century:

Zittel (1883) grouped all the Early Eocene beds up to the first appearance of

Nummulites gizehensis under the name ―LibyscheStufe‖

Beadnell (1905) described the section of Gebel Aweina in detail and applied the

term "Esna Shale" to the passage beds between the well dated Early Eocene

limestones with flints and the underlying late Cretaceous chalk beds.

Hume (1911) subdivided the Eocene rocks of both the Libyan Desert and the Nile

Valley into the following biozones from base to top;

OperculinalibycaSchwager, Ostreamulticostatadeshayes, Collianassafrass,

Nummulite gizehensis beds,Exogyra beds and Carolia beds.

Nakkady (1949 &1950) concluded that the assemblage of Esna Shale fauna is a

transitional having a Cretaceous affinity in the Lower part and Paleocene-

Eocene one in the Upper part.

Shukri (1954) interpreted the discontinuity in the sedimentation between the

Cretaceous and the Eocene at Gebel Shabraweet, due to the presence of ENE -

WSW structural highs belonging to the Syrian Arc System.

The term ―Thebes Formation‖ was first introduced in Egyptian Geology by Said

(1960) to designated the limestone succession with chert bands overlying the

Esna Shale in Luxor.

Said (1971) subdivided the Middle Eocene in the Nile Valley into four

lithostratigraphic units namely from base as; Minia, Samalut, Mokattam and

Giushi formations.

Haggag (1979) studied the biostratigraphy of the west-central part of the Western

Desert. She came to the conclusion that; the Upper Eocene deposits were

recorded for the first time in this part of Egypt.

Snavely et al. (1979) studied the stratigraphy and the regional depositional history

of the Thebes Formation (Lower Eocene). They examined the lithofacies

present within the Thebes Formation and proposed three stages of the

depositional evolution;

1) Deeper water phase of predominant pelagic deposits.

2) Gradual shallowing phase beside establishment of widespread benthonic

foraminiferal communities which occurred during intermittent pelagic

deposition and producing small carbonate platforms separated by deeper basins.

3) An abrupt lowering of the sea level and establishment of shallow water organic

build-up within the basin and erosionof the uplifted blocks to the east.

Al- Ahwani (1980) related the absence of both the Paleocene and Early Eocene

rocks in the northern part of the Eastern Desert to that, this part was

topographically too high to be reached by the Paleocene and Eocene seas during

that time. He also added that the Middle Eocene rocks in Shabraweet area

belong to Early and Late Lutatian.

Strougo et al. (1982) studied the Middle Mokattam beds of Darb El Fayum, west of

Cairo. They assigned a Middle Eocene age based on the planktonic

foraminiferal assemblages.

Strougo et al. (1983) subdivided the Eocene succession exposed in Beni Suef area

into four formations; El Fashn, Beni Suef, Shaibun and Maadi formations. They

also placed the boundary between the Middle and the Upper Eocene at the base

of the Shaibun Formation.

Hassanein et al. (1983) stated that the Thebes Formation exposed in the Eastern

Desert was deposited in deep to shallow neritic marine environment over a

gradually rising sea bottom. They also subdivided the Formation into three

members namely from the base as; Hamadat, Beida and Al Geer.

Mohammed (1984)based upon the microfacies associations of the Thebes

Formation in Gebel El-Shaghab near Esna; he concluded that, the Thebes

Formation was deposited through a regressive stage of the sea in an outer to

inner neritic zone.

Azab (1984) dealt with the biostratigraphy of the Middle Eocene at Minia,

Maghagha and Beni Suef. He subdivided the sequence from base as; Minia,

Maghagha and El-Fashn formations and recognized the following foraminiferal

biozones from the oldest to youngest; Hantkeninaaragonensis,

Globigerinatheka subconglobatasubconglobata, Globorotalialenheri and

Truncorotaloides rohri zones.

El-Dawoody (1984) dealt with discoaster stratigraphy of the Early Tertiary in Esna

/Luxor region. He subdivided the sequence into five nannobiostratigraphic

units.

Hassan et al. (1984) classified the Eocene rocks in the area East of Maadi into

Observatory and Maadi formations. They subdivided the succession into ten

microfacies associations and concluded that the Observatory Formation was

deposited in a shallow, open marine, neritic environment while the Maadi

Formation was deposited in shallower marine environment depending upon the

presence of Carolia sp. and Ostrea sp.

Kolkila et al. (1984) in their discussion about the microfacies and the depositional

environment of the Middle Eocene sequence in the area to the East of Helwan,

Egypt. They subdivided this sequence into Gebel Hof and Observatory

formations.

Strougo and Boukhary (1987) discussed the Middle/Upper Eocene boundary in

Egypt. They suggested that the contact between Middle and Upper Eocene can

be placed at the contact between the middle Mokattamian and the upper

Mokattamian Formation based on the Nummulites, whereas it can be placed

within the middle Mokattamian Formation based upon calcareous nannofossils.

Strougo and Hottinger (1987) studied some larger foraminifera

(AlveolinaandNummulites) from the Upper Eocene rocks of Egypt. They

concluded that the only occurrence of upper Eocene (Priabonian) in Egypt is

represented by Qasr El Sagha Formation and its equivalents (Wadi Hof and

Upper Mokattamian formations).

Abd El-Shafy (1988) recorded the Early Eocene Thebes Formation for the first

time in the Northern Galala, Gulf of Suez. He also introduced Naot Formation

(Upper Paleocene - Basal Eocene age).

Dabous and Awad (1989) studied the petrography and lithofacies of the Lower

Tertiary sediments of Esna - Qena district. They concluded that the upper part

of the Thebes Formation is homogeneous and composed of micrite whilst the

middle and lower parts display rather rapid changes in facies.

Omran (1989) dealt with the geology and stratigraphy of Shabraweet area and

introduced El Gosa El Hamra Formation as a new formation for Middle Eocene

age which is equivalent to the Mokattam Formation.

Selima (1989) studied the subsurface Eocene rocks on the western side of the Nile

Valley between Beni Suef and Cairo. He subdivided this succession into the

following rock units from the base; Apollonia, Dabaa and Moghra formations.

Said (1990) subdivided the Eocene succession in Egypt from base to top into the

following rock units;

1- Esna Formation and its equivalents.

2- Thebes Group comprising the stable shelf areas and its equivalents in other parts

of Egypt.

3- Minia Formation.

4- Mokattam Group S. L. divided into; a lower Mokattam Formation and Upper

Observatory Formation.

5- Maadi Group comprising from base to top: Qurn, WadiGarawi and Wadi Hof

formations and their equivalents in other parts of Egypt. He also summarized

the several local names which designate the different lithologies of the Eocene

in Egypt.

Hassan et al. (1990) studied the microfacies associations of the Mokattam and

Maadi formations at Gebel Mokattam area. They subdivided the Mokattam

Formation into two members Kait Bye at the base and Basateen at the top. They

(op. cit) concluded that the microfacies association prevailing in the lower part

of Kait Bye Member reflects deposition under relatively quite inner neritic

marine environment of normal salinity while the microfacies associations

dominated in upper part of the Kait Bye Member and in the lower part of

Basateen Member reflect deposition within a relatively turbid shallow inner

neritic environment. They also stated that the upper part of Basateen Member

reflects deposition under shallower part of inner neritic marine environment

during which slightly reducing conditions prevailed, while the overlying Maadi

Formation was deposited under shallow water conditions due to the abundance

of Carolia placunoides, Ostreaspecies and the presence of dolomitized

biomicrite microfacies associations.

Strougo (1992) studied the Middle / Upper Eocene transition in Egypt. He

concluded that the Upper Eocene is marked by the first appearance of

Nummulites ptukhianiand/or Globigerinatheka semiinvolutazones.

Strougo et al. (1992) studied the biostratigraphy and paleoenvironments of the

Middle Eocene benthonic foraminiferal assemblages of Gebel Abu Shama at

the north central Eastern Desert.

El-Dawoody (1994) investigated the Early Tertiary calcareous nannofossils

biostratigraphy of North Africa and correlated the available data from Egypt

with the Middle east section (Libya, Tunisia, Jordan, Syria, Iraq & Qatar).

El-Dawoody & El-Dawy (1998) dealt with the microbiostratigraphy of the

Maastrichtian- Early Eocene sediments in Dakhla-Kharga region, Western

Desert. They subdivided the exposed sequence into five nannobiozones in

addition to one devoid of nannofossils restricted to Paleocene.

El-Dawoody (2000) studied the calcareous nannoplanktons biostratigraphy of the

Paleocene exposures in W. Belayium, Esh El-Mellaha, G. Duwi, and G. Oweina

/G. Gurnah.

Speijer et al. (2000) investigated the upper Paleocene stratigraphic record in three

sections arranged on a depth transect across the southern Tethyan margin

namely; Wadi Nukhul, Gebel Qreiya and Gebel Duwi.

Anan (2001) dealt with vaginulinid benthic foraminifera comprise in the Paleocene

of Gebel Duwi. He introduced two nov. speciesCitharina plummerae and

Planularia berggreni. He prove that the nov. species beside Planularia

dissonia, Vaginulina trilobata and representatives of genus

Orthokarestina&Discorishave a restricted geographic range so far, in central

and southern Egypt (south of lat. 28 o N).

Galal and El-Halaby (2001) dealt with the stratigraphy of the area located at Wadi

Qena and Wadi El-Agramiya in northeastern desert. They subdivided the

sequence into three rock units; Minia (Upper Ypresian), Gebel Hof (lower

Middle Lutetian) and Observatory formations (Upper Lutetian) and three

biostratigraphic zones; Acarinina pentacamerata, Nummulite gizehensis and

Dictyorconus aegyptiensis zones. They mainly interpret the paleonvironment of

the Minia Formation that deposited in deep and open marine environment that

would be the first record in Egypt due to the planktonic associations.

Hewaidy and Strougo (2001) studied the Maastrichtian / Early Eocene (Dakhla

Shale, Tarawan Chalk and Esna Shale) benthic foraminifera from three sections

cropped out in Farafra namely; northern Gunna, El-Sheikh Marzouk and the

Twin spikes.

Speijer & Morsi (2002) studied the ostracode response to the oceanographic

changes during the Paleocene- Eocene in Gebel Duwi section (Egypt), within

the Esna Shale.

Nissif et al., (1992)examined the Miocene sediments in Wadi Feiran area (East

Wadi Withr, Wadi Khoriza, Gabal Hadahid and Southeast Gabal Hadahid

sections) and reported that the Nukhul, Lower Rudeis and Abu Gerfan

formations are overlain by undifferentiated rock units, possibly equivalent to

Upper Rudeis, Kareem, Belayim, South Gharib and Zeit formations altogether.

El-Ezzabi (2000) studied the sedimentary facies, paleoenvironment and facies

development of the Miocene-Pliocene sequences in the Sadat-Wadi Hagul

stretch, northwest Gulf of Suez and their time correlatives in the adjacent

basins and concluded that the Late Burdigalian Sadat Formation, which

denotes the first marine transgression of the Miocene Gulf Sea over its extreme

northwestern margin, is a unique back –reef limestone facies with characteristic

coral-mollusc-coralline algal association and basal foreshore clastics.

Texturally, the back-reef limestones are dominated by open shelf lagoon,

bioclastic wacke-/packstone with scattered in situ coral framestone and

oyster/operculina rudstones of small patch reef and shoal facies respectively.

Associated back-reef facies also includes a few nearshore restricted lagoons,

lime-mudstone and algal oncolite rudstone formed towards the lee side of the

reef barrier (reef-flank facies). These facies associated has been deposited on a

rimmed carbonate shelf under subtropical warm climate, in water depths

seldom surpass 10 m.

El- Fawal et al. (2005) dealt with the tectono-sedimentary evolution of the

Paleogene sediments across Sinai and concluded the depositional sequences

based upon the investigation of paleo-bathymetrical variations taken place

during the Paleogene of Sinai. The authors concluded that the deposition of the

Paleogene in Sinai was overprinted by the worldwide sea level fluctuations. In

addition, the tectonic pulses associated the final stages of the Syrian Arc

System together with those accompanied with the early formation of the Suez

Rift played important role in development of the Paleogene in Sinai. The

authors (op.cit) concluded five paleo-tectonic events during deposition of the

Paleogene,governed the nature of Paleogene depositional regime in Sinai; these

events are:

(a) Post Maastrichtian / Early Paleocene event.

(b) Late Paleocene / Early Eocene event.

(c) Middle/ Late Eocene event.

(d) Late Eocene/ Early Oligocene event.

(e) Post Early Oligocene event.

The authors (op.cit) reported that Red Beds are devoid of planktonic foraminifera,

so its age is questionable. They assigned it to the Late Eocene to Early Oligocene.

El- Fawal et al. (2005) dealt with the tectono-sedimentary evolution of the

Paleogene sediments across Sinai and concluded the depositional sequences based

upon the investigation of paleo-bathymetrical variations taken place during the

Paleogene of Sinai. The authors concluded that the deposition of the Paleogene in

Sinai was overprinted by the worldwide sea level fluctuations. In addition, the

tectonic pulses associated the final stages of the Syrian Arc System together with

those accompanied with the early formation of the Suez Rift played important role

in development of the Paleogene in Sinai. The authors (op.cit) concluded five

paleo-tectonic events during deposition of the Paleogene, governed the nature of

Paleogene depositional regime in Sinai; these events are:

(a) Post Maastrichtian / Early Paleocene event.

(b) Late Paleocene / Early Eocene event.

(c) Middle/ Late Eocene event.

(d) Late Eocene/ Early Oligocene event.

(e) Post Early Oligocene event.

The authors (op.cit) reported that Red Beds are devoid of planktonic

foraminifera, so its age is questionable. They assigned it to the Late Eocene to

Early Oligocene.

Hassan (2005) aimed to provide an integrated study to the sedimentological

evolution of the Paleogene rocks in Sinai in terms of the successive events

influencing their sedimentary basins. Therefore, it utilizes the principles of the

sequence stratigraphic analysis for successions in the outcrops to arrive the actual

sea level fluctuations taken place during that time. These fluctuations have

revealed seven third order depositional sequences. The maximum sea level rise in

the Paleogene over Sinai was recorded with the early deposition of Paleocene Esna

Shale evidenced by the plenty of upper bathyal arenaceous forms of the latest

Paleocene. The minimum sea level drop in the Paleogene was recorded at the top

of Eocene evidenced by the presence of benthonic lenticulinids-rich bed deposited

with peletoidal micrites of shallow restricted lagoons at this boundary. The

Paleogene sea level fluctuations recorded in Sinai were found generally matching

with the global sea level oscillations. However, some variations exist indicating

that the deposition of the Paleogene in Sinai was generally governed by the

worldwide sea level oscillations and the local tectonics related to the development

of the Syrian Arc system and the Gulf of Suez.

1.3. AIM OF THE WORK:

The aim of the work is to examine the Paleogene (Paleocene, Eocene, and

Oligocene) and the Neogene (Miocene) sedimentary succession cropping-out along

El-Qattamiya – El-Sokhna asphaltic road. The detailed lithological characteristics

will be discussed both in the field outcrops and according to the results obtained by

the laboratory analyses. The different sedimentary facies forming the sedimentary

succession and their mutual relationships are to be emphasized. The depositional

interpretations will be given to arrive the evolution of these sediments. The

tectono-sedimentary status of the given succession will be discussed in terms of the

sequence stratigraphic principles.

1.4 THE STUDY AREA AND THE EXAMINED ROCK UNITS:

The study area located between longitude 320 8

\ 13

\\ E and 32

020

\ 40

\ \ E

and latitude 290 35

\ 4.5

\ \ N and 29

0 41

\ 38

\\ N. The concerned road runs in two

segments (Fig. 1.2). Ongoing from El-Sokhna, the first segment of the road

continues northward beside the western coast of the Gulf of Sueztill the southern

reaches of the Suez City. At the junction of the 2nd

International Regional Road, the

second segment starts and continues northwestwards to El-Qattamiya – Cairo.

Along the first segment of the road, the rocks of Esna Shale (Paleocene) and

Thebes Formation (Early Eocene) and the coastal area of the western coast of the

Gulf of Suez constitute the main landforms at both sides of the road segment.

There, the (Paleocene) and Thebes Formation (Early Eocene) form a relatively

high massif of generally grayish-white and white shades. The sediments of the

Thebes Formation appear at the top of the tableland forming steep-sloped, bold

scarp sediments, overlying the sediments of the Paleocene Esna Shale. The latter

crops-out in darker shades and display slope-forming scarp with unexposed base,

till the two rock units disappear toward the start of the second segment of the road.

Along the second segment of the road (Fig. 1.3), the outcrops of the Early

Miocene Sadat Formation start to appear on both sides of the road with unexposed

base. The crossed area is strongly block-faulted area where the Early Miocene

sediments are seen block-faulted against, again, toward an Early Eocene facies of

Thebes Formation. Continuing as 20-25 km from the start of the second segment,

an elongated outcrop of Oligocene sediments is recorded run parallel to both the

road sides. These Oligocene sediments appear due to a block-faulting process

against the younger Early Miocene Sadat Formation. The Oligocene sediments are

represented by thick-bedded conglomerates, gravelly sandstones and sandstones,

displaying strong yellow and brownish-yellow colours.

Fig. (1.2): Location map of El-Qattamiya – El-Sokhna Road.

Fig. (1.3): Satellite image of the 2nd

international Regional Road (the second segment of El-Qattamiya –

El-Sokhna Road)

CHAPTER TWO

METHODS AND TECHNIQUES

The methods of study adopted herein are categorized in two broad classes; field

studies and laboratory studies.

2.1 FIELD STUDIES:

The field studies done in this study involved 4-days field trip to traverse the

Paleocene – Miocene sedimentary succession along the El-Qattamiya – El-Sokhna

Road according to the following scheme (Figs. 2.1, 2.2 and 2.3):

2.1.1. Choice of four outcrop-areas along Cairo – El-Sokhna Road that well-

representing the different rock belonging to the Paleocene – Miocene

sediments.

2.1.2. Choice the best sedimentary profiles, within the selected areas, having the

complete succession of the forming rock formations to be studied.

2.1.3. For each rock unit, the detailed lithological characteristics are identified and

described. The thickness variations are reported. The bed contacts and bed

geometries are recognized and recorded. The characteristic sedimentary

structures are identified, described and photographed.

2.1.4. A number of representative spot samples were taken for each rock unit

forming the examined sedimentary succession for further laboratory analyses.

Fig. (2.1): Esna Shale (Paleocene), and Thebes Formation (Early Eocene)

along El-Qattamiya – El-Sokhna Road.

Fig. (2.2): Gabal Ahmar Formation (Oligocene) outcrops along

El-Qattamiya – El-Sokhna Road.

Fig. (2.3): Sadat Formation (Early Miocene)outcrops along

El-Qattamiya – El-Sokhna Road.

2.2. LABORATORY ANALYSES:

The samples collected were subjected to the following methods of study:

2.2.1. Binocular examination:

Provisionally, all samples were separately examined under the binocular

microscope (Plate 2.2.a) before carrying out any analysis in order to determine

their color, lithology, texture, mineralization and fossil content. Results obtained

are given in detail in the appendix and are summarized in Chapter -Four

2.2.2. Disaggregation of the sample:

The collected samples were first disaggregated to their original

componentaccording the following steps:

i) Weakly consolidated samples were placed in 250 ml beaker containing 50 ml

distilled water, stirred for about ten minutes, left overnight, filtered and dried.

ii) Hardly consolidated samples were soaked in 250 ml beaker containing 50ml

distilled water and stirred. Careful pressing of the sample by a thick rubber was

applied to disaggregate it without causing damage of the grains (Plate 2.2.b).

In this concern, the argillaceous samples of Paleocene Esna Shale and the

Oligocene gravelly sandstones were disaggregated by soaking in water for a

few hours. The carbonate cemented samples were disaggregated using HCl and

applying little press on the sample. On the other hand, the hard lithified samples

from the Thebes Limestone and the Miocene Sadat Formations were left

without disaggregation where they were thin sectioned for petrographic

examination.

2.2.3. Determination of the Bulk Textural Composition of the Sediments:

The overall detailed textural composition of the components forming the examined

rock units is carried-out to arrive the accurate percentage composition, and to

arrive the accurate nomenclature of the examined sediments. The bulk textural

composition is done according to the following scheme:

2.2.3.1. Determination of Carbonate (CO3) percentage contents:

All samples were primarily analyzed to determine their Carbonate – Sand –

Mud percentage composition. A representative portion (30-50 gms) of each

sample was weighed (Plate 2.2.c), then soaked in 250 ml beaker containing

50 ml distilled water. Dilute (10%) HCL was added gradually till the pH

reached 3.5 to 4.0. Gentle heat was slowly applied till 800C (Plate 2.2.d).

When effervescence is stopped, the sample was cooled filtered using tri-

junction connection (Plate 2.2.e) and the residue was carefully washed by

distilled water (Plate 2.2.f),dried in electric oven and weighed (Plate 2.2.g).

The percentage of soluble carbonate was then calculated by weight-

difference as Carbonate percentages.

2.2.3.2. Removal of organic matters:

The residue extracted from the above step was placed in 500 ml beaker

containing 200 ml distilled water. Hydrogen-peroxide (H2O2) was added to

remove organic matter. Heat was applied for a few seconds then the sample

was left overnight.

2.2.3.3. Mud Dispersion:

The mud-rich residue of the step 2.2.3.1., a mud dispersion process is done to

disperse the clay minerals present. Accordingly, 10 mls of Sodium

Hexametaphosphate (Calgon) were added for complete dispersion of the

sample.

2.2.3.4. Determination of Sand and Mud percentage contents:

The collected dispersed residue after the above three steps was then placed in

0.063 mm sieve and a steady process of wet-sieving was applied under a

stream of distilled water (Plate 2.2.f). The sand fraction (+0.063mm) in the

residue was thus separated, dried and weighed. Then the weight percentages

of sand mud fractions were then calculated separately and listed together with

the carbonate content of the step (2.2.3.1.) in Table (4.2,4.4) in Chapter-Four.

2.2.4. Sand Grain Size Analysis:

A representative portion of the sand fraction separated from each sand-rich sample

in the step 2.2.3.4 was weighed and fractionated by dry sieving adopting the

Wentworth scale using a standard set of sieves of the openings 2.0, 1.0, 0.50, 0.25

and 0.063 mm (Plate 2.2.h). Using an electric shaker, continuous shaking was

applied for twenty minutes. The different grain size fractions obtained were

weighed and their weight percentages were calculated. The data was graphically

represented for producing percentage cumulative distribution curves using

probability papers. The grain size parameters of Folk and Ward (1957); MzФ, б1Ф,

SK1 and KG for each sample were also calculated and their mutual relationships

were graphically illustrated and discussed and all results are given in Chapter-Four.

2.2.5. Petrography and Microlithofacies Examination:-

Some representative thin sections were prepared for the hard or moderately hard

samples representing two rock units within the examined succession in the study

area, including Esna Shale, Thebes Formation and Sadat Formation. Detailed

petrographic description of the thin section was made using the Standard

Polarizing Microscope. Definitions and interpretations of the depositional

environment for each rock unit are discussed according to the clastic sediments

follows the schemes given by Folk (1980), whereas for the carbonate rock the

schemes of Dunham (1962), Emery and Klovan (1971) and Wilson (1975) were

adopted.

For the Gabal Ahmar Formation, where the sediments were examined in the field,

the description and depositional interpretations are given based upon the lithofacies

analysis of this formation.

Plate (2.1): Different steps of the laboratory analyses done in this work.

CHAPTER THREE

LITHOSTRATIGRAPHY

The detailed field study and the stratigraphic analysis have revealed that the

Paleogene-Miocene succession along El-Qattamiya-El-Sokhna Road includes the

following rock units starting from the oldest:

3.1 Esna shale (Thanetian —Early Ypresian)

3.2 Thebes Formation (Spamacian — Late Ypresian)

3.3 The Gebel Ahmar Formation (Early Oligocene)

3.4 Sadat Formation (Early Miocene)

The following is the description of each rock unit encountered in the study

area:

3.1 ESNA SHALE:

Esna Shale is the oldest rock unit recorded in the Paleogene of the study area.

3.1.1 Nomenclature:

The term Esna Shale was first introduced by Beadnell (1905) to describe the

shale sequence (60m) exposed in Gebel Aweina southeast of Esna, upper Nile

Valley. Later on, this term was widely accepted by many workers (e.g.: Said &

Kenawy (1956); Said (1962); Awad & Ghobrial (1965); Boukhary & Abdel

Malik (1983); Hermina et al., (1989); Ayyad & Hamama (1989); El-Heiny et

al. (1990); Said (1990); Shahin (1992); Speijer (1994); El-Nady (1995); Nassif,

(1997); Omran (1997); Youssef (1998); Issawi et al. (1999); Obaidalla (1999)

and El- Fawal et al. (2005).

3.1.2 Contacts:

In its type section, the Esna Shale conformably overlies the Tarawan Chalk

and underlies the Thebes Formation with gradational contact. In Sinai, Esna

Shale always overlies the Campanian – Upper Maastrichtian Sudr chalk and

underlies the Lower-Middle Eocene Thebes Formation with different

geometric relations. In the study area, Esna Shale Underlies the Eocene

Thebes Formation forming steep-cliffs, whereas its base is unexposed along

El-Qattamiya - El-Sokhna Road.

3.1.3 Occurrence, Lithology and Thickness variation:

In the study area, Esna Shale is encountered along the early half of El-

Qattamiya - El-Sokhna Road, displaying slope-forming cliffs below the steep

cliff-forming Thebes Formation (Fig. 3.1). Lithologically, the term Esna Shale

is applied for the rock exposures of grey to greenish grey shale intervened with

thin bedded limestone or marly limestone interbeds, sometimes associated

with gypsum veinlets and some iron nodules. It is observed that Esna Shale in

the study area is composed of white grey shale of calcareous facies with

limestone intercalations.

3.1.4. The Faunal content:

The examined levels of Esna shale are highly rich in its foraminiferal and

ostracodal contents (Hassan, 2005).

3.1.5 Aga relation:

According to Hassan (2005), the top parts of the Esna Shale are assigned to the

Late Paleocene, whereas the uppermost part is dated as Early Eocene

(Sparnacian - early Ypresian). Many workers assigned the Esna Shale to

different ages ranging from the Late Maastrichtian to the Early Eocene in

different localities in Egypt.

Fig. (3.1): Esna Shale displaying slope-forming cliffs below the

Thebes Formation.

Fig. (3.2): Lithologic Succession of Esna Shale Formation (after Hassan 2005).

It was dated as ‗Late Paleocene — Early Eocene at several localities such as at

G.Aweina by El-" Naggar (1966); at W. Tayiban – W.Feiran, Sinai by El-

Sheikh & El-Beshtawy (1992) and at Um El- Huetat at the Red Sea Coast by

Ismail & Ied (2005). Also, Esna Shale was assigned to the Paleocene by Said

& Kenawy (1956) at G. Nekhl, North Central Sinai; Said (I962) at Quseir area,

Red Sea Coast; Ismail (1996) at Qusaima and El- Fawal et al., (2005) at G.

Arief EL- Naga, northeast Sinai respectively. Moreover, it was assigned to the

Late Maastrichtian - Early Eocene by El - Nady (1995) at G. El- Muwaylih

northeastern Sinai; Ayaad & Hamama (I989) at G. Mokattab; Shahin (2005) at

G. Ekma and G. Matulla south western Sinai. In this study, the Late

Maastrichtian - Early Eocene Eocene age suggested by Hassan (2005) is

adopted.

3.1.6 Geographic Distribution & Equivalent Rock Units:

According to Said & Kenawy (I956) and Said (1962) the Esna Shale appears

in the cliffs of the Egma Plateau; in the northem flanks of El-Mineidra El-

Kebera and the floors of many wadies that cut G. Bodhiya and appears on the

surface in Nekhl (55m) and Darag domes.

The present Esna Shale is equivalent to the Beida Formation of Allam &

Khalil (1988) in Gebel Arief El-Naga and to the Taqiya Formation of Bartov

& Steinitz (1977) in Negev, southern Palestine. The term Beida Formation as

proposed by Bartov & Steinitz (1977) to refer the marly limestone and marls

overlying the Sudr chalk and underlying the Early Eocene Thebes Formation

should be drop according to the priority of the first term.

3.2. THEBES FORMATION

3.2.1 Nomenclature:-

Thebes Formation was introduced to describe 290 m of the Lower Eocene

limestone overlies the Esna Shale in its type locality G. Gurnah, opposite

Luxor, Nile Valley by Said (1960). El-Naggar (1966) applied the term

―Thebes Formation‖ to the succession overlying the Owaina Shale and

consisting of calcareous shale, muddy limestone and limestone in Esna - Idfu

region. The name of Thebes Formation met a great acceptance and wide usage

in the Nile Valley, Gulf of Suez, and Sinai. However, the rank of this

formation was raised to the Group rank by the workers of the Geological

Survey (1987) and Hermina et al. (1989). The Egma limestone described by

Beadnell (1927) from the Egma table-land, north Sinai has been considered by

some authors as synonym and equivalent to the Thebes Formation and occupy

the same stratigraphic position (e.g. Hermina et al., 1989; Zico et al.,1993;

Hamza et al., 1997 and Mattar, 1998). Hermina et al. (1989) considered that

Abu Rimth Formation in Southern Galala is a synonymous of Thebes

Formation with partly the same sedimentation origin and coeval in time range.

Strougo et al. (2003) used the name of "Southern Galala Formation" proposed

by Abdallah et al. (1972) in the Galala Plateau, instead of and equivalent to

Thebes Formation in Hammam Faraun and W. Bagha area.

3.2.2 Contacts:

In its type locality at G. Gurnah, Upper Egypt, Thebes Formation lies

unconformably above the Esna Shale with gradational lower boundary (Said,

1990). At W. Bagha, the Lower boundary of Thebes Formation is unexposed

on the surface. In central and eastern parts of Sinai, Thebes Formation lies

unconformably above the Esna shale with graditional boundary between them

(Hassan, 2005). In the present study, Thebes Formation gradationally overlies

the Esna Shale along Qattamiya-Sokhna Road.

3.2.3 Occurrence. Lithology and Thickness variation

In its type section, Thebes Formation is composed of white and off-white

massive thinly to thickly bedded limestone with flint bands and contains

Operculina libyca and Lucina thebaica below, while it is nummulitic,

argillaceous limestone with marl intercalations above (Said, 1960). In the study

area, the formation consists of regularly stacked, moderately thick (0.75 – 1.50

m) bedded limestone with occasional chert bands.

Fig. (3.3): Lithologic Succession of Thebes Formation (after Hassan 2005).

3.2.4 Faunal content:

According to Said (1990), Hassan (2005) and Matar (2008), Thebes Formation

is characterized by a considerable content of Planktonic foraminifera (e.g.: in

the lower parts:Morozovella formosa, M. lensiformis, M. aragonensis,

Parasubbotina inaequispira, Acarinina wilcoxensis, Ac. pseudotopilensis, Ac.

pentacamerata, Globigerina lozanoi, whereas, Acarinina topilensis,

Subbotinahagni and Turborotalia frontosaappeared at the upper parts. On the

other hand, Benthonic foraminifera such as Lenticulina midwayensis,

Marginulinopsis tuberculata, Bulimina farafraensis, Stilostomella

midwayensis, Anomalinoides zitteli, Gaudrjyina, Marginulinopsis tuberculata,

Gyroidina sp., Loxostomoides applinae, Alabamina midwayensis,

Pseudoclavulina farafraensis, Clavulinoides trilaterus, and Nodosaria

latejugata were recoreded within the present formation together with

considerable larger foraminiferal content (e.g. Nummulites, Alveolina and

Operculina, and Cuvillierina species). Moreover, Ostracods are also present in

noticeable content (e.g.: Reticulinaproteros, Mauritsina coronate, Costa

mokattamensis, Leguminocythereis lokossaensis, Cytherellasinaensis.

3.2.5 Aga relation:

Thebes Formation was dated by Said (1960) as Early Eocene in its type

locality. Moreover, the identified faunal assemblages and the detailed

biostratigraphic studies suggest an Early Eocene age to the Thebes Formation.

However, Said (1962), Viotti & El- Demerdash (1969), Boukhary & Abdel

Malik (1983), Abul-Nasr (1990, 1992a, b), Nassif (1997), and El-Fawal et

al.(2005) suggested an Early to early Middle Eocene age to the Thebes

Formation based on its foraminiferal content. However, an Early Eocene age

was applied by several authors (e.g. Hermina et al., 1989; El-Heiny et al.,

1990; Hamza et al., 1997 and Issawi et al., 1999).

3.2.6 Geographic Distribution & Equivalent Rock Units:

The Thebes Formation has a wide geographic distribution allover Egypt. in

Sinai, it forms the scarp-building limestone unit of southwestern and central

Sinai (Viotti & El-Demerdash, 1969); Boukhary & Abdel Malik, l983;

AbulNasr & Thunnel, 1987; El-Heiny et al., l990; Said, l990; Nassif,l997;

Strougo et al., 2003 and Hassan, 2005). lt crops out along the Nile Valley and

to the west of the Nile in the eastern scarp of Kharga and extends further to the

south to the latitude of Aswan and is developed in Quseir – Safaga district. The

Thebes Formation extends as far as Palestine and Jordan where it is called as

―Avedat Group‖ (Bartov et al., 1972). The present formation, along Qattamiya-

Sokhna Road, is stratigraphically correlated to Thebes Formation recorded by

Viotti & El- Demerdash (l969) in W. Nukhul, Boukhary & Abdel Malik

(1983), East Gulf of Suez; Nassif (1997) in W. Matulla ـ El- Markha plain area

and El- Fawal et al. (2005) in G. Hammam Faraun

3.3. THE GABAL AHMAR FORMATION

3.3.1 Nomenclature:

The Gabal Ahmer formation was introduced by Fourtau 1894, Barron 1907,

Shukri 1954 to describe the strata composed of sands and gravels of the

Oligocene age at its type locality east of Cairo below the Eocene limestone of

Gabal Mokattam.

3.3.2 Contacts

The Gebel Ahmar Formation is made of cross-bedded sandstone, sandy

gravels, pebbly sandstone and varicolours sands. Gravels are mainly flint and

form thick elongate hills and hummocks. The gravels are usually rounded, dark

coloured and of pebble to cobble size. Small fragments of silicified wood are

randomly scattered.

Gebel Ahmar Formation unconformably overlies the Upper Eocene rocks and

extends north and east along the Cairo – Suez road. Geysers and geyser

fissures were noted in many places along the stretch as reported by Barron

(1907) who also recorded a plugged-up fissure out of which silicate-rich water

evidently issued at Gebel Nasuri; it is now marked by a narrow dyke-like mass

of silicified sandstone. At Gebel Anqabia, denuded plugs of various fissures up

which the thermal waters came, were also recorded by Barron (1907). At Gebel

Shabraweet, the Gebel Ahmar Formation unconformably overlies the Early

Cretaceous Malha Formation at northern parts of G. Shabraweet.

Fig. (3.4): Cross-bedded sandstone, sandy gravels, pebbly sandstone and varicolours sands.

3.3.3 Occurrence. Lithology and Thickness variation:

Gebel Ahmar lies to the east of Cairo, forming a subdued dissected pediment

below the Eocene limestones of Gebel Mokattam. The many faults along the

peripheries of Gebel Mokattam displace the Oligocene sediments to a lower

level than the higher up thrown Eocene rocks of Gebel Mokattam, especially at

the area of the Gebel Ahmar (Geological Map of Greater Cairo Area,

Geological Survey of Egypt, 1983). The Gebel Ahmar Formation detours

Gebel Mokattam to the north where it covers the surface of the desert between

Cairo and Suez. Here also, the E - W faults displace the continental Miocene

sediments in the north against the Oligocene Gebel Ahmar Formation to the

south. Within this huge surface area, prominent hills (e.g.: Gebel Yahmoum El

Asmar, Gebel El Khashab -Petrified Forest- and Gebel Ahmar overlooking

Nasr City to the northeast of Cairo) rise up to 60 - 70 m above the desert plain.

At Gebel Ahmar, the type section of the formation, the sands are coarse-

grained, cross-bedded, vividly coloured mostly friable, with hard quartizitic

dark brown bed at top. The thickness of the sand varies from 40 to 100 m. At

Gebel Ahmar, geyser action is well seen in the dark red and dark brown

silicified tubes which cut erratically through the sands rising several meters in a

castle-like form. Unfortunately, this national park - as it should be - was

destroyed under the new buildings of a hospital and a stadium, even the name

was changed to Gebel Akhdar. Gravels are mostly medium to well-rounded,

pebble to cobble size flint, sometimes disc-shaped, earthy yellow to black in

colour form bands of limited extensions in the sands.

A shaft had been sunk in it, which shows the junction between the limestone

and the sandstone. At the junction the limestone is much decomposed and is of

all shades of colour from brown to purple. In places it has the appearance of

mortar owing to the admixture of sand. A little to the north of Gebel Mokattam,

some red hills rise up made of fine sand of various colours, consolidated in

places into sandstone, while in others they form sandy marl by the increase of

clay. These sandstones are strongly false-bedded and together with the loose

sands and the clays build these red hills, which owe their existence to the

presence of a hard plug of silicified rock in the center, which enables them to

withstand denudation (Hume 1965, p. 698 after Barron 1907). These hills are

the stumps of geysers and at their foot in the low ground many beautiful shades

of coloured sands are found. The thickness of the sand in these hills ranges

between 33 - 35 m. In the northern outcrops as in Gebel Shabraweet, Al

Ahwani (1982) described 30 m Oligocene sediments occupying the low lands

between the topographic and structural highs.

Fig. (3.5): Lithologic Succession of Gabal Ahmar Formation along El-Qattamiya – El-Sokhna Road.

3.3.4 Faunal content and Age assignment:

Silicified wood is very common in the Gebel Ahmar Formation, but very well

developed at Gebel El Khashab where a true forest, but petrified is known.

Most workers believe that the tree trunks (some of which reach 44 m in length)

were transported for long distances. Though some authors believe that

silicification took place after transportation from areas far to the south and that

they were rafted to their present positions by an ancestral Nile River (Kortland,

l980). Bown et al. (l982) believe that there is no geologic or palaeobotanical

evidence to support this contention. An Oligocene age was assigned to this

formation based upon the geometric-stratigraphical relationships and the

presence of the petrified wood remains resulted to a land-activity indicative of

this time.

3.3.5 Geographic Distribution & Equivalent rock units:

The Oligocene Gebel Ahmar Formationis also known from Gebel Qattamiya,

Gebel Gafra, Gebel Um Qamar, Gebel Aweibed and Gebel Genefa, mostly

associated with basalt and geyser eruptions. In general, the Gebel Ahmar

Formation is usually associated with geyser cones where silica water gushed

up and also with volcanic basalts erupted through vents giving rise to dykes,

sills and Plateau volcanics. The colour of the formation is usually vary-

coloured - but red, yellow and reddish colours are most common. At Gebel

Yahmoum El Asmar, a pile of black to dark grey gravels rises 40 - 50 m above

the surface of the encompassing desert. The gravels are loose, pebble to cobble

size and some are even larger.

The equivalents of the Oligocene Gebel Ahmar Formation are sporadically

present as far eastward as the Bitter Lakes and east Sinai and as far to the south

as the Northern Galala Plateau and even further south near Qusseir area.

3.4. SADAT FORMATION:

The Sadat Formation makes up the oldest studied rocks in the Sadat-Wadi

Hagul stretch. It has a relatively wide geographic distribution around EL-

Qattamiya – El-Sokhna Road.

3.4.1 Nomenclature:

The Sadat Formation was first introduced in the Egyptian Geology by

Abdallah and Abd El-Hady (1966) to designate 52 m thick coral and coralline

algal limestones that exposed at its type locality in the Sadat Quarry Hill, EL-

Sokhna area.

3.4.2 Contacts:

The Sadat Formation, in the study area, unconformably overlies the Oligocene

gravels and sands of the Gabal Ahmar Formation.The contact between the

Sadat Formation and the subjacent Eocene rocks along the northeastern limit of

the Miocene exposures is marked by fault-contact with clastic conglomerates

(Cherif, 1966; Youssef et al., 1971) and later considered as the Lower Sandy

Member of the Sadat Formation by Cherif and Yehia (1977) or the Taratir

Member by El Safori (1994).

3.4.3 Occurrence, Lithology and Thickness variation:

Ezzat (2000) assigns the Sadat Formation merely to the reefal limestone facies

as originally defined by Abdallah and Abd El Hady (1966) and dates it to the

Late Burdigalian. The latter authors commented that although Sadek (1926)

included the sandy limestone (20 m thick) on the top of the reefal limestone to

his Lower Miocene Series, they preferred to restrict all the sandy limestone to

the Hommath Formation, whereas the reefal limestone to the Sadat Formation.

Therefore, the present work supports the field observation early given by

Abdallah and Abel El Hady (1966). Lithologically, The Sadat Formation is a

unique carbonate sequence, made up of reefal limestones with a few thin

mudstone interbeds. It generally consists of the following sedimentary facies

(Fig. 3.6):

A) Basal Clastic Facies:

The basal part of the Sadat Formation is consisting of coarse clastic unit due to

the erosion of the underlying Eocene rocks. These coarse clastics are represented

by sandstones, chert pebbles and polymictic conglomerate. The conglomerates are

30-35 cm thick with rounded to with rounded clasts tightly embedded in a sandy

clayey lime mud matrix.

B) Reefal Limestone Facies:

The reefal limestones form the dominant lithofacies type in the Sadat Formation,

constituting 86% of the measured succession. The limestones are massive-bedded

with individual bed thickness ranging from 0.7-1.5 m. They have a characteristic

chalk appearance and weather into light grey rough surfaces. Coral reef and oyster

bivalve are the most common faunal assemblage. Scattered in situ coral reef

patches and coral fragments are widely distributed throughout the succession to

mark the reefal limestone facies.

3.4.4 Faunal content and Age assignment:

The formation is fossiliferous with a large number of shallow marine fauna

such as coral reef, bivalve, calcareous algae, large benthic, algal oncoid

andechinoderm. It yields the following micro faunal assemblage (Youssef el

al., 1971; Ezzat, 2000):

Operculinn eomplrmam (Defrance), Plmmslegilm (formerly Helerostegina)

IteterosteginaImlerosregina (Silvestri), P. lzererostegina praecosmm Papp

Miogypsimi inlermedin Dooger, Ampltislegilm sp. and Dasyelarlaccn sp.

Souaya (1961 & 1963) stated that the Operculina complanam strongly

allocate a Late Burdigalian to the Sadat Formation. Currently, Ismail and

Abdel-Ghany (1999) recorded a few planktonic species of Globigerinoirles

primonlius, Gs. lrilobus and Gs. alliuperturux in the top part of the Sadat

Formation, which are ranging from Zones NS-N7 (Burdigalian). Cherif and

Yehia (1977) extended the upper limit of the Sadat Formation to enclose the

highly fossiliferous sandy limestone above the reefal limestone and assigned

the whole limestone to a Late Burdigalian-Langhian age.

Fig. (3.6): Lithologic Succession of Sadat Formation along El-Qattamiya – El-Sokhna Road.

3.4.5 Geographic Distribution & Equivalent rock units:

The Sadat Formation, as a lower subdivision of the Miocene succession,

exclusively occupies the northeastern reach of the studied area along the

northern parts of El-Qattamiya-El-Sokhna Road. The formation also crops out

in the upper reach of Wadi Hagul. lt transgressively overlaps either the Middle

or Upper Eocene rocks and is downlaped westward by the younger Miocene

rocks.

CHAPTER FOUR

LITHOLOGICAL CHARACTERISTICS

AND SEDIMENT COMPOSITION

The textural characteristics of the different sedimentary rock units; Esna Shale,

Thebes Formation, Gabal Ahmar Formation and Sadat Formation in the study area

were studied to investigate the detailed lithological components. These include: -

4.1. THE GENERAL BULK TEXTURAL COMPOSITION:

The sediments of the Esna Shale and Gabal Ahmar formations were analyzed for

their bulk textural composition of the carbonate-sand-mud% composition and

gravel-sand-mud % composition. In this concern, the collected samples were

visually examined to prepare them for these analyses as given in Chapter-Two. The

number of the analyzed samples in different rock units is given in Table (4.1).

Table (4.1): The number and distribution of examined samples in different bulk textural composition

analyses

Analysis

Carbonate-Sand-Mud %Composition Gravel-Sand-Mud %composition

Esna Shale Gabal Ahmar Fm. Esna Shale Gabal Ahmar Fm.

2 4 1 4

The results obtained for the given bulk compositions are plotted on different

triangular diagrams of Füchtbaur and Müller (1970) and Folk et al. (1970) to arrive

the accurate composition of the examined sediments. The general investigation of

these data indicates the following characteristics of the encountered sedimentary

units:-

4.1.1 Esna Shale:

The sediments collected from the Esna Shale in the study area provide the

following composition:

4.1.1.1. Carbonate-Sand-Mud % composition:

Two (2) samples representing the Esna Shale at the study area were analyzed

for their carbonate-sand-mud % composition. The results obtained of this

analysis are given in Table (4.2) and are represented as triangular diagram

(Fig 4.1). Accordingly, the majority of the examined sediments includes

lesser content of carbonates (Fig 4.1) and has general sandy mud and mud

composition, reflecting almost uniform sources and unique depositional

regimes.

Table (4.2): The Carbonate-Sand-Mud% composition analysis of The Esna Shale sections

sample Carbonate % Sand % Mud % Composition

Fig(4.1): Carbonate-Sand-Mud% composition of The Esna Shale lithologic sections plotted on

Füchtbaur& Muller (1970) triangular diagram.

4.1.1.2. Gravel-Sand-Mud % composition:

One sample was analyzed from Esna Shale at the study areafor its gravel-

sand-mud % composition. The results obtained are given in Table (4.3) and

are represented as triangular diagrams (Fig 4.2). Generally, the examined

sediments are devoid of gravel contents, while include little amounts of sand

fraction. This supports deposition within a basin far from the reach of any

coarser clastics and quiet energy.

Table (4.3) The Gravel-Sand-Mud% composition analysis of The Esna shale sections.

Esna Sh-1 5.65% 1.6% 92.8% Mudstone

Esna Sh-2 3.3% 25.2% 71.4 Sandy mudstone

Composition Mud% Sand% Gravel % Sample

Mud 97.89% 2.1% 0% Esna sh-1

Sandy mud 75.02 24.97% 0% Esna sh-2

Fig (4.2): Gravel-Sand-Mud% composition of Esna Shalelithologic sections plotted on Folk et al

(1970) triangular diagram.

4.1.2. Gabal Ahmar Formation:-

The samples collected from Gabal Ahmar Formation in the study area provide the

following:

4.1.2.1. The Carbonate-Sand-Mud % composition:

Four (4) samples represent the Gabal Ahmar Formation in the study area were

analyzed for their carbonate-sand-mud % composition. The results obtained of

this analysis are given in Table (4.4) and are represented as triangular diagram of

Fig (4.3). The sediments of the Gabal Ahmar Formation show wide scattered

distribution in their forming constituents reflecting obvious variation in their

sources and variability in the depositional regime. Thus, the sediments vary in

composition between mudstones and sandstones. However, the muddy sand

constitutes the main composition, forming about 50% of the formation sediments,

sandy limestone form about 25% andcalcareous muddy sand form about 25%.

Table (4.4) The Carbonate-Sand-Mud% composition analysis of

The Gabal Ahmar Formation.

Sample Carbonate % Sand % Mud % Composition

G. Ahmar-1 5.69% 76.2% 17.8% muddy sand

G. Ahmar-2 0.1% 76.75% 23.15% muddy sand

G. Ahmar-3 38.1% 38.6% 23.2% calcareous sand

G. Ahmar-4 51.7% 30.5% 17.8% sandy lime stone

Fig (4.3): The carbonate-sand-mud% composition of Gabal Ahmar Formation plotted on the

Füchtbaur& Müller (1970) triangular diagram.

4.1.2.2. The Gravel-Sand-Mud % composition:

Four (4) samples were analyzed from Gabal Ahmar Formation for their gravel-

sand-mud % composition. The results obtained of this analysis are given in

Table (4.5, Appendix) and are represented as triangular diagram of Fig. (4.4).

The Gabal Ahmar Formation is generally poor in gravel fraction. They

commonly fall in the category of clayey to muddy composition.

Table (4.5) The Gravel--Sand-Mud% composition analysis of The Gabal Ahmar sections

Composition Mud% Sand% Gravel % sample

gravelly muddy sand 18.94% 61.00% 20.15% G. Ahmar 1

Slightly gravelly

muddy sand 23.17% 69.56% 7.25% G. Ahmar 2

Muddy sand 37.50% 62.50% 0% G. Ahmar 3

Muddy sand 36.85% 63.14% 0% G. Ahmar 4

Fig (4.4): Gravel-Sand-Mud% composition of Gabal Ahmar plotted on

Folk et al (1970) triangular diagram.

4.2. GRAIN SIZE ANALYSIS:

The grain size analysis was done in this study to emphasize the detailed grain size

characteristics of sand-rich formations. The present investigation encompasses the

sediments of Esna Shale and Gabal Ahmar Formations.

The grain size analysis was carried out using the dry mechanical analysis

techniques as described by Folk (1968 & 1980) and Carver (1971), given in details

in Chapter-Two. The data obtained of this analysis was given in Tables (4.3 and

4.5).

4.2.1. The graphic representation of the grain size data

The results of the mechanical analysis of the sand-rich samples were plotted as

percentage cumulative distribution curves using logarithmic scale (Figs. 4.5 and

4.6) as described by Folk (1980) to determine their grain size distribution and

calculate the grain size parameters Folk & Ward (1957). The discussion of the

given size distribution characteristics of each formation are given as follows:

4.2.1.1 Esna Shale:

The cumulative curve representing the size distribution of the analyzed sample is

given in Fig (4.5). It shows dispersed distribution indicating variable depositional

regimes. Generally, the curve displays relatively steep slope indicating more fining

grains and moderately to moderately well sorting (Folk, 1980). The segments of

suspension populations are generally of better sorting than the traction ones,

whereas the saltation populations are generally segmented indicating variation in

depositional current velocity (Visher, 1966).

Fig (4.5): The cumulative grain size distribution curve of Esna Shale.

4.2.1.2 Gabal Ahmar Formation:

Four sand samples were analyzed from the Gabal Ahmar Formation. The

cumulative curves representing the size distribution of these samples are

given in (Fig 4.6). They show wide dispersed distribution indicating variable

depositional regimes. Generally, the curves display relatively gentle slope

indicating moderate sorting (Folk, 1980). The segments of suspension

populations are generally of better sorting than the traction ones, whereas the

traction populations are generally segmented indicating variation in the

depositional current-velocity (Visher, 1966).

Fig. (4.6): The cumulative grain size distribution curve of Gabal Ahmar.

4.2.2. The Grain size parameters:

The statistical calculations of the grain size parameters of Folk & Ward (1957)

including the graphic mean size (MzØ), inclusive graphic standard deviation (δIØ),

inclusive graphic skewness (SKI) and graphic kurtosis (KG) have been calculated

using the phi-percentiles Ø5, Ø16, Ø25, Ø50, Ø75, Ø84 and Ø95 determined on

the cumulative curves. The formula used in calculating these grain size parameters

are as the following:-

i) Graphic Mean Size (MzØ) = Ø16+Ø50+Ø84/3

ii) Inclusive Graphic Standard Deviation δIØ)= (Ø84- Ø16) /4 + (Ø95- Ø5) /6.6

iii) Inclusive Graphic Skewness (SKI)= (Ø16+ Ø84)-2 Ø50/2(Ø84- Ø16) + (Ø95+ Ø5)-2

Ø50/2(Ø95- Ø5)

iv) Graphic Kurtosis (KG)= Ø95- Ø5/2.44(Ø75- Ø25)

The obtained data are given in Table (4.6) and their averages are summarized in

Table (4.7). The following notes are recorded for each examined Formation:-

4.2.2.1. Esna Shale

The sands of the Esna shaleFormation are generally fine to very fine grained

with MzØ3.45 (fine sands). The sands are generally poorly sorted withδIØof

1.21Ø. The grain size distribution is strongly coarse skewed (SKI = -

0.809Ø) and peaked distribution (KG = 5.05Ø).

4.2.2.2. Gabal Ahmar Formation:

The sands of the Gabal Ahmar Formation are generally coarse to fine

grained with Mz Ø ranges between 1.1Ø to 3.65Ø and average of 2.425Ø

(fine sands). The sands are generally poorly to moderately sorted withδIØ

average of 1.64Ø, (range 0.668 Ø – 3.51 Ø). The grain size distribution is

fine skewed (average SKI = 0.512Ø) and peaked distribution (average KG =

0.97 Ø).

Table (4.6): The grain size parameters of the examined samples

Form

ati

on

Sam

ple

Nos.

MzØ δIØ SKI KG Description

Esna

Shale 2 3.45 1.21

-0.809

5.05 Fine to very fine grained, poorly sorted, strongly

coarse skewed, peaked distribution.

Gabal

Ahmar

1 1.1

3.15 1.7

1.4

Coarse to medium grained, very poorly sorted,

strongly fine skewed, peaked distribution.

2 1.6 1.94 0.47 0.99 Coarse to medium grained, poorly sorted,

strongly fine skewed, flattened distribution.

3 3.35 0.813 0.104 0.655 Fine to very fine grained, moderately sorted,

fine skewed, flattened distribution.

4 3.65 0.668 -0.226 0.860 Fine to very fine grained, moderately well

sorted, coarse skewed, flattened distribution.

Table (4.7): Average of grain size parameters for the examined samples

Fo

rmati

on

MzØ δIØ SKI KG

Description

Ra

ng

e

Av

era

ge

Ra

ng

e

Av

era

ge

Ra

ng

e

Av

era

ge

Ra

ng

e

Av

era

ge

Esna

Shale 3.45 ــــــــــــ 5.05 --- 0.226- ــــــــــ 1.21 ــــــــــ

Fine to very fine

grained, poorly

sorted, coarse

skewed, peaked

distributed.

Gabal

Ahmar

1.1

ـ 3ـ

.65

2.4

25

0.6

683ــ

.15

1.6

42

-0.2

26ـــ

1.7

0.5

12

0.6

551ــ

.4

0.9

76

medium to fine

grained, poorly

sorted, strongly

fine skewed,

flattened

distribution.

CHAPTER-FIVE

MICROFACIES AND LITHOFACIES

INVESTIGATIONS

5.1 PRELUDE:

This chapter deals with the microfacies study of the thin sections prepared from the

examined rocks in the study area. This study aims to discuss the microfacies

characteristics and their paleo-ecological conditions of depositional settings. The

similar microfacies both in characteristics and depositional interpretations are

regarded here in as one association.

All microfacies were identified, described and photographed using the standard

polarizing microscope. The petrographic classification of limestone suggested by

Folk (1959) and (1962), the textural classification proposed by Dunham (1962) and

modified by Embry& Kolvan (1971) are followed herein with slight modifications

to describe and discuss the encountered microfacies. The recognized limestone

microfacies are correlated with the standard microfacies types (SMF) of Wilson

(1975) and their depositional environments as categorized by Flügel (1982) to

deduce the depositional environments of the studied rock units.

The nomenclature scheme of the present microfacies follows the textural

characteristics of Folk (1959) & (1962) and the depositional characteristics

proposed by Dunham (1962). For the clastic microfacies, the field and textural

characteristics are taken in consideration during their nomenclature. The different

microfacies associations encountered in the examined rocks in the study area are

summarized in the Table (5.1).

Table (5.1): The encountered Microfacies Associations in the examined rock units:

ROCK

UNIT AGE

ENCOUNTERED MICROFACIES

ASSOCIATIONS

SADAT

FORMATION

Early

Miocene

5.4.3. Lime-mudstone/dolostone

5.4.2. Reefal Limestone Facies

5.4.1. Basal Clastic Facies

GEBEL

AHMAR

FORMATION

Early

Oligocene See 5.4. Oligocene Lithofacies Analysis

THEBES

FORMATION Early Eocene

5.2.3. Silicified mudstone

5.2.2. Pel-foraminiferal dol- Packstone

5.2.1.Dolomitized Foraminiferal wackstone

ESNA SHALE

Latest

Maastrichtiant

o

Early Eocene

5.1.2. Ostracod-foraminiferal Wackstone

5.1.1. Foraminiferal-rich Packstone

The recognized microfacies associations in each rock units are discussed as

follows:

5.2 ESNA SHALE

The microscopic investigations of the thin sections of Esna Shale revealed the

following microfacies:

5.2.1. Forminiferal-rich Packstone:

It is very frequent microfacies, forming 95 % of the Esna Shale.

Petrographically, it is represented by microcrystalline homogenous micritic matrix

impregnated with abundant planktonic foraminiferal (P 1.1), deposited with some

benthonic foraminiferal genera (P1.2). Rare thin walled bivalve shell fragments

(less than 10%). Patches of microsparite and iron stains are scattered throughout

the micritic matrix.

Diagenesis:

This microfacies was subjected into neomorphism due to the presence of sparite

within the chambers of foraminiferal tests and the bivalve shell fragments, as well

as the patches throughout the matrix.

This microfacies was possibly deposited in outer neritic environment, below the

wave base (Wilson, 1975) with quite water and normal salinity (Plumely et al.

1962), possibly of bathyal environment (Hassan, 2005).

5.2.2. Ostracod-foraminiferal Wackstone:

This microfacies is identified in the marly limestone of the middle and upper parts

of the Esna Shale. Petrographically, it consists of 60% ostracod shell fragments in

addition to 40% planktonic and rare benthonic forms.(P1.3). They are partially or

completely filled with coarse crystalline cement ―sparite‖ and iron stains. All are

embedded in fine microcrystalline micrite matrix.

Diagenesis:

This microfacies shows evidence of neomorphism due to the presence of

foraminiferal chambers partially filled with coarse crystalline sparite.

This microfacies was possibly deposited in inner neritic environment (Wilson,

1975) with quite water and normal salinity (Plumely et al. 1962).

Plate (1):

-Planktonic Foraminifera, Foraminiferal-rich microfacies

-Benthonic fossils, Foraminiferal-rich microfacies

Ostracod test, Ostracod-foraminiferal wackstone microfacies.

(Plate figures are after Hassan, 2005).

5.3. THEBES FORMATION

The microfacies investigation of the thin sections from the Thebes Formation in

the study area revealed the recognition of the following microfacies associations:

5.3.1. Dolomitized foraminiferal Wackstone:

This microfacies association is distributed in the whole sequence of the Thebes

Formation. Petrographically, the foraminiferal tests (30-50%) mainly include

planktonic forms. Benthonic forms and reworked bivalve shell fragments

constitute about 15 %. The fossil walls are rimmed by micrite and the chambers

are frequently filled with sparite. Dolomite rhombs and dolomitic patches are seen

within the matrix, occasionally they replace the rock allochems. Iron stains

commonly mask the foraminiferal tests and some shell fragment. The micrite

matrix is homogenous microcrystalline and partially neomorphosed into

microsparite.

Diagenesis:

Neomorphism as evidenced by the foraminiferal tests filled with sparite as well as

presence of rare microsparite patches scattered throughout the microfacies.

Dolomitization process is also achieved due to the presence of the dolomite

rhombs in different parts of the microfacies replacing some components. Also, it

shows marks of high compaction as deduced by both the long grain-to-grain

contacts between the foraminiferal tests and the common stylolites.

This microfacies was possibly deposited within shallow outer neritic environment

(Wilson, 1975) with quite water and normal salinity (Plumely et al. 1962). Hassan

(2005) suggested deeper bathyal depositional setting due to the presence of

Spiroplectammina dentata, Anomalinoides rubignosus, Siphogenerinoides

elegantus and Nodosaria limbata.

5.3.2. Pel-foraminiferal dol-Packstone:

This microfacies is only represented in the uppermost part of the Thebes

Formation. The foraminiferal tests constitute about 40% of both planktonic and

benthic forms in association with calcareous algae. Frequent (15%) rounded,

tubular and irregular pellets are present. Iron patches are present and stain some

components. All components are embedded in a general dolomitized microsparite

matrix.

Diagenesis:

This microfacies undergoes neomorphism and dolomitization that responsible for

the distortion of most components in addition to the high compaction evidenced by

the presence of stylolites. This microfacies was possibly deposited in protected

coastal lagoon (Wilson, 1975) with quite water. (Plumely et al., 1962).

5.3.3. Silicified mudstone:

This microfacies is subsidiary microfacies. It is encountered only in the chert

bands intervened within the Thebes Formation. Petrographically; it consists of

microcrystalline silica patches and chalcedony of characteristic spherulitic

textures. The silica patches characterized by fine shrinkage structure due to

recrystallization rimed with microcrystalline quartz of 5-4m size. Frequent

foraminiferal chambers were completely filled with sparry quartz and in few cases

partially replaced by microcrystalline quartz. Few sparry calcite crystals as well as

some argillaceous materials were occasionally noticed in this microfacies.

Diagenesis:

Silicification process is evidenced by the silica replacing the foraminiferal

chambers, radiolaria and calcite veins by microcrystalline silica. This microfacies

was possibly deposited in basin margin environment (Wilson, 1975) probably as

quite water (Plumely et al. 1962).

5.4. THE SADAT FORMATION

The microfacies investigation of the thin sections from the Sadat Formation in the

study area revealed the recognition of the following microfacies associations:

5.4.1. The Basal Clastic Microfacies:

The Sadat basal clastic facies is of rather restricted and narrow extension. lt

onlaps and pinches out on the Eocene limestone forming the southwestern

dip-slope of Gebel Ataqa. The basal clastics consist of 7 m thick tangential

cross-bedded sandstones. Locally, they are replaced by thin coarse clastics

with reworked Eocene limestone and chert pebbles and cobbles (polymictic

conglomerates). The conglomerates are 30-35 cm thick with rounded to well

rounded clasts tightly embedded in a sandy clayey lime mud matrix. They

have a sharp erosive basal contact and merge gradationally into the overlying

reefal limestone. The good roundness of the clasts attests to a relatively long

period of abrasion before accumulation. The dominant cross-bedded

sandstones are yellowish brown, moderately consolidated, quartz-dominated,

calcareous and slightly glauconitic. They are moderately well sorted with fine

to medium sand grains. The cross-bedded sets are 30 cm in height with 1-2

cm thick foresets. The foresets dip with an average angle of 28° toward the

southwest. The sandstones are fossiliferous with dispersed Pecten shell debris,

echinoid spines and rare badly preserved benthonic foraminifera. The upper

sandstone beds are highly burrowed by simple vertical burrows (Skolithos)

that resulted in the disruption of the sedimentary structure and fabric.

Diagenesis :-

The quartz grains are rimmed with a thin euhedral silica overgrowth (Fig.

5.1). The quartz grains are enhanced by the post-depositional calcite-quartz

replacement, whereas most of the grains and their overgrowths are partially

corroded by calcite cement (Fig.5.2). Sparry calcite cement is filling

completely the intergranular pore spaces.

Fig. (5.1): Silica Overgrowths in the basal clastic microfacies.

Fig. (5.2): carbonate cement corrode the rims of the

Quartz grains, basal clastic microfacies.

5.4.2. Reefal Limestone Microfacies:

The reefal Iimestones form the dominant lithofacies type in the Sadat Formation,

constituting 90% of the measured succession. The limestones are massive-bedded

with individual bed thickness ranging from 0.7-1.5 m. They have a characteristic

chalky appearance and weather into light grey rough surfaces. Coral reef and large

fragments of bivalves (Fig.5.3) are the most common faunal assemblage. Scattered

coral reef patches and coral fragments are widely distributed throughout the

succession to mark the reefal limestone facies. Oyster bivalves occur as scattered

forms or as dense crowded assemblage forming fossil banks. Many large oyster-

bearing beds observed intercalating the limestones. Locally, corallinealgae,

foraminiferal species, algae and echinoid represent an important rock constituent.

Densely crowded operculina complanata carrying beds are common in the upper

part of the limestone facies, which date the Sadat Formation back to the Late

Burdigalian (El-Azabi, 2000). The reefal Iimestones are dominated by wide

varieties of microfacies types which have been deposited as reefal shelf

environment; including back-reef, reef-flank, and fore-reef assemblages.

Diagenesis:

Dolomitization and recrystallization is the most common diagenetic features in this

microfacies as recorded along the rock matrix and inside the fossil-shell fragments.

5.4.3. Lime-mudstone/dolostone Microfacies:

The lime-mudstone is not a common microfacies in this formation. It is recorded in

the basal and middle parts of the measured sequence. In outcrop, the rocks are pale

brownish white, moderately hard, highly argillaceous and partly dolomitic. They

contain abundant ill-sorted sands, never exceed 25% of the total rock (sandy

dolomitic lime-

Fig. (5.3): Large fragments of bivalves, reefal limestone microfacies

mudstone). The sands are quartz-dominated with fine- to medium-sized grains.

The quartz grains are angular to subrounded and largely exhibit calcitc-quartz

replacement along their outer peripheries. The lime-mudstone yields a few

scattered badly preserved bivalves (Pecten & Oyster) and echinoid debris. The

matrix is dense cloudy lime mud and fine diagenetic dolomite rhombs with small

clear patches of sparry calcite filling the cavities within the rock. Hematite is also

present as cavity and fissure fillings. Dolomite rhombs are euhedral to subhedral

and have a cloudy appearance and a dark clayey core with less clear zoning

(Fig.5.4).

Fig. (5.4): Euhedral to subhedral dolomite rhombs with less clear zoning,

Lime-mudstone/dolostone Microfacies.

Diagenesis:

Dolomitization is the most common diagenetic process reported for this

microfacies association. According to Hardie's (1987), a brackish-water mixing-

zone dolomitization model is assumed where there is no evidence of intense

evaporation during sediment accumulation. Dolomite rhombs are thought to have

formed during the early diagenetic stage.

5.5. THE LITHOFACIES ANALYSIS OF GEBEL AHMAR

FORMATION:

In the study area, the Gebel Ahmar Formation is entirely clastic unit. It is formed

of pebble and cobble-sized conglomerates deposited with a mixture of gravelly

sandstones and sandstones. This wide-range of clastics is highly ferruginous and

display characteristic different hues of dark red colouration.

Since the different rock facies forming this unit can only be examined in the

outcrops rather than under microscopic scale, the following is a discussion of the

different facies forming the lithologic succession of the Oligocene Gebel Ahmar

Formation as recorded in the field:

5.5.1. Imbricate lag pebble-cobble conglomerate

This lithofacies is commonly recorded at the basal parts of the clastic sequences

forming the present formation. It is seen in form of individual pebble and cobble

clasts strewn in imbricate form along extended liens at the base of gravelly

sandstone units (Fig.5.5). Cobbles and Pebbles are poorly sorted, subangular to

subrounded of dark grey to black colours.

Fig. (5.5): The imbricate lag pebble-cobble conglomerates.

5.5.2. Carbonate conglomerates:

This lithofacies is locally recorded in the succession of the Oligocene Gebel

Ahmar Formation. It is recorded in some parts admixed with the basal parts of the

Imbricate lag pebble-cobble conglomerate (5.4.1.). The lithofacies consists of

carbonate pebbly-sized rock fragments of white colours and less distinct

boundaries (Fig.5.6), possibly derived as cut-chunks from the underlying Eocene

rocks. These fragments are admixed within a ferruginous sandy matrix.

Fig. (5.6): The whit carbonate clasts, Carbonate conglomerate lithofacies.

5.5.3. Crudely non-stratified pebble-cobble-conglomerate:

This lithofacies constitutes a considerable part of the examined formation. It is

consisting of 1.50 – 2.00 m thick layers of very crowded clasts of pebbles and

cobbles embedded in a little amount of gravelly sandstones and sandstone,

exhibiting non-linear stratification (Fig.5.7). Clasts are subangular to subrounded

and poorly sorted with dark brown and black colours. The clasts are mainly of

basalt and minor contents of limestones and claystones. The sandy matrix is

generally highly ferruginous of reddish brown colours, with sands display badly-

sorted and subangular textural characters.

Fig. (5.7): The crudely non-stratified pebble-cobble-conglomerate.

5.5.4. Planar tabular cross-stratified ferruginous gravelly sandstone

This lithofacies is a common lithofacies, encountered in different parts of Gebel

Ahmar Formation. The lithofacies consists of gravelly sandstones displaying low-

angle planar tabular cross stratifications (Fig.5.8).

The gravelly sandstones are poorly sorted, subangular to subrounded with

yellowish brown colours. A few cobble sized-clasts are sometimes strewn within

the lithofacies body. The planar tabular cross-stratified foresets display low angles

ranging between 20° - 30º with general erosive basis. The slope faces of the cross-

stratified foresets display different directions of paleocurrent. Occasional wood

fragments are sometimes recorded along the slip-faces of the cross-sets.

Fig. (5.8): The Planar tabular cross-stratified cobble-boulder conglomerates.

5.5.5. Planar tabular cross-stratified cobble-boulder conglomerates.

This lithofacies is not common in the succession of the Oligocene Gebel Ahmar

Formation. It is only recorded in the field inform of relatively thin gravelly

sandstone units within which crowded foresets of cobble and boulder clasts display

low angle planar tabular cross-stratification (Fig.5.9). The architecture of this

lithofacies seems peculiar since the grain size-current velocity relation of Harms et

al (1975) did not explain the development of the low-angle cross-stratification by

cobble and boulder clasts. However, Coarse gravelly bars producing horizontal and

low angle cross-stratification are commonly reported in the deposits of active

short-lived low-sinuosity gravelly braided streams (e.g.: Smith, 1974; Harms et al.,

1982).

Fig. (5.9): The Planar tabular cross-stratified cobble-boulder conglomerates. (Arrows)

CHAPTER SIX

DEPOSITIONAL INTERPRETATIONS

The detailed study for the examined thin sections within different investigated rock

units revealed the presence of a number of microfacies association in these rock

units. These microfacies enabled the following depositional interpretations:

6.1 ESNA SHALE (LATE MAASTRICHTIAN-PALEOCENE):

The Esna shale comprises the following microlithofacies:

(b) Ostracod-foraminiferal Wackstone

(a) Foraminiferal-rich Packstone

1) By the Campanian-Late Maastrichtian times, the underlying Sudr Chalk was

reshaped due to the uplifts associated with the Syrian Arc pulses in the

north and eastern parts, while the western territories undergone early swales

of the Gulf of Suez rift. This tectonic situation resulted in the development

of remarkable unconformable boundary, and consequently permitted the

deposition of the lower levels of the Early - Middle Paleocene Esna Shale

under outer neritic to upper bathyal depositional environment.The

deposition started with shallow outer neritic benthonic-rich mud shale that

had been changed rapidly into the dominant deep outer neritic to bathyal

Planktonic-rich micrites. This rapid change into the deeper microfacies

indicates rapid subsidence and prevalence of deeper sedimentation of

bathyal affinity, which continued until the middle of Esna Shale.

2) The second phase of deposition encompasses development of conformable

sedimentary unit overlying the earliest levels of Esna Shale. However, they still

overprinted by the pulses of the Syrian Arc system till the middle part of Esna

Shale. The deposition was dominated within the realm of relatively shallow

marine environments.

3) By the middle times of the Paleocene, deposition underwent broadly under the

influence of further basin subsidence, confirmed by further basin deepening.

4) By the late Early Paleocene-Early Eocene times, toward the end of Esna Shale,

deposition continued within the upper bathyal depositional conditions. Toward

the close of the Esna Shale depositional history, the deposition took place

under relatively outer neritic environments.

6.2 THEBES FORMATION (LATEST PALEOCENE – EARLY EOCENE)

The Thebes formation comprises the following microlithofacies:-

(c) Silicified mudstone

(b) Pel-foraminiferal dol- Packstone

(a) Dolomitized Foraminiferal wackstone

5) With the Early Eocene times, the earliest levels of the Thebes Formation started

to be deposited. The deposition was accomplished within relatively similar

depositional conditions started with the end of the Esna Shale (i.e.; outer neritic

environments).By the deposition of the Thebes Formation, a quiet and gradual

sea level fall (through the outer neritic zone) started to dominate as indicated

by the dominance of Planktonic / Benthonic & Benthonic/Planktonic rich

calcareous mud shales in the lower half of the Thebes Formation (Hassan,

2005). Near the middle of the Thebes Formation, a marked sea level drop took

place, evidenced by the dominance of shallow inner neritic and coastal

lagoonal microfacies of algal and peloidal micrite (Hassan, 2005). This sea

level drop is believed to be the strongest in the Paleogene in Sinai. The allover

shallowing conditions were followed by inner neritic and shallow outer neritic

benthonic rich mud shale that successively dominated in the upper half of the

Thebes Formation. This indicates a subtle subsidence and sea level rise by the

upper half of the Thebes Formation. This subsidence reached maximum by the

end of Thebes Formation when the outer neritic-bathyal Planktonic rich

micrites dominated the top of Thebes Formation allover Sinai (El-Fawal et al,

2005).

6) Toward the end of the Early Eocene times, an observable shallowing took place,

as a result of mild basin uplift during these times (Hassan, 2005). During these

conditions, the upper part of Thebes Formation was developed under inner

neritic depositional conditions.

7) Due to the successive uplifts accompanied the Gulf of Suez rift, the study area

was elevated toward the earliest Oligocene times. Consequently, much erosion

took place for most of the Paleogene sequences to be redeposited as coarse

clastics within the Oligocene formations.

6.3 GABAL AHMAR FORMATION (OLIGOCENE):

The lithofacies analysis made for the Gabal Ahmar Formation has indicated

five lithofacies; all suggest the following remarks on the evolution of the given

formation:

8) With the Oligocene times, the cratonic lands of Egypt started t rise from the

south to the north (Issawi et al, 1999). This uplift continued intermittently,

associated with many episodes of volcanism and hot geysers. The magnitude

of uplift-relief documented for those times is considered in terms as high as

500-1000 ms (Issawi, et al, 1999). These uplifts were met eastwards by the

well-grown swales resulted with the openings of the Red sea and Gulf of Suez

rifts

9) Due to such semi-circular uplifts, wide drainage nets trending northwards and

northwestwards (Fig. 6.1) cut their courses into the significantly retreating

Tethys. These drainage nets eroded huge amounts of rock materials from the

underlying calcareous shale and limestones from the southern catchment areas

into the northern basins.

10) The voluminous detrital loads were spread along the northern stretch of Gabal

Ahmar area depositing the Gabal Ahmar Formation in form of red hills rich in

silicified wood remains of the plants that were developed along the many

flood-plains developed during those times.

11) The hot geysers commonly developed during the formation of Gabal Ahmar

Formation resulted in the silica solutions that petrified the wooden fragments

commonly encountered within such formation. In this concern, some workers

believe that the silicification took place in-situ before transportation, whereas

others believe that it was accomplished after transportation of plant debris into

their depositional area (Kortland, 1980). Brown et al (1982) supported that

there is no any paleo-botanical evidence of earlier transportation.

12) The continental depositional conditions prevailed during the evolution of the

Gabal Ahmar Formation created a long-lasted hiatus associated with land

emergence and sub-aerial erosion before the deposition of the earliest

sediments of the overlying Miocene rocks.

Fig. (6.1): Sketch showing the suggested water-nets during the early Oligocene

(reproduced from the Geol. Surv. Egypt., 1981).

6.4 SADAT FORMATION (EARLY MIOCENE):

The Sadat clastic/reefal limestone facies marks the first marine transgression of

the Miocene Gulf Sea over its extreme northwestern margin during the Late

Burdigalian.

13) The basal clastic facies attests to the gradual rise of the sea level, whereas

the overlying reefal limestone refers to the maximum sea level rise during

the Late Burdigalian transgression.

14) The basal clastic facies represents ebb-tidal channels formed along the

marginal marine shelf in the upper foreshore zone under the influence of

tidal processes. It records a period of large supply of detritus from the

north and northeast accompanied the gradual rise of the Late Burdigalian

Sea.

15) The progradational geometry of the basal clastics was changed upward into

a reefal limestone. The latter exhibits a rapid landward encroachment of

shallow water carbonate facies over the upper foreshore clastics. The

reefal limestone facies are thick deposits of a coral reef-rimmed carbonate

shelf with various facies associations, which tend to occur within more or

less linear belts. This carbonate shelf margin is closely compared with the

shelf model type of the organic reef (build-up) rim fringing a high energy

basin that given by Wilson (1975). The reefal limestones have been

formed under subtropical warm climatic conditions in water depths

seldom exceed 10 m. The main ecological requirements for modern

subtropical coral growth are shallow warm water (18-36°C), normal

salinities (27-40%), fairly strong sunlight, abundant nutrients and stable

substrates for attachment (Ginsburg, 1972).

16) The present Sadat rimmed carbonate shelf was subjected to a moderate to

high tidal influence, particularly towards the shelf margin. So, most of the

resultant sediments are dominated by high energy, back-reef, coarse-

grained facies. In this back-reef shell setting, the deposition took place

under a normal marine salinity, except in the nearshore restricted lagoon,

due to continual exchange between Iagoonal and open Gulf waters. The

warming of the sea-surface temperature never drops below l8°C, the

minimum threshold of surface water temperature for coral reef (Sheppard

et al., 1992).

17) The dominant biogenic association in the reefal limestone facies is the

coral-molluse-coralline algal assemblage (El-Azabi, 2008). lt falls into the

chlorozoan association of Lees and Buller (1972) and Lees (1975), which

contains hermatypic corals and calcareous green algae along with

numerous other organisms. The chlorozoan assemblage is interpreted to

have lived in low latitudes (30° S-30°N) where the shallow sea is always

exceed 15°C and the salinity is normal. Most areas with chlorozoan

sediments have mean temperatures of at least 20°C (Lees and Buller,

1972).

18) The influx of the terrigenous material in the rimmed carbonate shelf was

insignificant. Accidental influx of detritus may cause the deposition of

thin calcareous mudstone.

19) Actually, the Sadat shelf-margin carbonate deposits correspond to a

tectonic stable period during which sedimentation rates and biogenic

construction kept pace with progressive subsidence within the Late

Burdigalian Sea.

20) It is necessary to mention that the whole assemblage of fauna and

sediments of the Sadat reefal limestone appears to be comparable with

those of the nearby carbonate facies of the Gharamul Formation widely

reported along the western coast of the Gulf of Suez (Darwish and El-

Azabi, 1993; 1995) and along its northeastern reach (Eweda and Zalat,

1996).

GENERALIZED SEA LEVEL CURVE OF THE

PALEOGENE-EARLY MIOCENE IN

THE STUDY AREA

The overall emphasize for the different depositional settings and their

corresponding seal level fluctuations during the span time of the Paleogene

have indicated that the following:

1) The time-span of the Paleocene witnessed a phase of deep marine

submergence of the Egyptian territories. The phase started with outer neritic

deep marine environments. These deep marine conditions continued with

more sea-level rise where the environments reached deep to the bathyal

marine sub marine zones of the lower and middle parts of Esna Shale.

2) Toward the end of the Paleocene, the marine sub-environments started to get

shallow accompanied with gradual sea-level fall to the limit of outer neritic

realm.

3) With the start of the Eocene times, the outer neritic marine conditions

prevailed the deposition of the earliest parts of Thebes Formation. The final

stages of the Early Eocene times witnessed gradual, but accelerated sea-level

fall where the upper parts of Thebes Formation were deposited within inner

neritic marine conditions.

4) In the study area, the Upper Eocene sediments are not evident. The absence of

such sediments could be either due to (a) non-deposition where the area is

tectonically situated adjacent to the eastern uplifts associated to the Red Sea

and Gulf of Suez Rifts, or (b) due to subsequent removal by riverine processes

during the Oligocene times.

5) The Oligocene times were episodes of continental sedimentation by active

rivers. Thus, these time express marked sea-level drop associated with land

emergence.

6) The Early Miocene times witnessed a subtle transgression of shallow marine

levels, enough to deposit the clastic/reefal sediments of Sadat Formation.

Fig. (6.2): Fluctuation of the sea-level and depositional settings during the Paleogene/Miocene

over the study area.

CHAPTER SEVEN

SUMMARY AND CONCOLUSIONS

The present study is concerned with the Paleogene-Early Miocene sediments

cropping-out along El-Qattamiya-El Sokhna Road. The main objective of this

study is to conclude the depositional evolution of given sediments in the study

area. Detailed field studies and laboratory analyses were applied and the following

conclusions were achieved: -

7.1. LITHOSTRATIGRAPHY:

Lithologically, the Paleogene-Early Miocene sediments in the study area is

divided into four rock units; namely from older: Esna Shale Formation

(Paleocene), Thebes Formation (Eocene), Gabal Ahmer Formation

(Oligocene), Sadat Formation (Early Miocene).

7.1.1 Esna shale Formation: -

In the study area, Esna Shale is encountered along the eastern parts of El-

Qattamiya - El-Sokhna Road, displaying slope-forming cliffs below the steep

cliff-forming Thebes Formation. Lithologically, it is observed that Esna Shale

in the study area is composed of grey to greenish grey shale intervened with

thin bedded limestone or marly limestone interbeds.

7.1.2 Thebes Formation: -

In the study area, the succession of the Thebes Formation is well developed in

the western parts of El-Qattamiya – El-Sokhna Road. Along this part, the

formation consists of regularly well-stacked, moderately thick (0.75 – 1.50 m)

bedded limestone with occasional chert bands, especially in the lower parts.

The limestones are massive and display white and off-white colour, and are

highly fossiliferous, including many Early Eocene fauna.

7.1.3. Gabal Ahmar Formation: -

Gabal Ahmar Formation constitutes is a unique clastic unit in the Paleogene

succession of Egypt. In the study area, this formation consists of 30-40m thick

gravelly sandstones and pebble-cobble conglomerates, displaying different

yellow and red hues. The sandstones are cross-bedded, with hard quartzitic

dark brown bed at top. Gravels are mostly subrounded to well-rounded, pebble

to cobble size flint. The formation represents a continental phase of deposition

within active fluvial drainage net flowing toward the western and north-

western slopes of that time.

7.1.4 Sadat Formation: -

The Sadat Formation is a unique Early Miocene carbonate sequence, made up

of reefal limestones with a few thin mudstone interbeds. It generally consists of

the following facies:

A) Basal Clastic Facies:

The basal part of the Sadat Formation is consisting of coarse clastic unit due

to the erosion of the underlying Eocene rocks

B) Reefal Limestone Facies:

The reefal limestone facies is the dominant lithofacies type in the Sadat

Formation, constituting more than 80% of the measured succession. The

limestones are massive-bedded with individual beds ranging in thickness

from 0.7 to1.5 m.

7.2. TEXTURAL CHARACTERISTICS:

The detailed textural composition analysis of the clastic rock units (Esna Shale and

Gabal Ahmar Formations) gives the following conclusion:

7.2.1 Esna Shale: -

A- Carbonate-Sand-Mud % composition:

The majority of the examined sediments includes lesser content of

carbonates and has general sandy mud and mud composition, reflecting

almost uniform sources and unique depositional regime.

B- Gravel-Sand-Mud % composition:

Generally, the examined sediments are devoid of gravel contents, while

include little amounts of sand fraction. This supports deposition within a

basin far from the reach of any coarser clastics and quiet energy.

C-The grain size data

The cumulative curve shows dispersed distribution indicating variable

depositional regimes. Generally, the curve displays relatively steep slope

indicating more fining grains and moderately to moderately well sorting.

The segments of suspension populations are generally of better sorting

than the traction ones, whereas the saltation populations are generally

segmented indicating variation in depositional current velocity.

7.2.2 Gabal Ahmar Formation: -

A-The Carbonate-Sand-Mud % composition:

The sediments vary in composition between mudstones and sandstones.

However, the muddy sand constitutes the main composition, forming about

50% of the formation sediments, sandy limestone form about 25% and

calcareous muddy sand form about 25%.

C-The Gravel-Sand-Mud % composition:

Regardless to the thickly bedded conglomerates and the highly gravelly

sandstones, the sandstones commonly fall in the category of clayey- to

muddy-sandstone composition.

C-The grain size data:

The cumulative curves indicate variable depositional regimes. Generally,

the curves display relatively gentle slope indicating moderate sorting. The

segments of suspension populations are generally of better sorting than the

traction ones, whereas the traction populations are generally segmented

indicating variation in the depositional current-velocity.

7.3. MICROFACIES ANALYSIS AND DEPOSITIONAL TRENDS:

The microscopic investigations of the examined sediments provided the following:

7.3.1 Esna Shale Formation: -

The microscopic investigations of the thin sections revealed the following

microfacies:

A- Forminiferal-rich Packstone:

This microfacies was possibly deposited in outer neritic environment,

below the wave base with quite water and normal salinity (Plumely et al.

1962), possibly of bathyal environment.

B- Ostracod-foraminiferal Wackstone:

This microfacies was possibly deposited in inner neritic environment with

quite water and normal salinity.

7.3.2. Thebes Formation: -

The microfacies investigation of the thin sections from the Thebes Formation in

the study area revealed the recognition of the following microfacies associations:

A- Dolomitized foraminiferal Wackstone:

This microfacies was possibly deposited within shallow outer neritic

environment with quite water and normal salinity it suggested deeper

bathyal depositional setting due to the presence of Spiroplectammina

dentata, Anomalinoides rubignosus, Siphogenerinoides elegantus and

Nodosaria limbata.

B- Pel-foraminiferal dol-Packstone:

This microfacies was possibly deposited in protected coastal lagoon with

quite water.

C- Silicified mudstone:

This microfacies was possibly deposited in basin margin environment

probably as quite water

7.3.3 Sadat Formation: -

The microfacies investigation of the thin sections from the Sadat

Formation in the study area revealed the recognition of the following

microfacies associations:

A-The Basal Clastic Microfacies:

The quartz grains are rimmed with a thin euhedral silica overgrowth. The

quartz grains are enhanced by the post-depositional calcite-quartz

replacement, whereas most of the grains and their overgrowths are partially

corroded by calcite cement. Sparry calcite cement is filling completely the

intergranular pore spaces.

B- Reefal Limestone Microfacies:

Dolomitization and recrystallization is the most common diagenetic

features in this microfacies as recorded along the rock matrix and inside

the fossil-shell fragments.

C- Lime-mudstone/dolostone Microfacies:

Dolomitization is the most common diagenetic process reported for this

microfacies association. a brackish-water mixing-zone dolomitization

model is assumed where there is no evidence of intense evaporation during

sediment accumulation. Dolomite rhombs are thought to have formed

during the early diagenetic stage.

7.3.4. The lithofacies analysis of Gabal Ahmar Formation: -

Since the different rock facies forming this unit can only be examined in the

outcrops rather than under microscopic scale, the detailed lithofacies

examination of this rock unit is done in the field where the following

lithofacies are recorded:

A- Imbricate lag pebble-cobble conglomerate

B- Carbonate conglomerates:

C- Crudely non-stratified pebble-cobble-conglomerate:

D- Planar tabular cross-stratified gravelly sandstone

E- Planar tabular cross-stratified cobble-boulder conglomerates.

In the study area, the Gebel Ahmar Formation is entirely clastic unit deposited

by active fluvial streams derived from easterly and southerly situated

hinterlands (mostly occupy the present day Gulf of Suez area and the middle

parts of the present Western Desert), and debouched into westerly and north-

westerly low lands.

7.4. GENERALIZED SEA EVOLUTION OF THE PALEOGENE-EARLY

MIOCENE IN THE STUDY AREA:

The overall investigations of the different depositional settings and their

corresponding seal level fluctuations during the span time of the Paleogene have

indicated that the following:

7.4.1. The Late Maastrichtian – Middle Paleocene Phase:

The time-span of the Late MaastrichtianPaleocene witnessed a phase of deep

marine submergence of the Egyptian territories. The phase started with outer

neritic deep marine environments. These deep marine conditions continued

with more sea-level rise where the environments reached deep to the bathyal

marine sub marine zones of the lower and middle parts of the Esna Shale.

7.4.2. The Late Paleocene Phase:

Toward the end of the Paleocene, the marine sub-environments started to get

shallow accompanied with gradual sea-level fall to the limit of outer neritic

realm.

7.4.3. The Late Paleocene Early Eocene Phase:

With the end of the Paleocene and the start of the Eocene times, the outer

neritic marine conditions prevailed earlier have continued during the

deposition of the earliest parts of Thebes Formation. The final stages of the

Early Eocene times witnessed gradual, but accelerated sea-level fall where

the upper parts of Thebes Formation were deposited within inner neritic

marine conditions.

7.4.4. The Late Eocene Phase:

In the study area, the Upper Eocene sediments are not evident. The absence

of such sediments could be either due to (a) non-deposition where the area is

tectonically situated adjacent to the eastern uplifts associated to the Red Sea

and Gulf of Suez Rifts, or (b) due to subsequent removal by riverine

processes during the Oligocene times.

7.4.5. The Oligocene Phase:

The Oligocene times were episodes of continental sedimentation by active

rivers. Thus, these time express marked sea-level drop associated with land

emergence and the activities of land erosion agencies.

7.4.6. The Early Miocene Phase:

The Early Miocene times witnessed a subtle transgression of shallow marine

sea levels, enough to deposit the clastic/reefal sediments of Sadat Formation.

REFERENCES

Abdallah, A.M. and Abd El Hady, F.M., (1966): Geology of Sadat area,

Gulf of Suez. J. Geol. U. A. R., 10(1): 1-24

Abdallah, A. M., Helal, S.A. & Abdel Aziz, S. M., (2003):Planktonic

foraminiferal biostratigraphy of the eastern Fayum depression, Egypt. -3rd

Intern., Conf. Geol. Africa, V. 1, p.571 - 598.

Abd-Elshafy, E., (1988): First record and stratigraphy of Upper Paleocene,

Basal Eocene sediments in the Northern Galala, Gulf of Suez, Egypt. -Bull.

Fac. Sci., Zagazig Univ., V. 10/1: pp79-100; Zagazig.

Abdel-Ghany., (1999):In El-Azabi, M. H. (2000); Sesimentary facies,

palaeoenvironments and facies development of the Miocene-Pliocene

sequences in the Sadat-Wadi Hagul stretch, northwest Gulf of Suez and

their time correlatives in the adjacent basins, Egypt, 5th

International

Conference on the Geology of the Arab World, Cairo University,

Feb.2000/ pp.1135-1174.

Abul-Nasr, R. A., (1990):Re-evaluation of the Upper Eocene rock units in

West Central Sinai, Egypt -M.E.R.C. Ain Shams Univ. Earth Sci., Ser., V.

4, p.234-247.

Abul-Nasr, R. A., (1992a):Paleoecology and sedimentary environments of

Middle-Upper Eocene rocks in west central Sinai, Egypt- M.E.R.C. Ain

Shams Univ. Earth Sci., Ser., V.6, pp.127-138.

Abul-Nasr, R. A., (1992a):Occurrence of the planktonic foraminifera

Orbulinoides beckmanni and Globigerinatheka semiinvoluta in west

central Sinai, Egypt- M.E.R.C. Ain Shams Univ. Earth Sci., Ser., V.6,

pp.167-168.

Abul-Nasr, R.A. & Thunnel, R.C., (1987): Eocene eustatic sea level changes

evidences from Western Sinai, Egypt. -Palaeoeco., 58: pp1-9.

Al-Ahwani, M. M., (1980):Geological and sedimentological studies of Gabal

Shabraweet area, Suez Canal District, Egypt. –An.Geol. Surv. Egypt., 12:

pp 305-381; Cairo.

Al Ahwani, M. M., (1982):Geological and sedimentological studies of Gebel

Shabraweet area, Suez Cana District, Egypt. - Egy. Ann. Geo. Surv., 12: pp

305-381.

Allam, A. & Khalil, H., (1988): Geology and stratigraphy of the Arif El-Naqa

area, Sinai, Egypt- Egypt. J. Geol., 32/1-2: pp 199-211.

Anan, H. S., (2001): Paleocene Vaginulininae (benthic foraminifera) of Duwi

section, Red sea coast, Egypt. Egypt. Jour. Paleon.,1: pp135-139.

Awad, G. H. & Ghobrial, M. G., (1965): Zonal stratigraphy of the Kharga

Oasis. -Geol. Survey, Egypt.Paper no. 34, 77p.

Ayaad, S. N & Hamama, H. H., (1989): Biostratigraphy of the Upper

Cretaceous/Lower Tertiary Succession in Gebel Mokattab, southwestern

Sinai. -2nd.

Proc. Conf. Geol. Sinai. Develop. pp. 49-58. Ismailila.

Azab, M. M., (1984): Biostratigraphy of the Middle Eocene in Upper Egypt. -

Unpublished Ph.D. Thesis, Ain Shams Univ., 230 p.; Cairo.

Barron. T., (1907a): The topography and geology of the Peninsula of Sinai

(western portion). Egypt Surv. Dept., 133 p.

Barron. T., (1907b): The topography and geology of the district between

Cairo and Suez. Egypt Surv. Dept.

Bartov, J., Eyal, Y. Garfunkel, Z., & Steinitz, G., (1972):Late Cretaceous

and Tertiary Stratigraphy and Paleogeography of SothernIsrael. -Israel

Journ. Earth Sci. V.21, pp.130-144.

Bartov, Y. & Steinitz, G., (1977): The Judea and Mount Scopus groups in the

Negev and Sinai with trend surface analysis of the thickness data- Israel J.

Earth Sci., 26: pp119-148; Jerusalem.

Beadnell, H. J. L., (1905): The relations of the Eocene and Cretaceous

systems in the Esna-Aswan Reach of the Nile Valley. - Quart. J. Geol. Soc.

London, 61: pp667- 678.

Beadnell, H. J. L., (1927):The wilderness of Sinai, Amold, London, 108p.

Boukhary, M. A., & Abdel Malik, M. W., (1983):Revision to the stratigraphy

of the Eocene deposits in Egypt: N. Jb. Geol. Palaeont. Mh. 6, pp. 321-337;

Stuttgart.

Bown, T. M., (1982): Ichnofossils and rhizoliths of the nearshore fluvial Gebel

trainni Formation (Oligocene), Fayum province, Egypt. Plaeogeog.,

Palaeoclim, Palaeoeco., v.40, pp.255-309.

Carver, R. E., (1971): Procedures in sedimentary petrology, Wiley-

Interscience, New York, 653p.

Cherif, O. H., (1966): Geology of the Sadat area, southwest of Suez.

Unpublished M. Sc. Thesis, Fac. Sci., Ain Shams Univ., Egypt.

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(2): pp185-203.

Dabous, M. & Awad, M., (1989): Petrography and lithofacies studies on the

Lower Tertiary sediments of Esna - Qena district. - M. E. R. C., Ain Shams

Univ., Earth Sc., Ser. 3: pp137-149; Cairo.

Darwish, M. and El-Azabi, M., (1993): Contributions to the Miocene

sequences along the western coast, Gulf of Suez, Egypt. Egypt. J. Geol.,

37(1): pp21-47.

Darwish, M. and El-Azabi, M., (1995):The Miocene lithostratigraphic

sequence of St. Paul Area, western coast, Gulf of Suez: A field description.

Egypt. J. Geol., 39(1): pp37-55.

Dunham, R. J., (1962): Classification of carbonate rocks according to

depositional texture. - Bull. AAPG, Mem. 1: pp108 - 121; Tulsa/

Oklahoma.

El-Azabi (2008): Sesimentary facies, palaeoenvironments and facies

development of the Miocene-Pliocene sequences in the Sadat-Wadi Hagul

stretch, northwest Gulf of Suez and their time correlatives in the adjacent

basins, Egypt, 5th

International Conference on the Geology of the Arab

World, Cairo University, Feb.2000/ pp.1135-1174.

El-Dawoody, S. A., (1984):Discoaster-biostratigraphy of the early Tertiary

succession in the Esna/Luxour region, Nile valley, Egypt. - 12th

Colloq.

Afr. Geol., pp 261-280.

El-Dawoody, S. A., (1994):Early Tertiary calcareous nannoplankton

biostratigraphy of North Africa and the Middle east. - 2nd

Conf. Arab.

World, pp 429-461; Cairo.

El-Dawoody, S. A., (2000):Calcareous nannoplankton biostratigraphy of some

Paleocene rocks in Egypt. - 5th

Int. Conf. Geol. Arab. Wor., pp1433-1454;

Cairo.

El-Dawoody, S. A. & EL-DAWY, M. H., (1998):Microbiostratigraphy of the

Maastrichtian-early Eocene sediments in the Dakhla-Kharga region,

Western Desert, Egypt. - El-Minia Sc. Bull, 11/1: pp87-118.

El-Fawal, F. M., Sadek, A. & Hassan, H. F., (2005): Sequence Architecture

and platform evolution of the Paleogene rocks in Sinai, Egypt, Germina, v.

1, pp.67-105.

El-Heiny, I., Enani, N. & Morsi, S., (1990): Stratigraphic evaluation of

Eocene rocks in west central Sinai, Egypt. - E.G.P.C., 10th., Explor. Conf.

Cairo, 22p.

El-Nady, H. I. A., (1995): Biostratigraphy of the Upper Cretaceous-Lower

Tertiary successions in Northern Sinai, Egypt. -Unpublished Ph.D. Thesis,

Geol. Depart., Fac. Sci., Mansoura Univ., 350 p.; Mansoura.

El-Naggar, Z. A.,(1966): Stratigraphy and planktonic foraminifera in the

Esna-Idfu Region Nile Valley, U.A.R.- Bull. Brit. Mus. Nat. Hist., Geol.

Suppl., 2: 291p.

El Safori, Y.A.M.E., (1994): Stratigraphy and paleontology of some Miocene

exposures in the western side of the Gulf of Suez, Egypt. Unpublished Ph.

D. Thesis, Fac. Sci., Ain Shams Univ., Egypt, 298p.

El-Sheikh, H. A. & el-Beshtawy, M. K., (1992):Biostratigraphic studies on

the Late Creatceous / Early Tertiary Between Wadi Tayiba and Wadi

Feiran, West Central Sinai, Egypt. -Geology of the Arab World, Cairo

Univ., pp395-406.

Embry, A. F., and Klovan, J. E., (1971):A Late Devonian reef tract on

northeastern Banks Island, N.W.T.: Bul. Canadian Petroleum Geol., 19:

pp730-781.

Eweda, Sh. And Zalat, A., (1996): Stratigraphy and facies development of the

Miocene sequence of east Sudr area, Gulf of Suez, Egypt. Third Int. Conf.

Geology of the Arab World, Cairo Univ., Egypt, pp. 433-454.

Ezzat., (2000):In El-Azabi, M. H. (2000); Sesimentary facies,

palaeoenvironments and facies development of the Miocene-Pliocene

sequences in the Sadat-Wadi Hagul stretch, northwest Gulf of Suez and

their time correlatives in the adjacent basins, Egypt, 5th

International

Conference on the Geology of the Arab World, Cairo University,

Feb.2000/ pp.1135-1174.

Flügel, E., (1982):Microfacies Analysis of Limestones. Springer-Verlag,

Berlin, 633 p.

Folk, R. L.,(1959): Practical petrographic classification of limestone- Bull.

AAPG., Mem., 43: pp1-38.

Folk, R. L.,(1962): Spectral subdivision of limestone types. In: HAMED, W.E.

(ed.): Classification of carbonate rocks. - Bull. AAPG., Mem. No. 1: pp

62-84.

Folk, R. L., (1968):Petrology of Sedimentary Rocks. –Hemphill's, Publ. Co.,

170p.

Folk, R. L., (1980):Petrology of Sedimentary Rocks. –Hemphill, Publ. Co.,

184 p.

Folk, R. L. and Ward, W. C., (1957): Brazos River bar: a study in the

significance of grain size parameters. J. Sed. Petrol., 1: pp 3-26.

Folk, R. L., Andrews, P. B. and Lewis, D. W., (1970): Detrital sedimentary

rock classification and nomenclature for use in New Zealand. New Zealand

Jour. Geol. And Geophys. 13: pp 937-968.

Fourtau, R., (1894): Etude geologique sur le Gebel Ahmer.Bull. Inst.d’Egypte

(ser.iii), no.5, fasc.4, pp.377-386.

Füchtbaur, H. and Müller, G., (1970):Sedimente und sedimentgesteine.

Stuttgart, Schweizerbarth Verlag, 726 p.

Galal, A. & El-Halaby, O. M., (2001): Taxonomy and foraminiferal

biostratigraphy of the Mina Formation in wadi Qena and Wadi El-

Agraamiya, North eastern Desert, Egypt. Ann. Geol. Surv, XXIV: pp353-

376.

Ginsburg, R.N., (1972): South Florida carbonate sediments, Sediment ii,

Miami Univ., 72p.

Hamza, F., Ziko, A., & Kamel, S., (1997): Biostratigraphical analysis of the

Lower Paleogene succession in the north central Sinai. - N. Jb. Geol.

Paläont Abh., 204, V.3, pp.321-325.

Haggag, M. A., (1979): Biostratigraphy of the West-Central part of the

Western Desert Egypt. -Unpublished Ph.D. Thesis, Fac. of Sci., Ain Shams

Univ.; Cairo.

Hardie, L.A., (1987): Dolomitization, a critical view of some current views.

Jour. Sed. Petrology, 57(1), pp 166-183.

Harms, J. C., Southard, J. B., Spearig, D. R. and Walker, R. G.,

(1975):Depositional environment as interpreted from primary sedimentary

structures and classification sequences. Soc. Econ. Paleo. Min. short course

2: 161 p.

Harms, J.; Southard, J.; Spearing, D. and walker, R. (1982): Structures and

sequences in clastic rocks. Lect. Notes, short course-9, SEPM, Calgary.

Hassan, H. F., (2005): Paleogene sea level fluctuations across Sinai: A

sequence stratigraphic approach, unpublished Ph. D Thesis, Fac. Sci., Suez

Canal Univ., 425 p.; Ismailia.

Hassan, M. M., El Badry, O. A., Mohammad, M. H., Atawiya, M. Y. &

Zalat, A. A., (1984): Petrographical and geochemical studies on the

Tertiary rock units of the area east of Maadi, Egypt. -M.E.R.C., Ain Shams

Univ., Earth Sci. Res. Ser., 4: 207-238; Cairo.

Hassan, M. M., Hassanein, A. M., Mohammed, M. H. & Abdel Moneim, S.

A., (1990): Lithostratigraphical and microfacies studies of the Mokattam

and Maadi Formations, Gebel Mokattam area, Egypt. - Annals of

Geological Survey of Egypt, 6: 229 -233; Cairo.

Hassanein, A. M., Hassaan, M.M. & Mohamed, M. H., (1983):

Contributions to the lithostratigraphy of the Thebes Formation, Eastern

Desert, Egypt. -Scientific Engineering Bull., Fac. of Engineering, Cairo

Univ., 4: 209-233; Cairo.

Haq, B. U. & VAN EYSINGA, F.W.B. (1998):Geologic time table. - 5th

edition, El Sevier Pub.

Hermina, M, Klitsch, E. & Franz, K. (1989): Stratigraphic Lexicon and

Explanatory Notes to the Geological Map of Egypt 1:500000, Conoco Inc.,

Cairo, 250 p., 10 figs.

Hewaidy, A. A. & Strougo, A., (2001): Maastrichtian-lower Eocene benthic

foraminiferal distribution and paleoecology of three outcrop section in

farafra, Egypt. Jour. Paleon., 1: 1-22, 10 figs, 2 pls: Cairo.

Hume, W. F., (1911): The effects of secular oscillation in Egypt during the

Cretaceous and Eocene Periods. - Quart. J. Geol. Soc. 67 /1: 118-148;

London.

Ismail, A. S., (1996): Foraminiferal biostratigraphy, Paleoecology and

Paleogeography of some Lower Paleogene sediments in east central Sinai,

Egypt. - Bull. Fac., Sci., Zagazig Univ., V.18 (1), Geol., p. 15-40.

Ismail, A. & Ied, I. M., (2005):Maastrichtian – Lower Eocene Ostracods from

Safaga area, Eastern Desert, Egypt. – Egypt. Jour. Paleont. V.5, p. 119-

159.

Issawi, B., El Hinnawi, M., Francis, M. and Mazhar, A. (1999):The

Phanerozoic geology of Egypt (A Geodynamic Approach). Egypt. Geol.

Surv., 76: 462 p.

Kolkila A. A., Mohammed H. M., & Mohammad, M. H. (1984):

Microfacies and depositional environment of the Middle Eocene sequence

in the area to the west of Helwan, Egypt. - Ann. Geol. Surv. of Egypt, 14:

257-268; Cairo.

Lees, A., (1975): Possible influences of salinity and temperature on modern

shelf carbonate sedimentation. Mar. Geol., 13: M67-M73.

Lees, A. and Buller, A. T., (1972): Modern temperate water and warm water

shelf carbonate sediments contrasted. Mar. Geol., 13: M67-M73.

Mattar, Y. E., (1998): Biostratigraphy of some Paleogene sediments in the

Raha Plateau, west central Sinai, Egypt. - unpubl. M. Sc. Thesis, Zagazig

Univ., Fac. Sci., Dept. Geology, 228p., 13 figs., 16, pls.

Mattar, Y. E., (2008): Stratigraphy and Micropaleontology of some Eocene

rocks, in west central Sinai-Egypt, unpubl. Ph. D Thesis, Suez Canal

Univ., Fac. Sci., Dept. Geology.

Mohammed, M.H., (1984):Contriobution to the facies and depositional

environment of the Thebes Formation in Gebel El Shaghab, Nile Valley,

Egypt. Bull. Fac., Sci., Zagazig Univ.: 268-286; Zagazig.

Nakkady, S. E., (1949): The foraminiferal fauna of the Esna Shales of Egypt. -

Bull. Inst. Desert Egypt, 31: 209-247; Cairo.

Nakkady, S. E.,(1950): A new foraminiferal fauna from the Esna Shales and

Upper Cretaceous Chalk of Egypt. - J. Paleontology, 24/6: 675-692.

Nassif, M. S., (1997): Stratigraphy and sedimentology of the Eocene in

Southwset Sinai, Egypt. - Unpublished Ph.D. Thesis, Suez Canal Univ.,

169p.

Nassif, M. S., Abou EL-Enein, M. k., El-Heiny, I. A. and El-Ghawaby, M.

A., (1992):Stratigraphy of the Miocene rocks at Wadi Feiran, Southeast

Sinai, Proc. 3rd.

Conf Geol Sinai Develop., Ismailia, 161-174.

Obaidalla, N. A., (1999):Planktonic foraminiferal Biostratigraphy of the

Paleocene/Eocene boundary transition in Southwestern Sinai, Egypt. -1st

Intern. Conf. Geol. Africa, V. 1, p.55-64, Assiut, Egypt.

Omran, M. A., (1989):Geological studies in Shabraweet Area, Suez Canal,

Egypt. - Unpublished M.Sc. Thesis, 129p, Suez Canal University; Ismailia.

Omran, M. A. A., (1997): Stratigraphical studies of the Upper Cretaceous-

Lower Tertiary successions in some localities, Northern Sinai, Egypt-

Unpublished Ph.D. Thesis, Geol. Depart. Fac. Sci., Suez Canal Univ., 330

p.; Ismailia, Egypt.

Plumley, W. J., RISLEY, G. A., GRAVES, JR. R. W. & KALEY, M. E.

(1962):Energy index for limestone interpretation and classification, In:

HAM, W. E. (ed.): Classification of carbonate rocks. - Bull. AAPG.,

Mem.1: 85- 107; Sharon/Mass.

Sadek, H., (1926): The geography and geology of the district between Gebel

Ataqa and El Galala El Bahariya (Gulf of Suez). Geol. Surv. Min. Res.

Dept., Cairo, Paper No. 40, 120p.

Said, R., (1960): Planktonic foraminifera from the Thebes Formation, Luxor,

Egypt. - Micropaleontology, 6/3: 277-286; New York.

Said, R., (1962):The Geology of Egypt. - 377p., El Sevier, Amsterdam, New

York.

Said, R., (1971):Explanatory notes to accompany the geological map of Egypt.

- Geol. Survey of Egypt., 56: 1-23; Cairo.

Said, R., (1990): The Geology of Egypt. - 734 p., Balkema, Rotterdam, Berlin.

Said, R. & KENAWY, A., (1956):Upper Cretaceous and Lower Tertiary

Foraminifera from Northern Sinai, Egypt. - Micropaleontology, 2/2: 105-

173, 6 text-figs., pls. 1-7; New York.

Selima, A. M. A., (1989):Some stratigraphical studies on subsurface Eocene

sections in the western reach of the Nile Valley between Beni Suef and

Cairo. - Unpublished Ph. D. Thesis, Fac. of Sci., Ain Shams Univ., 326 p.;

Cairo.

Shahin, A. M., (1992):Contribution to the foraminiferal biostratigraphy and

paleobathymetry of the Late Cretaceous and Early Tertiary in West-Central

Sinai, Egypt. -Rev. Micropaleont., 35/2: 157-175; Paris.

Shahin, A. M., (2005):Maastrichtian to Middle Eocene ostracods from Sinai,

Egypt: systematics, biostratigraphy and paleobiogeography. - Revue de

Paléobiologie, Genéve, 24 (2), p. 749-779.

Sheppard, C.; Price, A. and Roberts, C., (1992): Marine ecology of the

Arabian region: patterns and processes in extreme tropical environments.

Academic Press, London, 359p.

Shukri, N. M., (1954): On cylindrical structures and coloration of Gebel Ahmar

near Cairo, Egypt. Bull. Fac. Sc., Cairo Univ., v.32, p.1-23.

Smith (1974):Sedimentology and bar formation in the upper kiking Horse River, a

braided outwash stream. J. Geol., Vol. 82, pp 205-224.

Snavely, P.D., Garrison, R. E. & Meguid, A. A., (1979): Stratigraphy and

regional depositional history of the Thebes Formation (Lower Eocene),

Egypt - Ann. Geol. Surv. Egypt, 9: 344-362; Cairo.

Souaya, F., (1961): Contribution to the study of Miogypsina s.l. from Egypt.

Proc. Konikl. Ned. Akad. Wetenshap., 64(B): 665-705.

Souaya, F., (1963):On the foraminifera of Gebel Ghara (Cairo-Suez road) and

some other Miocene samples. J. Paleontology, 37: 433-457.

Speijer, R. P. & Samir, A. M., (1994):Globanomalina luxuroensis, a pelagic

marker for the Paleocene/Eocene boundary. In: Extinction and recovery

patterns in benthic foraminiferal Paleo-communities across the

Cretaceous/Paleogene and Paleocene/Eocene boundaries. - Geol.Ultra.

Univ. Utrecht, 124: 65-75; Netherland.

Speijer, R. P., & van der Zwaan, G. J., (1994): The differential effect of the

Paleocene- Eocene boundary event: Extinction and survivorship in shallow

to deep- water Egyptian benthic foraminiferal assemblages: Geologica v.

124, p. 121– 168.

Speijer, R.P., & Morsi, A. M. (2002):Ostracode turnover and sea-level

changes associated with the Paleocene-Eocene thermal maximum. -

Geology, 30: 23–26.

Speijer, R.P., Schmitz, B., & Luger, P., (2000): Stratigraphy of late

Paleocene events in the Middle East: Implications for low- to middle-

latitude successions and correlations: Journal of the Geological Society of

London, 157: 37–47.

Strougo, A. & Boukhary, M., (1987): The Middle Eocene - Upper Eocene

boundary in Egypt: present state of the problem - Rev. Micropaleontologie,

30/2: 122-127; Paris.

Strougo, A. & Hottinger, L., (1987): Biostratigraphic significance of some

large foraminifera from Lower and Upper Eocene rocks of Egypt. -

M.E.R.C., Ain Shams Univ., Earth Sci., Ser., 1: 35-47; Cairo.

Strougo, A., Bignot, G. & Abd - Allah, A., (1992): Biostratigraphy and

paleoenvironments of Middle Eocene benthic foraminiferal assemblages of

northcentral Eastern Desert, Egypt. - M.E.R.C., Ain Shams Univ., Earth

Sci. Ser., 6: 1-12; Cairo.

Strougo, A., Haggag, M. A., Faris, M. & Azab, M., (1983):Eocene

Stratigraphy of the Beni Suef Area. - Bull. Fac. Sci., Ain Shams Univ., 24:

177-192; Cairo.

Visher, G. S., (1966):Grain size distribution and depositional processes. Sed.

Pet., 39, (3): 1074-1106.

Viotti, C. & El-Demerdash, G., (1969):Studies on the Eocene sediments of

Wadi Nukhul area, east coast Gulf of Suez, Proc. 3rd.

Africa. Micropaleont.

Colloq., Cairo 1968, p. 403-423.

Wilson, J. L., (1975):Carbonate Facies in Geologic history. Springer-Verlag,

New York, Heidelberg, Berlin, 471 p.

Youssef, H. F., (1998): Stratigraphic study of the upper Cretaceous- Lower

Tertiary in El-Hasana area, North Sinai, Egypt. - Unpublished M. Sc.

Thesis, Geol. Depart. Fac. Sci., Suez Canal Univ., 183 p.; Ismalia.

Youssef, M. and Abdel-Aziz, W., (1971):Biostratigraphy of the Upper

Cretaceous-Lower Tertiary in Farafra Oasis, Lib. Desert, Egypt. -Sympo.

Geol. of Libya, Fac. Sc. Libya Univ., 2: 227-249.

Ziko, A., Darwish, M. and Eweda, S., (1993):Late Cretaceous–early Tertiary

stratigraphy of the Themed area, east central Sinai, Egypt. Neues Jahrbuch

für Geologie und Palaontologie, Monatshefte, 135-149.

Zittel, K. A., (1883):Beitrage zur geologie und paleontologie der libyschen

Wuste und angrenzenden Gebiete von Agypten. Palaont., 30: 147 p.