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Journal of African Earth Sciences. Vol. 25, No. 3, pp. 435-451, 1997 o 1997 Elsevisr Science Ltd

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Planktonic foraminiferal biostratigraphy of the Miocene sequence in the area between

Wadi El-Tayiba and Wadi Sidri, west central Sinai, Egypt

G. PHILLIP,’ M. M. IMAM’ and G. I. ABDEL GAWAD2 ‘Geology Department, Faculty of Science, Cairo University, Egypt

2Cairo University (Beni Suef Branch), Egypt

Abstract-The present work deals with the study of lithostratigraphy and the planktonic foraminiferal biostratigraphy of the Early-Middle Miocene sequence in six measured stratigraphical surface sections in west central Sinai. They are namely, from north to south: Wadi El-Tayiba, Gabal Sarbut El-Gamal, Wadi Nukhul, Wadi Baba, Gabal Abu Alaqa and Wadi Sidri. The Miocene sequence, exposed in the study area, is represented lithostratigraphically by four rock units, arranged from base to top as follows: the Nukhul and Rudeis Formations (Early Miocene), the Sarbut El-Gamal Formation and the Hammam Faraun Member of the Belayim Formation (Middle Miocene). The planktonic foraminiferal biostratigraphical studies led to the recognition of 51 planktonic foraminiferal species. They are illustrated with the scanning electron microscope. Five planktonic foraminiferal biozones and one large benthonic foraminiferal zone have been recognised. They are arranged from top to bottom as follows: Orbulina suturalis/Globorotalia siakensis Zone (Middle Miocene); Borelis

me/o .Zone (larger foraminiferal zone) (Middle Miocene); Globigerinoides sicanus Zone (Early Miocene); Globigerinoides trilobus Zone (Early Miocene); Globigerinoides

altiap(erturus-Catapsydrax dissimilis Zone (Early Miocene): Globigerinoides primordius

Zone (Early Miocene). CorreIlation of these biozones with others from Egypt and the world is also attempted. o 1997 Elsevier Science Limited.

Resume-Cette etude concerne la lithostratigraphie et la biostratigraphie des foramliniferes planctoniques de la sequence miocene inferieur et moyen dans six coupes stratigraphiques mesurees de surface du Sinai’ centro-occidental. Ce sont, du nord au sud, les coupes de Wadi El Tayiba, Gabal Sarbut El-Gamal, Wadi Nukhul, Wadi Baba, Gabal Abu Alaqa et Wadi Sidri. La sequence miocene a I’affleurement comprend quatre unites lithostratigraphiques qui sont, de la base au sommet, les formations de Nukhul et Rudeis (Miocene inferieur), la formation de Sarbut El Gamal et le rnembre de Hammam Faraun de la formation de Belayim (Miocene moyen). Les etudes biostratigraphiques ont permis la reconnaissance de 51 especes de foraminiferes planctoniques, illustrees sur des cliches au microscope electronique a balayage. Cinq biozones de foraminiferes planctoniques et une grande zone de foraminiferes benthoniques ont bte determinees. Elles se placent du sommet a la base comme suit: Zone a Orbulina suturalis/Globorotal siakensis (Miocene moyen); Zone B Borelis melo (Miocene moyen); Zone a Globigerinoides sicanus (Miocene inferieur); Zone a Globigerinoides trilobus (Miocene inferieur); Zone a Globigerinoides altiaperturus-Catapsydrax dissimilis (Miocene inferieur); Zone a Globigerinoides

primordius (Miocene inferieur). La correlation de ces biozones avec celles d’Egypte et d’ailleurs dans le monde est tent&:. @ 1997 Elsevier Science Limited.

(Received 1 1 April 1996: revised version received 5 March 1997)

Journal of African Earth Sciences 435

G. PHILLIP et al.

INTRODUCTION During the last decades, many workers have discussed the Miocene planktonic foraminiferal zonations in the Gulf of Suez region and elsewhere in the Sinai Peninsula (e.g. Macfayden, 1931; Stainforth, 1949; Sadek, 1959; Said and Bassiouni, 1958; Stainforth, 1960; Souaya, 1965, 1966; Said and El-Heiny, 1967; Beckmann et al., 1969; Kerdany, 1968; Wasfi, 1968; El-Heiny and Martini, 1981; Imam, 1986, 1991; El Sayed et al., 1988; Rateb, 1988; Haggag et al., 1990; Cherif eta/., 1993). It is woth noting that all these works have not arrived at a definite planktonic foraminiferal zonal scheme which can be applied to the whole Gulf of Suez area. This may be attributed to the complicated tectonic setting of the Gulf of Suez Rift Basin.

The main purpose of the present work is to shed light on the essential Miocene lithostratigraphical units encountered in the study area and the details of the planktonic foraminiferal biozones recognised in this Miocene sequence, as well as correlating these biozones with others described in and outside Egypt.

The present work is based primarily on the study of 560 samples collected from six stratigraphical surface sections in west central Sinai, Egypt (Fig. 1). These sections are carefully measured, described and matched in the area under consideration (Fig. 2). They are arranged from north to south as follows:

i) the Wadi El Tayiba surface section (WT); ii) the Gabal Sarbut El-Gamal surface section

(GS); iii) the Wadi Nukhul surface section (WN); iv) the Wadi Baba surface section (WB); v) the Gabal Abu Alaqa surface section (GQ);

and vi) the Wadi Sidri surface section (WS).

LITHOSTRATIGRAPHY The lithostratigraphy of the Miocene sediments in the Gulf of Suez in general and west central Sinai in particular have been classified and discussed by many workers (Moon and Sadek, 1923, 1925; Sadek, 1959; Ghorab and Gezeery, 1969; National Committee for Geological

SINAI

i i i .y.

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Figure 7. Location map showing the studied sections. 1: W. Tayiba section; 2: G. Sarbut El-Gamalsection; 3: W. Mukhulsection; 4: W. Baba section: 5: G. Abu Alaqa section; 6: W. Sidri section.

436 Journal of African Earth Sciences

Planktonic foraminiferal biostratigraphy of the Miocene sequence in west central Sinai

Science (NCGS), 1976; Garfunkel and Bartov, 1977; Hamza, ‘1988; Imam, 1991). The most commonly used classification is that of the NCGS (19761, which will be adopted in this study (Table 1). Accordingly, two main facies types are recognised: open marine facies, represented in this work by the Nukhul, Rudeis and Belayim (Hammam Faraun Member) Formations, and non- marine to coastal facies, represented here by the Sarbut El-Gamal Formation. The Miocene succession in the area of investigation is represented by four lithostratigraphical units linking these types of f’acies. They are stratigraphically arranged from base to top as follows:

Hammam Faraun Member of Belayium Fm. (open shallow marine facies) (Serravallian) Base of Hammam Faraun unconformity (Middle Miocene) Sarbut El-Gamall Fm. (coastal to non-marine facies) (Langhian) Mid-Clysmic unconformity Rudeis Fm. (open marine facies) (Burdigalian) _----_-.-----_---_-_EEarly Miocene

Nukhul Fm. (shalllow marine facies) (Aquitanian) Early-Clysmic unconformity Tayiba Red Beds (Late Eocene to Oligocene).

Nukhul Formatio’n (Aquitanian, Early Miocene) The Nukhul Formlation is the oldest Miocene rock unit exposed in the study area and represents the first shallow marine transgressive deposits in the Gulf of Suez. It was first described by Waite and Pooely (I 953) and later adopted by the NCGS (1976). In the studied sections, this formation is represented mainly by basal polymictic conglomerates with oyster and pectinid shell fragments, cross-bedded, pebbly sandstone, sandy shale, oyster banks and shales with subordinate phosphatic sandy limestone interbeds dominated by shallow marine benthonic foraminifers(Bolivina dilalarata, Cibicides ellisi, Chilostomella ovoidea, Elphidium sp., Nonion boueanum, Siphonina reticulata and Nummulites fragments). This sequence unconformably overlies the Tayiba Red Beds (Late Eocene to Oligocene) and conformably underlies the Rudeis Form.ation. The Nukhul Formation is well developed in the studied sections, with a thickness of about 25 m in Wadi El Tayiba, 50 m in Gabal Sarbut Eil-Gamal, 70 m in Wadi Nukhul, 50 m in Wadi Baba, and 20 m in Gabal Abu Alaqa.

Rudeis Formation (Burdigalian, Early Miocene) The Rudeis Formation was first described at its type section (Rudeis well no. 20) and later

established by the NCGS (I 9761. In the studied sections, the Rudeis Formation conformably overlies the Nukhul Formation and unconformably underlies the Middle Miocene Sarbut El-Gamal Formation (Mid-Clysmic unconformity; Garfunkel and Bartov, 1977). The Rudeis Formation consists of yellow, hard, fossiliferous, argillaceous limestone beds with thin laminae of white calcareous mudstone. These beds are interbedded with cherty to sandy limestone beds highly fossiliferous with planktonic foraminifers, suggesting that a deep open marine environment prevailed during the deposition of the Rudeis Formation. It attains different thicknesses of, 100 m in Gabal Sarbut El Gamal, 150 m in Wadi Baba and 60 m in Gabal Abu Alaqa and becomes reduced in thickness toward south to be 50 m in Wadi Sidri.

Sarbut El-Gamal Formation (Langhian, Middle Miocene) The Sarbut El-Gamal Formation rock unit was first described by Heybroek (1949) in its type section (Gabal Sarbut El Gamal) and later established by Ghorab and Marzouk (1967). In the area under consideration, it unconformably overlies the Rudeis Formation and unconformably underlies the Belayim Formation (Hammam Faraun Member) with the unconformable surface termed the “Base of Hammam Faraun unconformity” (Garfunkel and Bartov, 1977). The Sarbut El-Gamal Formation is represented by an undifferentiated coarse elastic sequence of polymictic conglomerates composed of chert, limestone and reefal algal limestone clasts embedded in a sandy calcareous matrix , highly fossiliferous with in situ large benthonic foraminifers e.g. Borelis melo, Heterostegina spp. and Operculina spp. This coarse elastic sequence is interbedded with cherty, algal, reefal limestone, especially at the base of the nominated rock unit. In the present study, the Middle Miocene Sarbut El-Gamal Formation will be used to cover the stratigraphical interval between the mid-Clysmic event to the base of the Hammam Faraun event and is Langhian in age. The Sarbut El-Gamal Formation is well- developed in Gabal Sarbut El-Gamal (150 ml, Wadi Baba (40 m) and Gabal Abu Alaqa (100 m).

Hammam Faraun Member of the Belayim Formation (Serravallian, Middle Miocene) The Hammam Faraun Member was originally described by Moon and Sadek (I 923) in its type section in Gabal Hammam Faraun and later on was established by the NCGS (1976). In the


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present study, it unconformably overlies the Sarbut El-Gamal Formation and caps the topmost part of the studied sections, e.g. in Gabal Sarbut El-Gamal, Wadi Baba, Gabal Abu Alaqa and Wadi Sidri. It is composed of yellowish-white, porous, occasionally dolomitic, algal, reefal limestone beds highly fossiliferous with coralline red algae (Lithophyllum sp., Mesophyllum sp. and Lithoporella sp.),, corals, oysters and pectinid shell fragments, reflecting shallow marine warm water environments. These beds are interbedded with cherty limestone and argillaceous limestone beds with highly abundant planktonic foraminifers. This rock unit attains different thicknesses of about 50 m in Gabal Sarbut El- Gamal, 30 m in Wadi Baba, 40 m in Gabal Abu Alaqa and 20 m in Wadi Sidri, with a general southerly reduction (Fig. 2).

PLANKTONIC FORAMINIFERAL BIOSTRATIGRAPHY

The Miocene planktonic foraminiferal zonation used in this study was first established by Blow (I 969), Bizon and Bizon (I 972), and Cita (1975, 1976) and later on modified by laccarino and Salvatorini (1982), Kennett and Srinnivasan (1983) and laccarino (1985). This zonation has been widely used as an accepted biostratigraphical standard for warm water areas of the world, including the Mediterranean region. The zonal boundaries are established here on the basis of the first and last occurrence of the index taxa. The Oligocene-Early Miocene boundary is defined by the first appearance of Globigerinoides spp., especially Globigerinoides primordius Blow and Banner, whereas the Early- Middle Miocene contact is defined by the first evolutionary appearance of Praeorbulina glomerosa (Blow)(laccarino, op. cit.).

The study of the planktonic forminiferal assemblages obtained from six studied stratigraphical surface sections in west-central Sinai, resulted in the subdivision of the Miocene sequence into five planktonic foraminiferal zones and one large benthonic foraminiferal zone. These biozones are correlated with their equivalent biozones in the world and with special emphasis on the Mediterranean region (Tables 2 and 3). The stratigraphical distribution of these planktonic foraminiferal species are presented in Fig. 3. In addition, scanning electron micrographs of the identified taxa are illustrated in Figs 4-6. The following is a brief description of the identified biozones from base to top.

Globigerinoides primordius Zone Category: Interval zone; Age: Early Miocene (Aquitanian); Author: This zone was first named by Blow (I 969) as the Globigerinoides primordius/Goborota/ia kugleri Zone and later on, it was named the Globigerinoides primordius Zone in the Mediterranean region (Cati et a/., 1968; Bizon and Bizon, 1972); Definition: This zone is defined as the interval from the first appearance of Globigerinoides primordius Blow and Banner to the first evolutionary appearance of Globigerinoides altiaperturus Bolli.

Planktonic foraminiferal assemblage Globigerinoides primordius Blow and Banner - Globigerinoides trilobus (Reuss) - Globigerinoides immaturus Le Roy - Globigerinoides subquadratus Bronnimann - Globigerina ciperoensis ciperoensis Bolli - Globigerina ciperoensis angustiumbilicata Bolli - Globigerina ciperoensis anglusuturalis Bolli - Globigerina praebulloides Blow - Globigerina eamesi Blow - Globigerina woodi Jenkins - Globigerina juvenilis - Globorotalia mayeri Cushman and Ellisor - Globorotalia obesa (Bolli) - Cassigerinella chipolensis (Cushman and Ponton) - Catapsydrax dissimilis (Cushman and Bermudez) - Catapsydrax stainforthi Bolli, Loeblich and Tappan.

Remarks Many authors accepted that the first evolutionary appearance of the genus Globigerinoides marked the Oligocene-Miocene boundary (Banner and Blow, 1965; Blow, 1969; Bolli and Premoli Silva, 1973; Cita and Blow, 1969). On the other hand, some workers showed that Globigerinoides primordius Blow and Banner makes its first appearance earlier than the Miocene Datum (Jenkins, 1971; Lamb and Stainforth, 1976; Stainforth and Lamb, 1981). Therefore some investigators consider that the first evolutionary appearance of Globoquadrina dehiscens (Chapman, Parr and Collins) in the temperate regions distinguishes the Miocene Datum (laccarino and Salvatorini, 1982; laccarino, 1985).

In the present study, the Globoquadrina dehiscens (Chapman, Parr and Collins) is recorded in higher stratigraphical levels that definitely belong to the overlying Globigerinoides altiaperturus/Ca tapsydrax dissimilis Zone. This could be attributed to unfavourable ecological conditions. This phenomenon has also been noticed by Haggag et a/. (I 990) in the Gulf of Suez region.


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Occurrence This zone is recorded in Gabal Sarbut El Gamal, Wadi Baba and Gabal Abu Alaqa, where it conformably underlies the next zone (Globigerinoides altiaperturus/Catapsydrax dissimilisl and unconformably overlies the Eocene-Oligocene deposits.

Globigerinoides altiaperturus/Ca taps ydrax dissimilis 2 one Category: concurrent range zone; Age: Early Miocene (Burdigalian); Author: Bizon and Bizon (1972); Definition: This zone is defined as the interval from the first evolutionlary appearance of Globigerinoides altiaperturus Bolli to the last occurrence of Catapsydrax diss.imilis (Cushman and Bermudez).

Planktonic foraminiferal assemblage Globigerinoides altiaperturus Bolli - Globigerinoides trilobus (Reuss) - Globigerinoides immaturus Le Roy - Globigerinoides subquadratus Bronnimann - Globigerinoides diminutus Bolli - Globigerinoides sacculifer ( Brady) - Globigerina eamesi Blow - Globigerina praebulloides Blow - Globigerina ciperoensis ciperoensis Bolli - Globigerina falconensis Blow - GLobigerina woodi Jenkins - Globorotalia obesa Bolli - Globorotalia con tinuosa Jenkins - Globorotalia siakensis Le Roy - Globoquadrina dehiscens dehiscens - Globoquadrina #dehiscens praedehiscens Blow and Banner - Globoquadrina altispira altispira (Cushman and .Jarvis) - Catapsydrax dissimilis (Cushman and Bermudez) - Cassigerinella chipolensis (Cushman and Ponton).

Remarks This zone occupies the lowermost part of the Rudeis Formation. The most characteristic feature in this zone is that Globigerinoides spp. becomes more common in diversity and number of individuals. It is worth noting that the tropical forms of Globigerinatella insueta Cushman and Stainforth and Globorotalia kugleri Bolli are entirely absent in the studied sections and this could be attributed to unfavourable ecological factors. Moreovler, the Globoquadrina dehiscens dehiscens (Chapman, Parr and Collins) makes its first appearance in this zone, denoting that it is recorded in a higher stratigraphical level than that recorded by laccarino (I 985).

Occurrence This zone has been recorded conformably overlying the Globigerinoides primordius Zone

and also conformably underlying the Globigerinoides trilobus Zone in Gabal Sarbut El- Gamal, Wadi Baba and Gabal Abu Alaqa.

Giobigerinoides trilobus Zone Category: Interval zone; Age: Early Miocene (Burdigalian); Author: Bizon and Bizon (1972); Definition: In the studied material, this zone is emended to occupy the interval from extinction of Catapsydrax dissimilis (Cushman and Bermudez) to the first evolutionary appearance of Globigerinoides sicanus De Stefani.

Planktonic foraminiferal assemblage Globigerinoides trilobus (Reuss) - Globigerinoides immaturus Le Roy - Globigerinoides sacculifer Brady - Globigerinoides quadrilobatus (d’orbigny) - Globigerinoides subquadratus Bronnimann - Globigerinoides diminutus Bolli - Globigerinoides cf. quadrilobatus (d’orbigny) - Globigerina praebulloides Blow - Globigerina ciperoensis ciperoensis Bolli - Globigerina falconensis Blow - Globigerina woodi Jenkins - Globigerina juvenilis Jenkins - Globoquadrina dehiscens dehiscens (Chapman, Parr and Collins) - Globoquadrina altispira altispira (Cushman and Jarvis) - Globoro talia obesa (Bolli) - Globoro talia praescitula (Brady) - Globorotalia cf. peripheroronda Blow and Banner - Globorotalia siakensis Le Roy - Globigerinella siphonifera (Blow 1 - Cassigerinella chipolensis (Cushman and Ponton).

Remarks This zone was described before in Egypt by many authors. Kerdany (1968) mentioned that this zone represents the lower part of the Rudeis Formation in the Gulf of Suez. El-Heiny and Martini (I 981) also recorded this zone in the Gulf of Suez region and suggested a deep open marine facies, which corresponds to the Rudeis Formation. Haggag et al. (I 990) also recorded this zone in the same region and mentioned that it has different stratigraphical levels. In the present work, this zone encompassed the middle part of the Rudeis Formation and is equivalent to the standard planktonic foraminiferal zone N7 of Blow (I 969).

Occurrence This zone has been recorded conformably overlying the Globigerinoides altiaperturusl Catapsydrax dissimilis Zone in Gabal Sarbut El- Gamal, Gabal Abu Alaqa and Wadi Sidri, and unconformably underlying the large benthonic

Figure 2. Lithostratigraphical correlation chart of the different studied sections.


1 MIOCENE I EPOCH

1 Early Miocene ! Middle Miocene AGE

Aquitani Burdigalian Langhian to Serravallian oditer-Europeanian slag{

Biozones in the present

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zone (Bore/is me/o). However, in Wadi Baba, it unconformably underlies the Globigerinoides sicanus Zone.

Globigerinoides sicanus 2 one Category: Lineage zone; Age: Early Miocene (Late Burdigalian); Author: Bizon and Bizon (1972); Definition: In the present study the lower boundary of this zone is defined by the first evolutionary appearance of Globigerinoides sicanus De Stefani and its top is truncated by the Mid-Clysmic unconformity.

Planktonic foraminiferal assemblage There is no great difference between the planktonic forarniniferal assemblage of this zone and the underlying Globigerinoides trilobus Zone except for the common occurrence of Globigerinoides sicanus De Stefani with rare occurrences of Globoquadrina spp. and Globorotalia spp.

Remarks This zone is well-developed only in the Wadi Baba surface :section and encompasses the uppermost part of the Rudeis Formation. It is worth mentioning that the Baba section represents a nearly complete depositional sequence during the Early Miocene (Burdigalian) (Fig. 2). Moreover, the unconformity occurring at the top of the Globigerinoides sicanus Zone (top of the Rudeis Formation) is most probably due to a major tectonic event (Mid-Clysmic event) which was initiated at the beginning of the Middle Miocene and was responsible for the uplifting of Sinai (Garfunkel and Bartov, 19771, causing at the same time the absence of the Praeorbulina glomerosa Zone.

Occurrence This zone is recorded only in the Wadi Baba surface section, where it conformably overlies the Globigerinoides trilobus Zone and unconformably underlies the Middle Miocene Borelis melo Zone.

Bore/is melo Zone Category: Interval zone; Age: Middle Miocene (Langhian); Author: Fichtel and Moll (I 960); Definition: Interval of the total range of Borelis melo Fichtel and Molt.

Large benthonic foraminiferal assemblages This zone is characterised by the great abundance of shallow. water large benthonic

foraminifers. Among those identified are: Borelis melo Fichtel and Moll - Amphistegina Iessoni (d’orbigny) - Heterostegina costata costata Cushman - H. heterostegina heterostegina (Silvestri) - Miogypsina cf. globulina - M. cushmani as reworked micofossilsl - Operculina complanta (Defiance) - 0. cf. carpenteri (Silvestri) -Ammonia beccarii (Linnaeus) - Pyrgo bulloides d’orbigny - Gypsina vesicularis (Park and Jones).

Remarks The most conspicuous large benthonic foraminiferal taxon recorded in this zone is Borelis melo Fichtel and Mall. Many workers have discussed the stratigraphical importance of this taxon as a zonal marker for defining the boundary of the Middle Miocene in the absence of the Index Middle Miocene planktonic foraminifers Praeorbulina spp. and Orbulina spp. (Eames et al., 1962, Souaya, 1963; Reiss and Givertzmann, 1966; Bizon et al., 1978; Clark and Blow, 1969 and El-Heiny, 1982). In the present work, the presence of this zonal marker in the matrix of the Sarbut El-Gamal polymictic conglomerates provides a good and indirect linkage to the Middle Miocene planktonic foraminiferal zone (N9) of Blow (1969).

Occurrence This zone is recorded unconformably overlying the Globigerinoides trilobus Zone as in Gabal Sarbut El-Gamal, Gabal Abu Alaqa but exists unconformably above the Globigerinoides sicanus Zone in Wadi Baba. It is generally unconformably underlying the Orbulina suturalis/ Globorotalia siakensis Zone in the previous three localities.

Orbulina suturalis/Globorotalia siakensis Zone Category: Concurrent range zone; Age: Middle Miocene (Serravallian); Author: Bizon and Bizon (1972); Definition: Interval from the first occurrence of Orbulina suturalis Bronnimann to the last occurrence of Globorotalia siakensis Le Roy.

Planktonic assemblage Globigerinoides trilobus (Reuss) - Globigerinoides immaturus Le Roy - Globigerinoides sacculifer Brady - Globigerinoides ruber (d’orbigny) - Gfobigerinoides conglobatus (Brady) - Globigerinoides obliquus obliquus Bolli -

Figure 3. Distribution chart of the most common planktonic foraminiferal speoes recorded in the studied sections.


Figure 4. (I, 2) Cassigerinella chipolensis (Cushman and Ponton) umbilical and spiral views, Nukhul Formation, Gabal Sarbut El-Gamal. (3) Globigerina woodi Jenkins umbilical view, Nukhul Formation, Wadi Baba. (41 Globigerina bulloides d’orbigny umbilical view, Hammam Faraun Member, Gabal Sarbut El-Gamal. (51 Globigerina eamesi (Blow) umbilical view, Rudeis Formation, Wadi Baba. (6) Globigerina ciperoensis angustiumbilicata Bolliumbilical view, Rudeis Formation, Gabal Abu Alaqa. 17, 8) Globigerina ciperoensis ciperoensis Bolli umbilical views, Rudeis Formation, Gabal Sarbut El- Gamal. (9) Globigerina falconensis Blow umbilicalview, Hammam faraun Member, GabalAbu Alaqa. (10, 1 ll Globigerina decoraperta Takayanagi and Saito umbilical views, Hammam Faraun Member, Gabal Sarbut El-Gamal. 1121 Globigerina bulloides d’orbigny umbilical view, Hammam Faraun Member, Gabal Abu Alaqa. I1 31 Globigerina eamesi IBlow) umbilical view, Nukhul Formation, Wadi Baba. (741 Globigerina juvenilis Bolli umbilical view, Rudeis Formation, Wadi Baba. 115, 16) Globigerinoides bolli Blow umbilical and spiral views, Hammam Faraun Member, Gabal Sarbut El-Gamal. I1 71 Globigerinoides trilobus (Reussl umbilical view, Rudeis Formation, GabalSarbut El-Gamal. 1781 Globigerinoides immaturus Le Roy umbilical view, Rudeis Formation, Wadi Baba. (19) Globigerinoides altiaperturus Bolli umbilical view, Rudeis Formation, Gabal Sarbut El-Gamal. (20) Globigerinoides sacculifer (Brady) spiral view, Rudeis Formation, Wadi Baba. N. B. : II the figured specimens are magnified by 160x.

Fm ?i. il) GMigeMhdees secculifer IBradyf umbilical view, Hammam Faraun Member, Gabal Abu Alaqa. (2, 3) Globigerinoides primordius Blow and Banner umbilical and spiral views, Nukhul Formation, G. Sarbut El-Gamal. (4) Gl&gecii sacculifer Brady umbilical view, Hammam Feraun Member, W. Baba. 15) Globigerinoides obliquus obliquus BoRi umbilical view, Hammam Faraun Member, G. Abu Alaqa. 16) Globigerinoides mitra (Todd) spiral view, Hammam Faraun Member, 6. .%-but El-Gamal. (7) Globigerinoides subquadratus Bronnimann spiral view, Rudeis Formation, W. B&a. iB) Globigerinoides sicanus De Stefani umbilical view, Rudeis Formation, W. Baba. 19, 70) Orbulina bilobata (d’Orh&ny) apertural views, Hammam Faraun Member, G. Abu Alaqa. (11) Orbulina universa d’orbigny apertural view, Harnmam Faraurl Member, W. Baba. (12) Orbulina suturalis Bronnimann apertural view, Hammam Faraun Member, W. Baba. (13) Globoquadrina altispira globosa lBollil umbilical view, Rudeis Formation, W. Baba. 114) Globioquadrina dehiscens dehiwens (Cushman, Parr and Collinson) umbilical view, Rudeis Formation, G. Sarbut El-Gamel. (15) Globoquadrina altispira altispira lCushman and Jarvis) umbilical view, Rudeis Formation, W. Baba. 116) Globigerinoides akiaperturus BoLli umbilical view, Rudeis Formation, G. Abu Alaqa. N.B.: all the figured specimens are magnified by 160x.

Figure 6. (1,2 and 14) Globoquadrina altispira globosa (Bolli) spiral and umbilical views, Hammam Faraun Member, G. Sarbut El-Gamal. 13) Globquadrina venezuelana (HedbergJ umbilical view, Hammam Faraun Member, W. Baba. (4) Globigerinella praesiphonifera IBlowJ spiral view, Rudeis Formation, W. Baba. 151 Catapsydrax dissimilis fcushman and Bermudez) umbilical view, Rudeis Formation, W, Baba. 16, 15) Globorotalia obesa Bolliumbilical view, Rudeis Formation, G. Sarbut El-Gamal (Fig. 6J and W. Baba (Fig. 751. 17) Globorotalia praescitula Blow umbilical view, Rudeis Formation, W. Baba. 18) Praeorbulina glomerosa Blow apertural view, Rudeis Formation, W. Baba. (9. 10) Globorotalia pseudocontinuosa Jenkins umbilical views, Hammam Faraun Member, G. Abu Alaqa. (7 1) Globorotalia cf. peripheronda Blow and Banner spiral view, Hammam Faraun Member, W. Baba. 112) Globorotalia hexagona INatlandJ umbilical view, Hammam Faraun Member, W. Baba. (131 Globorotalia siakensis (Le Roy) umbilical view, Rudeis Formation, G. Sarbut El- Gamal. (16, 19) Globigerinoides obliquus obliquus Bolli-Hammam Faraun Member, G. Abu Alaqa 116: umbilical view, 19: spiral view). (17) Praeorbulina tranistoria (Blow) spiral view, Rudeis Formation, W. Baba. 1181 Globigerinoides helicnus d’orbigny umbilical view, Hammam Faraun Member, G. Sarbut El-Gamal. (20) Orbulina universa d’orbigny umbilical view, Hammam Faraun Member, W. Baba. N.8.: all the figured specimens are magnified by 160x.

Planktonic foraminiferal biostra tigraph y of the Miocene sequence in west ten tral Sinai

Globigerinoides obliquus extremus Bolli - Globigennoides mitra Todd - Globigerinoides cf. fistulosus (Schubert) - Globigerina bulloides d Orbigny - Globigerina falconensis Blow - Globigerina nepenthes - Globigerina decoraperta Takayanagi & Saito - Globorotalia hexagona (Natland) - Orbulina suturalis d Orbigny - Orbulina universa d’orbigny - Orbulina bilobata (d’orbigny) - Globigerinella praesiphonifera (Blow) - Globoquadrina altispira altispira (Cushman & Jarvis) - Globoquadrina altispira globosa (Bolli) - Globoquadrina venezulana (Hedberg) - Gl’oborotalia praescitula Blow - Globorotalia pseudocontinuosa Jenkins.

Remarks This zone represents the youngest planktonic foraminiferal biozone recorded in the studied sections and enscompasses the Hammam Faraun Member of the Belayim Formation (Middle Miocene). It occurs primarily in association with argillaceous limestone beds where abundant planktonic foraminifers are encountered. This zone has been recorded unconformably overlying the large benthonic foraminiferal zone (Borelis melo Zone) and occupying the uppermost part of the studied sections in Gabal Sarbut El-Gamal, Wadi Baba and Gabal Abu Alaqa.

SUMMARY AND CONCLUSIONS The lithostratigraphical studies carried out on six stratigraphical surface sections representing the Miocene succession in west central Sinai led to the recognition of four main rock units, arranged stratigraphically from older to younger:

Belayium Formation (Hammam Faraun Member) Hammam Faroun Unconformity

Middle Miocene Sarbut El-Gamal Formation Mid-Clysmic Unconformity Rudeis Formation Early Miocene Nukhul Formation Early Clysmic Unconformity Tayiba Red Bed.s (Abu Zenima Formation)

Late Eocene-Oligocene

The stratigrabhical distribution of the planktonic foraminiferal species and large benthonics allowed the subdivision of the Miocene sequence into five planktonic foraminiferal biozones and one large benthonic biozone. These biozones are correlated with other Miocene biozones in the world, with special emphasis on the Mediterranean regions (Tables 2 and 3).

Based on the Mediterranean chronostrati- graphical units, and the distribution of the planktonic foraminiferal taxa, as well as the large benthonic foraminiferal assemblages, it could be used to subdivide the Miocene sequence in the studied sections into the following chronostrati-graphical units; arranged from older to younger.

Aquitanian (Early Miocene) This time interval is represented by the Nukhul Formation (basal conglomerates, sandstone, shale sandy limestone beds with oyster banks reflecting an open shallow marine facies) and included the Globigerinoides primordius Zone (N4-5).

Burdigalian (Early Miocene) This time interval is represented by the Rudeis Formation (interbedded argillaceous limestone with sandy to cherty fossiliferous limestone suggesting open deep marine conditions) and encompasses the following biozones from base to top : Globigerinoides altiaperturus/Ca taps ydrax dissimilis Zone (N6), Globigerinoides trilobus Zone (N7) and Globigerinoides sicanus Zone (N8). The last zone is recorded only in the Wadi Baba surface section.

Langhian (Middle Miocene) This time interval is best represented by the Sarbut El-Gamal Formation (coarse elastic sequence of polymictic conglomerates and algal reefal limestone beds reflecting non-marine to coastal environments) and included the shallow large benthonic biozone, Borelis melo, which is equivalent to N9 of Blow (1969).

Serravallian (Middle Miocene) This time interval is represented by the Hammam Faraun Member of Belayim Formation (dolomitic algal reefal limestone of shallow warm marine environments with incursions of deep open marine facies, represented by argillaceous limestones with flooded planktonic foraminifers). This time interval includes the Orbulina suturalis/ Globoro talia siakensis Zone (N IO- 11).

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