Late Cretaceous - Early Paleogene bio- and sequence stratigraphy of west-central Sinai, Egypt

Accepted Manuscript Late Cretaceous - Early Paleogene bio- and sequence stratigraphy of west-central Sinai, Egypt Shehta Eweda, Ahmed Zakaria, Reda El Bahrawy PII:

S1464-343X(17)30137-1

DOI:

10.1016/j.jafrearsci.2017.03.021

Reference:

AES 2857

To appear in:

Journal of African Earth Sciences

Received Date: 20 October 2016 Revised Date:

11 February 2017

Accepted Date: 21 March 2017

Please cite this article as: Eweda, S., Zakaria, A., El Bahrawy, R., Late Cretaceous - Early Paleogene bio- and sequence stratigraphy of west-central Sinai, Egypt, Journal of African Earth Sciences (2017), doi: 10.1016/j.jafrearsci.2017.03.021. This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

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central Sinai, Egypt

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Shehta Ewedaa, Ahmed Zakariab* and Reda El Bahrawya

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Zagazig University, Faculty of Science, Zagazig, Egypt.

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Late Cretaceous - Early Paleogene bio- and sequence stratigraphy of west-

Cairo University, Faculty of Science, Cairo, Egypt.

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ABSTRACT: A sequence biostratigraphic analysis has been done for the Upper Cretaceous-

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areas in west-central Sinai. The sequences are subdivided into four carbonate rock units; from

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Lower Paleogene sedimentary outcrops at Wadi Raha, Sudr El-Hetan and Wadi El-Giddi

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The biostratigraphic analysis of the studied samples led to the identification of two main

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planktonic foraminiferal zones, three benthic foraminiferal zones with the ammonite zone.

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Eleven microfacies associations are recorded in the rock units. Nine constitutes a limestone

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base to top: the Wata, Themed, Sudr and Waseiyit formations.

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data, and the facies study support the identification of three major breaks (sequence

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boundaries) and four depositional sequences. The depositional sequences are subdivided into

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facies with one constitutes a dolostone facies and one a claystone facies. The stratigraphic

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The oldest break (~90-88.5Ma.) exists at the top of the Wata Formation coincides with the

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intra Turonian drop in the global sea level with the initiation of the Syrian Arc inversion

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phase. The second major break (85 - ~75Ma.) coincides with the major inversion phase and

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the evolution of the doubly plunging anticlines. The third major break (~68 through ~53Ma.)

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represents the last phase of the Syrian Arc inversion and complete the missing of Paleocene

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sequences

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Keywords: Upper Cretaceous, Lower Paleogene, Foraminifera, Sinai, Sequence Stratigraphy,

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four supercycles and seven cycles of 3rd order.

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The area of investigation lies in west-central Sinai between latitudes 29o 58′ 57″ & 30o 12′ 39″

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N and longitudes 32o 57′ 05″ & 33o 03′ 20″ E (Fig.1). The Upper Cretaceous-Lower

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1. Introduction

Paleogene outcrops have been measured and examined in detail from south to north as follow:

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Wadi Raha, Sudr El-Hetan and Wadi El-Giddi.

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The Upper Cretaceous-Lower Paleogene successions in Egypt are marked by widely

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vertical and lateral facies changes. A considerable body of works cover the biostratigraphy of

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distributed and well preserved planktonic and benthic foraminiferal assemblages with distinct

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(1989), Ismail (1992), Abbass et al. (1994), Abdel-Gawad (1999), Ayyad et al. (2003), El-

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Deeb et al. (2000), El-Nady & Shahin (2001), Obaidalla & Kassab (2002), Galal (2003), Faris

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et al. (2005), Faris & Salem (2007), Hamad (2009), Faris & Farouk (2012) and El Ayyat &

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the Upper Cretaceous-Lower Paleogene of Sinai; e.g. Allam et al. (1986), Ayyad & Hamama

Obaidalla (2016).

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(1990), Sehim (1993), Ayyad and Darwish (1996), Abd-Allah et al. (2004), Moustafa (2010)

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The tectonic framework of the Syrian Arc system has been analyzed by Moustafa and Khalil

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of the Neo-Tethys during the collision between the Afro-Arabian and Eurasian plates

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among others. The growth onset of the Syrian Arc System was triggered by the initial closure

(Guiraud, 1998). The main proposed classifications of the Upper Cretaceous-Lower

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Paleogene sequences in the Gulf of Suez region and Sinai are summarized in Table (1).

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The main purpose of this research is to describe and elucidate the stratigraphic sequence,

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microfacies characteristics and biostratigraphic analysis to discuss in details the sequence

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stratigraphic framework and its implication for building tectono-stratigraphic models of the

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Syrian Arc system.

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Lithostratigraphically, the studied Upper Cretaceous-Lower Paleogene sequences are

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distinguished into four formations, from base to top, as follows: Wata, Themed, Sudr and

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Waseiyit.

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2. Stratigraphic setting

Wata Formation

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Hetan sections (Fig. 2). The Wata Formation consists of fossiliferous and argillaceous

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The Wata Formation (Ghorab, 1961) measures about 41m thick at Wadi Raha and Sudr El-

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The middle and upper parts are highly fossiliferous with the occurrence of large-sized

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limestone with chert concretions and thin interbeds of claystone in the lower measured part.

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assemblages (eg. Orthossis rubella, Holectypus sp. and Phymosoma sp.) of Early to Middle

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Turonian age. The Wata Formation is assigned to the Early to Middle Turonian age based on

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the fossil assemblages and the absence of typical Late Turonian fossils as well as its

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stratigraphic position. Themed Formation

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ammonite (eg. Choffaticeras segne, Vascoseras sp. and Wrightoceras munieri) and echinoid

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The Themed Formation (Ziko et al., 1993) is exposed in the Wadi Raha and Sudr El-Hetan

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yellowish brown to yellowish green, hard, massive, thinly to thickly bedded, partially sandy,

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sections and ranges in thickness from 18 m to 27.5m respectively (Fig. 2). It consists of

dolomitic, glauconitic and argillaceous limestone with few interbeds of moderately hard

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claystone, marl and chert concretions. It is characterized by upward-increasing sand and

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glauconite grains. Themed Formation is assigned to Coniacian-Santonian based on its

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biostratigraphic analysis and the stratigraphic position.

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Sudr Formation

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thickness at Wadi Raha, 39m in Sudr El Hetan and 20m in Wadi El-Giddi (Fig. 2). It consists

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mainly of snow white, moderately hard to soft, massive to thickly bedded, slightly

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ferruginous, dolomitic, glauconitic, argillaceous and chalky limestone with abundant

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The Sudr Formation (Ghorab, 1961) is exposed in the studied sections and reaches 42.5m in

planktonic and some benthic foraminifera. It is assigned to the Late Campanian-Maastrichtian

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age based on the biostratigraphic analyses.

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Waseiyit Formation

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thickness of 46m at Wadi Raha, 36m at Sudr El-Hetan and 88m at Wadi El-Giddi sections

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The Waseiyit Formation (Barakat et al., 1985) is exposed in the studied sections with a

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yellowish brown, thinly to thickly bedded, massive, nodular in some parts, moderately hard,

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argillaceous, cherty and chalky limestone with few glauconitic marl intercalations at the lower

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part. According to the stratigraphic position and the biostratigraphic analyses, it is assigned to

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the Early Eocene age. 3. Material and methods

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(Fig. 2). It unconformably overlies the Sudr Formation and mainly composed of gray to

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Three stratigraphic sections were measured, described and sampled. Eighty two thin sections

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transmitting-polarizing and reflecting-light microscopes.

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representing the whole studied lithologic varieties were examined and photographed using

Two hundred grams of dry rock samples were treated for biostratigraphic analyses. The

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samples were disaggregated in water with a small amount of hydrogen peroxide (15% conc.)

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and then washed through a 63µm sieve. The residue obtained was separated, examined and

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photographed using a research grade stereo-binocular microscope and a Scanning Electron

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Microscope (SEM) at the Egyptian Mineral Resourses authority. Planktonic and benthic

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foraminifera were classified after Toumarkine & Luterbacher (1985), Caron (1985), Loeblich

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deposited in the Geology Department Museum, Cairo University, collection of

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micropaleontology.

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4. Results

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& Tappan (1988) and Berggren & Pearson (2005). The samples and microfossils were

4.1 Biostratigraphy

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foraminiferal species in the three investigated sections, two planktonic foraminiferal zones

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On the basis of the observed range and frequency of the recovered planktonic and benthic

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zones (Discorbis minutus, Bolivinoides draco draco & Bolivina incrassata and Nummulites

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(Globotruncana aegyptiaca and Morozovella subbotinae) and three benthic foraminiferal

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samples, the ammonite (Choffaticeras segne and Wrightoceras munieri zones) which widely

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discussed by Kassab (1991), Hewaidy et al. (2003) and El Qot (2008) are used. These zones

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are approximate stratigraphic equivalents to the standard ammonite zone of W.

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spp.) have been identified. Due to the absence of the foraminiferal assemblages in the washed

coloradoense/W.devonense, M. nodosoid and C. woollgari (Gradstein et al., 2012 & Haq,

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2014).

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The stratigraphic ranges of the identified species in the studied sections are tabulated in Figs.

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regions. The foraminiferal zones will be described based on Caron (1985) for the Cretaceous

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(3-5) and the zones were correlated with the corresponding zones in the geographically related

and of Toumarkine & Luterbacher (1985) and Berggren & Pearson (2005) for the Early

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Paleogene. Photographs of the most important foraminiferal taxa are shown in figures (6 and

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7). The characteristics of the identified planktonic and benthic biozones, from older to

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younger, are as follows:

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Zone 1: Discorbis minutus Zone

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Definition: Interval of total range of Discorbis minutus

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sections

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Correlation: In Egypt, the proposed zone is partly equivalent to the Discorbis turonicus

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minutus Zone of the Gulf of Suez (Ansary & Tewfik, 1969). The zone was also described in

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Occurrence: The zone has been recorded in Wadi Raha (11.5m) and Sudr El-Hetan (11.5m)

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the Western Desert by El Ashwah (1998) and in the north Western Desert by El Ashwah

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(2001).

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the northeastern part of the Western Desert by El Ashwah (1997), in the northwestern part of

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presence of common benthic foraminifera Discorbis minutus.

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Suggested age: Coniacian/Santonian

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Assemblage: The zone is characterized by the absence of planktonic foraminifera and the

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Definition: The base of this zone is defined based on the first occurrence of Bolivinoides

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draco draco Marsson (1878), while the top is delineated by the last occurrence of the

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Zone 2: Bolivinoides draco draco & Bolivina incrassata Zone

nominate species.

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Wadi-El Giddi section Bolivinoides draco draco is absent.

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Occurrence: This zone has been recorded in the Sudr El-Hetan (26m) section, while in the

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mayaroensis zones (Ayyad et al., 1997). The Bolivinoides draco draco is absent in Wadi El-

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Remarks: This zone is equivalent to the planktonics Gansserina gansseri and Abathomphalus

Giddi section, so the Maastrichtian age is assigned according to the presence of Bolivina

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incrassata (20m thick.).

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Correlation: The zone corresponds to the Bolivinoides draco draco Zone defined from the

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Upper Cretaceous (Maastrichtian) of the Gulf of Suez (Ghorab, 1961). Also, it was recorded

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from Sinai (Shahin, 1988 and El Nady, 2006) and from north Western Desert by El Ashwah

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(2001).

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assemblage of Bolivinoides draco draco, Gyroidinoides girardanus, Bolivina incrassata,

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Cibicides spp. and Praebulimina spp. associated with a planktonic foraminiferal assemblage

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of Contusotruncana fornicata, Heterohelix spp., and Globotruncana spp.

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Assemblage: The zone is characterized by the occurrence of a benthic foraminiferal

Suggested age: Maastrichtian Zone 3: Globotruncana aegyptiaca Zone

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Definition: Interval from the first occurrence of Globotruncana aegyptiaca to the first occurrence of Gansserina gansseri.

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Occurrence: This zone has been recorded in Sudr El-Hetan (16m) and Wadi Raha (42.5m) sections

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is correlated with Globotruncana aegyptiaca Zone of the Red Sea (El Dawy, 1993 and

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Obaidalla, 2000). In addition, this zone corresponds to that proposed for the Upper Cretaceous

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Correlation: The described zone is equivalent to the same zone of Caron (1985). In Egypt, it

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to Haq (2014), this zone is assigned to Late Campanian.

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Remarks: The upper boundary is characterized by the first occurrence of Gansserina

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rocks of Sinai (El-Nady, 2006) and of the north Western Desert (El Ashwah 2001). According

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could not be determined.

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gansseri. Since Gansserina gansseri is absent in the analyzed samples, the top of this zone

Assemblage: The planktonic assemblage is characterized by the occurrence of Heterohelix

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globulosa, Contusotruncana fornicata, Globotruncana arca, Globotruncana aegyptiaca,

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Globotruncana bulloides, and Globotruncana spp. The benthic foraminifera are characterized

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by the occurrence of Gyroidinoides girardanus, Pseudotextularia elegans, Bolivina

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incrassata, Pseudotextularia spp., Gavelinella spp., Nodosaria spp. and Praebulimina spp.

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Suggested age: Late Campanian-Maastrichtian

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Definition: Interval range of the nominate taxa between the FO of Morozovella subbotinae

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and the FO of Morozovella aragonensis.

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Occurrence: This zone has been recorded only in the Wadi El-Giddi section and encompasses

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Zone 4: Morozovella subbotinae Zone

a thickness of 34m.

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& Luterbacher (1985) and Berggren & Pearson (2005). In Egypt, it is equivalent to

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Correlation: Morozovella subbotinae Zone is correlated with that proposed by Toumarkine

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Obaidalla, 2016) and of Sinai (Faris et al., 2000 and El-Nady, 2005).

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Morozovella subbotinae Zone of the Eastern Desert (Galal & Kamel, 2007 and El-Ayyat &

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subbotinae due to the absence of Morozovella aragonensis. The absence of this zone in Wadi

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Raha and Sudr El-Hetan sections may be due to the preservation or the effect of the Syrian

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Arc.

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Remarks: This zone is defined here based mainly on the occurrence of Morozovella

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Morozovella spp., Acarinina quetra, Acarinina bullbbrooki and Acarinina spp. The benthic

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foraminifera throughout this interval are very rare.

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Assemblage: The zone is characterized by the occurrence of the Morozovella subbotinae,

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Zone 5: Nummulites spp. Zone

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Suggested age: Early Eocene.

Occurrence: It reaches up to thickness 6m, 12m and 20m in the Wadi Raha section, the Sudr

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El-Hetan section and the Wadi El-Giddi section respectively.

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Assemblage: The zone is characterized by the absence of planktonic foraminifera and the

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common occurrence of the benthic foraminifera Nummulites spp.

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Suggested age: Early Eocene.

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4.2 Microfacies examination

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and Flügel (2004) are used to describe the microfacies associations of the studied Upper

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Cretaceous-Lower Paleogene sequences.

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Ten carbonate microfacies are identified; each of these microfacies types could be subdivided into

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The classifications and terminology of Dunham (1962), Embry & Klovan (1972), Wilson (1975)

submicrofacies according to their own dominant carbonate and non-carbonate particles (Figs. 8-11

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and Table 2).

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5. Discussion

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level record of the Upper Cretaceous-Lower Paleogene sequence and their sedimentation

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The stratigraphic sequence interpretation provides a useful framework for refining the sea-

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vertical facies changes, the stacking patterns and upward changes in the cycles permit the

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identification of boundaries and depositional sequences.

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Based on the stratigraphic sequence analysis, four depositional sequences (SQ) bounded by

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history in the investigated area. The biostratigraphic analysis, microfacies types, the radical

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Coniacian-Santonian CSSQII, the Upper Campanian-Maastrichtian MSQIII and the Lower

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Eocene ESQIV (Fig. 2).

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three sequence boundaries (unconformities). The Lower to Middle Turonian TSQI, the

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The biostratigraphic study of the Upper Cretaceous-Lower Paleogene deposits records the

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5.1 Unconformities and stratigraphic boundaries

presence of three unconformities as sequence boundaries of type 1. These can be correlated

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with their counterparts in adjacent areas, as well as with those of the assumed global eustatic

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cycles (Haq et al., 1987, 1988) (Figs. 12 and 13). Such identified major breaks are

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characterized by paleontologic and physical criteria. The main characteristics of these

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sequence boundaries can be summarized as follows:

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5.1.1 Intra Middle Turonian/Coniacian (SB1)

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on which the Coniacian/Santonian Themed Formation rests unconformably. This boundary

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can be correlated with that described in Sinai by Chérif et al. (1989a, b). El-Azabi & El-Araby

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(2007) considered that this boundary has been terminated by a regressive phase in the Upper

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The Middle Turonian/Coniacian sequence boundary exists at the top of the Wata Formation,

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In the study area, this boundary is marked by a sub-aerial erosion surface at Wadi Raha and

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Sudr El-Hetan sections and is characterized by the presence of dense bioturbation with sharp

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Turonian succession of Sinai due to the effect of Syrian Arc movements.

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shoals facies with the absence of Late Turonian fossils.

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contacts and inflection of depositional setting from an open marine to shallow subtidal and

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This boundary is traced at the top of the Themed Formation in the Wadi Raha and Sudr El-

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Hetan sections and is also unexposed in Wadi Giddi section. It is characterized by an obvious

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lithological change from a shallow subtidal mollusk limestone of the Themed Formation to an

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5.1.2 Santonian/Upper Campanian (SB2)

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Paleontological criteria indicate the absence of the foraminiferal zones of Early-Middle

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Campanian age. This sequence boundary separates between the Discorbis minutus benthic

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open marine deep subtidal planktonic foraminiferal chalky limestone of the Sudr Formation.

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foraminiferal Zone (Late Campanian). In addition, the presence of glauconitic beds at the

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foraminiferal Zone (Coniacian-Santonian) and the Globotruncana aegyptiaca planktonic

upper part of the Themed Formation, these indicate oscillating shallow marine near shore

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environment. The absence of Lower and Middle Campanian deposits in the study area is

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probably due to the uplifting during that time as a result of the Syrian Arc system (Ayyad &

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Darwish, 1996 and Samuel et al., 2009).

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5.1.3 3 Upper Campanian-Maastrichtian/Lower Eocene (SB3)

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(K/Pg). It is well defined in the three studied sections. In the Wadi Raha section, this sequence

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boundary is characterized by a marked upward facies change from chalky limestone to

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nummulitic argillaceous limestone. While in the Sudr El-Hetan and the Wadi El-Giddi

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The third sequence boundary is between the Sudr Formation and the Waseiyit Formation

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glauconitic argillaceous limestone of the Waseiyit Formation. This sequence boundary is

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approximately equivalent to Syrian Arc tectonic phase 1 of El Ayyat and Obaidalla (2016).

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sections, this boundary is located between chalky limestone of the Sudr Formation and

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global sea level fall and tectonic inversion of the Syrian Arc system (Ayyad & Hamama,

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The K/Pg boundary in Sinai has been interpreted as being influenced by both the drastic

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Darwish, 1996, Obaidalla, 2005 and El-Ayyat & Obaidalla, 2016)

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5.2 Cyclicity and sequence stratigraphy

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The Upper Cretaceous-Lower Paleogene sequences in the study areas could be distinguished

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into seven 3rd order cycles based on the lithologic characteristics, biostratigraphic and facies

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analysis (Figs. 2-7). These cycles clearly point to repeated relative sea level fluctuations.

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The hierarchy of the sequences and cycles are interpreted according to the schemes given in

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1989, Moustafa & Khalil, 1990, Ismail, 1992, Sehim, 1993, Abbass et al., 1994, Ayyad &

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UZA-4 and TA2 which are subdivided into several 3rd order cycles (Table 1). Each of the

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Haq et al. (1987, 1988 and 2014). These cycles represent four supercycles; UZA-2, UZA-3,

studied sequences is composed of retrograding upward parasequence sets that formed as a

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result of normal transgression during sea level highstand.

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5.2.1 UZA-2 Supercycle

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According to Haq et al. (1988), this supercycle covers the time interval from the Late Albian

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to the Middle/Late Turonian boundary and is subdivided into seven 3rd order cycles. In the

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study area, it covers the Lower and Middle Turonian succession exposed at Wadi Raha and

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underlies unconformably the Themed Formation, while the base is unexposed.

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The maximum flooding surface in this supercycle was recorded by the abundance of nektonic

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fauna (ammonites). This supercycle is subdivided into two cycles; 2.5 and 2.6 of 3rd order and

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Sudr El-Hetan. It consists mainly of limestone with rare calcareous claystone interbeds and

is approximate equivalent to KTu1, KTu2 and KTu3 cycles of Haq (2014).

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5.2.1.1 3rd order cycle 2.5

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It covers the lower part of the Wata Formation at the Wadi Raha and the Sudr El-Hetan

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limestone with rare calcareous claystone interbeds. The thickness of this cycle ranges from

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sections which assigned to the Early Turonian age (Fig. 2). It is built up of argillaceous

about 18m thick at Wadi Raha to 26m thick at the Sudr El-Hetan section. According to Haq et

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al. (1988) this cycle represents a transitional cycle of the Late Cenomanian to the Early

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Turonian.

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The transgressive systems tract (TST): It is represented by samples no. 1-5 (9m thick) in the

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of bioturbated, fossiliferous, thinly- to thickly bedded, argillaceous limestone with burrows,

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chert concretions and thin calcareous claystone interbeds. Microscopically, at Wadi Raha

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Wadi Raha section and samples no. 1-5 (21m thick) in the Sudr El-Hetan section. It consists

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El-Hetan section, it includes MFT3, MFT11 and MFT21 microfacies (Table 2).

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section, it includes, from base to top, MFT1, MFT2, MFT12 and MFT30, while at the Sudr

The maximum flooding surface occurs at the top of MFT12 microfacies in the Wadi Raha

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section (at measured thickness point of 9m) and at the top of MFT21 microfacies in the Sudr

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El-Hetan section (at measured thickness point of 21m). The maximum accommodation and

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sedimentation rates are interpreted based on the presence and abundance of the ammonite

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fossils.

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Wadi Raha section and samples no. 6-7 (5m thick) in the Sudr El-Hetan section. It is built up

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of medium- to thickly bedded, rich in burrows, argillaceous limestone. Microscopically, it

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includes MFT14 microfacies at the Wadi Raha section and MFT27 microfacies at the Sudr El-

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The highstand systems tract (HST): It is represented by samples no. 6-9 (9m thick) in the

Hetan section. 5.2.1.2 3rd order cycle 2.6

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This cycle represents the upper part of the Wata Formation at the Wadi Raha and the Sudr El-

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composed of argillaceous limestone with a thickness of about 15m at the Sudr El-Hetan

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Hetan sections and is bounded at the top by the (SB1) sequence boundary (Fig. 2). It is

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only by transgressive systems tract. The presence of ammonite fauna in the upper part of this

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cycle indicates a rise in the sea level. This cycle corresponds to the lower part of the Middle

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Turonian succession (Haq et al., 1988).

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section and 22m at the Wadi Raha section. At the Wadi Raha section, this cycle is represented

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the Wadi Raha section and by samples no. 8-9 (10m thick) in the Sudr El-Hetan section. It

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consists mostly of fossiliferous, thickly bedded limestone with burrows, chert concretions and

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The transgressive systems tract (TST): It is represented by samples no. 10-12 (22m thick) in

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at the Sudr El-Hetan section, while at the Wadi Raha section, it includes MFT4 and MFT8

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large ammonites in the upper part. Microscopically, it includes MFT2 and MFT12 microfacies

microfacies (Table 2).

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The maximum flooding surface (MFS): at the Sudr El-Hetan section, it is recorded at 36.5m

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in the measured section and is represented by intraclastic bioclastic packstone microfacies

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(MFT12), while at the Wadi Raha section, it is difficult to discern. The maximum

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accommodation and sedimentation rates are recorded in this cycle based on the presence of

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supercycle (Haq et al., 1988).

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The highstand systems tract (HST) is recorded only at the Sudr El-Hetan attaining about 5m

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thick. It consists of fossiliferous, argillaceous limestone. Microscopically, it consists of

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the ammonite bed. This corresponds to the sea level rise at or near the end of the UZA-2

313

The Upper Turonian hiatus in the study area is probably related to the global eustatic sea level

314

falling during the intra-Turonian event that is recorded world-wide e.g. in North America,

315

SC

echinoidal bioclastic wacke/packstone (MFT8) microfacies (Table 2).

316

(Sieglie & Barker, 1984); in the Middle East (Harris et al., 1984 and Darwish, 1994).

317

M AN U

Western Interior and the Atlantic margin (Poag & Schlee, 1984); in central west Africa

5.2.2 UZA-3 Supercycle

318 319

Campanian interval and is subdivided into five 3rd order cycles. In the present study, this

320

supercycle covers the time interval of the Coniacian-Santonian of the Themed Formation at

321

TE D

According to Haq et al. (1988), this supercycle covers the Late Turonian to Middle

322

intercalated calcareous claystone and marl beds. It includes the benthic foraminiferal

323

Discorbis minutus Zone of the Coniacian-Santonian age. In the study area this supercycle is

324

EP

the Wadi Raha and the Sudr El-Hetan areas. It is mainly composed of limestone with few

325

KSa1 and KSa2 cycles of Haq (2014).

326

AC C

represented by two 3rd order cycles, 3.2 and 3.3. It is approximate equivalent to KCo1, KCo2,

5.2.2.1 3rd order cycle 3.2

327

This cycle is recorded in the lower and middle parts of the Themed Formation at the Sudr El-

328

Hetan section, while it represents the Themed Formation at the Wadi Raha section (Fig. 2). It

329

is essentially composed of argillaceous limestone with few claystone and marl interbeds. The

330

thickness of this cycle is about 16m at the Sudr El-Hetan section and 18m at the Wadi Raha

331

14

ACCEPTED MANUSCRIPT 332

(Haq et al., 1988).

333

The transgressive systems tract (TST): It is represented by samples no. 13-18 (about 6m

334

thick) in the Wadi Raha section and by samples no. 11-15 (about 14m thick) in the Sudr El-

335

RI PT

section. This cycle represents a transitional cycle of the Late Coniacian to the Early Santonian

336

limestone with few marl interbeds. Microscopically, the transgressive systems tract at the

337

Wadi Raha section includes MFT5, MFT14, MFT15, MFT28 and MFT29 microfacies, while

338

SC

Hetan section. It is mainly composed of bioturbated, thinly to thickly bedded, fossiliferous

339

The maximum flooding surface (MFS) of this cycle is recorded in the Wadi Raha section at

340

M AN U

at the Sudr El-Hetan section, it includes MFT1, MFT13 and MFT29 microfacies.

341

point of 47m and in the Sudr El-Hetan section at the top of the dolomitic lime-mudstone

342

(MFT1) at a measured thickness point of 54m.

343

The highstand systems tract (HST): It is represented by samples no. 19-26 attaining about

344

TE D

the top of the dolomitic bioclastic wackestone microfacies (MFT5) at a measured thickness

345

the Sudr El-Hetan section. It consists mainly of thinly to thickly bedded, fossiliferous,

346

argillaceous limestone with few fossiliferous calcareous claystone and marl interbeds.

347

EP

12.5m thick in the Wadi Raha section and by samples no. 16-18 attaining about 4m thick in

348

MFT8, MFT17, MFT22, MFT23 and MFT24 microfacies. At the Sudr El-Hetan section, it

349

AC C

Microscopically, at the Wadi Raha section, it is represented, from base to top, by MFT2,

includes MFT25 and MFT15 microfacies (Table 2).

350

5.2.2.2 3rd order cycle 3.3

351

This cycle represents the upper part of the Themed Formation at the Sudr El-Hetan section

352

(Fig. 2) and is represented only by the transgressive systems tract. The thickness of this cycle

353

is about 11.5m. It is mainly composed of limestone lithofacies with few intercalated

354

15

ACCEPTED MANUSCRIPT 355

Santonian (Haq et al., 1988).

356

The transgressive systems tract (TST) at the Sudr El-Hetan section is represented by

357

samples no. 19-23 (about 11.5m thick). It is composed of hard, argillaceous sandy limestone

358

RI PT

claystone. This cycle represents the transitional cycle of the Early Santonian to the Late

359

MFT22 microfacies (Table 2). It is terminated by the Santonian/Maastrichtian sequence

360

boundary (SB2).

361

SC

with soft fossiliferous calcareous claystone. Microscopically, it includes MFT14, MFT16 and

5.2.3 UZA-4 Supercycle

M AN U

The supercycle UZA-4 covers the time interval from the Middle Campanian to the Late

362 363 364

supercycle covers only the Late Campanian-Maastrichtian sequence. It consists essentially of

365

shallow subtidal limestone and deep subtidal chalky limestone. It is characterized by the

366

planktonic foraminiferal Globotruncana aegyptiaca Zone and the benthic foraminiferal

367

TE D

Maastrichtian and is subdivided into 5 cycles (Haq et al., 1988). In the study area, this

368

supercycle coincide with the major truncations of the global sea level changes due to a very

369

rapid sea level fall (Haq, et al., 1988). This supercycle could be subdivided into two 3rd order

370

EP

Bolivinoides draco draco & Bolivina incrassata Zone. The lower and upper boundaries of this

371

cycles of Haq (2014).

372

AC C

cycles (4.4 and 4.5). It is approximate equivalent to KCa7, KMa1, KMa2, KMa3 and KMa4

5.2.3.1 3rd order cycle 4.4

373

This cycle represents the lower part of the Sudr Formation at the Sudr El-Hetan section and

374

the entire Sudr Formation at the Wadi Raha area (Fig. 2). The thickness of this cycle

375

decreases northwards from about 42.5m thick at the Wadi Raha section to 19m thick at the

376

Sudr El-Hetan section. According to Haq et al. (1988), this cycle represents a transitional

377

cycle of the Late Campanian to the Early Maastrichtian.

378

16

ACCEPTED MANUSCRIPT 379

the Wadi Raha section and by samples no. 24-34 (16m thick) at the Sudr El-Hetan section. It

380

consists of thickly bedded, slightly bioturbated, chalky and argillaceous limestone with

381

abundant burrows of Thalassinoides. Microscopically, it is represented by a highly frequent

382

RI PT

The transgressive systems tract (TST): It is represented by samples no. 27-40 (29m thick) in

MFT6 and MFT9 microfacies (Table 2).

383 384

Hetan section at measured thickness point of 83m, while at the Wadi Raha section, it lies at

385

SC

The maximum flooding surface (MFS) lies at the top of MFT9 microfacies at the Sudr El-

386

the maximum abundance of planktonic foraminifera.

387

M AN U

the top of MFT6 microfacies with a measured thickness point of 88m. It is characterized by

388

the Wadi Raha section and by sample no. 35 (3m thick) in the Sudr El-Hetan section. It

389

consists of massive, slightly bioturbated, fossiliferous, chalky and argillaceous limestone.

390

Microscopically, it consists of (MFT4) (Table 2). It reflects the deposition in an open marine

391

TE D

The highstand systems tract (HST): It is represented by samples no. 41-48 of 13m thick in

392

and the amount of benthic foraminifera and echinoids and mollusk debris increases upward.

393

This is correlated with the beginning of a sea level fall at the end of the 4.4 cycle of Haq et al.

394

(1988).

EP

shallow subtidal environment. The frequency of the planktonic foraminifera decreases upward

395

5.2.3.2 3rd order cycle 4.5

AC C

396

This cycle represents the upper part of the Sudr Formation at the Sudr El-Hetan and Wadi El-

397

Giddi sections (Fig. 2). It is mainly composed of chalky limestone of an open marine deep

398

subtidal environment with 20m thick. The upper part of this cycle coincides with the global

399

eustatic sea level fall during the Late Maastrichtian events (Haq et al., 1988). The Late

400

Maastrichtian regression has also been recognized by Kuss (1989) at northeast Egypt & Sinai.

401

According to Haq et al. (1988), this cycle covers the upper part of the Maastrichtian sequence.

402

17

ACCEPTED MANUSCRIPT 403

in the Sudr El-Hetan section and by samples no. 1-5 (15 m thick) in the Wadi El-Giddi

404

section. It consists thickly bedded, highly fossiliferous, chalky limestone. Microscopically, it

405

is represented by MFT6, MFT9 and MFT18 microfacies (Table 2).

406

RI PT

The transgressive systems tract (TST): It is represented by samples no. 36-43 (15 m thick)

407

MFT9 at a measured thickness point of 100m, while at the Wadi El-Giddi section, it lies at the

408

top of MFT18 at a measured thickness point of 15m.

409

SC

The maximum flooding surface (MFS): at the Sudr El-Hetan section, it lies at the top of

410

Sudr El-Hetan section and by samples no. 6-7 (5m thick) in the Wadi El-Giddi section. It

411

M AN U

The highstand systems tract (HST): It is represented by samples no. 44-47 (5 m thick) in the

412

(Table 2). It shows upward shallowing at the end of the highstand systems tract that is

413

followed by the SB3 sequence boundary.

414

5.2.4 TEJAS A (TA2) 2nd order supercycle

415

TE D

consists of chalky limestone. Microscopically, it includes MFT9 and MFT18 microfacies

416

Paleocene to the Early Eocene and is subdivided into 9 cycles. In the study sequence, this

417

supercycle covers the Lower Eocene sequence that consists mainly of nummulitic limestone

418

EP

According to Haq et al. (1988), this supercycle covers the time interval from the Late

419

the Early Eocene. The maximum regression surface and falling of the sea level were proved

420

AC C

with chert nodules. It includes the planktonic foraminiferal Morozovella subbotinae Zone of

by the presence of abundant Nummulites sp. The TA2 Supercycle is represented by the (2.5)

421

3rd order cycle only.

422

5.2.4.1 3rd order cycle 2.5

423

This cycle represents the Waseiyit Formation at the Wadi Raha, Sudr El-Hetan and Wadi El-

424

Giddi sections (Fig. 2). The measured thickness of this cycle is about 88m thick at the Wadi

425

El Giddi section, 36m at the Sudr El-Hetan section and 46m thick at the Wadi Raha section.

426

18

ACCEPTED MANUSCRIPT 427

succession.

428

The transgressive systems tract (TST): It is represented by samples no. 49-56 (24 m thick),

429

samples no. 48-52 (24m thick) and samples no. 8-17 (25m thick) in the Wadi Raha, the Sudr

430

RI PT

According to Haq et al. (1988), this cycle covers the lower part of the Lower Eocene

431

chalky limestone associated with few thickly bedded and partly glauconitic marl interbed.

432

Microscopically, at the Wadi Raha section, it is represented by MFT2, MFT7, MFT10 and

433

SC

El-Hetan and the Wadi El-Giddi sections respectively. It consists of nodular, cherty, slightly

434

microfacies, and at the Wadi El-Giddi section, it is represented by repeated microfacies of

435

MFT9 and MFT18 on the top.

M AN U

MFT26 microfacies, at the Sudr El-Hetan section, it is represented by MFT9 and MFT18

436 437

Sudr El-Hetan and the Wadi El-Giddi sections while MFT10 microfacies in the Wadi Raha

438

section. It is recorded in the Wadi Raha section at the measured thickness point of 126 m, in

439

TE D

The maximum flooding surface (MFS) occurs at the top of the MFT18 microfacies in the

440

section at the measured thickness point of 45 m.

441

The highstand systems tract (HST): it is represented in the Wadi Raha section by samples

442

EP

the Sudr El-Hetan section at the measured thickness point of 129 m and in the Wadi El-Giddi

443

the Wadi El-Giddi section by samples no. 18-35 (63 m thick). It is composed of thinly to

444

AC C

no. 57-60 (22m thick), in the Sudr El-Hetan section, by samples no. 53-58 (12 m thick) and in

thickly bedded, glauconitic, rich in nummulites and burrows and chalky argillaceous cherty

445

limestone. Microscopically, it is represented in the Wadi Raha section by MFT2 and MFT5

446

microfacies, in the Sudr El-Hetan section, it is represented by MFT7 at the base and repeated

447

microfacies of MFT14 and MFT19 at the top, and at the Wadi El-Giddi section, it is

448

represented by MFT4, MFT10, MFT19 and MFT20 (Table 2).

449

Concluding remarks

450

19

ACCEPTED MANUSCRIPT 451

sequence stratigraphy of the Upper Cretaceous-Lower Paleogene successions that is exposed

452

in the west-central Sinai at Wadi Raha, Sudr El Hetan and Wadi El Giddi.

453

- The studied sequence is subdivided into four formations; from base to top, Wata (Early to

454

RI PT

- The present work is carried out to investigate the litho- and biostratigraphy as well as

455

Waseiyit (Early Eocene) formations. They consist essentially of limestone with rare claystone

456

and marl lithofacies intercalations.

457

SC

Middle Turonian), Themed (Coniacian-Santonian), Sudr (Late Campanian-Maastrichtian) and

458

identified. Arranged from older to younger, the planktonic foraminiferal zones are:

459

M AN U

- Two planktonic foraminiferal zones and three benthic foraminiferal zones have been

Globotruncana aegyptiaca and Morozovella subbotinae zones and the benthic foraminiferal

460

zones are: Discorbis minutus, Bolivinoides draco draco & Bolivina incrassata and

461

Nummulites spp. zones.

462

TE D

- The biostratigraphic analysis results indicate that the Upper Cretaceous-Lower Paleogene

463 464

events associated with the Syrian Arc development.

465

- Ten carbonate microfacies are encountered and are categorized as mudstone, wackestone,

466

EP

sequences were interrupted by erosion and/or non-deposition related to tectonic inversion

467

and lime- bioclastic dolostone microfacies, with one non-carbonate facies represented by

468

AC C

wacke/packstone, packstone, pack/grainstone, grainstone, floatstone, rudstone and framestone

calcareous claystone.

469

- The studied sequence could be distinguished into four depositional sequences, namely, the

470

Early to the Middle Turonian sequence (TSQI), the Coniacian-Santonian sequence (CSSQII),

471

the Late Campanian-Maastrichtian sequence (MSQIII) and the Early Eocene sequence

472

(ESQIV).

473

20

ACCEPTED MANUSCRIPT 474

sequences could be related to the four super (2nd order) cycles UZA-2, UZA-3, UZA-4 (of the

475

supercycle-set Upper Zuni A) and TA-2 (of the supercycle-set TEJAS). These four 2nd order

476

cycles could be further distinguished into seven 3rd order cycles

477

RI PT

- By correlation with the global sea level cycle chart, the four identified depositional

478

the eustatic sea level curves. These boundaries are caused by an uplift of the study area in

479

response to the events of the Syrian Arc System and they display its main effect during the

480

SC

- The four supercycles are separated by three Type 1 sequence boundaries as correlated with

481

are:

482

•

483

Formation coinciding with the intra Turonian drop in the global sea level with the

484

initiation of the Syrian Arc inversion phase.

485

The Santonian/Upper Campanian unconformity (85 - ~75Ma.) coinciding with the

486

major inversion phase and the evolution of the doubly plunging anticlines.

487

The upper Campanian-Maastrichtian/Lower Eocene (SB3) unconformity (~68 -

488

~53Ma.) representing the last phase of the Syrian Arc inversion and the complete

489

EP

•

The Middle Turonian/Coniacian unconformity (~90-88.5Ma.) at the top of the Wata

TE D

•

M AN U

evolution of the Late Cretaceous-Early Paleogene sequences. The three sequence boundaries

missing of Paleocene successions.

490 491

AC C

ACKNOWLEDGEMENTS

The authors express their sincere thanks to Prof. Mohamed Darwish for his helpful

492

suggestions and the authors appreciate the valuable comments from Prof. Mohamed El

493

Sharkawi and Dr. Abdel Aal Ayyad. The thorough language revision of Dr. Mathew Wenner

494

and Dr. Jeffrey John are highly acknowledged.

495

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496

21

ACCEPTED MANUSCRIPT 497

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Guiraud, R., 1998. Mesozoic rifting and basin inversion along the northern African Tethyan

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margin: An overview, In: Macgregor, D.S., Moody, R.T.J., Clark-Lowes, D.D. (Eds.),

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Petroleum Geology of North Africa 132, 217-229.

609

Hamad, M. M., 2009. Biostratigraphy of the Late Paleocene-Early Eocene deposits of Gebel

610

El Bruk area, north central Sinai, Egypt. Egyptian Journal of Paleontology 9, 1-29.

611

Haq, B. U., 2014. Cretaceous eustasy revisited. Glob, Planet, Charge 113, 44-58.

612

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ACCEPTED MANUSCRIPT 613

Triassic. Science 235, 1156-1167.

614

Haq, B. U., Hardenbol, J., Vail, P. R., 1988. Mesozoic and Cenozoic chronostratigraphy and

615

cycles of sea-level change, In: Wilgus, C. K., Hastings, B. S., Kendall, C. G. S. C.,

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Haq, B. U., Hardenbol, J., Vail, P. R., 1987. Chronology of Fluctuating Sea Levels since the

Posementier, H. W., Ross, C. A., Van Wagoner, J. C. (Eds.), An Integrated Approach. Society

617

of Economic Palaeontologists and Mineralogists 42, 71-108.

618

SC

Harris, P. M.; Frost, S. H., Sieglie, G. A., Schneldermann, N., 1984. Regional unconformities

619 620

Interregional Unconformities and hydrocarbon accumulation. American Association of

621

M AN U

and depositional cycles, Cretaceous of the Arabian Peninsula, In: Schlee, J.S. (Ed.),

622

Hewaidy, A. A., Azab, M.M., Farouk, S., 2003. Ammonite biostratigraphy of the Upper

623

Cretaceous succession in the area west of Wadi Araba, northern western desert, Egypt.

624

Journal of Paleontology 3, 331-359.

625

TE D

Petroleum Geologists Memoir 36, 67-80.

626

paleoecology of west central Sinai, Egypt. Middle East Research Center, Ain Shams

627

University, Cairo, Earth Science Series 6, 139-150.

628

EP

Ismail, A. A., 1992. Maastrichtian-Early Eocene benthonic foraminiferal biostratigraphy and

629

Egypt based on ammonites. Newslett. Stratig. 25, 25-35.

630

AC C

Kassab, A. S., 1991. Cenomanian- Coniacian biostratigraphy of the northern eastern desert,

Kora, M., Genedi, A., 1995. Lithostratigraphy and Facies Development of Upper Cretaceous

631

Carbonates in east central Sinai, Egypt. Facies 32, 223-236.

632

Kuss, J., 1989. Facies and paleogeographic importance of the pre-rift limestone from NE-

633

Egypt/Sinai. Geologische Rundschau 78, 487-498.

634

Loeblich, A.R., Tappan, H., 1988. Foraminiferal genera and their classification. Van Nostrand

635

Reinhold, New York, 2 vols. (text vol. 970; Plates vol. 212 p. and 874 pl).

636

27

ACCEPTED MANUSCRIPT 637

Cretaceous of central east Sinai, Egypt. Cretaceous Research 19, 153-196.

638

Marsson, Th., 1878. Die Foraminiferen der weissen Schreibkreide der Insel Rügen,

639

Mitteilungen des Naturwissenschaftlichen Vereins für Neu-Vorpomnern und Rugen in

640

Greifswald 10, 115 – 196.

RI PT

Lüning, S., Marzouk, A. M., Morsi A. M., Kuss, J., 1998. Sequence stratigraphy of the Upper

641 642

Geological Society, London, Special Publications 341, 37–63.

643

SC

Moustafa, A. R., 2010. Structural setting and tectonic evolution of North Sinai folds, Egypt.

644

Sinai fold belts, In: Said, R. (Ed.), The Geology of Egypt, Balkema, Rotterdam, pp. 381–389.

645

M AN U

Moustafa, A. R., Khalil, M. H., 1990. Structural characteristics and tectonic evolution of north

Obaidalla, N. A., 2000. Planktonic foraminiferal biostratigraphy and turnover events during

646

the Late Cretaceous–Early Tertiary along the Red Sea Coast, Egypt. Journal of African Earth

647

Sciences 3/4 (31), 571-595.

648

TE D

Obaidalla, N. A., 2005. Complete Cretaceous/Paleogene (K/P) boundary section at Wadi

649 650

Revue de Paléobiologie, Genève 24 (1), 201-224.

651

Obaidalla, N. A., Kassab, A. S., 2002. Integrated biostratigraphy of the Coniacian–Santonian

652

EP

Nukhul, southwestern Sinai, Egypt: inference from planktic foraminiferal biostratigraphy.

653

Poag, C. W., Schlee, J. S., 1984. Depositional sequences and stratigraphic gaps on submerged

654

AC C

sequence, southwestern Sinai, Egypt. Egyptian Journal of Paleontology 2, 85–104.

United States Atlantic Margin., In: Schlee (Ed.), Interregional Unconformities and

655

Hydrocarbon Accumulation. American Association of Petroleum Geologists Memoir 36, 184.

656

Rabie, M. A., 2004. Stratigraphy of some Upper Cretaceous formations exposed in the Raha

657

Plateau, west central Sinai, Egypt. M.Sc. Thesis, Faculty of Science, Zagazig University, pp

658

275.

659

28

ACCEPTED MANUSCRIPT 660

Faculty of Science, Mansaura University, pp 247.

661

Samuel, M. D., Ismail, A. A., Akarish, A. I. M., Zaky, A. H., 2009. Upper Cretaceous

662

stratigraphy of the Gebel Somar area, north central Sinai, Egypt. Cretaceous Research 30 (1),

663

RI PT

Sallam, H. M., 2002. The Senonian macrofauna of west central Sinai, Egypt. M. Sc. Thesis,

22-34.

664 665

Shahin, A., 1988. Fossil fauna and stable isotopic composition within the Late Cretaceous –

666

SC

Sehim, A., 1993. Cretaceous Tectonics in Egypt. Egyptian Journal of Geology 37, 335-372.

667

Mansoura University, Mansoura , Egypt , 212 pp .

668

M AN U

Early Tertiary at Gebel Nezzazat, Sinai, Egypt. Unpublished PhD. Thesis, Faculty of Science,

669

Cretaceous from Zaire to Cameroon, In: Schlee, J. S. (Ed.), Interregional Unconformities and

670

Hydrocarbon Accumulation. American Association of Petroleum Geologists Memoir 36, 81-

671

88.

672

TE D

Sieglie, G. A., Barker, M. B., 1984. Relative sea-level changes during the Middle and Late

673

H.M., Saunders, J.B., Perch-Nielsen, K. (Eds.). Plankton Stratigraphy, Cambridge: Cambridge

674

University Press, pp. 87-154.

675

EP

Toumarkine, Luterbacher 1985. Paleocene and Eocene planktonic foraminifera, In: Bolli,

676

York, pp. 1-471.

677

AC C

Wilson, J. L., 1975. Carbonate Facies in Geologic History. Springer, Berlin Heidelberg, New

Ziko, A., Darwish, M., Eweda, S., 1993. Late Cretaceous-Early Tertiary stratigraphy of the

678

Themed area, east central Sinai, Egypt. Neues Jahrbuch für Geologie und Paläontologie,

679

Monatshefte 13, 135–149.

680

Figure captions:

681

Fig. (1) Simplified geologic and location map of the study areas, west-central Sinai, Egypt.

682

Fig. (2) The sedimentological characteristics, sequence stratigraphy and depositional

683

environments of the studied rock units at Wadi Raha, Sudr El-Hetan and Wadi El-Giddi.

684

29

ACCEPTED MANUSCRIPT Fig. (3) Stratigraphic distribution chart of the recorded foraminifera in Wadi Raha section.

685

Fig. (4) Stratigraphic distribution chart of the recorded foraminifera in Sudr El-Hetan section.

686

Fig. (5) Stratigraphic distribution chart of the recorded foraminifera in Wadi El-Giddi section.

687

Fig. (6)

688

1-2: Morozovella subbotinae; Sample 10, Wadi El-Giddi section, Waseiyit Formation, Early

689

RI PT

Eocene (museum number 906).

3-7: Globotruncana aegyptiaca; Sample 30, Wadi Raha section, Sudr Formation, Maastrichtian, (museum number 907).

8-10: Globotruncana arca; Sample 33, Wadi Raha section, Sudr Formation, Maastrichtian,

SC

(museum number 909).

11-13: Globotruncana cf. lapparenti; Sample 33, Wadi Raha section, Sudr Formation,

M AN U

Maastrichtian, (museum number 910).

14-16: Globotruncana bulloides; Sample 30, Wadi Raha Section, Sudr Formation, Maastrichtian, (museum number 911). Fig. (7)

1-2: Bolivinoides draco draco; Sample 34, Sudr El-Hetan section, Sudr Formation, Maastrichtian, (museum number 912).

TE D

3: Bolivina incrassata; Sample 44, Sudr El-Hetan section, Sudr Formation, Maastrichtian, (museum number 913).

4: Praebulimina sp.; Sample 40, Sudr El-Hetan section, Sudr Formation, Maastrichtian, (museum number 914).

EP

5 -7: Discorbis minutus; Sample 26, Wadi Raha section, Themed Formation, Coniacian/Santonian (museum number 915).

AC C

8: Heterohelix globulosa; Sample 30, Wadi Raha section, Sudr Formation, Maastrichtian, (museum number 916).

690 691 692 693 694 695 696 697 698 699 700 701 702 703 704 705 706 707 708 709

9:10: Gyroidinoides girardanus; Sample 42, Wadi Raha section, Sudr Formation, Maastrichtian, (museum number 917).

710 711

11: Nodosaria sp.; Sample 47, Wadi Raha section, Sudr Formation, Maastrichtian, (museum number 918).

712 713

12: Pseudotextularia elegans; Sample 3, Wadi El-Giddi section, Sudr Formation, Maastrichtian, (museum number 919).

714 715

30

ACCEPTED MANUSCRIPT 13-16: Gavelinella spp.; Sample 46, Wadi Raha Section, Sudr Formation, Maastrichtian, (museum number 920).

716 717 718

(1) Dolomitic lime-mudstone (MFT1), restricted shallow subtidal environments,Wata

719

Formation, Bed 1, Wadi Raha.

720

(2) Bioclastic wackestone (MFT2), open marine shallow subtidal, Wata Formation, Bed 1,

721

Wadi Raha.

722

RI PT

Fig. (8): Photomicrographs of microfacies:

(3) Bioclastic peloidal wackestone (MFT3), restricted shallow subtidal environments, the Wata

723

Formation, Bed 3, Sudr El-Hetan.

724 725

Formation, Bed 5, Wadi Raha.

726

SC

(4) Bioclastic foraminiferal wackestone (MFT4), open marine shallow subtidal, the Wata

Formation, Bed 9, Wadi Raha.

M AN U

(5) Dolomitic bioclastic wackestone (MFT5), open marine shallow subtidal, the Themed

727 728

(6) Bioclastic planktonic foraminiferal wackestone (MFT6), open marine deep subtidal, the Sudr

729

Formation, Bed 14, Wadi Raha.

730

(7) Bioclastic nummulitic wackestone (MFT7), open marine shallow subtidal, the Waseiyit

731

Formation, Bed 20, Wadi Raha.

732 733

the Themed Formation, Bed 10, Wadi Raha.

734

Fig. (9): Photomicrographs of microfacies:

735

(1) Bioclastic planktonic foraminiferal wacke/packstone (MFT9), open marine deep subtidal, the

736

Sudr Formation, Bed 15, Sudr El-Hetan.

737

(2) Bioclastic benthic foraminiferal wacke/packstone (MFT10), open marine shallow subtidal

738

environment, the Waseiyit Formation, Bed 3, Wadi Giddi.

739

(3) Foraminiferal peloidal packstone (MFT11), restricted shallow subtidal environments,, the

740

Wata Formation, Bed 1, Sudr El-Hetan.

741

(4) Intraclastic bioclastic packstone (MFT12), open marine shallow subtidal, the Wata

742

Formation, Bed 6, Sudr El-Hetan.

743

(5) Orbitulinid miliolidal bioclastic packstone (MFT13), restricted shallow subtidal, the Themed

744

Formation, Bed 8, Sudr El-Hetan.

745

(6) Echinoidal bioclastic packstone (MFT14), open marine shallow subtidal, the Themed

746

Formation, Bed 7, Wadi Raha.

747

AC C

EP

TE D

(8) Echinoidal bioclastic wacke/packstone (MFT8), open marine shallow subtidal environment,

31

ACCEPTED MANUSCRIPT 748

Raha.

749

(8) Sandy echinoidal bioclastic packstone (MFT16), open marine shallow subtidal, the Themed

750

Formation, Bed 14, Sudr El-Hetan.

751

Fig. (10): Photomicrographs of microfacies:

752

(1) Glauconitic intraclastic oolitic packstone (MFT17), shoals, the Themed Formation, Bed 11,

753

Wadi Raha.

754

RI PT

(7) Dolomitic bioclastic oolitic packstone (MFT15), shoals, the Themed Formation, Bed 8, Wadi

(2) Bioclastic planktonic foraminiferal packstone (MFT18), open marine deep subtidal, the Sudr

755

Formation, Bed 1, Wadi El-Giddi.

756 757

Formation, Bed 20, Sudr El-Hetan.

758

SC

(3) Nummulitic bioclastic packstone (MFT19), open marine shallow subtidal, the Waseiyit

Formation, Bed 3, Wadi El-Giddi.

M AN U

(4) Bioclastic foraminiferal packstone (MFT20), open marine shallow subtidal, the Waseiyit

759 760

(5) Intraclastic peloidal pack/grainstone (MFT21), open marine shallow subtidal, the Wata

761

Formation, Bed 4, Sudr El-Hetan.

762

(6) Bioclastic oolitic pack/grainstone (MFT22), shoals, the Themed Formation, Bed 12, Sudr El-

763

Hetan.

764 765

Themed Formation, Bed 12, Wadi Raha.

766

(8) Oncoidal bioclastic pack/grainstone (MFT24), shoals, the Themed Formation, Bed 12, Wadi

767

Raha.

768

TE D

(7) Algal bryozoan bioclastic pack/grainstone (MFT23), open marine shallow subtidal, the

769

(1) Bioclastic oolitic grainstone (MFT25), shoals, the Themed Formation, Bed 10, Sudr El-Hetan.

770

(2) Bioclastic foraminiferal peloidal grainstone (MFT26), open marine shallow subtidal, the

771

Waseiyit Formation, Bed 20, Wadi Raha.

772

(3) Dolomitic molluscan peloidal floatstone (MFT27), restricted shallow subtidal, the Wata

773

Formation, Bed 5, Sudr El-Hetan.

774

(4) Stromatoporoid framestone (MFT29), shoals, the Themed Formation, Bed 7, Sudr El-Hetan.

775

(5) Lime- bioclastic dolostone (MFT30), restricted shallow subtidal environment, the Wata

776

Formation, Bed 2, Wadi Raha.

777

Fig. (12) Unconformities, cyclicity and sequence stratigraphy of the Upper Cretaceous/Lower

778

Paleogene sequence at the studied area.

779

AC C

EP

Fig. (11): Photomicrographs of microfacies:

32

ACCEPTED MANUSCRIPT 780

of depositional sequence of the Upper Cretaceous/Lower Paleogene sequence in the present

781

area.

782

Table Caption:

783

Table (1) Different rock units proposed by different authors for the Upper Cretaceous/Lower

784

Paleogene sequence in central Sinai and the present study area.

785

RI PT

Fig. (13) Schematic cross section illustrating the maximum flooding surfaces and boundaries

786

environments and sequence stratigraphy of the Upper Cretaceous/Lower Paleogene sequence

787

in the study area.

788

AC C

EP

TE D

M AN U

SC

Table (2) Summary of the lithology, biozones, microfacies analysis, depositional

33

E

Galala Fm.

Unstudied

Abu Qada Fm.

Hiatus

Abu Qada Fm.

Dep. Seq

Super cycles

3rdorder cycles

ESQIV

TA2

Fm.

Waseiyit

Farouk & Faris (2012)

El-Fiky (2010) Abu Qada Fm.

UZA-4 UZA-3

3.3

UZA-2

MSQIII

Sudr Fm.

Tectonic uplift

4.5

2.6

4.4

CSSQII

Themed Fm.

Sudr Chalk

Themed Fm.

3.2

Wata Fm. Wata Fm.

TSQI

Sudr Chalk Matulla Fm. Wata Fm.

Wata Fm.

Sudr Chalk

Markha Chalk member

Matulla Fm.

Dakhla Fm.

Sudr Chalk

2.5

Garra Fm.

Wata Fm.

Abu Qada Fm.

Abu Zenima Chalk member

Wata Fm. Butum Fm.

Rock units

Esna Shale

M AN U

TE D

Wata Fm.

Matulla Fm.

EP

AC C

Wata Fm.

Sudr Chalk

Markha Chalk member

Matulla Fm.

Sudr Chalk

Sudr Chalk

Markha Chalk member

Abu Zenima Chalk member

Wata Fm.

L M

Abu Zenima Chalk member

Matulla Fm.

Themed Fm. (to north)

Markha Chalk member

Matulla Fm. (to south)

Coniacian/ Santonian

Campanian

Abu Zenima Chalk member

Sudr Chalk

Maastrichtian

Turonian

Esna Shale

Esna Shale

Beida Fm.

Tarawan Fm.

RI PT

Thebes Fm.

Present work

SC

E

Darat Fm Minia Fm Thebes Fm

Matulla Fm.

Samalut Fm.

Samuel et al. (2009)

Sudr Chalk

M

Paleocene

Eocene

Age

Lȕning et al. (1998)

Rabei (2004)

Kora & Genedi (1995)

West-Central Sinai Sallam (2002)

East-Central Sinai Ziko et al. (1993)

Cenomanian

ACCEPTED MANUSCRIPT NorthCentral Sinai

Faris & Farouk (2012)

Author

2.5

ACCEPTED MANUSCRIPT

TST HST Bolivina incrassat a

4.5

UZA-4

MSQIII

Sudr Fm.

Thick-bedding and massive. Thick-bedding and massive. Thick-bedding and massive. Thick bedding and massive. Thick-bedding and massive. Thick-bedding and massive Thick-bedding and massive. Thick-bedding.

Thick bedding.

MFT18: Bioclastic planktic foraminiferal packstone

Abundant bioclasts and biomorpha of planktic foraminifera; few bioclasts of mollusks and echinoids.

Thick-bedding.

MFT18: Bioclastic planktic foraminiferal packstone

Abundant planktic foraminifera and bioclasts of foraminifera, mollusks; some benthic foraminifera and glauconite grains.

Thick-bedding and massive.

Open marine deep subtidal

Open marine

Sedimentary features

Shoals

RI PT

EP

TE D

M AN U

SC

Abundant benthic foraminifera and fragments of mollusks, echinoids and serpulid worm tubes Abundant benthic foraminifera MFT19: Nummulitic bioclastic (nummulites, discocyclinids, operculinids); packstone some fragments of bivalves and echinoids. MFT10: Bioclastic Abundant benthic foraminifera and foraminiferal wacke/packstone fragments of mollusks and echinoids MFT4: Bioclastic Abundant fragments of mollusks and foraminiferal wackestone echinoids and benthic foraminifera. Abundant bioclasts of mollusks and MFT20: Bioclastic echinoids and benthic foraminifera; few foraminiferal packstone glauconitic grains MFT10:Bioclastic Abundant benthic foraminifera and foraminiferal wacke/packstone fragments of mollusks and echinoids. MFT20: Bioclastic Abundant bioclasts of mollusks and foraminiferal packstone echinoids and benthic foraminifera. Abundant bioclasts and biomorpha of MFT18: Bioclastic planktic planktic foraminifera; few bioclasts of foraminiferal packstone echinoids and glauconitic grains. MFT9: Bioclastic Abundant bioclasts and biomorpha of planktic foraminiferal planktic foraminifera. wacke/packstone

SQ3 Late Maastric htian

Main components

MFT10: Bioclastic foraminiferal wacke/packstone

AC C

Biozones Morozovella subbotinae

2.5

TA2

ESQIV

Waseiyit Fm.

HST

Nummulites spp.

Stratigraphic surfaces System tracts

3rd order cycles

Super cycles

Depositional sequence

Rock units

Age Early Eocene

MF S

Microfacies types (MFT)

Restricted

Depositional Environments Shallow subtidal

Sequence

ACCEPTED MANUSCRIPT

Abundant planktic foraminifera and bioclasts of foraminifera, mollusks; some benthic foraminifera and glauconite grains. Abundant bioclasts and biomorpha of planktic foraminifera; some benthic foraminifera (biserial, planispiral and rotaliids). Abundant planktic foraminifera and bioclasts of mollusks and foraminifera; few benthic foraminifera. Abundant planktic foraminifera and bioclasts of foraminifera, mollusks; some benthic foraminifera and glauconite grains. Abundant fragments of mollusks and echinoids; some planktic and benthic foraminifera and peloids. Abundant planktic foraminifera; some benthic foraminifera and bioclasts of foraminifera, mollusks and echinoids. Abundant biomorpha and bioclasts of planktic foraminifera; few bioclasts of mollusks, echinoids, and benthic foraminifera.

MFT14: Echinoidal Bioclastic packstone

Abundant fragments of echinoids and mollusks; some ostracods, bryozoans, planktic and benthic foraminiferal tests, peloids, intraclasts, quartz and glauconite grains.

Discorbis minutus

TST

SC

M AN U

TE D

EP

AC C

HST

TST Globotrunca na aegyptiaca

4.4 3.3

SQ2 UZA-3

Bolivinoides draco draco&Bolivina incrassata

HST TST

4.5 UZA-4

MSQIII

MFS

CSSQII

Sudr Fm.

Coniacian Santonian Themed Fm.

Late Campanian-Maastrichtian

MFS

Thick-bedding and massive. Thick bedding and massive. Thick bedding and massive. Thick-bedding and massive. Thick bedding and massive. Thick bedding, massive. Thick bedding and massive. Thin- to thick bedding, massive and bioturbation.

Open marine deep subtidal

MFT18: Bioclastic planktic foraminiferal packstone MFT9: Bioclastic planktic foraminiferal wacke/packstone MFT6: Bioclastic planktic foraminiferal wackestone MFT18: Bioclastic planktic foraminiferal packstone MFT4: Bioclastic foraminiferal wackestone MFT9: Bioclastic planktic foraminiferal wacke/packstone MFT6: Bioclastic planktic foraminiferal wackestone

SQ3

Thick-bedding.

Open marine

Abundant bioclasts and biomorpha of planktic foraminifera; few bioclasts of mollusks and echinoids and glauconitic grains.

RI PT

MFT18: Bioclastic planktic foraminiferal packstone

Sedimentary features

Shoals

Biozones

System tracts

Main components

TST Morozov ella subbotin ae

Stratigraphic surfaces

3rd order cycles 2.5

Super cycles TA2

Depositional sequence

Rock units Waseiyit Fm.

ESQIV

Age Early Eocene

Microfacies types (MFT)

Restricted

Depositional Environments Shallow subtidal

Sequence

ACCEPTED MANUSCRIPT

MFT29:Stromatoporoid framestone

Abundant stromatoporoids of Steineria sp. and Actinostromariania sp.; some gastropods.

SC

MFT1: Dolomitic limemudstone MFT13: Orbitulinid miliolid bioclastic packstone

Abundant fragments of echinoids and mollusks; some ostracods, bryozoans, planktic and benthic foraminiferal tests, peloids, intraclasts, quartz and glauconite grains. Abundant fragments of molluscan shells, echinoids and bryozoans and detrital quartz; few benthic and planktonic foraminifera, glauconite and phosphatic grains. Oysters, echinoids and gastropods. Abundant ooids and bioclasts of molluscan debris and echinoids; some intraclasts, benthic foraminiferal tests and bryozoans. Oysters, echinoids and gastropods. Abundant ooids and bioclasts of mollusks and echinoids; some benthic foraminiferal tests (planispiral and rotaliids) and intraclasts. Abundant ooids and bioclasts of mollusks and echinoids; some benthic foraminiferal tests, bryozoans, intraclasts and peloids. Few bioclasts of molluscan shells and echinoids; foraminiferal tests. Abundant benthic foraminifera (orbitolinids, miliolids and planispiral); few bioclasts of molluscan shells, intraclasts and peloids.

MFT14: Echinoidal Bioclastic packstone

3.3

TST

MFT16: Sandy echinoidal bioclastic packstone

SQ1

TE D

Calc. claystone MFT15: Dolomitic bioclastic oolitic packstone

EP

Discorbis minutus

MFT22: Bioclastic oolitic pack/grainstone

MFT25: Bioclastic oolitic grainstone

AC C

MFS

TST

3.2

HST

UZA-3

CSSQII

Themed Fm.

Coniacian-Santonian

Calc. claystone

Thin- to thick bedding, massive, and bioturbation. Thin-bedding. Lamination Thin- to medium bedding, burrowing Lamination medium bedding and burrowing. Thin-bedding. Thick-bedding, and burrowing Thin-bedding. Thick bedding, burrowing and bioturbation.

Open marine deep subtidal

Open marine

Sedimentary features

Shoals

RI PT

Main components

M AN U

Biozones

System tracts

Stratigraphic surfaces

3rd order cycles

Super cycles

Depositional sequence

Rock units

Age

Microfacies types (MFT)

Restricted

Depositional Environments Shallow subtidal

Sequence

ACCEPTED MANUSCRIPT

MFT27: Dolomitic molluscan peloidal floatstone

Abundant bioclasts of molluscan shells and echinoids and peloids.

MFT21: Intraclastic peloidal pack/grainstone MFT3: Bioclastic peloidal wackestone

Abundant peloids and intraclasts; some bioclasts of mollusks, echinoids and ammonites and benthic foraminiferal tests.

Calc. claystone MFT11: Foraminiferal peloidal packstone

Oysters Abundant peloids and benthic foraminifera (miliolids, orbitolinids and biserial); few fragments of molluscan shells, echinoids and ostracods

Abundant peloids; molluscan shells and echinoids.

thick bedding, burrowing and bioturbation. Thin- to thick bedding, burrowing. Thinbedding, bioturbation Medium bedding, bioturbation, burrowing Thick-bedding, massive. Thinbedding and bioturbation Thickbedding and massive Lamination Thick-bedding and massive

Open marine deep subtidal

Open marine

Sedimentary features

Shoals

RI PT

SC

Abundant bioclasts of molluscan shells, echinoids and ammonites; few benthic foraminiferal tests and intraclasts and peloids.

TE D

MFT2: Bioclastic wackestone

Abundant bioclasts of echinoids, ammonites and mollusks; few ostracods, bryozoans, benthic foraminifera, peloids and intraclasts. Abundant fragments of molluscan shells, echinoids, ammonites and intraclasts; few benthic foraminiferal tests and peloids.

EP

Choffaticeras segne

HST TST

2.5

Abundant stromatoporoids of Steineria sp. and Actinostromariania sp.; some gastropods.

AC C

HST TST

2.6 UZA-2

TSQI

Wata Fm.

Early-Middle Turonian

MFT29: Stromatoporoid framestone MFT8: Echinoidal bioclastic wacke/packstone MFT12: Intraclastic bioclastic packstone

MFS

MFS

Main components

M AN U

Biozones Discorbis minutus

System tracts TST

Stratigraphic surfaces

3rd order cycles 3.2

Super cycles UZA-3

Depositional sequence

Rock units Themed Fm.

CSSQII

Age ConiacianSantonian

SQ1

Microfacies types (MFT)

Restricted

Depositional Environments Shallow subtidal

Sequence

AC C

EP

TE D

M AN U

SC

RI PT

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AC C

EP

TE D

M AN U

SC

RI PT

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AC C

EP

TE D

M AN U

SC

RI PT

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AC C

EP

TE D

M AN U

SC

RI PT

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AC C

EP

TE D

M AN U

SC

RI PT

ACCEPTED MANUSCRIPT

AC C

EP

TE D

M AN U

SC

RI PT

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AC C

EP

TE D

M AN U

SC

RI PT

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AC C

EP

TE D

M AN U

SC

RI PT

ACCEPTED MANUSCRIPT

AC C

EP

TE D

M AN U

SC

RI PT

ACCEPTED MANUSCRIPT

AC C

EP

TE D

M AN U

SC

RI PT

ACCEPTED MANUSCRIPT

AC C

EP

TE D

M AN U

SC

RI PT

ACCEPTED MANUSCRIPT

AC C

EP

TE D

M AN U

SC

RI PT

ACCEPTED MANUSCRIPT

AC C

EP

TE D

M AN U

SC

RI PT

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Highlights

1- Bio- and sequence stratigraphy of Cretaceous/Paleogene sequence in central Sinai

RI PT

achieved. 2- Two planktonic foraminiferal zones and three benthic foraminiferal zones are identified. 3- Four depositional sequences separated by three sequence boundaries of type 1 are defined.

SC

4- The sequence was interrupted by erosion or non-deposition events related to the Syrian

AC C

EP

TE D

M AN U

Arc.