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Cenomanian-Turonian boundary in Wadi Watir, southeastern Sinai, Gulf of Aqaba, Egypt
Journal of African Earth Sciences, Vol. 15, No. 2, pp. 281-291, 1992.
0899-5362192 $5.00+0.00 © 1992 Pergamon Press Ltd
Printed in Great Britain
Cenomanian-Turonian boundary in Wadi Watir, Southeastern Sinai, Gulf of Aqaba, Egypt ORABX H. OghBI
Geology Department, Faculty of Science Menoufia University, Shiben E1-Kom, Egypt (First received 1st April, 1992; revised form received 26th June, 1992) Abstract - The foraminiferal content and microfacies characteristics of the Raha and Abu Qada Formations at WadiWarir (in which the mausoleum of the Sheikh Atria is located) in southeastern Sinai, Gulf of Aqaba are discussed and illustrated. They help identify sea level fluctuations, establish a stratigraphic subdivision and suggest a shallow marine facies and a Cenomanian age for the Raha Formation and deeper marine facies and Turonian age for the Abu Qada Formation. The Abu Had Member (lower part of the Raha Formation) yields mainly arenaceous foraminifera of early to middle Cenomanian with some calcareous forms. The Mukattab Member (middle part of the Raha Formation) comprises Nezzazatinae with very rare planktonic tests identified in thin sections of late Cenomanian. The upper part of the Raha Formation is the Ekma Member which yields no foraminifera and is predominantly a clastic sequence with some thin beds of limestone including oyster banks. From microfacies study, the Abu Qada Formation was deposited during a period of deepening of the sea, which was related to a global rise in sea level. It is more convenient to draw the boundary between Cenomanian and Turonian sequences where a new pelagic faunal assemblage is found to appear with the first appearance of Heterohelix reussi and Globotruncanids in the Abu Qada Formation rocks. The Cenomanianffuronian boundary in the Wadi Watir is correlated with similar rock units in Western Sinai, Palestine and Jordan.
c o n s i d e r e d h e r e is o v e r l a i n b y t h e W a t a F o r m a t i o n (middle Turonian) and underlain by the Malha F o r m a t i o n (Albian?) The identification of foraminifera in thin sections h e r e is b a s e d o n t h a t s h o w e d in S c h r o e d e r a n d N e u m a n n (1985).
INTRODUCTION
In the last three decades, the Cenomanian/ T u r o n i a n b o u n d a r y in E g y p t h a s b e e n t h e o b j e c t of numerous macro and micropalentological studies, mostly based on mega-invertebrates, planktonic and benthonic foraminifera. T h e r e is n o p u b l i c a t i o n o n t h e s t r a t i g r a p h y of t h e Cenomanian-Turonian r o c k s of s o u t h e r n Sinai. Most previous works were on northern and western Sinai except for a few on macro-fossils ( K o r a & H a m a m a , 1 9 8 7 a n d O r a b i , 1992). The present work presents foraminifera fauna recovered from the Raha and Abu Qada Formations at the Wadi Watir, southeastern Sinai, G u l f o f A q a b a (Fig. 1). T h e f o r a m i n f f e r a l c o n t e n t s i n thin sections or picked tests have helped to define more accurately the boundary between the Cenomanian and Turonian sequences which follows v e r t i c a l v a r i a t i o n s in t h e c o n d i t i o n s o f s e d i m e n t a t i o n of t h e s e d e p o s i t s . The studied exposures were compared with s i m i l a r o u t c r o p s in E g y p t , P a l e s t i n e a n d J o r d a n . T h e r o c k u n i t s a r e c l a s s i f i e d a f t e r C h e r i f e t aL (1989). T h e s e r o c k u n i t s a r e e a s y t o r e c o g n i z e i n the area under study. The stratigraphic sequence
REGIONAL
STRATIGRAPHY
T h e p r e s e n t a t i o n of r e g i o n a l p i c t u r e o f s e d i m e n t a t i o n a n d f a c i e s v a r i a t i o n s of t h e C r e t a c e o u s in Sinai seems to be a useful tool for understanding t h e s e c t i o n s t u d i e d in t h e p r e s e n t w o r k . Early
Cretaceous
and
Cenomanian
The Cretaceous trangressions started from the n o r t h , in t h e s o - c a l l e d M e s o z o i c N e o t e t h y s d u r i n g t h e A p t i a n , i n r e s p o n s e to w o r l d w i d e r i s e in s e a level (Vail e t aL, 1977). T h e o l d e s t C r e t a c e o u s r o c k s a r e r e f e r r e d to a n a l l u v i a l n e a r s h o r e e n v i r o n m e n t of t h e s o c a l l e d " N u b i a S a n d s t o n e . " T h e s e s a n d s t o nes were given different formation names: the Malha Formation in Sinai and northeastern Egypt ( A b d a l l a h a n d A d i n d a n i , 1963); t h e H a t i r a F o r m a t i o n i n P a l e s t i n e ( S h a w , 1947) a n d t h e K u r n u b S a n d s t o n e i n J o r d a n ( Q u e n n e l l , 1951).
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The C e n o m a n i a n s t r a t a r e p r e s e n t the first exposed m a r i n e beds of the Cretaceous period. This u n i t is n a m e d t h e Halal F o r m a t i o n in n o r t h e r n Sinai by Said (1971), the Raha Formation in west central Sinai by Ghorab (1961), the Hazera Formation in Palestine by Arkin a n d B r a u n (1965) a n d the Na'ur, Fuheis and H u m m a r Formations of J o r d a n by Masri (1963). The C e n o m a n i a n sedim e n t s are shallow m a r i n e marl, s a n d y marl a n d shales with n u m e r o u s oyster b a n k s characteristic of inner sublittoral to littoral sedimentation.
starts with deep m a r l s a n d shales yielding planktonic foraminifera (mainly Hoterohelicidae a n d some Globotruncanidae). This is the Abu Qada Formation of Sinai (Ghorab, 1961), the Ora Shales of P a l e s t i n e (Arkin a n d Braun, 1965) a n d tentatively Shuoib Formation of J o r d a n (Masri, 1963). Here it is interesting to observe t h a t the ammonite bed found in the marly limestone in m a n y parts of the Gulf of Suez, topped the C e n o m a n l a n succession a n d is the key to the C e n o m a n i a n / Turonian b o u n d a r y in Egypt (Said, 1962).
Turonian The T u r o n i a n is r e p r e s e n t e d in Sinai and the Gulf of Suez by two distinct formations: The Abu Qada a n d Wata Formations of early a n d late Turonian ages, respectively.
T h e W a t a F o r m a t i o n This f o r m a t i o n w a s established by Ghorab (1961). It is late Turonian in age and is coeval with the Gerofit Formation of Palestine {Eckstem a n d Rosenthal, In Hamaoul, 1966). The Wata Formation is a h a r d cllff-forming carbonate, conformably overlying the Ora Shales. Fig. 2 shows the relation of the m a i n C e n o m a n i a n / Turonian rock units in various regions in the facies belt discussed in this paper.
T h e A b u Qada F o r m a t i o n The T u r o n i a n above the inner sublittoral deposits of the C e n o m a n i a n in south-central Sinai and s o u t h e r n Palestine
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tina (Begia a s y n o n y m of Nezzazata) for the Middle Cretaceous boreholes near Basra, Iraq. Reiss ( 1957) recorded Nezzazata in late C e n o m a n i a n and posThe stratigraphy of the Cenomanian-Turonian sibly earliest Turonian age in Palestine. The microe x p o s u r e s in s o u t h e r n Sinai w a s referred to by paleontologists of the oil i n d u s t r y (Wasfi a n d several a u t h o r s working on localities of Egypt, Hataba, 1984) stated t h a t g e n u s Nezzazata exPalestine a n d J o r d a n . Several a u t h o r s b a s e d their t e n d s into the earliest Turonian rock and the Abu age a s s i g n m e n t o n m e g a - i n v e r t e b r a t e s (El Qada Formation is d i a c h r o n o u s with respect to the Nakkady, 1958; Said, 1982; Awad a n d Issawi, C e n o m a n i a n / T u r o n i a n time line. Ghorab (1961) identified in Ras Gharib off field 1975; Mazhar etal. 1979; Kassab, 1985; Kora and 'Thomasinella aegyptica fauna" including arenaH a m a m a , 1987) c e o u s forms (Nezzazata a n d F/abel/amtna) and Irving (1945) reported the occurrence of the calcareous form (Discorbis), along with typical ammonite b e d in the Galala El Qibliya and El Cenomanian oysters. Bahariya (Eastern Desert). These observations are In 1962, Ansary and others reported two foramit a k e n into consideration. Said (1962) mentioned nfferal zones in B a k r and Kareem oil fields at the t h a t the C e n o m a n i a n in m a n y parts of the Gulf of western side of Gulf of Suez: the u p p e r zone with Suez is topped b y a unit of yellowish marly limeThomasinella aegyptiaca, Nezzazata samples and stone rich in early Turonian ammonites (the sothe lower zone with Thomasinellafragmentario_ called ammonite bed). Ansary and Tewfik (1969) studied the Upper Kora and Hamama (1987) s t u d i e d the Cenomanian R a h a Formation at Ezz EI-Orban well C e n o m a n i a n / T u r o n i a n m e g a - i n v e r t e b r a t e s of Gebel Gunna, s o u t h e a s t e r n Sinai. They assigned and subdivided this formation into two zones: the their second zone Mammites nodosoides to the lower zone of ThomasineUafragmentaria and the early Turonian Wata Formation which lies con- u p p e r zone of Thomasinella punica. Both are very formably over the R a h a Formation neglecting the rich in a r e n a c e o u s forms with a few calcareous Abu Q a d a Formation of Ghorab (1961) in this area Discorbis sp. El Shinnawi and Sultan (1972) studied the Abu of s o u t h e a s t e m Sinai. The first detailed work on the biostratigraphy of H a d M e m b e r (lower m e m b e r of t h e R a h a C e n o m a n i a n b e n t h o n i c foraminifera in Egypt w a s Formation) in five marine wells drilled in the Gulf initiated by O m a r a (1956). He described Thomasi- of Suez. They assigned a late C e n o m a n i a n age to neUa aegyptla, T. fragmentaria, Cribrostomoides Thomasinellapunica zone which is confined to the slnaica, C. paralens a n d Nezzazata simplex as new Abu Had Member. Also the s a m e a u t h o r s in 1973, species from the C e n o m a n i a n deposits at Gebel identified and described Heterohelixglobulosafrom Nezzazat, W e s t e m Sinai. S m o u t (1956) also de- the Abu Qada Formation of lower Turonian and scribed the new genera Begia, Coxites and Rabani- Thomasinella punica from the Abu Had Member of PREVIOUS WORKS
284
ORABI H. ORABX
(1961). At Wadi Watir section it is a sequence of shales, calcareous sandstones, marls and thin beds of dolomltic limestone. The Abu Had Member yields no oyster banks. It Is 27.2 m thick and yields the following a r e n a c e o u s foraminifera: Thomasinella punica, T. fragmentaria, T. aegyptia, Haplophragmoides globosa, H. gilbertl, Ammomarginulina paterella, Ammobaculites impexus, A. agrestls, Dorothia oxycona, Marsonella trochus, Textularia rioensts, T. subconiea, Mayncina orbignyi, Spiroplectammina arabica, S. laevis, S. macfadyeni a n d S. obscura (picked tests constitute about 95 % of t h e total f a u n a ) . T h e c a l c a r e o u s t e s t s are represented by Discorbis minutus, D. beadnellt The presence of simple walled a r e n a c e o u s foraminfferal tests are affected by postmortem decalcification c a u s e d by the reducing conditions prevails b e n e a t h the superficial oxidized sediment layer in the e n v i r o n m e n t s in which t h e y lived. These reducing conditions induce organic decay, producing toxic s u b s t a n c e s and organic acids dissolving calcareous foraminfferal tests (Phleger, 1960, and Murray, 1967, 1973). The whole assemblage of foraminifera found In this rock unit suggests a C e n o m a n i a n age (Omara, 1956; Ansary et a / 1962; Ansary andTewfik, 1989; Schroeder and Neumann, 1985; Abdel-Kireem, 1988 and Cherif et al., 1989). The studied thin sections are from base to top: (a) Ferrigenous sandstone, the m a i n constituent, about 70 % is represented by s u b a n g u l a r to rounded quartz grains, c e m e n t e d by Iron oxide. This association is devoid of fossils and is represented by sample 2. It reflects a shallow marine nearshore environment within the littoral zone. (b) Glauconitic s a n d y mlcrite, glauconite, about 10 %, is represented by generally r o u n d e d m e d i u m grains, quartz constitutes about 30%, represented by s u b a n g u l a r to r o u n d e d grains. The presence of glauconite indicates conditions of slow sedimentation u n d e r reducing environment in waters of normal salinity (Cloud, 1955 & Krumbein and BIO AND LITHOFACIES Sloss, 1959). This observation coincides with the The stratigraphical range chart of the identified above discussion c o n c e r n i n g the p r e s e n c e of foraminiferal species is given in Fig. 3, including a r e n a c e o u s foraminiferal tests in reducing condithe most important microfossils recognized in thin tions. This association is r e p r e s e n t e d by sample 4. (c) Dolomitized micrite, t h e s e microfacles are sections. The lithologic characteristics and foraminfferal represented by samples 6, 8 and 10 and denote a assemblages of each stratlgraphic unit are dis- shallow marine condition. (d) Calcarenite, the m a i n constituent is representc u s s e d from the base to the top. ed by s u b a n g u l a r to r o u n d e d quartz grains, embedded in a microsparitic calcareous matrix. It Raha F o n ~ a t l o n (Cenomanlan) reflects a shallow marine near-shore environment. Ghorab (1961) established this rock unit. This This microfacies is represented by sample 12. f o r m a t i o n is subdivided into t h r e e m e m b e r s The Abu Had Member represents a relatively according to Cherif et al. (1989) as follows: shallow marine condition in the locality of Wadl Watir. This area also includes the highest proAbu Had Member (early-middle Cenomanlan) This m e m b e r was also established by Ghorab portion o f siliciclastic beds, a n d received a n
the Upper C e n o m a n i a n in the Gulf of Suez area. Here it is interestingly noted t h a t the presence of Heterohelix globulosa in the Abu Qada Formation indicates C a m p a n i a n age, w h e n Heterohelix reussi appears only in earlyTuronlan as defined by Caron {1985). Kerdany et aL (1973) described a C e n o m a n i a n foraminiferal assemblage from the area of Ain S u k h n a Western Coast, Gulf of Suez. Arenaceous species only are present, with the exception of Peneroplis turonicus a n d Discrobis turonicus belonging to a neritic environment. It is interesting to note t h a t Peneroplis turonicus is a s y n o n y m of Biconcava bentori Hamaoui & Saint Marc, 1970 (see SchrSeder and Neumann, 1985). In 1973, El D a k k a k studied the Cenomanian r o c k s at Gebel Nezzazat, W e s t e r n Sinai. He described two new lituolid genera; Ismailla a n d Sinainella. These genera show at least homeom o r p h i c r e s e m b l a n c e with the C e n o m a n i a n Hemicyclammina sigali Maync, 1953. L i t h o s t r a t i g r a p h i c a l s u b d i v i s i o n of t h e C e n o m a n i a n / T u r o n i a n in the s o u t h e r n part of the Suez region is mainly based on the work of Ghorab (1961). Also Bartov and Steinitz (1977) provided a lithostratigraphical scheme to link lithostratigraphic units of Sinaiwith those of Negev. In 1987, Al Rifaiy and Cherif studied the microfacies characteristic of the H a m m a r and Shueib F o r m a t i o n s in J o r d a n . They s u g g e s t e d a C e n o m a n i a n and shallow facies for the H u m m a r Formation a n d a T u r o n i a n age and deeper facies for the Shueib Formation. Recently, Cherif et a l (1989) subdivided the Conomanian Turonian succession of west-central Sinai into five rock units from base to top as follows: Abu Had, Mukattab and E k m a Members of the Raha Formation (Cenomanian), and the Abu Qada and Wata Formations which are of Turonian age.
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clastics from the s o u t h e r n elevated land m a s s (tidal fiat). Here, it is observed t h a t the late Cenomanian Mukattab Member increases in depth of the sea over the studied area. This s e e m s to be a reflection of relative highs of sea level graphs in n o r t h e m Europe and west of USA introduced by Hancock and Kauffman (1979), (Fig. 4) as well as a reflection Mukattab Member (late C e n o m a n i a n ) Cherif et of a global increase in depths of the sea, which a t (1989) introduced this subdivision of the Raha occurred some 95 Ma ago Haq etat (1987), (Fig. 5). Formation. In the studied area, it is a cliff-forming, These graphs and eustatic curve published by hard, predominantly calcareous sequence over- those a u t h o r s suggest a strong transgression in lying the Abu Had Member. The tops of these the early Turonian (Abu Qada Formation). limestones include oyster b a n k s mainly Gyrostrea delettrel, Ilymatogyra africana and Phynchostreon Abu Qada F o r m a t i o n (early Turonian) suborbiculata. The Mukattab Member is easy to Ghorab (1961) established this rock unit. In the trace across the area u n d e r s t u d y a n d in west- studied area, it is a sequence of shales and thin central Sinai due to its consistent and contrasting beds of limestones yielding oyster b a n k s and some h a r d calcareous lithologies. It reaches 30 m in casts of pelecypods. The middle part of this format h i c k n e s s a n d only its top yields: Trochospira tion (Sample 33 & 33*) yields early Turonian avenimelechi, Pseudorhipidionina casertana, ammonites (ChoffaHceras meslei and Ch. segne). Biconcava bentorl, Nezzazata simplex, N. convexa The Abu Qada Formation overlies conformably N. gyra, N. conica and Quinqueloculina cf. the E k m a Member. It is 38.25 m thick. The studied sandiegoensls as picked tests. In thin section, two thin section of sample 27 donates a foraminiferal microfacies types are recognized from base to top: biomicrite. It yields Heterohelixreussi, Hedbergella a) Foraminiferal biomicrite: The foraminiferal sp. and Nummofallotia apula. This microfacies faunae are represented by benthonic forms with indicates a relatively deep inner neritic environvery rare planktonic ones. This microfacies is m e n t (abundance of planktonic and relatively represented by samples 15" and 15"* which yield: frequent coiled hyaline benthonic foraminifera). Chrysalidina gradata, Nezzazata sp., PseudolituoThe presence of Heterohellx reussi in the foraminella reichell, Pseudorhapydionlna dubia, Textula- niferal assemblages of the Abu Qada Formation r/a sp., Trochospira avenimelechi, Massilina sp. suggests a Turonian age (see Caron, 1985). Also, and HedbergeUa sp. The whole assemblage of Said (1962) m e n t i o n s that at the Sheikh Attia area foraminifera found suggests a late C e n o m a n i a n the presence of ammonites in the lower part of the age (Neumann, 1967; Hamaoui and Saint-Marc, Abu Qada Formation suggests early Turonian age. 1970; S c h r o e d e r a n d N e u m a n n , 1985) a n d Bartov a n d Steinitz (1977) noticed t h a t the isodonates shallow marine deposition (inner sub- p a c h e o u s variation of the earlyTuronian Ora Shale littoral). The presence of a n appreciable a m o u n t of (equivalent to the Abu Qada Formation of Egypt planktonic foraminifera suggests sedimentation in and the Shueib Formation of Jordan) showed a deeper environment t h a n i n t h e A b u Had Member. markedly more erratic distribution t h a n that of the b) S a n d y shelly biomicrite, is composed of about older C e n o m a n i a n strata in Sinai and Negev. This 30% s u b a n g u l a r to r o u n d e d quartz grains and would suggest a change in the tectonic regime of some molluscal fragments. This microfacies is the region at the appearance of the Turonian age. represented by sample 17. It indicates deposition The Abu Qada Formation is characterized by in a shallow m a r i n e condition. abrupt proliferation of planktonic foraminifera, suggesting a n increase in depth of sea. The appearE k m a M e m b e r (late C e n o m a n i a n ) ance of a b u n d a n t Heterohelicidae, easy to detect in This subdivision of the Raha Formation was also microfacies, is a good criterion for determining the introduced by Cherif et aL (1989). At Wadi Watir b o u n d a r y b e t w e e n the R a h a a n d Abu Qada section, it is a sequence of shales, with thin lime- Formations. stone beds including oyster b a n k s and echinoid. This m e m b e r overlies t h e h a r d cliff-forming CONCLUSION Mukattab limestone. It is 24.4 m thick and yields no foraminifera as In west-central Sinai which was The analysis of the foraminiferal f a u n a of the studied by Cherif et at (1989). The E k m a Member Cenomanian-Turonian successions in the area of constitutes sediments laid down during m a r k e d Wadi Watir enables u s to determine the b o u n d a r y regressive episodes of the late C e n o m a n i a n sea a n d vertical changes in b a t h y m e t r y of the sea of receiving appreciable a m o u n t s of t e r r i g e n o u s these times. The following conclusions are made: appreciable a m o u n t of terrigenous material from the hinterland lying to the south. T h u s it c a n be stated t h a t in Wadi Watir section during the early and middle Cenomanian, the sea was always covering the area and the subsidence was active, where siliclastics a c c u m u l a t e d at a relatively high rate.
287
Ceaomanian-Turonianboundaryin Wadi Watir, SoutheasternSinai, Gulf of Aqaba, Egypt I) T h e C e n o m a n i a n R a h a F o r m a t i o n c a n b e s u b d i v i d e d into v a r i o u s r o c k u n i t s reflecting t h e m a j o r f l u c t u a t i o n in s e a levels e s t a b l i s h e d b y H a n c o c k a n d K a u f f m a n (1979), (Fig. 4} a n d H a q et aL (1987), (Fig. 5). T h e first t r a n s g r e s s i v e p h a s e of t h e s e a d u r i n g t h e C e n o m a n i a n time overlies t h e c o n t i n e n t a l M a l h a F o r m a t i o n is t h e A b u H a d M e m b e r (a s e q u e n c e of shales, c a l c a r e o u s s a n d s t o n e s a n d m a r l s with very a b u n d a n t a r e n a c e o u s foraminifera). T h e p e a k of this t r a n s g r e s s i o n is t h e M u k a t t a b M e m b e r (a c a l c a r e o u s u n i t rich in
Nezzazatinae). The regression of this cycle is the Ekma Member (a sequence of shales with thinbeds of limestone including oyster banks). This regressive phase is expressed by a slight drop in sea level m t h e e u s t a t i c c u r v e of H a q et al. (1987). 2) The early T u r o n i a n (Abu Q a d a Formation} s t a r t s with a n i n c r e a s e in t h e d e p t h of t h e s e a (presence of Heterahelix r e u s s l a n d HedbergeUa sp. in t h i n sections). This m a r i n e t r a n s g r e s s i o n m a y b e a reflection of t h e global rise of s e a level noticed m t h e early T u r o n i a n b y H a q et aL (1987)
Turonian 0 0',.
Cenomanian 0,-
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oE the USA
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o
Relative height of sea Fig. 4. The relative highs and lows of sea level in northern Europe and the western interior of the USA as defined by Hancock and Kauffman, 1979.
PLANKTONIC STAGES
FORAMINIFERAL ZONES
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ROCK UNITS
,~o,.
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.
Fig. 5. Correlation of the Cenomanian-Turonian sequence of the studied area with cycles of sea level changes as defined by Haq et al., 1987.
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.
-
. .
.
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288
ORABI H. ORABI
PLATE I I- Quinqueloculina sp. Mukattab Member of the Raha Formation (middle Cenomanian), equatorial section, sample 15", X 100. 2- Hedbergella sp. Abu Qada Formation (early Turonian), sample 27, X I00. 3- Heterohelix reussL Abu Qada Formation (earlyTuronian), long. axial section, sample 27, X 100. 4- HeteroheltrreussL Abu Qada Formation (earlyTuronian). long. section, sample 27, X 100. 5- Globotruncanidae (Dicarinella sp.) Abu Qada Formation (early Turonian), sample 27, X 100. 6- Pseuclolltuonella reicheIL Mukattab Member of the Raha formation (middle Cenomanian), longitudinal section, sample 15", X 50 7,8- Pseudorhapydionlna dubia. Mukattab Member of the Raha Formation (Middle Cenomanian), 7- oblique section, 8- equatorial section, sample 15", X 50, 100.
Cenomanian-Turonian boundary in Wadi Watir, Southeastern Sinai, Gulf of Aqaba, Egypt
PLATE 2
i - Miliolidae ( M a s s i l i n a sp.) Mukattab Member of the Raha Formation (middle Cenomanian), axial section, sample 15" X I00. 2 - Textulanidae. Mukattab Member of the Raha Formation (middle Cenomanian), long. axial section, sample 15"**, X 100. 3, 4 - C h r y s a l l d i m a g r a d a t a . Mukattab Member of the Raha Formation (middle Cenomanian), axial section, sample 15" X 100. 5 - N u m m o f a l l o t i a a p u l o . Abu Qada Formation (early Turonian), axial section, sample 27, X 50. 6 - T r o c h o s p i r a a v n i m e l e c h L Mukattab. Member of the Raha Formation (middle Cenomanian). subaxial section, sample 15", X 100.
289
ORABI H. ORABI
29O
a n d b y H a n c o c k a n d K a u f f m a n g r a p h s (1979). 3) The k e y h o r i z o n t h a t solves t h e C e n o m a v i a n / T u r o n i a n b o u n d a r y in t h e s t u d i e d a r e a is c h a r a c terized b y t h e a b r u p t proliferaUon of p l a n k t o n i c foraminifera, especially t h e first a p p e a r a n c e of Heleroheltx r e u s s i t h a t i n d i c a t e s early "I~ronian (see C a r o n 1985). T h i s biozone lies u n d e r t h e k e y h o r i z o n of a m m o n i t e b e d of Said (I 962) with a few meters. 4) The a b u n d a n c e of a r e n a c e o u s foraminiferal f a u n a in t h e A b u H a d M e m b e r a n d t h e p r e s e n c e of g l a u c o n i t e g r a i n s in t h e lower p a r t of t h i s m e m b e r i n d i c a t e r e d u c i n g c o n d i t i o n s prevailed b e n e a t h t h e superficial oxidized s e d i m e n t layer in t h e environm e n t s in w h i c h t h e y lived. T h e s e r e d u c i n g condit i o n s i n d u c e d organic d e c a y a n d organic acids which dissolved calcareous foraminifera. (Phleger, 1960. M u r r a y , 1967, 1973). 5) At t h e b a s e of t h e A b u Q a d a F o r m a t i o n , t h e planktonics are mostly Heterohelicidae. G l o b o t r u n c a n i d s o c c u r a l o n g w i t h Heterohelix reussiindicating e a r l y T u r o n i a n age (Caron, 1985). The d e e p e n i n g of t h e s e a n o t i c e d in Egypt a n d t h e time of d e p o s i t i o n of t h e Abu Q a d a F o r m a t i o n is very similar to t h a t recognized in J o r d a n a n d t h e time of d e p o s i t i o n of t h e S h u e i b F o r m a t i o n w h i c h yielded Heterohelicidae a n d Heluetoglobotruncana helvetica (AI Rifaiy a n d Cherif, 1987). It s e e m s t h a t t h i s d e e p e n i n g w a s d u e to t h e global rise in sea level w h i c h o c c u r r e d close to t h e C e n o m a n i a n / T u r o n i a n b o u n d a r y (Vail et al., 1977). REFERENCES AdaUah, A. M. and Adindanl, A. 1963. Stratigraphy of Upper Paleozolc rocks, western side of the Gulf of Suez. Geo/. Survey Egypt. Paper 25, 18p., Cairo. Abdel-Kireem, M. R. and Sultan, I. Z. 1988. Conomanian agglutinated foraminifera from Bahariya Oasis Western Desert, Egypt. Revue de Pal~obtologle 2, 259270, Gen~ve. Al Rffaiy, I. A. and Cherlf, O. H. 1987. Biostratlgraphic a s p e c t s a n d r e g i o n a l c o r r e l a t i o n of s o m e C e n o m a n i a n / T u r o n i a n e x p o s u r e s in J o r d a n . G~,ologle Mc~dltbrran~enne Tome XIV, 3, 181-193. Ansary, S. E., Andrawls, S. E. and Fahmy, S. E. 1962. Biostratigraphic studies of the Upper Cretaceous section in the G. P. C. wells in the Eastern Desert and Sinai. 4thArab Pet. Congr. 17, Beirut. 10 p. Ansary, S. E. and Tewfik, N. M. 1969. Biostratigraphy a n d time s t r a t i g r a p h y of s u b s u r f a c e Upper Cretaceous of Ezz El Orban area, Gulf of Suez region, U. A. R. Proceed. 3rd African MicropaL Colloq. Cairo, 95-106, 2 pl. Arkin, Y. and Braun, M. 1965. Type sections of Upper Cretaceous formations in the Northern Negev (Southern Israel), Geo/Surv. Israel, Stratigraphic Team 2, 19p.
Awad, G. H. and Issawi, B. 1975. Biostratigraphical zonation of Upper Cretaceous-Paleocene in Egypt. J. Geo/. 18, No. 2, 61-75. Bartov, Y. and Steintiz, G. 1977. The J u d e a and Mount Scopus Groups in the Negev and Sinai, wlth trend surface analysis of the thickness data. Isr. J. EarthScL 26, 119-148. Caron, M. 1985. Cretaceous planktonic foraminifera. In: Plankton stratigraphy (Edited by Bolli, H. M., Saunders, J. B. & Perch-Nielsen), 17-86, 37 figs. Cambridge. Cambridge Univ. press. Cherif, O. H., Al Rifaiy, I. A., Al Aflfl, F. I. and Orabi, H. O. 1989. Foraminiferal biostratigraphy and paleoecology of some Cenomanian-Turonian exposures in West-Central Sinai (Egypt) Revue de Micropal~o. 31, No. 4, 243-262, Paris. Cloud, P. E. Jr. 1955. Physical limits of glauconite formation. A. A. P. G. Bull 39, No 4, 484-492. El Dakkak, M. W. 1973. IsmatlaneumannaeGen. N. sp. de la famllle des Lituolidae du Cenomanian du DJebel Nezzazat, Sinai, Egypt. Rev. Micropal. 16, No 4, 173175. El Nakkady, S. E. 1958. StraUgraphical and petroleum geology of Egypt. Univ. of Assiut, Monograph No 1, Assiut. El Shinnawi, M. A. and Sultan, I. Z. 1972. BiostraUgraphy of some s u b s u r f a c e Upper Cretaceous sections in the Gulf of Suez area, Egypt. Addls-Abeba Vth. Afra. Collog on M~ro. 263-292, 1 pl. El- Shinnawi, M. A. and Sultan, I. Z. 1973. Lithostratigraphy of some subsurface Upper Cretaceous secUons in the Gulf of Suez area, Egypt. Acta GeoL Acad. Scl Hungar~cae 17, 4B9- 494, Budapest. Ghorab, M. ,~ 1961. Abnormal stratigraphic features in Ras Gharib oil field. 3rd Arab Petroleum Congr. 2, 1I0, Alexandria. Hamaoui, M. 1966. Microfossils from Cenomanian sections in the Negev, Geological Survey of Israel. Report PALl3/66,12p. Hamaoui, M. and Saint-Marc, P. 1970. Microfaune et microfacles du Cenomanien du Proche Orient. Bull Centre Rechu Pau, SNPA 4, 2, 257- 352. Hancock, J. M. and Kauffman, E. G. 1979. The great transgressions of the late Cretaceous. Geo/. Soc. Lond. 138, 175-186, 5 figs, 4 tables. Haq, B. U., Hardenbol, J. and Vail, P. R. 1987. Chronology of fluctuating sea levels since the Triassic. Science 235,1156-1167, New York. Irving, F. 1945. Report on a detailed reconnaissance of Wadi Araba (Gulf of Suez, West Cast). Unpublished report of A. E. O. C. Kassab, A. S. 1985. Palaeontological and stratigraphical studies of the Cretaceous sections in Wadi Qena and Wadi Tarfa, Eastern Desert, Egypt, Ph.D. thesis, Fac. Sc. Assiut Univ., Egypt, 221 p., Assiut. Kerdany, M. T., Eissa, R. A~ and Labib, F. 1973. Quelques foraminiferes Cenomanien de la pattie Ouest de la region du Oolfe de Suez, Egypt. Rev. M~'opaL 18, 2, 89-96, 1 pl. Kora, M. and Hamama, H. 1987. Biostratlgraphy of the Cenomanian-Turonian succession of Oebel Gunna, southeastern Sinai, Egypt. Bull. Fac. ScL Mansoura Univ. 14, No. 2, 288-301.
Cenomanian-Turonian boundary in Wadi Watir, Southeastern Sinai, Gulf of Aqaba, Egypt Krumbein, W. C. and Sloss, L. L. 1959. Stratigraphy and sedimentation. Freemann and Co., San-Francisco, California, 497. Masri, M. R. 1963, Report on the Amman-Zerka area. Central Water Authority, Jordan. Mazhar, A., Ennany, N. and Abdel Kader, Y. 1979. Contributions to the Cretaceous-EarlyTertiarystratigraphy of El Galala El Qibltya plateau. Ann. Geol. Survey, Egypt 9, 377-387, Cairo. Murray, J. W. 1967. Living foraminfferids of tidal marshes: a review. Journ. Forarn. Res. I, 153-16 I, New York. Murray, J. W. 1973. Distribution and ecology of living benthic foraminlferids. Heinemann Educ. Book, 274, London. Neumann, M. 1967. Manuel de mlcropal(.,ontologie des foraminlferes, 297 p., 182 text figs., 60 pls. GauthlerVlllars, Paris. Omara, S. 1956. N e w foraminifera from the Cenomanian
of Sinai, Egypt. doum. Paleont. 30, No. 4, 883-890, London. Orabi, O. H. 1992. Blostratigraphy and paleoecology of some Cenomanlan- early Turonlan exposures of Wadi Watir and Wadl Taba, southeastern Sinai, Egypt (in preparatkm). Phleger, F. B. 1960. Foraminifera] population in Laguna Madre, Texas. Sc/. Rep. Tohoku Univ., Spec. 4, 83-91, Tohoku.
291
QuenneU, A. M. 1951. The geology a n d mineral resources of (former) TransJordan. Co/onta/Geo/ogy and Mineral Resources 2, 85-115, London. Relss, Z 1957. Occurrence of Nezzazzata in Israel. Micropal. 3 (3), 259-262, 14 fig, I pl. Sald, R. 1962. The geology of Egypt 377, Elsevier Pub. Co., Amsterdam. Said. R. 1971. Explanatory notes to accompany the geological map of Egypt. Geol. Surv. F_,gyptPaper58, 123, Cairo, Schroeder, R. and Neumann, M. (editors) 1985. Les grands Foraminiferes du Cr~tace moyen de la r~gion m~diterran~'ene. ~ i o s , Mbm. Spec. 7, 156, Lyon. Shaw, S. H. 1947. Southern Palestine geological map on a scale of 1250,000 with explanatory note. Governmental Printer. Gov. of Palestlne 42, Jerusalem. Smout, A. H. 1956. Three new Cretaceous genera of foraminifera related to the Ceratobulimindae. MicrqOa£ 2, No 4, 335-348, 2 fig. 2 pl. Vail, P. 11., Mltchum, R. M. Jr. & Thompson, S. 1977. Seismic stratigraphy and global changes in sea level. Part 4: Global cycles of relative changes sea level. In: Payton, 1977, 127-35. Wasfi, S. and Hataba, H. 1984. Observations on the genus Nezzazata Omara and its significance to the Cenomanian-Turonian boundary in the Gulf of Suez. Benthos 83; 2nd Int. Syrup. Benthic Foraminifera (Pau, April 1983), 597-603, 2 fig., 1 tab., 2 pl.
0899-5362192 $5.00+0.00 © 1992 Pergamon Press Ltd
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Cenomanian-Turonian boundary in Wadi Watir, Southeastern Sinai, Gulf of Aqaba, Egypt ORABX H. OghBI
Geology Department, Faculty of Science Menoufia University, Shiben E1-Kom, Egypt (First received 1st April, 1992; revised form received 26th June, 1992) Abstract - The foraminiferal content and microfacies characteristics of the Raha and Abu Qada Formations at WadiWarir (in which the mausoleum of the Sheikh Atria is located) in southeastern Sinai, Gulf of Aqaba are discussed and illustrated. They help identify sea level fluctuations, establish a stratigraphic subdivision and suggest a shallow marine facies and a Cenomanian age for the Raha Formation and deeper marine facies and Turonian age for the Abu Qada Formation. The Abu Had Member (lower part of the Raha Formation) yields mainly arenaceous foraminifera of early to middle Cenomanian with some calcareous forms. The Mukattab Member (middle part of the Raha Formation) comprises Nezzazatinae with very rare planktonic tests identified in thin sections of late Cenomanian. The upper part of the Raha Formation is the Ekma Member which yields no foraminifera and is predominantly a clastic sequence with some thin beds of limestone including oyster banks. From microfacies study, the Abu Qada Formation was deposited during a period of deepening of the sea, which was related to a global rise in sea level. It is more convenient to draw the boundary between Cenomanian and Turonian sequences where a new pelagic faunal assemblage is found to appear with the first appearance of Heterohelix reussi and Globotruncanids in the Abu Qada Formation rocks. The Cenomanianffuronian boundary in the Wadi Watir is correlated with similar rock units in Western Sinai, Palestine and Jordan.
c o n s i d e r e d h e r e is o v e r l a i n b y t h e W a t a F o r m a t i o n (middle Turonian) and underlain by the Malha F o r m a t i o n (Albian?) The identification of foraminifera in thin sections h e r e is b a s e d o n t h a t s h o w e d in S c h r o e d e r a n d N e u m a n n (1985).
INTRODUCTION
In the last three decades, the Cenomanian/ T u r o n i a n b o u n d a r y in E g y p t h a s b e e n t h e o b j e c t of numerous macro and micropalentological studies, mostly based on mega-invertebrates, planktonic and benthonic foraminifera. T h e r e is n o p u b l i c a t i o n o n t h e s t r a t i g r a p h y of t h e Cenomanian-Turonian r o c k s of s o u t h e r n Sinai. Most previous works were on northern and western Sinai except for a few on macro-fossils ( K o r a & H a m a m a , 1 9 8 7 a n d O r a b i , 1992). The present work presents foraminifera fauna recovered from the Raha and Abu Qada Formations at the Wadi Watir, southeastern Sinai, G u l f o f A q a b a (Fig. 1). T h e f o r a m i n f f e r a l c o n t e n t s i n thin sections or picked tests have helped to define more accurately the boundary between the Cenomanian and Turonian sequences which follows v e r t i c a l v a r i a t i o n s in t h e c o n d i t i o n s o f s e d i m e n t a t i o n of t h e s e d e p o s i t s . The studied exposures were compared with s i m i l a r o u t c r o p s in E g y p t , P a l e s t i n e a n d J o r d a n . T h e r o c k u n i t s a r e c l a s s i f i e d a f t e r C h e r i f e t aL (1989). T h e s e r o c k u n i t s a r e e a s y t o r e c o g n i z e i n the area under study. The stratigraphic sequence
REGIONAL
STRATIGRAPHY
T h e p r e s e n t a t i o n of r e g i o n a l p i c t u r e o f s e d i m e n t a t i o n a n d f a c i e s v a r i a t i o n s of t h e C r e t a c e o u s in Sinai seems to be a useful tool for understanding t h e s e c t i o n s t u d i e d in t h e p r e s e n t w o r k . Early
Cretaceous
and
Cenomanian
The Cretaceous trangressions started from the n o r t h , in t h e s o - c a l l e d M e s o z o i c N e o t e t h y s d u r i n g t h e A p t i a n , i n r e s p o n s e to w o r l d w i d e r i s e in s e a level (Vail e t aL, 1977). T h e o l d e s t C r e t a c e o u s r o c k s a r e r e f e r r e d to a n a l l u v i a l n e a r s h o r e e n v i r o n m e n t of t h e s o c a l l e d " N u b i a S a n d s t o n e . " T h e s e s a n d s t o nes were given different formation names: the Malha Formation in Sinai and northeastern Egypt ( A b d a l l a h a n d A d i n d a n i , 1963); t h e H a t i r a F o r m a t i o n i n P a l e s t i n e ( S h a w , 1947) a n d t h e K u r n u b S a n d s t o n e i n J o r d a n ( Q u e n n e l l , 1951).
281
282
ORABI H. ORABI
The C e n o m a n i a n s t r a t a r e p r e s e n t the first exposed m a r i n e beds of the Cretaceous period. This u n i t is n a m e d t h e Halal F o r m a t i o n in n o r t h e r n Sinai by Said (1971), the Raha Formation in west central Sinai by Ghorab (1961), the Hazera Formation in Palestine by Arkin a n d B r a u n (1965) a n d the Na'ur, Fuheis and H u m m a r Formations of J o r d a n by Masri (1963). The C e n o m a n i a n sedim e n t s are shallow m a r i n e marl, s a n d y marl a n d shales with n u m e r o u s oyster b a n k s characteristic of inner sublittoral to littoral sedimentation.
starts with deep m a r l s a n d shales yielding planktonic foraminifera (mainly Hoterohelicidae a n d some Globotruncanidae). This is the Abu Qada Formation of Sinai (Ghorab, 1961), the Ora Shales of P a l e s t i n e (Arkin a n d Braun, 1965) a n d tentatively Shuoib Formation of J o r d a n (Masri, 1963). Here it is interesting to observe t h a t the ammonite bed found in the marly limestone in m a n y parts of the Gulf of Suez, topped the C e n o m a n l a n succession a n d is the key to the C e n o m a n i a n / Turonian b o u n d a r y in Egypt (Said, 1962).
Turonian The T u r o n i a n is r e p r e s e n t e d in Sinai and the Gulf of Suez by two distinct formations: The Abu Qada a n d Wata Formations of early a n d late Turonian ages, respectively.
T h e W a t a F o r m a t i o n This f o r m a t i o n w a s established by Ghorab (1961). It is late Turonian in age and is coeval with the Gerofit Formation of Palestine {Eckstem a n d Rosenthal, In Hamaoul, 1966). The Wata Formation is a h a r d cllff-forming carbonate, conformably overlying the Ora Shales. Fig. 2 shows the relation of the m a i n C e n o m a n i a n / Turonian rock units in various regions in the facies belt discussed in this paper.
T h e A b u Qada F o r m a t i o n The T u r o n i a n above the inner sublittoral deposits of the C e n o m a n i a n in south-central Sinai and s o u t h e r n Palestine
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Fig. 2. The relation of the main Cenomanlan/Turonlan rock units in Egypt, Palestine and Jordan (modified after A1 Rlfaly and Cherff, 1987)
tina (Begia a s y n o n y m of Nezzazata) for the Middle Cretaceous boreholes near Basra, Iraq. Reiss ( 1957) recorded Nezzazata in late C e n o m a n i a n and posThe stratigraphy of the Cenomanian-Turonian sibly earliest Turonian age in Palestine. The microe x p o s u r e s in s o u t h e r n Sinai w a s referred to by paleontologists of the oil i n d u s t r y (Wasfi a n d several a u t h o r s working on localities of Egypt, Hataba, 1984) stated t h a t g e n u s Nezzazata exPalestine a n d J o r d a n . Several a u t h o r s b a s e d their t e n d s into the earliest Turonian rock and the Abu age a s s i g n m e n t o n m e g a - i n v e r t e b r a t e s (El Qada Formation is d i a c h r o n o u s with respect to the Nakkady, 1958; Said, 1982; Awad a n d Issawi, C e n o m a n i a n / T u r o n i a n time line. Ghorab (1961) identified in Ras Gharib off field 1975; Mazhar etal. 1979; Kassab, 1985; Kora and 'Thomasinella aegyptica fauna" including arenaH a m a m a , 1987) c e o u s forms (Nezzazata a n d F/abel/amtna) and Irving (1945) reported the occurrence of the calcareous form (Discorbis), along with typical ammonite b e d in the Galala El Qibliya and El Cenomanian oysters. Bahariya (Eastern Desert). These observations are In 1962, Ansary and others reported two foramit a k e n into consideration. Said (1962) mentioned nfferal zones in B a k r and Kareem oil fields at the t h a t the C e n o m a n i a n in m a n y parts of the Gulf of western side of Gulf of Suez: the u p p e r zone with Suez is topped b y a unit of yellowish marly limeThomasinella aegyptiaca, Nezzazata samples and stone rich in early Turonian ammonites (the sothe lower zone with Thomasinellafragmentario_ called ammonite bed). Ansary and Tewfik (1969) studied the Upper Kora and Hamama (1987) s t u d i e d the Cenomanian R a h a Formation at Ezz EI-Orban well C e n o m a n i a n / T u r o n i a n m e g a - i n v e r t e b r a t e s of Gebel Gunna, s o u t h e a s t e r n Sinai. They assigned and subdivided this formation into two zones: the their second zone Mammites nodosoides to the lower zone of ThomasineUafragmentaria and the early Turonian Wata Formation which lies con- u p p e r zone of Thomasinella punica. Both are very formably over the R a h a Formation neglecting the rich in a r e n a c e o u s forms with a few calcareous Abu Q a d a Formation of Ghorab (1961) in this area Discorbis sp. El Shinnawi and Sultan (1972) studied the Abu of s o u t h e a s t e m Sinai. The first detailed work on the biostratigraphy of H a d M e m b e r (lower m e m b e r of t h e R a h a C e n o m a n i a n b e n t h o n i c foraminifera in Egypt w a s Formation) in five marine wells drilled in the Gulf initiated by O m a r a (1956). He described Thomasi- of Suez. They assigned a late C e n o m a n i a n age to neUa aegyptla, T. fragmentaria, Cribrostomoides Thomasinellapunica zone which is confined to the slnaica, C. paralens a n d Nezzazata simplex as new Abu Had Member. Also the s a m e a u t h o r s in 1973, species from the C e n o m a n i a n deposits at Gebel identified and described Heterohelixglobulosafrom Nezzazat, W e s t e m Sinai. S m o u t (1956) also de- the Abu Qada Formation of lower Turonian and scribed the new genera Begia, Coxites and Rabani- Thomasinella punica from the Abu Had Member of PREVIOUS WORKS
284
ORABI H. ORABX
(1961). At Wadi Watir section it is a sequence of shales, calcareous sandstones, marls and thin beds of dolomltic limestone. The Abu Had Member yields no oyster banks. It Is 27.2 m thick and yields the following a r e n a c e o u s foraminifera: Thomasinella punica, T. fragmentaria, T. aegyptia, Haplophragmoides globosa, H. gilbertl, Ammomarginulina paterella, Ammobaculites impexus, A. agrestls, Dorothia oxycona, Marsonella trochus, Textularia rioensts, T. subconiea, Mayncina orbignyi, Spiroplectammina arabica, S. laevis, S. macfadyeni a n d S. obscura (picked tests constitute about 95 % of t h e total f a u n a ) . T h e c a l c a r e o u s t e s t s are represented by Discorbis minutus, D. beadnellt The presence of simple walled a r e n a c e o u s foraminfferal tests are affected by postmortem decalcification c a u s e d by the reducing conditions prevails b e n e a t h the superficial oxidized sediment layer in the e n v i r o n m e n t s in which t h e y lived. These reducing conditions induce organic decay, producing toxic s u b s t a n c e s and organic acids dissolving calcareous foraminfferal tests (Phleger, 1960, and Murray, 1967, 1973). The whole assemblage of foraminifera found In this rock unit suggests a C e n o m a n i a n age (Omara, 1956; Ansary et a / 1962; Ansary andTewfik, 1989; Schroeder and Neumann, 1985; Abdel-Kireem, 1988 and Cherif et al., 1989). The studied thin sections are from base to top: (a) Ferrigenous sandstone, the m a i n constituent, about 70 % is represented by s u b a n g u l a r to rounded quartz grains, c e m e n t e d by Iron oxide. This association is devoid of fossils and is represented by sample 2. It reflects a shallow marine nearshore environment within the littoral zone. (b) Glauconitic s a n d y mlcrite, glauconite, about 10 %, is represented by generally r o u n d e d m e d i u m grains, quartz constitutes about 30%, represented by s u b a n g u l a r to r o u n d e d grains. The presence of glauconite indicates conditions of slow sedimentation u n d e r reducing environment in waters of normal salinity (Cloud, 1955 & Krumbein and BIO AND LITHOFACIES Sloss, 1959). This observation coincides with the The stratigraphical range chart of the identified above discussion c o n c e r n i n g the p r e s e n c e of foraminiferal species is given in Fig. 3, including a r e n a c e o u s foraminiferal tests in reducing condithe most important microfossils recognized in thin tions. This association is r e p r e s e n t e d by sample 4. (c) Dolomitized micrite, t h e s e microfacles are sections. The lithologic characteristics and foraminfferal represented by samples 6, 8 and 10 and denote a assemblages of each stratlgraphic unit are dis- shallow marine condition. (d) Calcarenite, the m a i n constituent is representc u s s e d from the base to the top. ed by s u b a n g u l a r to r o u n d e d quartz grains, embedded in a microsparitic calcareous matrix. It Raha F o n ~ a t l o n (Cenomanlan) reflects a shallow marine near-shore environment. Ghorab (1961) established this rock unit. This This microfacies is represented by sample 12. f o r m a t i o n is subdivided into t h r e e m e m b e r s The Abu Had Member represents a relatively according to Cherif et al. (1989) as follows: shallow marine condition in the locality of Wadl Watir. This area also includes the highest proAbu Had Member (early-middle Cenomanlan) This m e m b e r was also established by Ghorab portion o f siliciclastic beds, a n d received a n
the Upper C e n o m a n i a n in the Gulf of Suez area. Here it is interestingly noted t h a t the presence of Heterohelix globulosa in the Abu Qada Formation indicates C a m p a n i a n age, w h e n Heterohelix reussi appears only in earlyTuronlan as defined by Caron {1985). Kerdany et aL (1973) described a C e n o m a n i a n foraminiferal assemblage from the area of Ain S u k h n a Western Coast, Gulf of Suez. Arenaceous species only are present, with the exception of Peneroplis turonicus a n d Discrobis turonicus belonging to a neritic environment. It is interesting to note t h a t Peneroplis turonicus is a s y n o n y m of Biconcava bentori Hamaoui & Saint Marc, 1970 (see SchrSeder and Neumann, 1985). In 1973, El D a k k a k studied the Cenomanian r o c k s at Gebel Nezzazat, W e s t e r n Sinai. He described two new lituolid genera; Ismailla a n d Sinainella. These genera show at least homeom o r p h i c r e s e m b l a n c e with the C e n o m a n i a n Hemicyclammina sigali Maync, 1953. L i t h o s t r a t i g r a p h i c a l s u b d i v i s i o n of t h e C e n o m a n i a n / T u r o n i a n in the s o u t h e r n part of the Suez region is mainly based on the work of Ghorab (1961). Also Bartov and Steinitz (1977) provided a lithostratigraphical scheme to link lithostratigraphic units of Sinaiwith those of Negev. In 1987, Al Rifaiy and Cherif studied the microfacies characteristic of the H a m m a r and Shueib F o r m a t i o n s in J o r d a n . They s u g g e s t e d a C e n o m a n i a n and shallow facies for the H u m m a r Formation a n d a T u r o n i a n age and deeper facies for the Shueib Formation. Recently, Cherif et a l (1989) subdivided the Conomanian Turonian succession of west-central Sinai into five rock units from base to top as follows: Abu Had, Mukattab and E k m a Members of the Raha Formation (Cenomanian), and the Abu Qada and Wata Formations which are of Turonian age.
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clastics from the s o u t h e r n elevated land m a s s (tidal fiat). Here, it is observed t h a t the late Cenomanian Mukattab Member increases in depth of the sea over the studied area. This s e e m s to be a reflection of relative highs of sea level graphs in n o r t h e m Europe and west of USA introduced by Hancock and Kauffman (1979), (Fig. 4) as well as a reflection Mukattab Member (late C e n o m a n i a n ) Cherif et of a global increase in depths of the sea, which a t (1989) introduced this subdivision of the Raha occurred some 95 Ma ago Haq etat (1987), (Fig. 5). Formation. In the studied area, it is a cliff-forming, These graphs and eustatic curve published by hard, predominantly calcareous sequence over- those a u t h o r s suggest a strong transgression in lying the Abu Had Member. The tops of these the early Turonian (Abu Qada Formation). limestones include oyster b a n k s mainly Gyrostrea delettrel, Ilymatogyra africana and Phynchostreon Abu Qada F o r m a t i o n (early Turonian) suborbiculata. The Mukattab Member is easy to Ghorab (1961) established this rock unit. In the trace across the area u n d e r s t u d y a n d in west- studied area, it is a sequence of shales and thin central Sinai due to its consistent and contrasting beds of limestones yielding oyster b a n k s and some h a r d calcareous lithologies. It reaches 30 m in casts of pelecypods. The middle part of this format h i c k n e s s a n d only its top yields: Trochospira tion (Sample 33 & 33*) yields early Turonian avenimelechi, Pseudorhipidionina casertana, ammonites (ChoffaHceras meslei and Ch. segne). Biconcava bentorl, Nezzazata simplex, N. convexa The Abu Qada Formation overlies conformably N. gyra, N. conica and Quinqueloculina cf. the E k m a Member. It is 38.25 m thick. The studied sandiegoensls as picked tests. In thin section, two thin section of sample 27 donates a foraminiferal microfacies types are recognized from base to top: biomicrite. It yields Heterohelixreussi, Hedbergella a) Foraminiferal biomicrite: The foraminiferal sp. and Nummofallotia apula. This microfacies faunae are represented by benthonic forms with indicates a relatively deep inner neritic environvery rare planktonic ones. This microfacies is m e n t (abundance of planktonic and relatively represented by samples 15" and 15"* which yield: frequent coiled hyaline benthonic foraminifera). Chrysalidina gradata, Nezzazata sp., PseudolituoThe presence of Heterohellx reussi in the foraminella reichell, Pseudorhapydionlna dubia, Textula- niferal assemblages of the Abu Qada Formation r/a sp., Trochospira avenimelechi, Massilina sp. suggests a Turonian age (see Caron, 1985). Also, and HedbergeUa sp. The whole assemblage of Said (1962) m e n t i o n s that at the Sheikh Attia area foraminifera found suggests a late C e n o m a n i a n the presence of ammonites in the lower part of the age (Neumann, 1967; Hamaoui and Saint-Marc, Abu Qada Formation suggests early Turonian age. 1970; S c h r o e d e r a n d N e u m a n n , 1985) a n d Bartov a n d Steinitz (1977) noticed t h a t the isodonates shallow marine deposition (inner sub- p a c h e o u s variation of the earlyTuronian Ora Shale littoral). The presence of a n appreciable a m o u n t of (equivalent to the Abu Qada Formation of Egypt planktonic foraminifera suggests sedimentation in and the Shueib Formation of Jordan) showed a deeper environment t h a n i n t h e A b u Had Member. markedly more erratic distribution t h a n that of the b) S a n d y shelly biomicrite, is composed of about older C e n o m a n i a n strata in Sinai and Negev. This 30% s u b a n g u l a r to r o u n d e d quartz grains and would suggest a change in the tectonic regime of some molluscal fragments. This microfacies is the region at the appearance of the Turonian age. represented by sample 17. It indicates deposition The Abu Qada Formation is characterized by in a shallow m a r i n e condition. abrupt proliferation of planktonic foraminifera, suggesting a n increase in depth of sea. The appearE k m a M e m b e r (late C e n o m a n i a n ) ance of a b u n d a n t Heterohelicidae, easy to detect in This subdivision of the Raha Formation was also microfacies, is a good criterion for determining the introduced by Cherif et aL (1989). At Wadi Watir b o u n d a r y b e t w e e n the R a h a a n d Abu Qada section, it is a sequence of shales, with thin lime- Formations. stone beds including oyster b a n k s and echinoid. This m e m b e r overlies t h e h a r d cliff-forming CONCLUSION Mukattab limestone. It is 24.4 m thick and yields no foraminifera as In west-central Sinai which was The analysis of the foraminiferal f a u n a of the studied by Cherif et at (1989). The E k m a Member Cenomanian-Turonian successions in the area of constitutes sediments laid down during m a r k e d Wadi Watir enables u s to determine the b o u n d a r y regressive episodes of the late C e n o m a n i a n sea a n d vertical changes in b a t h y m e t r y of the sea of receiving appreciable a m o u n t s of t e r r i g e n o u s these times. The following conclusions are made: appreciable a m o u n t of terrigenous material from the hinterland lying to the south. T h u s it c a n be stated t h a t in Wadi Watir section during the early and middle Cenomanian, the sea was always covering the area and the subsidence was active, where siliclastics a c c u m u l a t e d at a relatively high rate.
287
Ceaomanian-Turonianboundaryin Wadi Watir, SoutheasternSinai, Gulf of Aqaba, Egypt I) T h e C e n o m a n i a n R a h a F o r m a t i o n c a n b e s u b d i v i d e d into v a r i o u s r o c k u n i t s reflecting t h e m a j o r f l u c t u a t i o n in s e a levels e s t a b l i s h e d b y H a n c o c k a n d K a u f f m a n (1979), (Fig. 4} a n d H a q et aL (1987), (Fig. 5). T h e first t r a n s g r e s s i v e p h a s e of t h e s e a d u r i n g t h e C e n o m a n i a n time overlies t h e c o n t i n e n t a l M a l h a F o r m a t i o n is t h e A b u H a d M e m b e r (a s e q u e n c e of shales, c a l c a r e o u s s a n d s t o n e s a n d m a r l s with very a b u n d a n t a r e n a c e o u s foraminifera). T h e p e a k of this t r a n s g r e s s i o n is t h e M u k a t t a b M e m b e r (a c a l c a r e o u s u n i t rich in
Nezzazatinae). The regression of this cycle is the Ekma Member (a sequence of shales with thinbeds of limestone including oyster banks). This regressive phase is expressed by a slight drop in sea level m t h e e u s t a t i c c u r v e of H a q et al. (1987). 2) The early T u r o n i a n (Abu Q a d a Formation} s t a r t s with a n i n c r e a s e in t h e d e p t h of t h e s e a (presence of Heterahelix r e u s s l a n d HedbergeUa sp. in t h i n sections). This m a r i n e t r a n s g r e s s i o n m a y b e a reflection of t h e global rise of s e a level noticed m t h e early T u r o n i a n b y H a q et aL (1987)
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288
ORABI H. ORABI
PLATE I I- Quinqueloculina sp. Mukattab Member of the Raha Formation (middle Cenomanian), equatorial section, sample 15", X 100. 2- Hedbergella sp. Abu Qada Formation (early Turonian), sample 27, X I00. 3- Heterohelix reussL Abu Qada Formation (earlyTuronian), long. axial section, sample 27, X 100. 4- HeteroheltrreussL Abu Qada Formation (earlyTuronian). long. section, sample 27, X 100. 5- Globotruncanidae (Dicarinella sp.) Abu Qada Formation (early Turonian), sample 27, X 100. 6- Pseuclolltuonella reicheIL Mukattab Member of the Raha formation (middle Cenomanian), longitudinal section, sample 15", X 50 7,8- Pseudorhapydionlna dubia. Mukattab Member of the Raha Formation (Middle Cenomanian), 7- oblique section, 8- equatorial section, sample 15", X 50, 100.
Cenomanian-Turonian boundary in Wadi Watir, Southeastern Sinai, Gulf of Aqaba, Egypt
PLATE 2
i - Miliolidae ( M a s s i l i n a sp.) Mukattab Member of the Raha Formation (middle Cenomanian), axial section, sample 15" X I00. 2 - Textulanidae. Mukattab Member of the Raha Formation (middle Cenomanian), long. axial section, sample 15"**, X 100. 3, 4 - C h r y s a l l d i m a g r a d a t a . Mukattab Member of the Raha Formation (middle Cenomanian), axial section, sample 15" X 100. 5 - N u m m o f a l l o t i a a p u l o . Abu Qada Formation (early Turonian), axial section, sample 27, X 50. 6 - T r o c h o s p i r a a v n i m e l e c h L Mukattab. Member of the Raha Formation (middle Cenomanian). subaxial section, sample 15", X 100.
289
ORABI H. ORABI
29O
a n d b y H a n c o c k a n d K a u f f m a n g r a p h s (1979). 3) The k e y h o r i z o n t h a t solves t h e C e n o m a v i a n / T u r o n i a n b o u n d a r y in t h e s t u d i e d a r e a is c h a r a c terized b y t h e a b r u p t proliferaUon of p l a n k t o n i c foraminifera, especially t h e first a p p e a r a n c e of Heleroheltx r e u s s i t h a t i n d i c a t e s early "I~ronian (see C a r o n 1985). T h i s biozone lies u n d e r t h e k e y h o r i z o n of a m m o n i t e b e d of Said (I 962) with a few meters. 4) The a b u n d a n c e of a r e n a c e o u s foraminiferal f a u n a in t h e A b u H a d M e m b e r a n d t h e p r e s e n c e of g l a u c o n i t e g r a i n s in t h e lower p a r t of t h i s m e m b e r i n d i c a t e r e d u c i n g c o n d i t i o n s prevailed b e n e a t h t h e superficial oxidized s e d i m e n t layer in t h e environm e n t s in w h i c h t h e y lived. T h e s e r e d u c i n g condit i o n s i n d u c e d organic d e c a y a n d organic acids which dissolved calcareous foraminifera. (Phleger, 1960. M u r r a y , 1967, 1973). 5) At t h e b a s e of t h e A b u Q a d a F o r m a t i o n , t h e planktonics are mostly Heterohelicidae. G l o b o t r u n c a n i d s o c c u r a l o n g w i t h Heterohelix reussiindicating e a r l y T u r o n i a n age (Caron, 1985). The d e e p e n i n g of t h e s e a n o t i c e d in Egypt a n d t h e time of d e p o s i t i o n of t h e Abu Q a d a F o r m a t i o n is very similar to t h a t recognized in J o r d a n a n d t h e time of d e p o s i t i o n of t h e S h u e i b F o r m a t i o n w h i c h yielded Heterohelicidae a n d Heluetoglobotruncana helvetica (AI Rifaiy a n d Cherif, 1987). It s e e m s t h a t t h i s d e e p e n i n g w a s d u e to t h e global rise in sea level w h i c h o c c u r r e d close to t h e C e n o m a n i a n / T u r o n i a n b o u n d a r y (Vail et al., 1977). REFERENCES AdaUah, A. M. and Adindanl, A. 1963. Stratigraphy of Upper Paleozolc rocks, western side of the Gulf of Suez. Geo/. Survey Egypt. Paper 25, 18p., Cairo. Abdel-Kireem, M. R. and Sultan, I. Z. 1988. Conomanian agglutinated foraminifera from Bahariya Oasis Western Desert, Egypt. Revue de Pal~obtologle 2, 259270, Gen~ve. Al Rffaiy, I. A. and Cherlf, O. H. 1987. Biostratlgraphic a s p e c t s a n d r e g i o n a l c o r r e l a t i o n of s o m e C e n o m a n i a n / T u r o n i a n e x p o s u r e s in J o r d a n . G~,ologle Mc~dltbrran~enne Tome XIV, 3, 181-193. Ansary, S. E., Andrawls, S. E. and Fahmy, S. E. 1962. Biostratigraphic studies of the Upper Cretaceous section in the G. P. C. wells in the Eastern Desert and Sinai. 4thArab Pet. Congr. 17, Beirut. 10 p. Ansary, S. E. and Tewfik, N. M. 1969. Biostratigraphy a n d time s t r a t i g r a p h y of s u b s u r f a c e Upper Cretaceous of Ezz El Orban area, Gulf of Suez region, U. A. R. Proceed. 3rd African MicropaL Colloq. Cairo, 95-106, 2 pl. Arkin, Y. and Braun, M. 1965. Type sections of Upper Cretaceous formations in the Northern Negev (Southern Israel), Geo/Surv. Israel, Stratigraphic Team 2, 19p.
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Cenomanian-Turonian boundary in Wadi Watir, Southeastern Sinai, Gulf of Aqaba, Egypt Krumbein, W. C. and Sloss, L. L. 1959. Stratigraphy and sedimentation. Freemann and Co., San-Francisco, California, 497. Masri, M. R. 1963, Report on the Amman-Zerka area. Central Water Authority, Jordan. Mazhar, A., Ennany, N. and Abdel Kader, Y. 1979. Contributions to the Cretaceous-EarlyTertiarystratigraphy of El Galala El Qibltya plateau. Ann. Geol. Survey, Egypt 9, 377-387, Cairo. Murray, J. W. 1967. Living foraminfferids of tidal marshes: a review. Journ. Forarn. Res. I, 153-16 I, New York. Murray, J. W. 1973. Distribution and ecology of living benthic foraminlferids. Heinemann Educ. Book, 274, London. Neumann, M. 1967. Manuel de mlcropal(.,ontologie des foraminlferes, 297 p., 182 text figs., 60 pls. GauthlerVlllars, Paris. Omara, S. 1956. N e w foraminifera from the Cenomanian
of Sinai, Egypt. doum. Paleont. 30, No. 4, 883-890, London. Orabi, O. H. 1992. Blostratigraphy and paleoecology of some Cenomanlan- early Turonlan exposures of Wadi Watir and Wadl Taba, southeastern Sinai, Egypt (in preparatkm). Phleger, F. B. 1960. Foraminifera] population in Laguna Madre, Texas. Sc/. Rep. Tohoku Univ., Spec. 4, 83-91, Tohoku.
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QuenneU, A. M. 1951. The geology a n d mineral resources of (former) TransJordan. Co/onta/Geo/ogy and Mineral Resources 2, 85-115, London. Relss, Z 1957. Occurrence of Nezzazzata in Israel. Micropal. 3 (3), 259-262, 14 fig, I pl. Sald, R. 1962. The geology of Egypt 377, Elsevier Pub. Co., Amsterdam. Said. R. 1971. Explanatory notes to accompany the geological map of Egypt. Geol. Surv. F_,gyptPaper58, 123, Cairo, Schroeder, R. and Neumann, M. (editors) 1985. Les grands Foraminiferes du Cr~tace moyen de la r~gion m~diterran~'ene. ~ i o s , Mbm. Spec. 7, 156, Lyon. Shaw, S. H. 1947. Southern Palestine geological map on a scale of 1250,000 with explanatory note. Governmental Printer. Gov. of Palestlne 42, Jerusalem. Smout, A. H. 1956. Three new Cretaceous genera of foraminifera related to the Ceratobulimindae. MicrqOa£ 2, No 4, 335-348, 2 fig. 2 pl. Vail, P. 11., Mltchum, R. M. Jr. & Thompson, S. 1977. Seismic stratigraphy and global changes in sea level. Part 4: Global cycles of relative changes sea level. In: Payton, 1977, 127-35. Wasfi, S. and Hataba, H. 1984. Observations on the genus Nezzazata Omara and its significance to the Cenomanian-Turonian boundary in the Gulf of Suez. Benthos 83; 2nd Int. Syrup. Benthic Foraminifera (Pau, April 1983), 597-603, 2 fig., 1 tab., 2 pl.