PLANKTONIC FORAMINIFERA AND CHRONOSTRATIGRAPHY OF SENONIAN EXPOSURE IN WEST CENTRAL SINAI

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A EXO CTIROI\OSTTTTGRAPHYPLANKT.NI' t*#-1HS"K1^ ExPos I rRE s

IN WEST.CENTRAL SINAI, EG}PT

rES ET CHROIYOSTR'ATIGR,4PNTE'Fo RAtutI i'i t rEnt s P L-4li cTl Q Lr V,U:' '

ig qi*"OUE-S ,4FFLE(IRDMENTS SENOflIENS

otl six'ln'l cnnwnaL ouEST' E'GWTE

O*t. H' CFIERIF ' Ibrahim A' AI'-RIFAIY ' Farouk I'

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B.P. 11705

75224 PARTS CEDEX 05

t68

INTRODUCTION

In the last three decades, the stratigraphy of theSenonian in Egypt has been the object of numerousmicropaleontological studies, mostly based on plank-tonic foraminifera. Such studies mainly concernMaastrichtian sequences, as these are widely exposedin southern Egypt and in Sinai, constituting conspi-cuous topographic features of highly fossiliferouschalks or shales, yielding large quantities of plank-tonic foraminiferal tests. The underlying Campanianor older Senonian sediments are almost devoid ofplanktonic foraminifera and have been relativelyneglected by micropaleontologists.

The study of the biostratigraphy of Maastrichtianplanktonic foraminifera in Egypt started in connectionto the solution of the problem of tracing exactly theCretaceous-Tertiary boundary in the region a.rd *asinitiated by Nakkady (1949, 1950, l95la, b, 1955,1957, 1959) and Tromp (1949, 1952). These authorsare the first to have introduced the use of the modernbiostratigraphical criterion based on planktonic fora-minifera to trace this boundary, namely : the extinc-tion of Globotruncanae u.rd the appearance ofGloborotaliidae in the early Tertiary. Nakkady alsofurther noticed in Egypt that sometimes keeledgloborotalids appear immediately after the extinctionof globotruncanids, but that in other instances, thefirst appearance of keeled Globorotallidae is separa-ted from the level of extinction of the Globotruncanaeby a zone characterized by the complete absence orextreme scarcity of. Globorotalia and Globotruncana(the so-called "Buffer Zone", believed to be of Danianage by Nakkady, 1951b). This author, however, wasnot able to interpret properly the reason of the erraticdistribution of his "Buffer Zone", as at these times noproper chronostratigraphical evaluation of the rangesof Cretaceous and early Tertiary foraminifera wasavailable. Nakkady advocated that continuous sedi-mentation prevailed all-over Egypt between theCretaceous and the Tertiary and that differences inthe distribution of his "Buffer Zone" was due to localecological reasons. The existence of a gap betweenthe Cretaceous and the Tertiary in some parts ofEgypt, however, was suggested by Le Roy (1953).This author based his conclusion on field observationand on the study of the foraminiferal fauna of theMaqfi section near Farafra (Western Desert). Thisfauna includes, in addition to some planktonic forms,mainly benthonic small foraminifera. But it is onlyafter the appearance of the work of Bolli (1957,

1959) in Trinidad (Central America) that a world-wide standard was provided for the detailed chro-

PLANKTONIC FORAMINIFERA SENONIAN SINAI

nostratigraphic subdivision of late Cretaceous-earlyTertiary sequences by means of planktonic forami-nifera. This helped authors like Said (1960, 1961,1962), Said and Kerdany (1961), Said and Sabry(1964), El-Shinnawi (1964, 1967) and El-Naggar(1966a, b, 1970) to establish a detailed zonation forthe Egyptian Maastrichtian-lower Tertiary sequencein different localities. The last mentioned author is thefirst to attempt to give a coherent picture of the hiatuswhich exists in.many places in Egypt between theCretaceous and the Tertiary.

Meanwhile, micropaleontologists of the oil industryexpanded the use of planktonic Foraminifera for thestudy of late Cretaceous sediments in subsurfacesequences in northern Egypt and in the Culf of Suez(Ansary and Fakhr, l95B; Ansary et a1.,1962,1969;Ansary and Tewfik, 1966; Beckmann et al., 1969;Andrawis, 1976). The last two publications make use

of the biostratigraphical scheme established by Barr(l96Ba, b; 1972) for the late Cretaceous of Libya, as

the subdivision proposed by Bolli (1957, 1959) wastoo detailed to be followed with accuracy in manysubsurface Egyptian sequences. Other works carriedon Maastrichtian planktonic foraminifera of Egyptduring these times are those of Abdou and AbdelKireem (1969), Abdou et al. (1969), El-Naggar(1970), Issawi el al. (1971), El-Dawoodi and Zidan(1976) and El-Shinnawi and Sultan (1973). In the lastdecade, additional work was carried on the subject(Abdel-Kireem and Abdou, 1979; Barthel andHermann-Degen, l981; Faris, 1982; Masters, l9B4;Luger, 1985). Table I gives details on the subdivi-sions of some authors for the late Senonian in Egypt.

In 1984 a group of European micropaleontologistsrevised the taxonomy and stratigraphic ranges ofCretaceous planktonic foraminifera and presented a

r new bio-stratigraphic scheme for world-wide correla-

\ tion by means of these organisms (Robaszinski et al.,

".' l9B4). A similar scheme, but with some simplifica-', tion, is given by Caron (1985). In the present work,,i the taxonomy and biostratigraphical concepts of theI last mentioned author is followed as it was foundi. simple and easy to apply to the studied sequence.

With the exception of the works of Ansary et al.(1962), Ansary and Tewfik (1966) and El-Shinnawiand Sultan (1973), which concern subsurface se-

quences of the Culf of Suez area, and the ancientstudies of Omara (1954) in Gebel Nezzazat, Youssefand Shinnawi (1953) at Wadi Sudr, Said and Kenawy(1956) on northern Sinai and Allam e/ o/. (1986) onGebel Qabiliat, most publications on Cretaceousplanktonic foraminifera of Egypt deal with the .Eastern and Western Deserts. The present studydeals with the planktonic foraminifera of the late

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CHERIF, AL.RIFAIY, AL-AFIFI and ORABI

EGEND

l:EEl rr Nubio Sondstonc"E-3J (Pot"ozoic-Eorly L:J Neo93n2

Cretoceous )

-t i-l euoternory

El Lenomonton I uronton

ffi s"nonion-polcocene

area, showing the major structures and the

ffi ,o*-"nt(Prccombrion) ffi'eo""n"

Ott d'Estevou et al., lg86, wtth, montmnt les stru.ciures pincipales et

$r>

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Boundory between blocks

Fo ult

Folds

Meosured section

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mpled sectrons.

des coupes str,modifications).

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location of sr

fications).'emplacement

uec quelques

I the locationmodifications

et I'emplace76. auec ouel

he study a

m 6tudibe,regian 6tut(Structures

map of {

ln.filil- Geologic

ghologique d.e

tmcdes d'aprAs Oft d'Esteoou et al., 1986,

170

Correlation

?O PLANKTONIC F(

lorrelation chart of Senonian formations' biostratigraphic

of the Gulf of Suez and in southern E

WEST CE

)RAM]

1

marke

5ypt as

NT

;NIEERA SENONIAN SINAI

\tlt,lt I

rs and time stratigraphic interpretations in Central Sinai' in the s<

given b1 various authors and in the presenl worK'

RAL SINAI & GULF O$

-iSl

iB.tii$'

ifi$,

&'lf:,

-dh

{iffi,s:

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TARTOV & srElNlr4(1e77t I

Negev & Sinai I

ISS'et.

(1eW.Fr

GHORAB( 1 e61)

Ras Gharib Oil Field

ANSARY & TEWFIK( 1e66 )

Ezz-El Orban area

ili$

o-loGoofoooC,,

Fzlo=

Taqiye Formation leNot studied

Ghareb

Formation

(

al6lEIola6a2

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Bolivinoidesdracodraco

lNeobulimina

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GlobotruncanagansSeri

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=

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lornicatatornacata

draGomiliaris

6ccoE6

qqf

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a.ECt5:=

Globolruncanavonlricosa,Neobuliminacanadangia'o)

ilobotruncanaca!arontiS

l^.aicale

Lacostolns

cE.9EE>.EEE

lli^l.aah

c.gtrotrG,o

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=

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<tnlcoc6oIc.!o.!Coo

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Formation

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no

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cerorit Formation lE

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=

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t

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Campanian to Maastrichtian pqt 'l tl-". Senonian

*""Jr.ion of four surface sections in West-Central

$;;.-Th;t. are : Gebels Nezzazat, Mukattab' Ekma

""JOJfii"t (Fig.f). This stratigraphical interval is

f"""a-t" [" titei"ly part of the succession yielding

"l""Ht.i" foraminifera suitable for ehronostratigra-

lhr. Tl'," aim of this publication is to presenl an

iii;ti';il ;;.J to. the planktonic foraminifera of

ifr"" rt"aila area" which hu' ""'"t been attempted

nlio.". and, to discuss the chronostratigraphy of the

S;;;;il i, the investigated localitv and-.in other"Err"tt""

o""rt """" in lf,e light of the application of

uf io date bioslratigraphical standards'

STRATTGRAPTTY OF THE sEIOIig{N IN"'iffist--einrrRAt sINAr AnD rN TIIE GULF

OF ST]EZ REGION "

The lithostratigraphic subdivision of the Senonian

i" W;ti;;t"f Bi""i and in the Gulf of. Suez area

;;";;; uft". u long series of investigations which

ril;'Jl;'the beginning of the century (B.at91'

iffo?r M;;;";;J Sadek," 1e23; Beadn^ell' te27;

i';;i ;;J Shinnawi, 1953; Shata' ^19?6.i

Ghorab'

ig6i;'Vr;tt"f, fssz; Bartov .and Steinitz' 1.97!,

irru*i ,t o/., l9B1). But up till now' ^there

rs no

*r""-"r,t on the nomenclature of the fine subdivi-

-f#;;;-'S;;;"i;" rock units in the region' Bv

"lrnp..l"g-ift" ,"q,"""" in the studied area with the

I

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CHERIF, AL-RIFAIY, AL-AFIFI and ORABI 17

Taur.r:.rl I (suite)

) Tableau dp aonesnondance des subdiuisions litho-, bio- et chronostmtigraphiques prbsentdes par dffirentE auteurs pour Le Sdnonit

t du Sinai central, du Sud du golfu de Suez et du Sud de I'Egypte.

Fs 7. SOU.THERN EGYPTlssl- et.l(r grhr-r'"

PRESENT WORKiluth -East Abu Rudeis

area

LUGER( 1 e85)Kharga/

DOMINIT( 1 e85)Dakhla/Raris

KLITZSCH( 1 e78)

Dakhla

EL NAGGAF( 1 966)

Nile ValleY

NAKKADY( 1 959)

YOUSSEF( 1 e57)

)osseir-Saf agc

t-.1 Eg ESNAQh Morozovella uncinata (E

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TAREF

SANDSTONE

descriptions given in the above mentioned literature,and also with the results of studies earried in southernEg5rpt (Youssef, 1957; El-Naggar, 1966b; Klitzsch,l97B; Barthel and Hermann-Degen, l98l; Dominik,l9B5; Luger, l9B5), the following lithostratigraphicsubdivisions for the Senonian in West-Central Sinaiare proposed, from the base to the top (see alsoTable 1) :

1. Mlrulta Gnoup (late Turonian to ? early Cam-panian)

This rock unit has been defined as a Formationby Ghorab (1961) in Wadi Matulla in West-CentralSinai, some kilometers to the north of the study area.The original diagnosis of Ghorab designates a thick-

ness of 170 m of sediments in the type section. Inthe present work it was possible to subdivide this

rock unit into three lithostratigraphic units reasonablycorrelatable with Senonian formations established insouthern Egypt. For this reason, it is thought betterto consider the Matulla as a group comprising threeformations (See also Issawi el aL, l98l). The for-mations are as follows from base to top :

a) The Taref Sandstone : This rock unit wasrecognized by Awad and Ghobrial (196$ in theKharga oasis. It consists of coarse grained sandstones,constituting a regressive, continental sequence abovea slightly transgressive fluviomarine rock unit (Mag-hrabi Formation of Barthel and Hermann-Degen,l98l). The last mentioned authors give to the TarelSandstone a Turonian to Santonian age in the south

Sdnoni.e,n

ls rock unrt was

'l (1966 in therined sandstones,sequence aboverock unit (Mag-

Hermann-Degen,qive to the Taref

betterthreee for-

q(r-ro u\ '.

172 PLANKTONIC FORAMINIFERA SENONIAN SINAI

of the Western Desert. In the study area, the lowerpart of the Matulla . Formalion ,consists of coarsegrained, often cross-bedded sandstones with siltsto-nes, shales and rare beds of brown limestone anddolomite. It yields sometimes marine mega-inverte-brate remains, but also rain prints. This sequence canbe without much difficulty correlated to the TarefSandstone of southern Egypt.

b) The Qosseir Yarriegated Shale : This rockunit was described by many authors in the south ofthe Eastern desert (Youssef, 1957; Said, 1962). It isa senior synonym of the Mut Formation of Bartheland Hermann-Degen (1981) recognized in the southof the Western Desert. In the study area a sequenceof fossiliferous varriegated sandstones and shalesoverlying the Taref Sandstone has been assigned tothis rock unit. The fossils are mainly oysters. No

pi r-r1;. i foraminifera have been found in this rock unit. Most' . workers consider the Mut (or Varriegated Shale)'/ Formation as early Campanian in age"(see Lugeri

l eB5).

c) The Iluwi Formation : This unit was descri-bed by many authors (Youssef, 1957; Said, 1962),but it has been named by Ghorab (1961). This is thephosphate-producipg sequence of Qosseir, Safaga,Abu Tartur and other localities in southern Egypt. Inthe studied are1 a sequence of marls, sandstones,shales and carbonates yielding an appreciable amountof mega-invertebrates and sometimes foraminifera has

been designated by this name. The most conspicuousmega-fossil in this rock unit is Pychnodonta uesicu'/oris, present mainly in its upper part. The upper partof the rock unit also contains planktonic foraminiferasuggesting an age which may range from the lateCampanian to the early Maastrichtian. At its typelocality at Qosseir, Youssef (1957) and Said (1962)give to the Duwi Formation a Campanian age. In thesouth of the Western Desert, Said (1962), Klitzsch(1978) and Luger (l9BS) eonsider that the DuwiFormation is of late Campanian to early Maastrichtianage.

lrle2. Tua Suon Cuar (?.4V Campanian-Maastrichtian)

This rock unit has been defined by Ghorab (1961).It is a sequence of chalk yielding sometimes chertbands or nodules. It is generally very rich inplanktonic foraminifera. This formation yielded mostof the species discussed in this paper. Ghorab (1961)subdivides the Sudr chalk into two members :

a) A lower or Markha Chalk Merrber : This isa sequence of chalks of characteristically browncolour in subsurface sections of the Gulf of Suez. Inthe studied area, however, this name is applied to a

white chalk unit yielding numerous banks of Pychno-donta aesicularis. lt is considered in the subsurfaceby Ghorab (1961) and El-Shinnawi and Sultan(1973) as belonging to the Campanian. In the regionof Gebels Gharamul and Dara on the west coasts ofthe Gulf of Suez, Ott d'Estevou et al. (1986b),noticed that above a sequence yielding phosphaticbeds and banks of Pychnodonta uesicularis (probablyequivalent to what is referred as Duwi Formation inthe present work), the Maastrichtian starts withchalky beds devoid of P. aesicularis, bil yieldingsmall pectinids. These authors also notice the pre-r".r"" bf Globotruncanfracalcarata in the beds withP. uesicularis, suggesting a Campanian age. The bedswith pectinids are separated from the Campanian byan unconformity surface marked by an horizon ofreworked and rubified Pchynodonta and yield variousplanktonic foraminifera suggesting a Maastrichtianage. In the study area the planktonic Foraminiferafound in the Markha Chalk Member and the un-derlying Duwi Formation are similar but not dia-gnostic for precise age determination. They suggestan age ranging from the late Campanian to the earlyMaastrichtian.

b) An upper or Abu Zeneima Member : In thestudy area this member is very similar to theunderlying Markha Member but it yields no P.uesicularis. The rich planktonic foraminiferal faunain this member in the sludy area suggests a Maastrich-tian age. The latest Maastrichtian, however, is missingand the sequence is capped by a sequence of shalesand marls (Esna Shale) of Paleocene age.

PLANKTONIC FORA]IIINIFERAL ZONATION

33 out of the I l0 Senonian samples collected forthe present work yielded 25 species of planktonicforaminifera suitable for the establishment of chrono-zones for world-wide correlation. The distribution ofthese species in the four studied sections are givenin the charts of figures 2-5. Fig. 6 is a correlationchart for the four sections studied. The chronozonesrecognized in the studied succession are as follow,from the base to the top :

a) An interval probably equivalent to most of therange of the chronozones of Globotruncanita calca-rata and Globotruncanita hauanensis as defined inCaron (1985). In the studied sections, the lower limitof this interval is to be placed, strictly speaking, withthe first appearance of planktonic foraminifera in theSenonian section, i.e. at the base of the Sudr Chalkat Gebels Nezzazat and Mukattab, near the top of the

Ir'.

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CHERIF, AL-RIFAIY, AL-AFIFI and ORABI

Ftc' 2' - stratigraphic range chad for Senonian planktonic foraminifera identified in the sur{ace section of Gebel Nezzazat.Tablcau de distribfitian *tratigraphique des Fomminifires plnrrctiques identrys d.ans la successian s1nonienne d.e la coupe de GebelNezzazat-

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PLANKTONIC FORAMINIFERA SENONIAN SINAI174

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Tablcau de distibution stratigr:aphique des Foraminifires planc-tiques -identifiis dans la succession sdnonienne de la coupe d'e Gebel

Mukattab.

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Flc. 4. - Stratigraphic range chart for Senonian planktonic foraminifera identified in the surface section of Gebel Ekma.Tabteau dc distribution stratigraphique d.es Foraminiferes planctiques identfus dans la succession sdnonienne d.e la coupe d,e Gebel

Ekma.

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Tabl.eau de d.istributian stmtigraphique d,es Foraminiferes planctiques iilentififis dans la succession sdnoni'enne de la coupe ile Gebel

Qabilint.

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CHERIF, AL-RIFAIY, AL-AFIFI and ORABI

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Tabl.eau de corrdlation d.es coupes 6tudi.6es.

lhrvi Formation at Gebel Qabiliat and near the based lh€ Duwi Formation at Gebel Ekma. The appea-rm of this lower limit at different levels of theffi lithostratigraphic succession is probably rela-hd to local ancient ecologic conditions, as planktonicheminifera tend to proliferate only under relatively&cp open marine waters. Thus, we have placed thehicr limit of the time-stratigraphic interval recogni-Ed in the study area as equivalent to the chrono-nnes of G. calcarata and G. hauanensis with themoshatigraphic limit between the Duvi Formationfr dislinct marine sedimentary cycle with carbonatenfimentation) and the Qosseir Varriegated Shale (aLuft>marine sequence of predominantly terrigenousnfimentation). This is justified by the most probabler,mption that the transgressive episode expressedLf lh" Duwi Formation was a synchronous eventIover the study area. Thus, it may tre said that theilEval equivalent to the zones of. G. calcarata and,(^ lwoancnsis (considered as a chronostratigraphic

subdivision) comprises in the study area the Duwiand the lower part of the Sudr.Chalk Formations. Theupper limit of this interval is characterizedby the firstappearance oI Globotruncana aegwtiacaand, of otherspecies as Heterohelix nauanoensis , Rugoglobige-ina hexacamerata, Pseudoguembelina excolata and,P. palpebra.

At Gebel Nezzazat, the interval equivalent to theGlobotruncanita calcarato"/Globotruncanella haaa-nensis chronozone (i.e. the Duwi Formation and thelower parts of the Sudr Chalk) is 95 m thick (40 min the Duwi Formation and 55 m in the lower partof the Sudr Chalk). It yields : Heteroheli,x globulosa(EunuNnenc), H. stiata(Euneunnnc), Globotruncanaorco CUSHMAN, G. bulloides VoI-GeR, G. linneiana(d'Onucm), G. cf. aenticoso WHITE, Pseudoguembe-lina costulata (CusHir,rlx), Pseudotextulaia elegans(RHrz.t.x) and Rosita fomicata (Pr-unrnren). This faunais only concentrated in the Sudr Chalk.

NORTH

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ABU ZENEIMA MEMBER

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178 PI,ANKTONIC FORAMINIFERA SENONIAN SINAI

At Gebel Mukattab, this interval is 28 m thick(12 m in the Duwi Formation and 16 m in the lowerpart of the Sudr Chalk). It yields : Hedbergellaholmdelensis Ot-ssotl, Globigerinelloides cf . subcai-nala (Bn0IINIMANN), Heterohelix globulosa (EunnN-

BERG), 1L striata (EHnrrunrnc), Globotruncana arca(Cusuntan), G. lapparenli BnorzeN, C. linneiana(d'Onnrclv), Globotruncanita stuartifurmis (Dar--

ntez), Rosita fomicata (Pr-unruan) and Rugoglobige'rina rugosa (Pr-uuuan). This fauna is only concentra-ted in the Sudr Chalk. Z4 *

At Gebel Ekma, this interval is B0 m thick (50 min the Duwi Formation andfrm in the lower partof the Sudr Chalk). In tKe Duwi Formation thefollowing planctonic foraminifera are found : Hedber-gella holmdelensis Or,sso N, G lob igeinelloides ultra-micro (SusnorINA), Heterohelix globulosa (Eunuu-BERG), H. stiata (EHnrunanc), Globotruncanellahauanensis (Woonwur), Pseudoguembelina co stulata(Cusunrm,r), Rosita fomicata (Pluurrlan) and, Rugo-globigeina rugosa (PI-unnton).

The lower part of the Sudr Chalk yields at GebelEkma : Hedbergella holmdelensis (Or,sson), Hetero-helix globulosa (ErtnoNnrnc), 1L striata (Eunr:unonc),Glo bigeinelloides prairiehillensis Pessacno, G lobo -

truncana orco (Cusuu,tru), G. linneiana (d'Onnrcnv),Rosita fomicata (Pr,uunaan) and Rugoglobigeinarugosa (PI-uuunn).

At Gebel Qabiliat, the interval equivalent to theGlobotruncanita calcarata"/Globotruncanella haaa'nensis chronozone is 137 m thick (69 m in the DuwiFormation and 68 m in the Sudr Chalk). Planktonicforaminifera start to appear at the top of the DuwiFormation, in which the following species are found :

Globigeinelloid,es praiiehillensis PESSa.GNo, Hetero-helix globulosa (EHnuunrRc) and Rosita fomicata(Pluunarn).

The lower part of the Sudr Formation yields :

Globigeinelloides praiihillensis Pnssacuo, Globige-inelliides ultrami,cra (Sunnorma), Heteroheli,x glo-bulosa (Eunrnnnnc), H. striata (Eunounnnc), Globo-truncana arca (CusHuAN), G. linneiana (d'Onnrcxv),G. cf. aenticoso WHITE, Rosita fomicata (Pt-ulturn),Pseudotextulaia elegans (RHnzar) and Rugoglobige-ina rugosa (Pr,uuuon).

The distribution of the planktonic foraminiferalassemblages of this interval does not enable toseparate the chronozone oL Globotruncanita calcaratafrom the chronozone of Globotruncanella haaanensisand thus, it was not possible to draw the limitbetween the Campanian and the Maastrichtian in the

study area by means of the identified planktonicspecies. The presence of Globigeinelloid,es ultrami-cra in the Duwi Formation of the Gebel Ekma

Section, however, suggests that if this interval is notCampanian, it can not be younger than the lower partof the Globotruncanella haaanensis chronozone, i.e.the lowermost Maastrichtian. On the other hand, thepresence of Clobotruncanella haaanensis in the DuwiFormation of the same locality suggests that thissequence can not be older than the upper part of theGlobotruncanita calcaralo chronozone.

Ott d'Estevou et al. (1986) noticed in the regionof Gebels Gharamul and Dara in the Eastern Desert(this is a region lying almost on the same latitude as

the study area, but across the Gilf of Suez) thatsequences yielding banks of Pychnodonta oesicularisare restricted to the Campanian, as these beds yieldGl.obotruncanita calcaralo. These authors also noti-ced the presence of a marked unconformity and ahiatus between the Campanian (mostly belonging tothe Duwi Formation as defined in the present work)and the Maastrichtian, which consists of marly beds(probably equivalent to the Sudr Chalk of thepresently studied locality). The Maastrichtian seems

to belong entirely in the region of Gebels Gharamuland Dara to the chronozone of Gansseina ganssei.Similar relations have been noted at Gebels El Zeitand Eshel Mellaha (Prat et o/., 1986). For thesereasons, in the study area, the Campanian/Maas-trichtian boundary has been tentatively traced bet-ween the Markha and Abu Zeneima Chalk Members,i.e. at the level of disappearance of the banks ofPychnodonta a es i.culais.

6/ The chronozone of. Clobotruncana aeglptiaca.The top of this zone can be recognized in the studyarea by the first appearance of. Gansseina gansseiand species like Racemiguembelina fructicosa.

At Gebel Nezzazat the Globotruncana aegyptiacachronozone is 35 m thick and it yields : Globigeinel-loides praiiehillensis PessacNo, Heterohelie naaar-roensii LoenucH, H. stiata (EunrNnrnc), Globo-truncana aegyptinca Nlrx-LoY, G. area CusHuau, G.

bulloides VoLGun, G, linneiana (d'Onnrcl'v), G. cf.uenticosa WHItt, Rosita fornicata (Pruuuan), ftu-go globigerina rugo sa (Pr-ultnrnn), Pseudo guembelinaioitulata (CusHnrmt), P. excolata (Cusurr.ratl) andPseudotextulaia el,egans (Ruozar)'

At Gebel Mukattab the chronozone is 65 m thickand yields : Globigeinelloides praiiehillensis Pss-sAGNo, Heterohelix globulosa (BHnomnenc), H. stiata(EHnounonc), Globotruncana aegwliaca Narraov,G. arca Cusunta.N, G. bulloides VoLcsR, G. lappa-renti Bnorzsx, G. linneinna (d'Onucnx), G. cf.uenticosa WuITE, G. stuartifurmrs (Dar,nmz), Rosita

fornicata (Pr,urravmn) and. Pseudoguembelina costu'/alo (Cusnnlm).

At Gebel Ekma the chronozone is 67 m thick and

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CHERIF, AL.RIFAIY, AL-AFIFI and ORABI 179

aeglptiaca is 40 m thic}. It yields the followingtonic foraminifera : Globigerinelloides praiii-

fu_ Prss,c,cmo, Heterohelix globulosa (EHnru_H. stiata (EHnrNnrnc) , H.-naaanorrri" Lor_Glabotruncana aegyptinca Nlx,tnv, G. arca

&e appearance ol Morozouella uncinala and'otherIdll_nic species characterising the middle paleo_

;a- 1"T it is interesting to notice that a gap exists

), G. bulloides Volcen, G. 'linneinna

*), G. cf, uentriroso WHnE, Rosita fornieatai),, R. rugosa (Pruuurn), pseudogubmbelina(Cusnrr,laN) and Pseudotextulaiia el,egans

r) The chronozone of Gansserina ganssei. Thep

-of fiis zone in the studied section

"is reeognized

Af Gebel Qabiliat the chronozone of Gl,obotrun-

At Gebel Qabiliat the chronozone is 20 m thickand yields : Heteroheli.x

-striata (Eunrunrnc), 1Lnaaarroensis Lornr.ICH, Clobotruncana aegyp,tiacaNaxKADy, Globotruncanita conica(WHrrr), frLgoglo-bigeina -

-rugosa (Pr,unrnarn), Rugotruncina subcir_cumnodifur (Gn Nnor,n), Gansseiia gans seri (Bor,r,r),Pseudoguembelina costulata (CusnulN), p. ixcolaia(CusunaaN), Pseudotextulaia elegans (Ruozax) andRacem igue.mbeli na lru cticosa (EIcen).'

Here it is interesting to notice the relatively smallthickness of the Gazsieina ganssen chronozone inall the studied sections and the fact that it is overlainby. a conspicuous hiatus, separating it from thePaleocene sequences. The presenc e oI Globotrun_cana bulloides at Gebel Neziazatamong the plankto_nic foraminiferal assemblage of the cf,ronozone ofGansseina gansseri r,rgggrtr that only its lower partis represented in the si"aiea sedimentary suite

'and

that its top has been eroded or non deplsited.

CONCLUSION

. The analysis of the vertical distribution of plankto_nic foraminifera in four sections in the a""u to thesouth-east of the settlement of Abu Rudeis lnWest-Central Sinai, enables to date the upper part ofthe,Senonian exposure in the region. Theiower partis.devoid of planktonic foramini6ra and can b" 6rrfylitho.stratigraphically subdivided and correlated withsrmrlar exposures in the south of the Eastern andWestern Deserts of Egypt.

Planktonic foraminifera suggest a late Campanianage for the Duwi Formatio-n (phosphate-bearingsequence yield ing G lo b o t rune a nita'ca lcirata at GebejGharamul, in the east central part of the EasternDesert). In the study area it seems that the Markhallember of the Sudr Chalk is also of late Campanianage, as Pychnodonta aesiculais banks seems to berestricted to these times in the central regions of Sinaiand the Eastera Desert.

_ The upper part of the Sudr Chalk (the AbuZeneima Member) in the study area .ungl, in agelrom the early jg early late Maastrichtianlincludiigthe zones oI Globotruncanella hauanensis, Globi-\tnlana aegyptiaca and the lower part of the zoneoI Gan.sseina ganssei, as defined by Caron, lgBS).Here it seems that sedimentatio., *u, almost conti_nuous between the Campanian and the Maastrichtianand that no stratigraphicil gap exists between the two9t1g"r: as that observed by Ott d,Estevou et al.(l9BGb) in Gebel Garamul and Esh El-Mellha in theeast-central part of the Eastern Desert.

shrdied sections.between the Ma.t i"itia, a.,d

fuIillcnsis Pessacno, Heterohelix i.auarroensis

Tyd"V.-The hFtE coresponds to the missingMaastuichtian Abathomphalus mayaroensrs chrolne and to, at least, the whole eaily paleocerre.

Gebel Nezzazat the Gansseina ganssei chro-

".i:.15m thick and yields : Globigeineltoi.des

ry, !I: stiata (EHnrxrrnc), Globotruncanailiizca NxxaDy, G. orco (CusilnrAN), G. builoi-

Globotruncanita conica (Wrirrr), Globo-haaanensis (Voonwur), Rugoglobigeina/a Bn0mqnmNN, ,R. *gosa (pr,uuurn),ganssei (Borrr), Pseudoguembelina cosl-I (CusHu,ru), P excolata (Cusnnaax), p. palpe_

hOuNruaNN and, Pseudotextulaia "igr"i 1daa.

,mbelinq costulata (CusHnrau) and, pseudo-elegans (Rnrzar).

I

180 PLANKTONIC FORAMINIFERA SENONIAN SINAI cdilThe latest late Maastrichtian is missing in the study

area and middle Pa-leocene marls (Esna Shale) restdirectly over early late Maastrichtian chalks.

Here it is interesting to notice that in the northernpart of the studied area, the first massive influx ofplanktonic foraminifera in the exposed Senoniansequence appears at the base of the Sudr Chalk. Inthe south-western part of the area, at Gebels Qabiliatand Ekma, however, this influx is noticed near thetop and near the base of the Duwi Formation (lyingbelow the Sudr Chalk) respectively. This suggests thatthe south-western part of the study area wis situatedin a relatively more depressed ("hasinal") region thanthe northern part of the area during the late Cam-panian transgression, and that deeper marine watersreached it before the northern part df the area. Thecenter, or the axis, of this southern basin must havepassed near to the site of Gebel Ekma.

, Lastly, it must be pointed out that the transgressionwhich started in the late Campanian by the depositionof the Duwi Formation in the studied area seems tocorrespond to a global riie in sea level whichoecurred some 74.$ m.a. ago (see Haq et al., l9B7).

BIBLIOGRAPITY

Annr:i.:Ktnr:uv M.R. and Arnou H.F. (1979) : Upper Creta-ceous-Lower Tertiary planktonic Foraminifera from SouthGalirla Plateau, Eastern Desert, Egypt. Rea. Esp. Micropal.,vol. 1l (2), p. 175-222, pl. l-12, Madrid.

Asoou H,F. and Allnrl. Krru:r:n M.R. (1969): Upper Creta-ceous-Lower Tertiary planktonic Foraminifera from GebelGhanima, Kh'arga Oasis, Western Desert, Egypt. Iiull. Fac.Sci., Alex. Uniu., vol.9, p.451-509, pl. l-8, Alexandria.

Asoor- H.F., N.,rrn E.M. and Atuur. Krrruun M.R. (1969) :

Planktonic foraminiferal zonation of the Upper Cretaceous-Lower Tertiary rocks of Gebel Ghanima, Kharga Oasis,Western Desert, Egypt. U.A.R. Bull. Fac. Sci., Alex. Unia.,vol. 9, p. 251-270, Alexandria.

At.r.,ut A., Srr,,rrr,rn K. and Krr,u.rr. H. (1986) : Biostratigraphyof the Campanian-Maastrichtian succession of Gebel Qabeliat,Sinai, Egypt. loum. Fac. Sci., Tanta Unia.,vol.5, l0 p., 2 pl.,4 texlfig., Tanta.

Artrn,twts S.f. (1976): Biostratigraphy sfudy of the UpperCretaceous rocks with special reference to the rock strati-graphic units in Mubarak area, Western Desert, Egypt. 7thAfrican Micropal. Colloqium (in manuscript), IleJfe (Nigeria).

"A.rs,rnv S.E., Aruu,turs S.E. and F,rrtur, S.E. (1962): Biostra-

tigraphic studies of the Upper Cretaceous sections in theG.P.C. wells in the Eastern Deserl and Sinai. Bull. 4th Arab.Pet. Congr., 17 p., Beirut.

Ars.,rtn S.E., Arurr,rvrs S.8., Fulur, S.E. and Tr:nrrx N.M.(1969): Biostratigraphy and time stratigraphy of sub-surfaceUpper Cretaceous of. Ezz El-Orban area, Gulf of Suez region,U.A.\. Proceed. 3rd African Micropal. Coll., p. 1-95, Cairo.

Ars,tHt S.E. and F.rxtur B.Y. (1958) : Maastrichtian Foraminiferafrom El Hueitat area, West of Safaga, Egypt. Journ. Geol.,vol.2 (2), p.105-146, Cairo.

Ars.,tnr S.E. and Tuwrtx N.M. (1966) : Planktonic Foraminiferaand some new bentonic species from the sub-surface UpperCretaceous of Ezz El-Orban area, Gulf of Suez."Journ. Geol.Soc. U.A.R., vol. l0 (l), p.37-76, pl. l-9, Cairo.

Av,rtl G.H. and Grtttnt,rt. M.G. (1966) : Zonal stratigraphy ofKharga oasis. Geol. Suru. Eg1pt., Pap. 34, 77 p., Cairo.

B,qt.t. J. (1916): Topography and geology of west central Sinai,Eglpt Sun:. Dept., 219 p., Cairo.

B,tnttr T. (1907): The topography and geology of the peninsulaof Sinai (western portion). Eppt Sun:ey Dept.,241 p., Cairo.

PLATE I

l. 'Gansserina ganssei (Boru). Gebel Mokattab, Abu ZeneimaMember of Sudr Chalk (Maastrichtian). (a) Spiral view,(b) umbilical view, (c) peripheral view. X aprox. 40.

Globigeinellaides prairichill.ensis (PEssacuo). Getrel Ekma,Markha Member of Sudr Chalk (Campanian). Spiral view.X aprox. 40.

Glabigeinellaid.es ct. subcainata (Bn0NNrumu). GebelEkma, Markha Member of Sudr Chalk (Campanian). (a) Spi-ral view, (b) peripheral view. X aprox. 40.

Glbbigeinelloid.es ultramira (Sunnotue). Gebel Ekma,Duwi Formation (Campanian). (a) Spiral view, (b) peripheralview. X aprox- 40.

Rosita fomicata (Pr,uuutn). Gebel Qabiliat, Abu Zeneima.Member of Sudr Chalk. (a) Spiral view, (b) peripheral view.X aprox. 40.

Glbbotruncana aegyptiaca N.q.rKAoy. Specimen referable toG. duwi N.nx-a,ov. Abu Zenenima Member of Sudr Chalk(Maastrichtian). (a) Spiral view, (b) peripheral view. X aprox.35.

7. Globotruncana arca (CusuueN). Gebel Qabiliyat, AbuZeneima Member of Sudr Chalk (Maastrichtian). (a) Spiralview, (b) peripheral view. X aprox. 35-

Glabotruncana bulloid.es (Yot-cnn). Gebel Qabiliyat, AbuZeneima Member of Sudr Chalk (Maastrichtian). (a) Spiralview, (b) peripheral view. X aprox. 35.

Globotruncana lapparenti (BnorzEN). Gebel Mokattab,Markha Member of Sudr Chalk (Campanian). (a) Spiralview, (b) tilted umbilical view, (c) peripheral view. X aprox.40.

Globotruncana linneinna (d'Onurcrw). Gebel Ekma, AbuZeneima Member of Sudr Chalk (Maastrichtian). (a) Spiralview, (b) peripheral view. X aprox. 30.

Globotruncana ct. aentricosa (Wune). Gebel Mokattab, AbuZeneima Member of Sudr Chalk (Maastrichtian). (a) Spiralview, (b) peripheral view. X aprox. 70.

Clobolruncanella hooanensis (VDoRwUh). Cebel Ekma.Duwi Formation (Campanian). (a) Spiral view, (b) peripheralview. X aprox. 30.

9.

10.

I l.

12.

F-. \L.RII.'AIY, Ai,-AFIFI AND ORABI PI,ATE 1

I, '. - E DE \IICROPALEON'I'OI,OGIE. VOL, 32. N" 3

182 PLANKTONIC FORAMINIFERA SENONIAN SINAI

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Btrn F.T. (1968 b) : Upper Cretaceous Stratigraphy of JabalAkhdar, northern Cyrenaica. Geol. and Archaeol. of northernCyrenaica, Libya. Pet. Soc. Expl. Libya, p. 131-147, Tripoli.

B,lnn F.T. (1972) : Cretaceous biostratigraphy and planktonicForaminiiera of Libya. Micropaleontology, vol. 1B (1)'p. l-46, pl. 1-10, l0 texlfig., New York.

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and Early Tertiary stratigraphy in the GreatSand Sea and itsSE margins (Farafra and Dakhla oasis) SW Desert, Egypt.Mitt. Erye. Staatsslg. Palaont. hist. Geol.' vol. 2l'p. 141-182, Munchen.

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p. ll9-148. Jerusalem.

Butorr:t.t. H.J.L. (1927): The Weitdemess of Sinai. Arnold,lB0 p., London'

Bucrvlrr J.-P., El.-Hunr I., Kt:nn'rrt M.T., SllD R. and VtorrtL. (1969): Standard planktonic zones Egypt. Proc. lst Int'Conf. Plankt. Microfossils, Geneva (1967), vol. 1, p' 92-103,lext-[ig. l. pl. l. Ceneva.

Bor.r.r H.M. (1957) : The genera Praeglobotru-ncana, Rotalipora,

G lo bo truncana and Abithomphalu s in the Uppper Cretaceous

of Trinidad, B.W'I. U.S. Nat. Mus. Bull.,vol.215, p' 51-60,pl. 12-14, text fig. 10, Wahington.

'Bot.t,t H. (1959): Planktpnic Foraminifera form the Cretaceous

of Trinidad, B.\l.l. Bull. Amer. Pal., vol. 39(179),p. 257-277.

Crnor M. (1985) : Cretaceous planktic foraminifera, in Plankton

Stratigraphy edited by Bolli H.M., Saunders J.B. and

Pe.chlNielsen K. Carlrbidge llnix. Press., p. 17-86, Cam-

bridge.

Dorttrtx, W. (1985): Stratigraphie und Sedimentologie derOberkreide von Bahariya und ihre Korrelation zum DakhlaBecken (Westem Desert, Agypten). Berliner Geouiss' Abh',Reihe A(62), 173 p., 53 fig., 22 tab., lB pl., Berlin.

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I IIERIT

PLATE 2

l. Globotruncanita stuartformis (Drr-emz). Gebel Mokattab,Abu Zeneima Member of Sudr Chalk (Maastrichtian)'(a) Spiral view, (b) tilted umbilical view' (c) peripheral view'X aprox. 40.

2. Globotruncanita cf, stuartifurnis (Duntrz). Gebel Ekma,

Abu Zeneima Member 'of Sudr Chalk (Maastrichtian)'(a) Spiral view, (b) peripheral view. X aprox' 40.

3. Hedbergella holmdelensis (Or,ssoN). Gebel Bkma, DuwiFormation (Campanian). (a) Spiral view, (b) peripheral view'X aprox. 40.

4. Heteroheli.tc globulosa (Eunnnnrinc). Gebel Nezzazat, AbuZeneima Member of Sudr Chalk (Maastrichtian). X aprox'40.

5, Heterohelis naaarrciensis (LoEnr-Icu). Gebel Qabiliat, AbuZeneima Member of Sudr Chalk (Maastrichtian). X aprox.40.

6. Heterohelix srridla (EHRENnlnc). Gebel Nezzazat, AbuZeneima Member of Sudr Chalk (Maastrichtian). X aprox.40.

7. Pseudoguembelina excolata (Cusnltm). Gebel Nezzazat,

Abu Z"eneima Member of Sudr Chalk (Maastrichtian)' X

aprox. 40.

B. Pseudoguembelina palpebra (Bn0ruurr and Bnowu)' Gebel

Qabiliai, Abu Zeneima Member of Sudr Chalk (Maastrich-

tian). \ aprox. 40.

9. Pseud.oguembelina costulata (Cusnuln). -Gebel.

Nezzazat,

Abu Z"eneima Member of Sudr Chalk (Maastrichtian)' Xaprox. 40.

10. Racemiguembelina fructicosa (Er;cun). Gebel Qabiliat, AbuZeneima Member of Sudr Chalk (Maastrichtian). X aprox'40.

ll. Pseudotextulaia elegans-(Rnr:znr). Gebel Mokattab, AbuZeneima Member of Sud" Chalk (Maastrichtian). X aprox'40.

12. Glnbotruncanita conica (WHrrc). Gebel Qabiliat, AbuZeneima Member of Sudr Chalk (Maastrichtian)' X aprox'

40.

73. Rosita fornicata (Pr,uuur:n). Gebel Qabiliat, Abu Zeneima

Membei of Sudr Chalk (Maastrichtian). X aprox. 40'

1 4. Rugoglobigerina hexacanterola (Bn0rxtu,lNrl)' Gebel Ekma'AbL Zenei*a Member o{ Sudr Chalk (Maastrichtian)' Xaprox. 75.

15. Rugoglobigeina rugosa (Pr-uuurn). Gebel Qqhiliat, AbuZenei-a Member of Sudr Chalk (Maastrichtian). X aprox'

40.

(]tIERIIT, AL-RIFAIY. .\L.AFIFI ANI) ORABT PLAI'E 2

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