dinoflagellate cyst biostratigraphy and palaeoenvironment of the early - middle miocene of the gulf...

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Lower and Middle Miocene biostratigraphy, Gulfof Suez, Egypt based on dinoflagellate cysts andcalcareous nannofossilsAli Soliman a b , Stjepan Ćorić c , Martin J. Head d , Werner E. Piller a & Salah Y. El Beialy e

a Institute of Earth Sciences (Geology and Palaeontology), University of Graz,Heinrichstrasse 26, A-8010 Graz, Austriab Geology Department, Faculty of Science, Tanta University, Tanta, 31527, Egyptc Geological Survey of Austria, Sedimentary Geology Sector, Neulinggasse 38, A-1030,Vienna, Austriad Department of Earth Sciences, Brock University, 500 Glenridge Avenue, St. Catharines,Ontario L2S 3A1, Canadae Geology Department, Faculty of Science, Mansoura University, Mansoura, 35516, Egypt

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Lower and Middle Miocene biostratigraphy, Gulf of Suez, Egypt based on dinoflagellate cysts and

calcareous nannofossils

Ali Solimana,b*, Stjepan Coricc, Martin J. Headd, Werner E. Pillera and Salah Y. El Beialye

aInstitute of Earth Sciences (Geology and Palaeontology), University of Graz, Heinrichstrasse 26, A-8010 Graz, Austria;bGeology Department, Faculty of Science, Tanta University, Tanta 31527, Egypt; cGeological Survey of Austria, Sedimentary

Geology Sector, Neulinggasse 38, A-1030 Vienna, Austria; dDepartment of Earth Sciences, Brock University, 500 Glenridge Avenue,St. Catharines, Ontario L2S 3A1, Canada; eGeology Department, Faculty of Science, Mansoura University,

Mansoura 35516, Egypt

This is the first detailed stratigraphic correlation of Lower and Middle Miocene deposits in the Gulf of Suez, Egyptusing dinoflagellate cysts. The correlation is based on 273 ditch-cutting samples from five onshore boreholes locatedalong the southwestern margin of the Gulf of Suez. The interval studied is represented by the Nukhul, Rudeis andKareem formations of the Gharandal Group, and the lower part of the Belayim Formation of the Ras MalaabGroup. These Miocene deposits unconformably overlie the Lower or lower Middle Eocene. The dinoflagellate cystrecord is more diverse than previously reported and many taxa are documented for the first time in Egypt. Fivebiozones are established and tied to a chronostratigraphic framework by calibration to calcareous nannofossils (NNbiozones) obtained from the same set of samples: (1) Lingulodinium machaerophorum Assemblage Biozone (GOS1),Aquitanian through mid-Burdigalian; (2) Exochosphaeridium insigne Taxon-range Biozone (GOS2), lower throughmid-Burdigalian; (3) Apteodinium spiridoides Interval Biozone (GOS3), mid-Burdigalian through lower Langhian;(4) Cleistosphaeridium placacanthum Interval Biozone (GOS4), upper Burdigalian, Langhian, and lowerSerravallian?); and (5) Polysphaeridium zoharyi Assemblage Biozone (GOS5), upper Langhian and Serravallian?Comparison with other Miocene biozonations from the Mediterranean, Central Paratethys, North Atlantic

region, and eastern USA indicate that the highest occurrences of Apteodinium spiridoides, Cordosphaeridiumcantharellus, Distatodinium paradoxum, Exochosphaeridium insigne and Cleistosphaeridium placacanthum, and thelowest occurrences of Exochosphaeridium insigne and Sumatradinium soucouyantiae are important datums, whereasthe lowest occurrences of Hystrichosphaeropsis obscura, Labyrinthodinium truncatum, and Operculodinium?borgerholtense provide useful supporting age control.

Keywords: dinoflagellate cysts; calcareous nannofossils; Miocene; Gulf of Suez; Egypt

1. Introduction

Dinoflagellate cysts are proving increasingly useful forbiostratigraphy in the Neogene of the Mediterraneanrealm, Central Paratethys, northern Atlantic region,eastern United States, and various other localities (e.g.Powell 1986a, 1986b, 1992; Head et al. 1989a, 1989b;Brinkhuis et al. 1992; Zevenboom 1995; de Verteuiland Norris 1996; Jimenez-Moreno et al. 2006; Dybkjærand Piasecki, 2008, 2010). Although they have beenused to solve problems of correlation in Miocenedeposits in the Gulf of Suez, Egypt (Mahmoud 1993;Ahmed and Pocknall 1994; El Beialy and Ali 2002), adetailed dinoflagellate cyst biostratigraphy has not yetbeen established. Calcareous nannofossils are ofunquestionable stratigraphic value in the MiddleEast, but have been considered only infrequently inpublished stratigraphic investigations of the Neogeneof the Gulf of Suez area (El-Heiny and Martini 1981;

Arafa 1982; El-Heiny 1982; Marzouk 1998, 2009;Mandur 2009).

Our study is based on 273 ditch-cutting samplesfrom five deep onshore boreholes, Shukheir-1, EastShukheir-1, Shukheir-11, Shukheir-13A, and Kareem-30, that penetrated siliciclastics and carbonates ofEarly and Middle Miocene age along the southwesternmargin of the Gulf of Suez (Figures 1 and 2). We aimto document the distribution of calcareous nannofossil(Figures 3–7) and palynomorph (Figures 8–12) taxapresent in the Lower and Middle Miocene of theseboreholes, establish a dinoflagellate cyst biostratigra-phy calibrated to the calcareous nannofossil data, andcompare the dinoflagellate cyst assemblages from theGulf of Suez with published data from the Mediterra-nean, North Atlantic and other regions. The timescales of Luterbacher et al. (2005) for the Paleogeneand Lourens et al. (2005) for the Neogene are used

*Corresponding author. Email: [email protected]

Palynology

iFirst article 2012, 1–42

ISSN 0191-6122 print/ISSN 1558-9188 online

� 2012 AASP – The Palynological Society

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throughout, and ages in the literature based on earliertime scales have been updated accordingly.

2. Geologic setting

The Gulf of Suez is a shallow and narrow body ofwater extending for 350 km from Suez southwards tothe tip of the Sinai Peninsula, and covering an area ofabout 25,000 km2 at an average depth of 55–100 m(Schlumberger 1984). This elongated depression sepa-rates the massifs of south and central Sinai from thoseforming the backbone of the Eastern Desert of Egypt.The comparatively low relief either side of the Gulf ofSuez consists chiefly of Miocene and younger deposits(Figure 1). The Gulf of Suez is an intensely faultedarea, and its present shape has been determined byfracture systems caused by movements of the Nubianand Arabian shields and Sinai micro-plate.

The Gulf of Suez is the main oil province in Egypt,oil being produced from Paleozoic, Mesozoic andCenozoic rocks. The Miocene reservoirs are the mostprolific producers in many fields both on land andoffshore. The evaporite beds in the lower Kareem,Belayim and South Gharib formations represent aneffective seal. Among the potential oil-prone sourcerocks are the Kareem and Rudeis formations, whereasthe Belayim Formation is classified as oil- and gas-prone source rock (El Ayouty 1990; figure 2).

The stratigraphy of the Gulf of Suez can besubdivided into pre-rift, syn-rift and post-rift succes-sions (Plaziat et al. 1998). The pre-rift successionincludes strata that were deposited prior to rifting andare represented by Paleozoic to Lower Eocenedeposits. Syn-rift strata were deposited during activemechanical extension and subsidence, and are repre-sented by the Miocene deposits. The post-rift succes-sion includes strata that overlie syn-rift strata and arerepresented by Pliocene and Quaternary deposits(Figures 1 and 2).

The Miocene in the Gulf of Suez basin ischaracterized by rapid lateral changes in facies inresponse to Miocene block-faulting and an irregularbottom topography. Up to 5000 m of Neogene syn-riftand post-rift deposits overlie up to 2000 m of Eoceneand older pre-rift strata in the axial trough of the Gulfof Suez graben (Evans 1988). All these deposits arewell exposed and penetrated by hundreds of explora-tory boreholes.

The lithostratigraphy of the Miocene deposits inthe Gulf of Suez in general, and outcrops in west Sinaiin particular, have been studied and classified by manyworkers (e.g. Moon and Sadek 1923, 1925; Sadek 1959;Ghorab and Gezeery 1969; National Committee forGeological Sciences (NCGS) 1976). The most com-monly used classification is that of the NCGS (1976),which is adopted in the present study (Figure 2).According to the NCGS, the Miocene in the Gulf

Figure 1. Location of the studied area. A, the Gulf of Suez;B: locations of the studied boreholes; and C, simplifiedgeological map showing Miocene exposures around the Gulfof Suez (Conoco 1989).

Figure 2. Lithostratigraphy of the Miocene in the Gulf ofSuez according to NCGS (1976). *Member names as definedin the study area (e.g. GPC 1966).

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of Suez region is classified into two major litho-stratigraphic units. The Gharandal Group (syn-rift)contains the richest petroleum source rocks in com-bination with excellent reservoir deposits formed underfavorable structural conditions. The Ras MalaabGroup (syn- and post-rift) provides an efficient sealfor both pre-Miocene and Miocene reservoirs. TheMiocene rock units in the Gulf of Suez, arranged fromolder to younger (NCGS 1976; figure 2), are givenbelow.

2.1. Gharandal Group

Nukhul Formation. In the study area, this formationunconformably overlies Eocene deposits and conform-ably underlies the Rudeis Formation of the Gharandal

Group. In general, it mostly comprises unfossiliferoussandstones, conglomerates, carbonates, shales andevaporites. In the study area, it consists predominantlyof light grey argillaceous limestone in the Shukheir-11(questionably identified) and Shukheir-13A boreholes,whereas in the East Shukheir-1 borehole its lower partis mainly limestone and it becomes predominantlysandy towards the top. The Nukhul Formation ispoorly dated due to the scarcity of diagnosticplanktonic foraminifera and calcareous nannofossils(El-Heiny and Martini 1981; present study), althoughit has generally been considered to predate nannofossilzone NN3 (Evans 1988).

Rudeis Formation. The Rudeis Formation is laterallyequivalent to an outcrop in the northern part of theGulf of Suez known as the Globigerina marl of Humeet al. (1920). It represents a thick clastic section abovethe Nukhul Formation and below the first anhydritebed of the Kareem Formation, and is cyclicallyinterbedded with fine-grained, deep-water limestones(Bosworth et al. 1998). At its type section, the RudeisFormation (780 m) consists of sandy shales, fossilifer-ous calcareous shales with hard sandstone beds, andminor limestone intercalations (NCGS 1976). In thestudied boreholes, it consists mainly of intercalatedsand, sandstone, and shale, with sporadic occurrencesof thin beds of limestone and evaporites. A majorlateral thickness variation, between 213 m in theKareem-30 borehole and 619 m in the Shukheir-1borehole, is observed.

Kareem Formation. This is the uppermost formationin the Gharandal Group. Its lower part represents theoldest extensive evaporite development in the Gulf ofSuez (the older Nukhul Formation representing onlyminor development). It is differentiated into theRahmi and Shagar members. It overlies conformablythe Rudeis Formation and is overlain conformably bythe Belayim Formation. It consists of white to lightgrey massive anhydrite interbeds in the RahmiMember, and mostly grey highly-calcareous shales,grading into marl, with occasional grey argillaceouslimestone intercalations in the overlying ShagarMember.

2.2. Ras Malaab Group

Belayim Formation. This formation is differentiatedinto four members: Baba, Sidri, Feiran, and HammamFaraun. It represents the beginning of the majorMiocene evaporite cycle following the shales of theKareem Formation. The overlying South Gharib andZeit formations are not considered here due to theunavailability of samples.

Figure 3. Distribution of stratigraphically importantcalcareous nannofossils in the Shukheir-1 borehole, Gulf ofSuez. The sample depth refers to an interval, usually 3 m,and is abbreviated, e.g. 1200–3 m¼ 1200–1203 m. Thenannofossil zonation is after Martini (1971). Preservation(also for Figures 4–7) was ranked using the following scale:G¼ good, M¼moderate, and P¼ poor. Abundances (alsofor Figures 4–7) are as follows: a¼ abundant (450%),c¼ common (10–50%), f¼ few (510%), r¼ rare (fewspecimens at most). An ‘x’ indicates that because of ascarcity of nannofossils no relationships between theabundances of species could be established.

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3. Material and methods

This study is based on 273 ditch-cutting samples fromthe Kareem-30, Shukheir-1, Shukheir-11, Shukheir-13A and East Shukheir-1 boreholes that penetrated theNukhul, Rudeis, Kareem and Belayim formations(Figure 1). Standard palynological processing techni-ques were used to extract and concentrate thedinoflagellate cysts (Wood et al. 1996; Green 2001).Approximately 5 to 10 g of sediment were processed foreach sample. Up to 50 ml of cold 35%HCl followed by30 to 50 ml of cold, concentrated 48% HF for 48–72 hwere employed to dissolve carbonates and silicates,respectively. The residues were washed repeatedly withdistilled water until neutral. Material coarser than

125 mm was removed with a brass sieve. The 5125 mmfraction was decanted and washed through a 10 mmnylon sieve for counting. For photography and SEMinvestigations, the residues of some samples were re-sieved using 20 mm nylon sieves. Residues were treatedfor ca. 30 s in an ultrasonic bath before sieving.Schulz’s solution (50:50% mixture of HNO3þKClO3)was applied to some samples. The residues were stainedwith safranin ‘o’, and mounted onto microscope slidesusing glycerine jelly. Specimens were counted until ca.250 dinoflagellate cysts had been registered on a slide,where possible. Counts are given in Figures 8–12. Theremainder of the slide was then searched for rare taxa,which are represented by an ‘x’ in Figures 8–12. For

Figure 4. Distribution of stratigraphically important calcareous nannofossils in the East Shukheir-1 borehole, Gulf of Suez.The nannofossil zonation is after Martini (1971). See Figure 3 for abbreviations of relative abundance, preservation, and sampledepth.

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samples in which dinoflagellates are rare, at least twoslides were scanned and counted. Specimens werephotographed under light microscopy using a LeicaDMRmicroscope and Leica DFC 490 camera at BrockUniversity (Plates 1–5). An England Finder referencefollows the sample and slide number for each illustratedspecimen. Sample preparation for SEM investigationfollows Head et al. (1989a). Mounts for SEM studieswere made by air drying water-suspended residues onglass coverslips that were mounted on aluminium stubswith thin double-sided sticky tape. Stubs were coatedwith platinum. Observations and photographs weremade using a DSM 982 Gemini SEM, operating at a

working voltage of 10 to 15 kV, housed in the Instituteof Earth Sciences, University of Graz, Austria. Selectedtaxa are illustrated on Plate 6. All slides, SEM stubs,and residues are housed in the paleontological collec-tion of the Institute of Earth Sciences, University ofGraz, Austria.

In total, 268 samples were analyzed for nannofos-sils, using the same samples as those analyzed fordinoflagellate cysts. Before preparing microscope slidesfor calcareous nannofossil investigation, a smallquantity of sediment was treated for a few seconds inan ultrasonic bath. One or more sedimentary cuttingsper sample was processed, depending upon the size ofcuttings for each sample. Microscope slides wereanalyzed to determine zonal boundaries as accuratelyas possible. The biostratigraphic interpretation of theinvestigated sections is based on the calcareousnannofossil zonation of Martini (1971). The relativeabundances of species were determined using a lightmicroscope with a magnification of 10006. Selectedtaxa are illustrated on Plate 7, and the stratigraphicdistributions of diagnostic taxa are given in Figures3–7.

We use the dinoflagellate cyst nomenclature ofFensome et al. (2008), where the taxonomic referencesare cited. The thicknesses of formations are calculatedon the mid-point between the lowest sample of oneformation and the highest sample of the subjacentformation.

4. Nannofossil biozonation

4.1. Paleocene–Eocene interval

In the East Shukheir-1 borehole (Figure 4), the lowestpart of the investigated section, 2088–2025 m (samples65–61), contains Lower Eocene and lower MiddleEocene calcareous nannofossils with Coccolithus for-mosus, Discoaster kuepperi, Ericsonia cava, Neococco-lithus dubius, Pontosphaera plana, Sphenolithus radiansetc., and can be attributed to the mid-Ypresian tolower Lutetian (zones NP12–NP14).

The occurrence of Discoaster kuepperi in theShukheir-13A borehole (Figure 6), sample 41 (1500–1503 m), also allows attribution to the mid-Ypresian tolower Lutetian (NP12–NP14). Based on rich, well-preserved calcareous nannofossils with Campulo-sphaera dela, Discoater multiradiatus, Ellipsolithusmacellus, Neochiastozygus concinnus, Toweius crassus,Toweius rotundus, etc., sample 42 (1515–1518 m) isattributed to nannofossil zone NP9 (uppermost Tha-netian–lower Ypresian).

The lowermost part of the Shukheir-1 borehole(Figure 3) belongs to the mid-Ypresian to lowerLutetian and can be subdivided into zones NP12–14(sample 39, 1815–1818 m with Discoaster kuepperi)

Figure 5. Distribution of stratigraphically importantcalcareous nannofossils in the Shukheir-11 borehole, Gulfof Suez. The nannofossil zonation is after Martini (1971). SeeFigure 3 for abbreviations of relative abundance,preservation, and sample depth.

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and zone NP11 (samples 44 to 41, 1923–1860 m, basedon the presence of Discoaster multiradiatus and theabsence of Discoaster lodoensis). Within this interval,sample 40 (1845–1848 m) contains downhole contam-ination as evidenced by a Lower Miocene nannofossilassemblage including Sphenolithus disbelemnos.

4.2. Unzoned Lower Miocene interval

In the Shukheir-1 borehole, an unzoned LowerMiocene interval is defined in samples 38 through 36(1803–1770 m). There are no Oligocene markers, butSphenolithus dissimilis in sample 38 ranges from theuppermost Oligocene to lowermost NN4 (mid-Burdi-galian), and Helicosphaera carteri in the same samplepoints to a Miocene age.

4.3. Discoaster druggii Zone (NN2)

Zone NN2 is defined as the interval from the lowestoccurrence (LO) of Discoaster druggii to the highest

occurrence (HO) of Triquetrorhabdulus carinatus. Itspans an interval from lowermost Aquitanian to mid-Burdigalian (22.76–18.28 Ma; Lourens et al. 2005).Calcareous nannofossils of this zone are generally oflow diversity. Discoaster druggii is often difficult todetermine or to distinguish from other discoasterids(especially from Discoaster deflandrei) because of itspropensity to become overgrown and thereby losediagnostic features. The highest occurrence datum(HOD) of Helicosphaera ampliaperta (20.43 Ma;Lourens et al. 2005) is recorded in the upper part ofthis zone.

In the Kareem-30 borehole (Figure 7), zone NN2 isnot clearly defined but samples 60 (798–801 m) and 59(795–798 m) may be attributable to it.

In the East Shukheir-1 borehole, zone NN2 isdefined in samples 56 through 43 (1938–1680 m). Basedon the co-occurrence of Helicosphaera ampliapertawith Triquetrorhabdulus carinatus in the East Shukheir-1, the upper part of zone NN2 is suggested. Calcareousnannofossil assemblages are characterized by scarce,

Figure 6. Distribution of stratigraphically important calcareous nannofossils in the Shukheir-13A borehole, Gulf of Suez. Thenannofossil zonation is after Martini (1971). See Figure 3 for abbreviations of relative abundance, preservation, and sampledepth. R.M.¼Ras Malaab, S.Gh.¼ South Gharib.

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generally moderately preserved nannofossils with:Coccolithus pelagicus, Cyclicargolithus floridanus, Re-ticulofenestra bisecta, Reticulofenestra minuta, Reticu-lofenestra pseudoumbilica, Sphenolithus moriformis,

Thoracosphaera heimii, Thoracosphaera saxea andUmbilicosphaera jafari. The scarcity of specimens insamples 59 and 58 (1998–1980 m) of the East Shukheir-1 borehole does not allow an exact stratigraphic

Figure 7. Distribution of stratigraphically important calcareous nannofossils in the Kareem-30 borehole, Gulf of Suez. Thenannofossil zonation is after Martini (1971). See Figure 3 for abbreviations of relative abundance and preservation.

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Figure

8.

Stratigraphic

distributionofdinoflagellate

cystsandother

aquaticpalynomorphsin

theShukheir-1borehole,GulfofSuez.Thesample

depth

refers

toaninterval,

usually3m,andisabbreviated,e.g.1200–3m¼1200–1203m.Numbersindicate

raw

counts.Thegeochronologyisbasedonthepresentednannofossilzonation(Figure

3)and

usesthetimescale

ofLuterbacher

etal.(2005)andLourenset

al.(2005).

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Figure

9.

Stratigraphic


cystsandother


theEast

Shukheir-1borehole,GulfofSuez.Thesample

depth

refers

toan

interval,usually3m,andisabbreviated,e.g.1050–3m¼1050–1053m.Numbersindicate

raw

counts.Thegeochronologyisbasedonthepresentednannofossilzonation

(Figure

4)andusesthetimescale

ofLuterbacher


al.(2005).

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Figure

10.

Stratigraphic


cystsandother


theShukheir-11borehole,GulfofSuez.Thesample

depth

refers

toan

interval,usually3m,andisabbreviated,e.g.675–8m¼675–678m.Thegeochronologyisbasedonthepresentednannofossilzonation(Figure

5)andusesthetimescaleof

Lourenset

al.(2005).

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Figure

11.

Stratigraphicdistributionofdinoflagellate

cystsandother


theShukheir-13A

borehole,GulfofSuez.Numbersindicate

rawcounts.The

geochronologyisbasedonthepresentednannofossilzonation(Figure


ofLuterbacher


al.(2005).

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Figure

12.

Stratigraphic


cystsandother


theKareem

-30borehole,GulfofSuez.Numbersindicate

raw

counts.The

geochronologyisbasedonthepresentednannofossilzonation(Figure


ofLourenset

al.(2005).


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determination, but an Early Miocene age (zones NN1–NN2) is suggested, based on the absence of olderforms.

4.4. Sphenolithus belemnos Zone (NN3)

This nannofossil zone was defined by Bramlette andWilcoxon (1967) and emended by Martini (1971) as theinterval from the HO of Triquetrorhabdulus carinatusto the HO of Sphenolithus belemnos. Zone NN3 spansan interval from 18.28 to 17.95 Ma (Lourens et al.2005) within the mid-Burdigalian. Because Triquetror-habdulus carinatus is common only in open marinedeposits, the LO of Sphenolithus belemnos can be usedas a secondary marker for the base of zone NN3. ZoneNN3 is a very short zone and not defined in allboreholes.

In the Kareem-30 borehole, the HO of Sphenolithusbelemnos was observed in sample 48 (732–735 m). Theinterval from this sample down to sample 58 (789–792m) would be assignable to zone NN3. However,Sphenolithus heteromorphus also occurs throughoutthis interval, and S. belemnos and S. heteromorphus co-occur only in the lowermost NN4. It is not known ifthe occurrence of S. heteromorphus in this interval iscaused by downhole contamination, or if that of S.belemnos is caused by reworking. This interval istherefore assigned to NN3 and/or NN4. All investi-gated samples contain well-preserved, common nan-nofossils, with the nannoflora being similar to theupper part of the hole, dominated by reticulofenestrids(Reticulofenestra gelida, Reticulofenestra haqii, Reticu-lofenestra minuta, Reticulofenestra pseudoumblica). TheLower Miocene Sphenolithus disbelemnos is rare butpresent.

In the East Shukheir-1 borehole, Triquetrorhabdu-lus carinatus has its HO between samples 43 (1680–1683 m) and 42 (1665–1668 m). Sphenolithus belemnoswas determined only in sample 41 (1650–1653 m). Itallows the attribution of this interval to zone NN3.

4.5. Helicosphaera ampliaperta Zone (NN4)

The interval from the HO of Sphenolithus belemnos tothe HO of Helicosphaera ampliaperta defines theHelicosphaera ampliaperta Zone (NN4) of Bramletteand Wilcoxon (1967) as emended by Martini (1971).The time from the mid-Burdigalian to the mid-Langhian (17.95–14.91 Ma; Lourens et al. 2005) isrepresented by this zone. The LO of Sphenolithusheteromorphus (17.71 Ma) is close to the HO ofSphenolithus belemnos and can be used as an additionalmarker for the base of zone NN4.

In the Kareem-30 borehole, an interval betweensamples 47 (726–729 m) and 29 (621–624 m) is

characterized by the presence of Helicosphaera amplia-perta, Helicosphaera scissura and Sphenolithus hetero-morphus, and the absence of Sphenolithus belemnos.Nannofossil assemblages from this interval do notcontain small helicoliths (Helicosphaera minuta andHelicosphaera walbersdorfensis). Deposits from zoneNN4 contain more Reticulofenestra pseudoumbilicaand Coccolithus pelagicus than sediments from zoneNN5 (see below).

In the Shukheir-13A borehole, the HO of Helico-sphaera ampliaperta in sample 16 (1125–1128 m) andthe LO of Helicosphaera ampliaperta in sample 36(1425–1428 m) are clearly expressed. This interval istherefore attributed to zone NN4, based on the HO ofHelicosphaera ampliaperta. The lower part of thisinterval contains Helicosphaera scissura. In samples 35(1410–1413 m) to 31 (1350–1353 m), Sphenolithusdisbelemnos is recorded. Sample 39 (1470–1473 m)contains Sphenolithus heteromorphus (few) and istherefore attributed to zone NN4.

In the Shukheir-1 borehole, the HO of Helico-sphaera ampliaperta was judged to be in sample 8(1335–1338 m), although a few specimens occur insample 4 (1275–1278 m). Based on the highestcontinuous occurrence of Helicosphaera ampliapertaand the presence of Sphenolithus heteromorphus, theinterval from sample 8 down to sample 35 (1755–1758 m) can be attributed to zone NN4. The intervalwith Helicosphaera ampliaperta (1335–1743 m) ischaracterized by well-preserved assemblages similarto the interval assigned to zone NN5 (see below). Theabundance of Braarudosphaera bigelowii in zone NN4of this borehole is notable as it implies lower salinites.

In the Shukheir-11 borehole (Figure 5), Spheno-lithus heteromorphus co-occurs continuously withHelicosphaera ampliaperta from sample 34 (1170–1173 m) down to sample 62 (1590–1593 m), allowingthis interval to be attributed to zone NN4. Accom-panying forms are: Coccolithus miopelagicus, Cocco-lithus pelagicus, Cyclicargolithus floridanus,Helicosphaera carteri, reticulofenestrids (Reticulofenes-tra daviesii, Reticulofenestra gelida, Reticulofenestrahaqii, Reticulofenestra minuta, Reticulofenestra pseu-doumbilica) Sphenolithus moriformis, Thoracosphaeraheimii, Thoracosphaera saxea, and Umbilicosphaerajafari.

In the East Shukheir-1 borehole, the intervalbetween the HO of Sphenolithus belemnos in sample41 (1650–1653 m) and the HO of Helicosphaeraampliaperta in sample 24 (1395–1398 m) is assignedto zone NN4. The assemblages contain suchhelicoliths as Helicosphaera ampliaperta, Helicosphaeracarteri, Helicosphaera euphratis, and Helicosphaerascissura, which occur continuously throughout thisinterval.

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4.6. Sphenolithus heteromorphus Zone (NN5)

Zone NN5 is defined as the interval from the HO ofHelicosphaera ampliaperta to the HO of Sphenolithusheteromorphus. It spans an interval from mid-Lan-ghian to lowermost Serravallian (14.91–13.53 Ma;

Lourens et al. 2005). The stratigraphically importantshort-ranging species Helicosphaera waltrans, de-scribed from the Mediterranean (Theodoridis 1984)where it occurs in the uppermost part of zone NN4 andthe lowermost part of NN5, was indentified in samples


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from the Kareem-30, Shukheir-13A, Shukheir-11 andEast Shukheir-1 boreholes. Abdul Aziz et al. (2008)determined a lowest common occurrence at 15.476 Maand a highest common occurrence at 14.357 Ma forthis species in the western Mediterranean. The restric-tion of Helicosphaera waltrans to the lowermostsamples of zone NN5 could point to a hiatus ataround the NN4/NN5 boundary.

In the Kareem-30 borehole, the absence of Helico-sphaera ampliaperta and the presence of Sphenolithusheteromorphus in the interval between samples 28 (615–618 m) and 1 (435–438 m) allows its allocation to zoneNN5. The upper part of this interval (samples 18–1) ischaracterized by well-preserved and abundant calcar-eous nannofossils with abundant Reticulofenestraminuta. Regularly occurring species are: Coccolithusmiopelagicus, Coccolithus pelagicus, Cyclicargolithusfloridanus, Helicosphaera carteri, Helicosphaera minu-ta, Helicosphaera walbersdorfensis, Micrantholithusvesper, Reticulofenestra gelida, Reticulofenestra haqii,Reticulofenestra pseudoumbilica, Sphenolithus hetero-morphus, Sphenolithus moriformis, Thoracosphaeraspp., and Umbilicosphaera jafari. The lower part ofthis interval (samples 28–20) contains common andgenerally well-preserved nannofossils, as for the upperpart, but with a greater percentage of Coccolithuspelagicus. This part of the hole also contains higheramounts of Middle Miocene discoasterids, namelyDiscoaster adamanteus, Discoaster exilis, Discoastermusicus, and Discoaster variabilis. The two lowermostsamples from this interval (samples 28, 615–618 m; and27, 609–612 m) contain the biostratigraphically im-portant species Helicosphaera waltrans.

In the Shukheir-13A borehole, the assignment ofsamples 12 and 13 to zone NN5 is based on the absenceof Helicosphaera ampliaperta and the presence ofSphenolithus heteromorphus and Helicosphaera wal-trans. The following species also occur: Coccolithusmiopelagicus, Coccolithus pelagicus, Helicosphaera

carteri, Pontosphaera multipora, Reticulofenestra haqii,Reticulofenestra minuta, and Sphenolithus moriformis.Samples 14 and 15 are barren of nannofossils.

In the Shukheir-1 borehole, calcareous nannofossilsfrom zone NN5 (1323–1200 m) are generally wellpreserved and contain common Coccolithus pelagicus.Accompanying forms are: Cyclicargolithus floridanus,Helicosphaera carteri, Reticulofenestra gelida, Reticu-lofenestra haqii, Reticulofenestra minuta, Reticulofenes-tra pseudoumbilica, Sphenolithus heteromorphus,Sphenolithus moriformis, Thoracosphaera heimii, andThoracosphaera saxea.

In the Shukheir-11 borehole, Helicosphaera amplia-perta has its HO in sample 34 (1170–1173 m). There-fore, the interval from sample 33 (1155–1158 m) to 11(825–828 m), which contains Sphenolithus heteromor-phus, is attributed to zone NN5. Overlying deposits(samples 10–8; 813–780 m) contain sparse nannofossilassemblages without Sphenolithus heteromorphus, butwith an otherwise typical NN5 nannoflora. Thisinterval probably also belongs to zone NN5. Thebiostratigraphically important species Helicosphaerawaltrans was recognized in the lowermost part of zoneNN5, in sample 31 (1125–1128 m). Small reticulofe-nestrids are the most abundant component of thenannofossil assemblages. The following species occurcontinuously, except for an interval of low recoveryfrom samples 19 (945–948 m) to 12 (840–843 m):Coccolithus pelagicus, Helicosphaera carteri, Reticulo-fenestra pseudoumbilica, Sphenolithus heteromorphus,Sphenolithus moriformis, and Umbilicosphaera jafari.

In the East Shukheir-1 borehole, the NN4/NN5zonal boundary, defined by HO of Helicosphaeraampliaperta, is placed between samples 24 (1395–1398m) and 23 (1380–1383 m). Although deposits of zoneNN5 are characterized by scarce assemblages, mostsamples contain Sphenolithus heteromorphus. Accom-panying species are: Coccolithus miopelagicus, Cocco-lithus pelagicus, reticulofenestrids (Reticulofenestra

Plate 1. Dinoflagellate cysts from the Gulf of Suez. All images are in bright field illumination except for Figures 1, 2, 5, and 6which are in interference contrast illumination. The sample number, slide number (in parentheses), and England Finder referenceare given sequentially for each specimen, where K30¼Kareem-30 borehole, Sh1¼ Shukheir-1 borehole, and ESh1¼EastShukheir-1 borehole. Various magnifications. Max. dia.¼maximum diameter. Figures 1, 2. Apteodinium spiridoides Benedek1972. Ventral view (1) of ventral surface, and (2) at mid-focus; length¼ 88 mm. Sample Sh1-23 (2), D45/0. Figures 3, 4.Apteodinium sp. 1. Left lateral view (3) of upper surface, and (4) at mid-focus; note thick (ca. 2.0 mm) wall with coarselygranulated/pitted surface, and shallow grooves faintly indicating tabulation along the cingular margins and incompletelyelsewhere on epi- and hypocyst; grouped with ‘Apteodinium/Cribroperidinium spp. indet.’ in the range chart; length¼ 67 mm.Sample K30-55 (3), T54/0. Figures 5, 6. Cribroperidinium giuseppei (Morgenroth 1966) Helenes 1984. Ventral view (5) of ventralsurface, and (6) at slightly lower focus; length¼ 94 mm. Sample K30-55 (3), Q52/2. Figures 7, 8. Cribroperidinium sp. 1. Leftlateral view (7) at mid-focus, and (8) of right lateral surface; length¼ 105 mm. Sample K30-13 (3), G37/3. Figures 9, 10.Hystrichokolpoma rigaudiae Deflandre & Cookson 1955. Equatorial view at (9) low focus and (10) lower focus; central bodylength¼ 43 mm. Sample K30–55 (3) E38/0. Figure 11. Cordosphaeridium cantharellus (Brosius 1963) Gocht 1969. Antapical viewat mid-focus; central body max. dia.¼ 85 mm. Sample ESh1-38 (2) N45/0. Figures 12, 13. Operculodinium? borgerholtense Louwye2001, emend. Soliman et al. 2009. Uncertain view (12) of upper surface, and (13) at slightly lower focus; central body max.dia.¼ 36 mm. Sample K30-28 (4) W34/4. Figures 14, 15. Operculodinium piaseckii Strauss & Lund 1992. Uncertain view (14) ofupper surface, and (15) at mid-focus. Central body max. dia.¼ 46 mm. Sample K30-14 (3) K49/0.

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gelida, Reticulofenestra haqii, Reticulofenestra minuta,Reticulofenestra pseudoumbilica), Sphenolithus morifor-mis, Thoracosphaera heimii, Thoracosphaera saxea, andUmbilicosphaera jafari. Helicoliths are represented by:Helicosphaera carteri, Helicosphaera euphratis, Helico-sphaera intermedia, Helicosphaera perch-nielseniae,Helicosphaera vedderi, Helicosphaera walbersdorfensis,Helicosphaera wallichii, and Helicosphaera waltrans.Sample 12 contains Sphenolithus heteromorphus and isassigned to zone NN5, whereas samples 9 and 8 areplaced questionably in NN5, as discussed below.

4.7. Upper unzoned interval

In the East Shukheir-1 borehole, the uppermost part ofthe investigated sequence (samples 11–1, 1203–1050 m)includes evaporites and typically lacks nannofossils.Samples 9 (1200–1203 m) and 8 (1170–1173 m) containvery scarce and poorly-preserved nannofossils thatprobably belong to nannofossil zone NN5. In theShukheir-13A borehole, evaporitic deposits from sam-ples 11 (1050–1053 m) to 1 (903–906 m) contain rarenannofossils with no stratigraphic significance. In theShukheir-11 borehole, the two uppermost samples 7(765–768 m) and 6 (750–753 m) retrieved from asandstone interval contain only reworked Paleogenenannofossils. Samples 1–5 were not available foranalysis.

5. Dinoflagellate cyst zonation and age significance

More than 88 in situ species of dinoflagellate cystbelonging to 50 genera have been identified, indicatinga higher diversity than previously reported for theLower and Middle Miocene of the Gulf of Suez and

indeed Egypt (e.g. El Beialy and Ali 2002). Preserva-tion is generally good, although abundance and speciesrichness vary significantly throughout the successionsstudied.

The identification of marker species has allowed theestablishment of five local dinoflagellate cyst biozones(GOS1–GOS5) for the Lower and Middle Miocene ofthe southern Gulf of Suez basin. These species havebeen selected on the basis of their persistent occur-rence. Secondary markers occur less persistently. Thecomposite ranges of all dinoflagellate cyst and acri-tarch taxa are presented in Tables 1 and 2, and theirdistributions in the studied boreholes are documentedin Figures 8–12. In the East Shukheir-1 borehole,dinoflagellate cyst abundance and diversity are good,and the calcareous nannofossil zonal boundaries aredefined unambiguously. Accordingly, this borehole isused as a reference section.

One unzoned interval, dated as Paleocene–Eocenefrom our nannofossil biostratigraphy, immediatelyunderlies the lowest dinoflagellate cyst biozone(GOS1). It contains relatively undiagnostic Paleogenedinoflagellate cyst species and is therefore not definedformally.

All samples used are from ditch cuttings, whichmight have rendered the lowest occurrences of taxaunreliable for biostratigraphy due to caving (Stoveret al., 1996). We have therefore used the highestoccurrences of taxa to define the tops of our zoneswhere possible, but zone GOS2 is defined by the LO ofExochosphaeridium insigne owing to a paucity ofmarker species in the subjacent zone GOS1. Weconsider both highest and lowest occurrences whencomparing with records from Egypt, the Mediterra-nean, North Atlantic, eastern USA, and elsewhere, to

Plate 2. Dinoflagellate cysts from the Gulf of Suez. All images are in bright field illumination except for Figures 9 and 10 whichare in interference contrast illumination. The sample number, slide number (in parentheses), and England Finder reference aregiven sequentially for each specimen, where K30¼Kareem-30 borehole, Sh1¼ Shukheir-1 borehole, and Sh11¼ Shukheir-11borehole. Various magnifications. Max. dia.¼maximum diameter. Figures 1, 2. Hystrichosphaeropsis obscura Habib 1972. Leftlateral view (1) of left lateral surface, and (2) at mid-focus; length¼ 95 mm. Sample Sh1-1 (3), X36/4. Figures 3, 4.‘Hystrichosphaeropsis minimum’ of Zevenboom & Santarelli in Zevenboom 1995. Left latero-dorsal view (3) of left latero-dorsalsurface, and (4) at mid-focus; note strongly reduced apical pericoel that characterizes this morphotype; periblast length¼ 62 mm.Sample K30-20 (4), D35/3. Figures 5–8. ‘Hystrichosphaeropsis minimum’ Zevenboom & Santarelli in Zevenboom 1995. Dorsalview of (5) dorsal surface, and at progressively lower foci to (8) ventral surface; periblast length¼ 75 mm. Sample K30-3 (3),C34/0. Figures 9, 10. Nematosphaeropsis labyrinthus (Ostenfeld 1903) Reid 1974. Uncertain view at (9) upper focus, and (10)lower focus; central body max. dia.¼ 27 mm. Sample K30-13 (3), T39/0. Figures 11, 12. Nematosphaeropsis lativittata Wrenn1988. Uncertain view at (11) mid-focus, and (12) lower focus; ectoblast max. dia.¼ 47 mm. Sample K30-14 (3), P46/2. Figures 13,14. Nematosphaeropsis sp. 1. Equatorial? view at (13) mid-focus showing coarsely granulate central body surface, and (14) lowerfocus; grouped with ‘Nematosphaeropsis spp. indet.’ in the range chart; central body max. dia.¼ 42 mm. Sample K30-52 (4), J51/1. Figures 15, 16. Spiniferites mirabilis (Rossignol 1964) Sarjeant 1970. Dorsoventral view at (15) mid-focus, and (16) lower focus;central body length¼ 50 mm. Sample K30-55 (3), H38/3. Figures 17, 18. Spiniferites pseudofurcatus (Klumpp 1953) Sarjeant 1970.Uncertain view at (17) upper focus, and (18) mid-focus; central body length¼ 64 mm. Sample K30-12 (4), X29/0. Figures 19, 20.Spiniferites solidago de Verteuil & Norris 1996. Uncertain view at (19) upper focus, and (20) mid-focus; note that most processstems have one vacuole, although some have several and a few none; that the central body wall is more-or-less homogenousexcept for some barely visible and sparsely scattered perforations (dia. 51.0 mm); and that processes are mostly gonal but someare intergonal; central body max. dia.¼ 47 mm. Sample Sh11-31 (2), S34/2.

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determine the age significance of taxa in the Gulf ofSuez. The calcareous nannofossil data on our samplesprovide independent chronostratigraphic control forthe dinoflagellate cyst datums.

5.1. Unzoned Paleocene–Eocene interval

This interval is assigned on the basis of nannofossils tothe uppermost Paleocene or lowermost Eocene (zoneNN9) through Lower or lower Middle Eocene(undifferentiated zones NN12–14), and occurs at thebase of the East Shukheir-1 borehole (zones NP12–14),the base of the Shukheir-1 borehole (NP11 and NP12–14), and the base of the Shukheir-13A borehole (NP9and NP12–14). The dinoflagellate cyst assemblages areof low taxonomic richness and variously characterizedby abundant Glaphyrocysta spp., Homotryblium spp.,Hystrichokolpoma spp., Operculodinium spp., andSpiniferites/Achomosphaera spp., which appear to bein place. However, the presence of Cordosphaeridiumcantharellus (LO upper Lutetian, Stover et al. 1996),Distatodinium paradoxum (LO Upper Eocene, Kotheand Piesker 2007), Sumatradinium soucouyantiae (LOmid-Aquitanian, see discussion under zone GOS1),Trinovantedinium? xylochoporum (not recorded belowthe Upper Oligocene, de Verteuil 1996), and Tubercu-lodinium vancampoae (LO upper Chattian, Stover et al.1996) attest to contamination by caving. It is assumedthat several other taxa recorded in this interval,including Selenopemphix spp., Sumatradinium spp.,and Trinovantedinium cf. applanatum, also representcaving, and it is possible that Cleistosphaeridiumplacacanthum and Lejeunecysta spp. are caved, as thesetaxa do not extend below the mid-Lutetian elsewhere(e.g. Stover et al. 1996; Eaton et al. 2001). Miocene

caving is indeed confirmed by nannofossils for sample40 of the Shukheir-1 borehole.

In the Shukheir-13A borehole, sample 41 warrantsparticular comment, as it is assigned to nannofossilzones NP12–14 (mid-Ypresian–lower Lutetian) butcontains a dinoflagellate cyst assemblage of generallyMiocene aspect including Sumatradinium soucouyan-tiae and Trinovantedinium? xylochoporum. It is as-sumed that this sample has been affected by at leastsome, but possibly substantial, caving.

5.2. Lingulodinium machaerophorum AssemblageBiozone (GOS1) (Aquitanian through mid-Burdigalian)

Definition. The body of strata occurring below the LOof Exochosphaeridium insigne and containing a tax-onomically-depleted association otherwise resemblingthe superjacent GOS2. GOS1 rests unconformably onPaleocene–Eocene deposits.Characteristic taxa. These include Apteodinium/Cribro-peridinium spp., Apteodinium spiridoides, Cribroperidi-nium sp. 1, Cleistosphaeridium diversispinosum,Cleistosphaeridium placacanthum, Cordosphaeridiumcantharellus, Deflandrea spp. (including D. phosphor-itica), Dinopterygium cladoides sensu Morgenroth(1966), Glaphyrocysta spp., Heteraulacacysta sp. A ofCosta and Downie (1979), Homotryblium spp., Hystri-chokolpoma rigaudiae, Melitasphaeridium choanophor-um, round brown cysts, Selenopemphix brevispinosa,Selenopemphix nephroides, Selenopemphix quanta, Spi-niferites pseudofurcatus, Spiniferites mirabilis, Sumatra-dinium soucouyantiae, Tectatodinium pellitum,Trinovantedinium cf. applanatum, Tuberculodinium van-campoae, Xandarodinium sp. 1, Xandarodinium sp. ofSoliman (2006), and the acritarch Quadrina? condita.

Plate 3. Dinoflagellate cysts from the Gulf of Suez. All images are in bright field illumination except for Figure 10 which is ininterference contrast illumination. The sample number, slide number (in parentheses), and England Finder reference are givensequentially for each specimen, where K30¼Kareem-30 borehole, Sh1¼ Shukheir-1 borehole, Sh11¼ Shukheir-11 borehole, andESh1¼East Shukheir-1 borehole. Various magnifications. Max. dia.¼maximum diameter. Figures 1–3. Spiniferites solidago deVerteuil & Norris 1996. Uncertain view at (1) upper focus, (2) mid-focus, and (3) slightly lower focus; detailed morphologicalobservations as for Plate 2, figures 19, 20; central body max. dia.¼ 48 mm. Sample K30-14 (3), N32/1. Figures 4, 5. Tectatodiniumpellitum Wall 1967. Right-lateral? view at (4) upper focus, and (5) mid-focus; cyst max. dia. (including luxuria)¼ 44 mm. SampleK30-52 (4), H50/2. Figures 6, 7. Melitasphaeridium choanophorum (Deflandre & Cookson 1955) Harland & Hill 1979 var.choanophorum. Uncertain view at (6) upper focus, and (7) lower focus; central body max. dia.¼ 32 mm. Sample K30-35 (3),T43/0. Figures 8, 9. Saturnodinium cf. perforatum of de Verteuil and Norris (1996). Polar view at (8) upper focus, and (9) mid-focus; max. dia. 76 mm. Sample ESh1-39 (2), F29/0. Dinopterygium cladoides sensu Morgenroth (1966). Apical view of apicalsurface; max. dia.¼ 82 mm. Sample Sh1-9 (3), W50/0. Polysphaeridium zoharyi (Rossignol 1962) Bujak et al. 1980 subsp. zoharyi.Uncertain view at lower focus; central body max. dia.¼ 52 mm. Sample K30-3 (3), G30/2. Figures 12–14. Cleistosphaeridiumancyreum (Cookson & Eisenack 1965) Eaton et al. 2001. Apical view (12) of apical surface, (13) at mid-focus, and (14) ofantapical surface; note that penitabular ridges are moderately developed; central body max. dia.¼ 60 mm. Sample K30-57, (4)Q51/0. Figures 15, 16. Cleistosphaeridium diversispinosum Davey et al. 1966. Equatorial view at (15) mid-focus, and (16) lowerfocus; note that penitabular ridges are absent or only weakly developed; central body width¼ 65 mm. Sample K30-13 (3), F44/0.Figures 17–19. Cleistosphaeridium placacanthum (Deflandre & Cookson 1955) Eaton et al. 2001. Antapical view (17) of antapicalsurface, (18) at mid-focus, and (19) of apical surface; note that penitabular ridges are strongly developed; central body max.dia.¼ 63 mm. Sample Sh11-31 (2), N57/2.

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Most species occur sporadically, and only long rangingspecies including Cleistosphaeridium placacanthum(Middle Eocene–upper Middle Miocene; Eaton et al.

2001; Jimenez-Moreno et al. 2006) and the eponymousLingulodinium machaerophorum (Upper Paleocene topresent; Head 1996) occur in all five boreholes where


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this zone is recognized. Only Chiropteridium galea(possibly reworked), Spinidinium cf. macmurdoense(presumed reworked) and species of Glaphyrocystahave their HOs within GOS1.Reference section. East Shukheir-1 borehole, samples59–49, depth 1995–1998 to 1830–1833 m, thickness ca.247 m, Nukhul and lowermost Rudeis formations.Calibrated to nannofossil zone NN2 and possiblyNN1.Thickness. East Shukheir-1 (ca. 247 m; samples 59–49;Nukhul and possible lowermost Rudeis formations);Shukheir-1 (60 m; samples 38–35; lowermost RudeisFormation); Shukheir-11 (67.5 m; samples 62–58;Nukhul? Formation); Kareem-30 (6 m; samples 60–59; not attributed to a specific formation); Shukheir-13A borehole (30 m; samples 40, 39; NukhulFormation).Calibration. Base: lower nannofossil zone NN2 (andpossibly NN1) through lower NN4. Top: upper NN2through lower NN4.Age. Base: Aquitanian through mid-Burdigalian. Top:early through mid-Burdigalian. Based on nannofossils.Not younger than early or mid-Burdigalian based ondinoflagellate cysts in the superjacent GOS2.Comments. In all five boreholes where GOS1 isrecognized, the low taxonomic richness, sporadicoccurrences of species, and the likelihood of significantreworking and caving, all hinder attempts to interpretthis zone. Samples from the Shukheir-1, Shukheir-13A,and East Shukheir-1 boreholes are low-yielding, and insome cases barren, presumably owing to the relativelycoarse nature of the deposits.

Sumatradinium soucouyantiae (Plate 5, figures 14,15) is perhaps the most stratigraphically significantspecies in this zone, although it is restricted to theShukheir-11 borehole, where it occurs only in theupper part of the zone, and to the Shukheir-13A

borehole. It is the eponymous species of zone DN2 ofde Verteuil and Norris (1996) and has its LO at, or justabove, the base (mid-Aquitanian) of this zone both inthe eastern USA (de Verteuil and Norris 1996; deVerteuil 1997) and off New Jersey, eastern USA (deVerteuil 1996). According to Brinkhuis et al. (2009),Sumatradinium soucouyantiae has a LO within the mid-Aquitanian at about 21.4 Ma in the northern mid-latitudes.

Specimens of the genus Glaphyrocysta occur only inthe Shukheir-11 borehole, where they are restricted tothe lower part of the zone. They may be reworkedjudging from records elsewhere, although the genushas been reported as high as the mid-Burdigalian inAustria (Jimenez-Moreno et al. 2006; and records anddiscussion therein).

Deflandrea spp. are found in moderate abundance(15 specimens, some of which are D. phosphoritica) insample 59 of the East Shukheir-1 borehole, which isassigned to nannofossil zone NN1–2. Deflandreaphosphoritica has a highest occurrence at around 21.2Ma (mid-Aquitanian) in both low and mid-latitudes ofthe Northern Hemisphere (Brinkhuis et al. 2009), inagreement with its position in the East Shukheir-1borehole. Rare and sporadic occurrences higher in thisstudy are attributed to reworking.

The stratigraphic range of Quadrina? condita (Plate5, figure 1) is not known with certainty, but it was firstdescribed from the eastern USA where it has a lowestoccurrence at the base of zone DN6 which is correlatedto the mid-Serravallian (de Verteuil and Norris 1992,1996). Its lowest occurrence in the present study iswithin the upper part of nannofossil zone NN2 (mid-Burdigalian) in the East Shukheir-1 borehole. If it doesnot represent caving, this occurrence is possibly thelowest recorded to date. We treat Quadrina? condita asan acritarch because it is tentatively assigned to an

Plate 4. Dinoflagellate cysts from the Gulf of Suez. All images are in bright field illumination except for Figures 8, 9, 12, 13 and15 which are in interference contrast illumination. The sample number, slide number (in parentheses), and England Finderreference are given sequentially for each specimen, where K30¼Kareem-30 borehole, Sh1¼ Shukheir-1 borehole,Sh11¼ Shukheir-11 borehole, and ESh1¼East Shukheir-1 borehole. Various magnifications. Max. dia.¼maximum diameter.Figures 1–3. Exochosphaeridium insigne de Verteuil and Norris 1996. Ventral view (1) of ventral surface, (2) at mid-focus showingdetached operculum within cyst, and (3) at lower focus; central body max. dia.¼ 82 mm. Sample K30-55 (3), K31/0. Figures 4, 5.Reticulatosphaera actinocoronata (Benedek 1972) Bujak & Matsuoka 1986. Uncertain view at (4) mid-focus, and (5) lower focus;central body max. dia.¼ 32 mm. Sample ESh1-41 (2), U61/1. Figures 6, 7. Dapsilidinium pseudocolligerum (Stover 1977) Bujaket al. 1980. Antapical view of (6) antapical surface, and (7) apical surface; central body max. dia.¼ 36 mm. Sample K30-55 (3),C36/0. This typical morphotype is grouped with Dapsilidinium pastielsii/pseudocolligerum in the range charts. Figures 8, 9, 12, 13.Capillicysta sp. cf. C. fusca Matsuoka & Bujak in Matsuoka et al. 1987. Ventral? view of (8) upper surface, and at successivelylower foci; note both sutural alignment of spinules and intratabular distribution of spinules and granules, spinules are round-topped, hollow at base; length 64 mm. Sample Sh11-27 (2), K54/2. Figures 10, 11. Labyrinthodinium truncatum Piasecki 1980subsp. truncatum. Uncertain view at (10) upper focus, and (11) mid-focus; central body max. dia.¼ 44 mm, process length¼ ca. 6mm. Sample K30-35 (3), Y38/3. Grouped with Labyrinthodinium truncatum in the range charts. Lejeunecysta diversiforma(Bradford 1977) Artzner & Dorhofer 1978. Dorsal view at low focus; length 74 mm. Sample ESh1-38 (2), W48/3. Xandarodiniumsp. 1. Uncertain view at mid-focus; length including processes, 62 mm. Sample Sh1-31 (1), W40/0.

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acritarch genus by virtue of its lack of tabulation.However, the overall aspect of its morphology, itssize, and particularly its thin, brown-colored wallsuggests that it is a protoperidiniacean dinoflagellatecyst.

5.3. Exochosphaeridium insigne Taxon-range Biozone(GOS2) (lower through mid-Burdigalian)

Definition. The body of strata representing the totalstratigraphic range of Exochosphaeridium insigne.

Characteristic taxa. Exochosphaeridium insigne, Pro-toperidinioid sp. 1 (two specimens recorded in theKareem-30 borehole), Saturnodinium sp. cf. S. perfor-atum of de Verteuil and Norris (1996) (a singlespecimen recorded in the East Shukheir-1 borehole),and Sumatradinium sp. cf. S. hispidum (a singlespecimen recorded in the East Shukheir-1 borehole)are restricted to this zone. No other taxa have theirhighest occurrences in this zone, although Cordo-sphaeridium cantharellus extends to the top of thezone in the Shukheir-1 and Shukheir-11 boreholes,but extends slightly higher in the East Shukheir-1 andShukheir 13A boreholes. The following taxa havelowest occurrences within zone GOS2 and continueabove it: Batiacasphaera sphaerica, Cordosphaeridiumminimum sensu Benedek and Sarjeant (1981), Echini-dinium euaxum, Hystrichosphaeropsis obscura,

‘Hystrichosphaeropsis minimum’ of Zevenboom andSantarelli in Zevenboom (1995), Impletosphaeridiumprolatum, Kallosphaeridium biornatum, Labyrinthodi-nium truncatum (presumably caved), Lejeunecystasp. A of Powell (1986a), Lejeunecysta cinctoria,Lejeunecysta convexa, Lejeunecysta diversiforma, Le-jeunecysta fallax, Lejeunecysta pulchra, Nemato-sphaeropsis labyrinthus, Palaeocystodinium powellii,Pentadinium laticinctum, Polysphaeridium zoharyiktana, Pyxidinopsis spp. indet., Reticulatosphaeraactinocoronata, Spiniferites solidago, Sumatradiniumdruggii, Sumatradinium hispidum s.l., Trinovantedi-nium? xylochoporum (an Eocene occurrence in theShukheir-13A borehole is attributed to caving), andTrinovantedinium spp. indet.; and the acritarchNannobarbophora gedlii. The following species occurbelow, above and within GOS2: Dinopterygiumcladoides sensu Morgenroth (1966), and Sumatradi-nium soucouyantiae.Reference section. East Shukheir-1 borehole, samples48–39, depth 1755–1758 to 1620–1623 m, thickness142.5 m, lower Rudeis Formation. Calibrated to uppernannofossil zone NN2 through lower NN4.Thickness. East Shukheir-1 (142.5 m; samples 48–39;lower Rudeis Formation); Shukheir-1 (105 m; samples34–28; lowermost Rudeis Formation); Shukheir-11 (60m; samples 57–54; upper Nukhul? and basal Rudeisformations); Shukheir-13A (60 m; samples 38–35;upper Nukhul Formation and lowermost Rudeis

Plate 5. Dinoflagellate cysts and an acritarch from the Gulf of Suez. All images are in bright field illumination. The samplenumber, slide number (in parentheses), and England Finder reference are given sequentially for each specimen, whereK30¼Kareem-30 borehole, Sh11¼ Shukheir-11 borehole, and ESh1¼East Shukheir-1 borehole. Various magnifications. Max.dia.¼maximum diameter. Quadrina? condita de Verteuil & Norris 1992. Uncertain view at mid-focus; central body max.dia.¼ 36 mm. Sample Sh11-31 (2), H39/4. Selenopemphix brevispinosa Head et al. 1989. Antapical? view at mid-focus; centralbody max. dia.¼ 48 mm. Sample Sh11-27 (2), L50/0. Selenopemphix quanta (Bradford 1975) Matsuoka 1985. Polar view at mid-focus; the minutely bulbous terminations on many processes (e.g. as shown by the arrow) are a preservational artifact (see alsoFigure 5); Central body width¼ 49 mm. Sample ESh1-39 (2), L23/1. Protoperidinioid cyst A of Head in Head and Westphal(1999). Uncertain view at mid-focus; central body max. dia.¼ 45 mm, process length � ca. 2.0 mm. Sample Sh11-28 (2) N55/0.Trinovantedinium? xylochoporum de Verteuil & Norris 1992. Dorsoventral view at mid-focus; the minutely bulbous terminationson many processes (e.g. as shown by the arrow) are a preservational artifact (see also Figure 3); central body width¼ 46 mm.Sample Sh11-31 (2), D55/0. Figures 6–8. Protoperidinioid sp. 1. Dorsal view (6) of dorsal surface showing alignment of processesalong cingular margins, (7) at mid-focus, and (8) mid-focus at high-magnification; note faintly granulate central body surfacebearing thin solid hair-like processes, some of which have finely capitate tips although it is uncertain whether this ispreservational (see comment for Plate 5, figure 3). Central body length¼ 60 mm. Sample K30-57 (4), O60/0. Figures 9, 12, 13.Sumatradinium sp. cf. S. hispidum (Drugg 1970) Lentin & Williams 1976. Dorsal view (9) at mid-focus, high-magnification, (12)of dorsal surface showing operculum in place, and (13) at mid-focus; central body surface is faintly and irregularlymicroreticulate and bears short hollow processes, mostly acuminate, some truncated, both kinds may have annular thickenings(not reported previously for S. hispidum); central body length¼ 75 mm. Sample ESh1-39 (2), P53/4. Figures 10, 11.Sumatradinium druggii Lentin et al. 1994. Uncertain view at (10) mid-focus, (11) lower focus; central body length¼ 73 mm.Sample Sh11-31 (2), D47/0. Figures 14, 15. Sumatradinium soucouyantiae de Verteuil & Norris 1992. Dorsal view at (14) mid-focus, (15) of ventral surface; central body length¼ 58 mm. Sample ESh1-38 (2), D24/4. Trinovantedinium? sp. 1. Dorsoventralview at mid-focus; central body surface is faintly and irregularly microreticulate and bears short processes, mostly hollow, somedistally open and others acuminate; antapical horns terminate as minute thickened points; central body length¼ 82 mm. SampleSh11-36 (2), H27/0. Figures 17–19. Trinovantedinium sp. cf. T. applanatum (Bradford 1977) Bujak & Davies 1983. Ventral view(17) of ventral surface, (18) at mid-focus showing a flagellar scar in the sulcal area as indicated by an arrow, (19) of dorsalsurface; central body length¼ 85 mm. Sample Sh11-31 (2), J37/1.

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Formation); Kareem-30 (81 m; samples 58–45; lowerRudeis Formation).Calibration. Base: upper nannofossil zone NN2through lower NN4. Top: lower NN4.Age. Base: early through mid-Burdigalian based onnannofossils and presence of Exochosphaeridium in-signe. Top: mid-Burdigalian based on nannofossils.Comments. The presence of Exochosphaeridium in-signe (Plate 4, figures 1–3) throughout this zone is ofkey significance. This species was reported from themid-Burdigalian of Austria by Jimenez-Moreno et al.(2006) who also reviewed its stratigraphic range.They accepted an age of about 20–18.2 Ma for therange of Exochosphaeridium insigne in the easternUSA (de Verteuil and Norris 1996), and an ageequivalent to nannofossil zone NN3 and possibleupper NN2, and the lower part of NN4 for its rangein Denmark. In Denmark, a lowest occurrence withinupper NN2 and estimated at between 20 and 18.7Ma has been confirmed by Dybkjær and Piasecki(2008, 2010), but a highest occurrence is nowplaced at ca. 18.1 Ma. The present study confirmsthe HO of Exochosphaeridium insigne within thelower part of nannofossil zone NN4 and establishesan early through mid-Burdigalian range for thisspecies.

The highest occurrence of Cordosphaeridiumcantharellus (Plate 1, figure 11) at the top of thiszone (Shukheir-1, Shukheir-11) or just above it (EastShukheir-1, Shukheir-13A) corroborates a Burdigalianage for zone GOS2. This species is stated to have arange top at 17.8 Ma in equatorial latitudes and 19.2Ma in Northern Hemisphere mid-latitudes (Williams

et al. 2004), although in Denmark it appears to have aHO at 18.4 Ma based on Sr-isotope dating (Dybkjærand Piasecki 2010). In the Nile Delta and north Sinai,Egypt, its HO is lower Lower Miocene, probably lowerBurdigalian (El Beialy 1985, 1988; El Beialy andGheith 1989), and in northern Germany its HO occursat the mid-Burdigalian DN2–DN3 boundary (Kothe2003, text-figure 5). In the Contessa section of centralItaly, it has a range top within the Hystrichokolpomareductum dinocyst zone (Hre), which is calibrated tothe lowermost part of NN4 (Zevenboom 1995). In thecentral Paratethys, it has a highest recorded occurrenceat the top of the mid-Burdigalian Exochosphaeridiuminsigne Assemblage Biozone (Ein) (Jimenez-Morenoet al. 2006). The HO of Cordosphaeridium cantharellushas been observed slightly below that of Exocho-sphaeridium insigne (e.g. de Verteuil and Norris 1996;de Verteuil 1997; Dybkjær and Piasecki 2008, 2010),whereas these datums in the present study are eithercoeval or Cordosphaeridium cantharellus ranges slightlyhigher.

Additional age diagnostic species include Hystri-chosphaeropsis obscura (Plate 2, figures 1, 2), whichelsewhere has a LO in the mid-Aquitanian to lowerBurdigalian (nannofossil zone NN2) (e.g. Haq et al.1987; Manum et al. 1989; Powell 1992; Stover et al.1996; Hardenbol et al. 1998; Dybkjær 2004). Thisspecies has a persistent occurrence in the Aquitanianthrough Tortonian of the eastern USA (dinocyst zonesDN1 through DN9; de Verteuil and Norris 1996).

The LO of Sumatradinium druggii (Plate 5, figures10, 11) within GOS2 supports a Burdigalian age. In theeastern USA, this species has a LO at the base of

Plate 6. Dinoflagellate cysts from the Gulf of Suez. All are scanning electron micrographs. The sample number is given for eachspecimen, where K30¼Kareem-30 borehole, Sh1¼ Shukheir-1 borehole, and ESh1¼East Shukheir-1 borehole. Scale barsindicate 10 mm. Figure 1. Cordosphaeridium minimum (Morgenroth 1966) Benedek 1972 sensu Benedek and Sarjeant (1981). Notethe finely ribbed nature of the process shafts. Sample K30-14. Figure 2. Hystrichokolpoma sp. Left lateral view of ventral surface;large processes are ornamented with fine striations. Sample ESh1-24. Grouped with Hystrichokolpoma spp. indet. in the rangecharts. Figure 3. Spiniferites pseudofurcatus (Klumpp) Sarjeant 1970 emend. Sarjeant 1981. Dorsal view showing the precingulararcheopyle. Sample K30-14. Figures 4, 5. Spiniferites solidago de Verteuil & Norris 1996. Specimen in dorsal view showingprecingular archeopyle and weakly developed sutural crests, and (4) close-up showing process details with characteristic mid-shaft vacuoles, and perforations at base (5). Sample K30-35. Figure 6. Batiacasphaera sphaerica Stover 1977. Oblique apical view.Sample K30-12. Figure 7. Cleistosphaeridium placacanthum (Deflandre & Cookson 1955) Eaton et al. 2001. Uncertainorientation, note the well developed penitabular ridges and coarsely granulate surface. Sample K30-34. Figure 8.Cleistosphaeridium ancyreum (Cookson & Eisenack 1965) Eaton et al. 2001. Apical view; note the penitabular distribution ofprocesses and plate boundaries. Sample K30-52. Figure 9. Distatodinium paradoxum (Brosius 1963) Eaton 1976. Lateral view,note the smooth wall, broad equatorial area devoid of processes, and ‘apical’ archeopyle. Sample ESh1-31. Figure 10.Labyrinthodinium truncatum Piasecki 1980 emend. de Verteuil & Norris 1996 subsp. truncatum. Apical view showing large apicalarcheopyle. Sample K30-52. Grouped with Labyrinthodinium truncatum in the range charts. Figure 11. Dapsilidiniumpseudocolligerum (Stover 1977) Bujak et al. 1980. Uncertain orientation showing granulate central body surface. Sample Sh1-31.Grouped with Dapsilidinium pastielsii/pseudocolligerum in the range charts. Figure 12. Hystrichokolpoma rigaudiae Deflandre andCookson 1955. Right lateral view of ventral surface. Sample Sh1-31. Figure 13. Organic wall of calcareous dinoflagellate cyst.Apical view, note surface reticulation indicating position of crystals originally external to this organic layer (see Head et al. 2006).Sample K30-14. Figure 14. Operculodinium? borgerholtense Louwye 2001 emend. Soliman et al. 2009. Oblique antapical view,note the antapical plate (arrow) and the small spines on process surfaces. Sample K30-14.

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dinoflagellate cyst zone DN3, which is correlated tonannofossil zone NN3 and dated as mid-Burdigalian(de Verteuil and Norris 1996). It appears to have a

slightly lower LO in Belgium, where it is correlated tothe upper part of nannofossil zone NN2 within thelower Burdigalian (Louwye et al. 2000). The LO of


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Sumatradinium druggii is always higher than that ofSumatradinium soucouyantiae (de Verteuil and Norris1996; Lourens et al. 2005).

Saturnodinium cf. perforatum of de Verteuil andNorris (1996) (Plate 3, figures 8, 9) occurs as a singlespecimen in the upper part of zone GOS2 in the EastShukheir-1 borehole. This distinctive species has arange top within the upper part of zone DN2 (lowerBurdigalian) in the eastern USA (de Verteuil andNorris 1996), ranges as high as the top of zoneDN2 in ODP Hole 903C off New Jersey, easternUSA (de Verteuil 1996), and occurs within depositsassigned to zone DN2 in Belgium (Louwye et al.2000).

Palaeocystodinium powellii has a LO in the lowerSerravallian of Northern Germany (Strauss et al. 2001)and Serravallian of Italy (as Palaeocystodinium cf.golzowense in Powell 1986a), although it has beenreported from the Lower Miocene of Baffin Bay (asPalaeocystodinium cf. golzowense of Powell 1986a, inHead et al. 1989b) and mid-Burdigalian of Austria(Jimenez-Moreno et al. 2006). These records call intoquestion the phylogenetic lineage proposed by Strausset al. (2001), which has Palaeocystodinium powelliievolving from P. miocaenicum in the mid-Miocenewhen a more plausible ancestry would be withPalaeocystodinium golzowense-like morphotypes inthe Oligocene and Early Miocene.

Spiniferites solidago de Verteuil and Norris 1996(Plate 2, figures 19, 20; Plate 3, figures 1–3; Plate 6,figures 4, 5), from the Upper Oligocene throughUpper Miocene of the eastern USA, was treated asa taxonomic junior synonym of Spiniferites grallae-formis (Brosius 1963) Strauss et al. 2001, from theUpper Oligocene of Northern Germany, by Strausset al. (2001). We prefer to maintain Spiniferitessolidago as a distinct and separate species pendingre-examination of the type material of Spiniferitesgrallaeformis. We note that Spiniferites solidago has

one or two prominent vacuoles in the stems of mostprocesses, a feature not clearly evident in Spiniferitesgrallaeformis.

5.4. Apteodinium spiridoides Interval Biozone (GOS3)(mid-Burdigalian through lower Langhian)

Definition. The body of strata between the HO ofExochosphaeridium insigne and the HO of Apteodiniumspiridoides. In the Shukheir-13A borehole, the HO ofDistatodinium paradoxum is used as a substitute for thetop of this zone.Characteristic taxa. Most taxa recorded in zone GOS2continue through zone GOS3. Species with highestoccurrences in this zone include Apteodinium spir-idoides and Distatodinium paradoxum. Species withlowest occurrences in this zone include Labyrinthodi-nium truncatum (assuming GOS2 records in theKareem-30 borehole are caved), Operculodinium?borgerholtense, Operculodinium piaseckii, and Seleno-pemphix conspicua. Species restricted to this zoneinclude Lejeunecysta beninensis, Lejeunecysta marieae,and Palaeocystodinium minor.Reference section. East Shukheir-1 borehole, samples38–31, depth 1605–1608 to 1500–1503 m, thickness120 m, mid-Rudeis Formation. Calibrated to the lowerand middle part of nannofossil zone NN4.Thickness. East Shukheir-1 (120 m; samples 38–31;mid-Rudeis Formation); Shukheir-1 (240 m; samples27–13; mid-Rudeis Formation); Shukheir-11 (135 m;samples 53–45; lower Rudeis Formation); Shukheir-13A (105 m; samples 34–28; lower Rudeis Formation);Kareem-30 (39 m; samples 44–38; mid-RudeisFormation).Calibration. Base: lower nannofossil zone NN4. Top:middle through upper NN4.Age. Base: mid-Burdigalian based on nannofossils.Top: late Burdigalian through early Langhian basedon nannofossils.

Plate 7. Light micrographs of calacreous nannofossils. The sample number, where K30¼Kareem-30 borehole, andSh13A¼ Shukheir-13A borehole, is given for each specimen. Figures 1, 2. Geminilithella rotula Kamptner 1956. Sample K30-43. Figure 3. Reticulofenestra pseudoumbilica (Gartner 1967) Gartner 1969. Sample K30-63. Figure 4. Reticulofenestrapseudoumbilica (Gartner 1967) Gartner 1969. Sample K30-43. Figure 5. Reticulofenestra gelida (Geitzenauer 1972) Backman1978. Sample K30-43. Figures 6, 7. Umbilicosphaera jafari Muller 1974. Sample K30-43. Figure 8. Sphenolithus moriformis(Bronnimann & Stradner 1960) Bramlette & Wilcoxon 1967. Sample Sh13A-42. Figure 9. Holodiscolithus macroporus (Deflandre1954) Roth 1970. Sample K30-43. Figure 10. Helicosphaera euphratis Haq 1966. Sample K30-81. Figure 11. Helicosphaeraampliaperta Bramlette & Wilcoxon 1967. Sample K30-81. Figure 12. Helicosphaera ampliaperta Bramlette & Wilcoxon 1967.Sample K30-63. Figure 13. Helicosphaera carteri (Wallich 1877) Kamptner 1954. Sample K30-43. Figure 14. Helicosphaerascissura Miller 1981. Sample K30-63. Figure 15. Pontosphaera multipora (Kamptner 1948) Roth 1970. Sample K30-43. Figures16, 17, 21. Sphenolithus heteromorphus Deflandre 1953. Sample K30-43. Figure 18. Helicosphaera walbersdorfensis Muller 1974.Sample K30-43. Figures 19, 20. Coronocyclus nitescens (Kamptner 1963) Bramlette & Wilcoxon 1967. Sample K30-81. Figure 22.Micrantholithus flos Deflandre 1954. Sample K30-43. Figures 23, 24. Coccolithus pelagicus (Wallich 1871) Schiller 1930. SampleK30-43. Figure 25. Coronosphaera mediterranea (Lohmann 1902) Gaarder 1977. Sample K30-43. Figure 26. Cyclicargolithusfloridanus (Roth & Hay 1967) Bukry 1971. Sample K30-81. Figure 27. Tribrachiatus orthostylus Shamrai 1963. Sample Sh13A-41.Figure 28. Discoaster multiradiatus Bramlette & Riedell 1954. Sample Sh13A-42. Figure 29. Ascidian spicule. Sample K30-43.

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Table 1. Compilation of the ranges of dinoflagellate cysts and other aquatic palynomorphs for all five boreholes (EastShukheir-1, Shukheir-1, Shukheir-11, Shukheir-13A, and Kareem-30), plotted against the nannofossil zonation established in thepresent study. The time scales of Luterbacher et al. (2005) and Lourens et al. (2005) are used, along with the nannofossil zonationof Martini (1971). x¼ occurrence, c¼ suspected caving, r¼ suspected reworking.


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Comments. The dinoflagellate cyst taxa reflect a typicalBurdigalian association (Londeix and Jan du Chene1998). The HOs of Apteodinium spiridoides (Plate 1,figures 1, 2) and Distatodinium paradoxum (Plate 6,figure 9) are contemporaneous, except in the Kareem-30 borehole where the HO of Distatodinium paradoxumis two samples lower than that of Apteodiniumspiridoides, and in the Shukheir-13A borehole wherethe HO of Distatodinium paradoxum is five sampleshigher. This discrepancy is likely explained by the rare

and sporadic occurrences of Distatodinium paradoxumin the Kareem-30 borehole and of Apteodiniumspiridoides (a single specimen recorded) in the Shu-kheir-13A borehole. Consequently, the HO of Dis-tatodinium paradoxum is used as a substitute forApteodinium spiridoides in the Shukheir-13A borehole.

Apteodinium spiridoides has a HO in the upperBurdigalian (16.6 Ma) of northwestern Italy (Zeven-boom 1995), lower Langhian at the top of zone Mio2in the Norwegian–Greenland Sea (Poulsen et al. 1996),

Table 1. (Continued).

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mid-Langhian of the eastern USA (de Verteuil andNorris 1996), mid-Langhian of Belgium (Louwye et al.2000), mid-Langhian of northern Germany (Kothe2005; Kothe and Piesker 2007), mid-Langhian toSerravallian zone SNSM7 of the southern North Sea(Munsterman and Brinkhuis 2004), and mid-Langhianof the Danish North Sea (Schiøler et al. 2007). Its HOis somewhat diachronous, and seems to be lower in theMediterranean region and Gulf of Suez than in morenorthern localities.

Distatodinium paradoxum has a HO in the upper-most Serravallian within the lower part of zone Mio4in the Norwegian–Greenland Sea (Poulsen et al. 1996),and occurs persistently up to about 15 Ma in the lowerLanghian of northwestern Italy (Zevenboom 1995),mid-Langhian of the eastern USA (de Verteuil and

Norris 1996), mid-Langhian of Belgium (Louwye et al.2000), mid-Langhian of northern Germany (Kothe2005; Kothe and Piesker 2007), and mid-Langhianzone SNSM6 of the southern North Sea (Munstermanand Brinkhuis 2004). It has a highest persistentoccurrence at the base of the Langhian in the easternNorth Atlantic IODP Hole 1318B (Louwye et al.2007). El Beialy (1985, 1988) recorded its HO at theLower/Middle Miocene boundary in the Nile Delta,Egypt.

Although both subspecies of Labyrinthodiniumtruncatum (truncatum and modicum) were identifiedin the sections studied, they were not countedseparately during routine microscopic investiga-tion. However, both subspecies were discriminatedwithin GOS2 in the Kareem-30 borehole, with

Table 2. Compilation of the ranges of dinoflagellate cysts and other aquatic palynomorphs for all five boreholes, plotted againstthe dinoflagellate cyst zonation (GOS1–5) established in the present study. x¼ occurrence, c¼ suspected caving, r¼ suspectedreworking, X¼ datum used to define or characterize zone.


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Labyrinthodinium truncatum truncatum (Plate 4,figures 10, 11; Plate 6, figure 10) extending to thebase of this zone (assigned to nannofossil zone NN3or NN4). Judging from the stratigraphic range of thissubspecies elsewhere, and because it does not extendthis far down in our other boreholes, these specimensand those in GOS3 in the Kareem-30 borehole aresuspected of being caved. Specimens in GOS3–5 inthe other boreholes are treated as in place. Mostreports show Labyrinthodinium truncatum modicum asranging lower than Labyrinthodinium truncatumtruncatum (e.g. de Verteuil and Norris 1996; Louwyeet al. 2000, 2007). Labyrinthodinium truncatummodicum has a range base in the uppermostBurdigalian of the eastern USA where it marks thebase of dinoflagellate cyst zone DN4 (de Verteuil andNorris 1996), and has a LO dated magnetostrati-graphically at 16.5 Ma near the base of easternNorth Atlantic IODP Hole 1318B (Louwye et al.2007). Labyrinthodinium truncatum modicum wasreported (without Labyrinthodinium truncatum trun-catum) from the type Burdigalian of France indeposits assigned to nannofossil zone NN2 anddated at ca. 20.0 Ma, which places this record inthe early Burdigalian (unillustrated in Londeix andJan du Chene 1998). Labyrinthodinium truncatumtruncatum has a LO in the uppermost Burdigalian ofthe eastern USA, occurring just above the base ofdinoflagellate cyst zone DN4 (de Verteuil and Norris1996), and a LO dated magnetostratigraphically at16.3 Ma (uppermost Burdigalian) in eastern NorthAtlantic IODP Hole 1318B (Louwye et al. 2007). InItaly, the LO of Labyrinthodinium truncatum is at15.1 Ma (lower Langhian) within Subchron C5Bn2n(Zevenboom 1995; but see discussion in Jimenez-Moreno et al. 2006), and occurs at the top ofdinoflagellate cyst zone Pmc of the Nieder Ochten-hausen borehole in northern Germany which iscalibrated to the upper part of nannofossil zoneNN4 (lower Langhian) (Strauss et al. 2001). Thepresence of Labyrinthodinium truncatum in GOS3 istherefore consistent with a late Burdigalian to earlyLanghian age for this zone.

The LO of Operculodinium? borgerholtense (Plate 1,figures 12, 13; Plate 6, figure 14) in GOS3 is similarlyconsistent with a late Burdigalian to early Langhianage, as this species has a lowest occurrence at 16.5 Main the upper Burdigalian (Soliman et al. 2009).

5.5. Cleistosphaeridium placacanthum IntervalBiozone (GOS4) (upper Burdigalian, Langhian, andlower Serravallian?)

Definition. The body of strata between the HO ofApteodinium spiridoides (or Distatodinium paradoxum

in the Shukheir-13A borehole) and the HO of Cleisto-sphaeridium placacanthum. The HO of Cleistosphaer-idium diversispinosum is used as a substitute for the topof this zone in the Kareem-30 borehole.Characteristic taxa. Many of the taxa recorded in zoneGOS3 continue into GOS4. Taxa with highest occur-rences in this zone include Apteodinium/Cribroperidi-nium spp. indet. (although a single specimen ofCribroperidinium sp. 1 is found above this zone),Cleistosphaeridium ancyreum, Cleistosphaeridium diver-sispinosum, Cleistosphaeridium placacanthum, Dinop-terygium cladoides sensu Morgenroth (1966),Echinidinium euaxum, Impletosphaeridium prolatum,Palaeocystodinium powellii, Palaeocystodinium spp.indet., Pentadinium laticinctum, Trinovantedinium cf.applanatum, Trinovantedinium? xylochoporum, Xandar-odinium sp. 1, Xandarodinium sp. of Soliman (2006),and the acritarch Quadrina? condita. Species restrictedto this zone include Achomosphaera cf. andalousiensisof Strauss in Strauss and Lund (1992), Capillicysta cf.fusca, Nematosphaeropsis lativittata (caved?), Opercu-lodinium janduchenei (caved?), and Trinovantediniumsp. 1 (a single specimen recorded from the Shukheir-11borehole).Reference section. East Shukheir-1 borehole, samples30–8, depth 1485–1488 to 1155–1158 m, thickness345 m, upper Rudeis and Kareem formations.Calibrated to upper nannofossil zone NN4 throughNN5.Thickness. East Shukheir-1 (345 m; samples 30–8;upper Rudeis and Kareem formations); Shukheir-1(202.5 m; samples 12–1; upper Rudeis Formation);Shukheir-11 (525 m; samples 44–10; Rudeis, Kareemand lower Belayim formations); Shukheir-13A (285 m;samples 27–9; mid-Rudeis and lowermost Kareemformations); Kareem-30 (192 m; samples 37–5; upperRudeis and Kareem formations).Calibration. Base: middle through upper nannofossilzone NN4. Top: NN5 and NN5?Age. Base: late Burdigalian through early Langhian.Top: late Langhian and questionable earlySerravallian.Comments. The most biostratigraphically significantdatum in this zone is the HO of Cleistosphaeridiumplacacanthum (Plate 3, figures 17–19), which is welldocumented both in the eastern USA (de Verteuil andNorris 1996) and in Europe (e.g. Zevenboom 1995;Jimenez-Moreno et al. 2006) and varies from ca. 13.5to ca. 11.6 Ma (lower through upper Serravallian),with younger records being attributed to reworking(Jimenez-Moreno et al. 2006). Indeed, the record fromthe Porcupine Basin, eastern North Atlantic (Louwyeet al. 2007) shows that this datum is influenced stronglyby environmental controls, as the species is abundantand persistent only as high as the upper Langhian,

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becoming sporadic and rare in the Serravallian. InEgypt, the HO of Cleistosphaeridium placacanthum isclearly recognized near the top of the KareemFormation and dated as Langhian or Serravallian (ElBeialy and Ali 2002) and Serravallian (Mahmoud1993; Ahmed and Pocknall 1994).

Other species that have potentially useful HOs inthis zone include Dinopterygium cladoides sensuMorgenroth (1966) (Plate 3, figure 10) that has ahighest persistent occurrence in the lowermost Serra-vallian (13.6 Ma) of IODP Hole 1318C in the easternNorth Atlantic (Louwye et al. 2007).

Achomosphaera cf. andalousiensis of Strauss inStrauss and Lund (1992), which is restricted to thiszone and to deposits assigned to nannofossil zone NN5,has been recorded in the uppermost? Lower to lower-most Middle Miocene of eastern Germany (as Spinifer-ites cf. andalousiensis in Strauss and Lund 1992; Strausset al. 2001), has a LO in the upper Langhian or lowestSerravallian of North Germany (Strauss et al. 2001),and is restricted to the upper Langhian (ca. 14.5 Ma) inHungary and Austria (Jimenez-Moreno et al. 2006).

Capillicysta cf. fusca (Plate 4, figures 8, 9, 12, 13) isrepresented by only a few specimens, and restricted tonannofossil zone NN4. It differs from the type materialand other specimens illustrated from Japan (Matsuokaet al. 1987; Head 1994, plate 2, figures 7–9) in having aless dense wall ornament. However, it is identical to aspecimen illustrated from the lower Middle Miocene ofItaly (Head 1994, plate 2, figures 10, 11), which is ofsimilar age.

It is uncertain whether specimens of Nemato-sphaeropsis lativittata (Plate 2, figures 11, 12) andOperculodinium janduchenei, which are rare andrestricted to this zone, are in place or represent caving.The LO of Nematosphaeropsis lativittata, while usuallyreported within the Upper Miocene (e.g. off NewJersey, western North Atlantic, in zone DN8; deVerteuil 1996), has been reported as low as the upperSerravallian of NW Italy (Zevenboom 1995), upperMiddle Miocene of northern North Atlantic DSDPHole 408 (as Nematosphaeropsis sp. A of Wrenn andKokinos 1986 in Engel 1992), and Oligocene of thePolish Outer Carpathians (Barski and Bojanowski2010, unillustrated). Nematosphaeropsis cf. lativittatahas been reported near the Oligocene/Miocene bound-ary in Argentina (Guerstein et al. 2004, unillustrated).Operculodinium janduchenei is likewise not usuallyrecorded below the Upper Miocene, but has beenreported from the Middle Miocene of Indian OceanODP Site 765 (McMinn 1992), Middle Miocene offSouth Africa (Udeze and Oboh-Ikuenobe 2005), andupper Middle Miocene of northern North AtlanticDSDP Hole 408 and eastern North Atlantic DSDP

Hole 400A (as Operculodinium sp. of Jan du Chene1977 in Engel 1992).

In summary, the dinoflagellate cyst evidence forGOS4 generally supports a late Burdigalian, Lan-ghian–early Serravallian? age for this zone.

5.6. Polysphaeridium zoharyi Assemblage Biozone(GOS5) (upper Langhian and Serravallian?)

Definition. The body of strata occurring above thehighest occurrence of Cleistosphaeridium placacanthum(or Cleistosphaeridium ancyreum in the Kareem-30borehole) and containing a taxonomically-depletedassociation otherwise resembling the subjacent GOS4.The upper boundary was not observed.Characteristic taxa. Species occurring within andbelow GOS5 include: Achomosphaera/Spiniferitesspp., Cordosphaeridium minimum sensu Benedek andSarjeant (1981), Cribroperidinium giuseppei, Cribroper-idinium sp. 1, Dapsilidinium pastielsii/pseudocolligerum,Hystrichokolpoma spp., ‘Hystrichosphaeropsis mini-mum’ of Zevenboom and Santarelli in Zevenboom(1995), Hystrichosphaeropsis obscura, Hystrichostrogy-lon membraniphorum, Kallosphaeridium biornatum,Labyrinthodinium truncatum, Lejeunecysta cinctoria,Lejeunecysta sp. A of Powell (1986a), Lejeunecystaspp. indet., Operculodinium piaseckii, Operculodinium?borgerholtense, Operculodinium spp. indet., Polysphaer-idium zoharyi, Reticulatosphaera actinocoronata, Sele-nopemphix conspicua, Selenopemphix spp. indet.,Spiniferites solidago, Sumatradinium druggii, Sumatra-dinium hispidum s.l., Sumatradinium soucouyantiae,Trinovantedinium spp. indet., Tuberculodinium vancam-poae, and the acritarch Nannobarbophora gedlii. Fewtaxa occur in all boreholes where this zone isrecognized, many taxa have rare and sporadic occur-rences, and no taxa have lowest occurrences within thiszone.Reference section. East Shukheir-1 borehole, samples7–2, depth 1140–1143 to 1065–1068 m, thickness 90 m,Belayim Formation. No diagnostic nannofossils buttop of subjacent zone GOS4 is calibrated to question-able NN5.Thickness. East Shukheir-1 (90 m; samples 7–2;Belayim Formation; although it should be noted thatthe interval 1140–1143 m represented by sample 7spans the boundary between the shale of the KareemFormation and evaporites of the overlying BelayimFormation, at 1142.5 m according to the well logs);Shukheir-11 (ca. 113 m; samples 9–2; Belayim Forma-tion); Shukheir-13A (ca. 98 m; samples 8–2; KareemFormation); Kareem-30 (21 m; samples 4–1; upperKareem Formation). Not recognized in the Shukheir-1borehole.


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Calibration. Base: nannofossil zone NN5. Top: notcalibrated.Age. Late Langhian and possibly younger, based onnannofossils; possibly no younger than Serravallianfor at least part of this zone, based on dinoflagellatecysts.Comments. Most species in this zone extend into theTortonian (e.g. Cordosphaeridium minimum sensuBenedek and Sarjeant 1981 (Plate 6, figure 1),Sumatradinium druggii, Sumatradinium hispidum s.l.,and Sumatradinium soucouyantiae (Plate 5, figures 14,15); Zevenboom 1995; de Verteuil and Norris 1996) orabove; or are represented by single specimens andmight therefore be reworked (e.g. Cribroperidiniumgiuseppei, Hystrichostrogylon membraniphorum, Kallo-sphaeridium biornatum) judging from their rangeselsewhere.

However, Cribroperidinium sp. 1 (Plate 1, figures7, 8), represented within GOS5 by a single specimenin the Kareem-30 borehole, is similar to specimensillustrated in the literature as Cribroperidinium tenui-tabulatum, a species that has a highest occurence inthe lower Serravallian of eastern North Atlantic,Porcupine Basin, IODP Hole 1318C (Louwye et al.2007) and elsewhere (Jimenez-Moreno et al. 2006).‘Hystrichosphaeropsis minimum’ of Zevenboom andSantarelli in Zevenboom (1995) (Plate 2, figures 3–8)occurs fairly commonly in the Kareem-30 and EastShukheir-1 boreholes. It has not been reportedfrequently in the literature but has a highestoccurrence within the upper Serravallian of NW Italy(Zevenboom 1995), and is restricted to the MiddleMiocene of northern North Atlantic DSDP Hole 408(as Hystrichosphaeropsis complanata in Engel 1992).Operculodinium? borgerholtense, represented by asingle specimen in the Kareem-30 borehole, has ahighest recorded occurrence in the mid-Serravallian ofHungary and the eastern North Atlantic (Solimanet al. 2009).

Based on the limited evidence given above, an ageno younger than Serravallian, and perhaps no youngerthan early Serravallian, may be assigned to at least partof GOS5.

6. Comparison with other Miocene dinoflagellate cyst

zonations

The present study reveals a higher diversity ofdinoflagellate cysts than previously reported for theMiocene of the Gulf of Suez, with more than 88 in situspecies identified. However, many of the stratigraphi-cally restricted species have sporadic and rare occur-rences, or are not found in all our wells. Theselimitations, together with the absence of certain index

species and the inherent problems of caving, hinder theapplication of existing zonations for the NorthAtlantic region and Europe to our study. Nonetheless,broad comparisons may be made with these zonationsand with local schemes from the Gulf of Suez and NileDelta.

For the Gulf of Suez area, Mahmoud (1993)proposed two dinoflagellate cyst assemblages zones(A and B) from the Kareem Formation of theShagar-1 borehole, equivalent to standard foraminif-eral biozones N9 to N13 of Blow (1969). Theassemblages recorded within these two zones consistmostly of long ranging taxa, but are comparablewith GOS3–5 based on the presence of Labyrintho-dinium truncatum, although no exact correlation ispossible.

Ahmed and Pocknall (1994) published a tentativebiozonation for the Miocene of the Gulf of Suez,establishing seven assemblage zones based largely onthe range tops of such marker species as Cordo-sphaeridium cantharellus, Cleistosphaeridium placa-canthum and Labyrinthodinium truncatum. Theirzonation does not have independent age control,and the Burdigalian is not represented on their rangechart (Ahmed and Pocknall 1994, figure 2). TheirZone A is broadly equivalent to our zone GOS2,based on the HO of Cordosphaeridium cantharellus.The top of their superjacent Zone B is characterizedby the HO of Distatodinium craterum (probably ourDistatodinium paradoxum), which would be equiva-lent to the top of our zone GOS3. The top of theirZone C is characterized by the HO of Cribroper-idinium tenuitabulatum (probably our Cribroperidi-nium sp. 1), and the top of their Zone D ischaracterized by the HO of Cleistosphaeridiumplacacanthum (as Systematophora placacantha). Cri-broperidinium sp. 1 ranges to the top of our studyinterval. However, the HO of Cleistosphaeridiumplacacanthum defines the top of our GOS4, implyingthat Ahmed and Pocknall’s Zone D is equivalent atleast in part to our GOS4. Ahmed and Pocknallsuggested a Serravallian age for the top of their ZoneD, which agrees with other records for the HO ofCleistosphaeridium placacanthum.

El Beialy (1988) established a zonation for theUpper Paleogene–Neogene of the Kafr El Dawar-1well, north Nile Delta. He proposed three assem-blage zones (C, D, E) for the Miocene interval basedon the highest occurrences of selected dinoflagellatecyst taxa, which were constrained by foraminiferaldata. The top of El Beialy’s Assemblage Zone C isbased on the HO of Cordosphaeridium cantharellus,which in our material occurs at the top of zoneGOS2 or just into the lower part of GOS3.

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Assemblage Zone C, which is dated as EarlyMiocene, therefore appears to be partly equivalentto our GOS2.

The mid- to high latitudes of the North Atlanticand adjacent areas are characterized by many Earlyand Middle Miocene datums that are broadly recog-nizable throughout this region. Hence, the zonation ofthe eastern USA (de Verteuil and Norris 1996) can beapplied not only to offshore sequences on the adjacentshelf (de Verteuil 1996, 1997) but across the NorthAtlantic to the North Sea region (e.g. Louwye 2000;Louwye et al. 2000; Dybkjær and Piasecki 2008, 2010).Many elements of the de Verteuil and Norris (1996)zonation are recognizable in Baffin Bay (Head et al.1989b), the Norwegian–Greenland Sea (Manum et al.1989), Northern Europe (Strauss et al. 2001; Kothe2003, 2005; Kothe and Piesker 2007), Central Para-tethys (Jimenez-Moreno et al. 2006), and the Medi-terranean region (e.g. Powell 1986a, 1986b; Biffi andManum 1988; El Beialy, 1988; Brinkhuis et al. 1992;Zevenboom 1995).

GOS1 is partly equivalent to the lower half of zoneDN2 of de Verteuil and Norris (1996), which ischaracterized by the LO of Sumatradinium soucouyan-tiae at its base and the LO of Exochosphaeridiuminsigne about half way up this zone. Comparisonscannot be made precisely, however, because Sumatra-dinium soucouyantiae occurs sparsely in GOS1, and ispresent only in the Shukheir-11 and Shukheir-13Aboreholes. Moreover, it appears to have been cavedinto older horizons in the East Shukheir-1 andShukheir-13A boreholes. We accept a date of about21.4 Ma (mid-Aquitanian) for the LO of Sumatradi-nium soucouyantiae in northern mid-latitudes (Brin-khuis et al. 2009).

The upper part of zone DN2 of de Verteuil andNorris (1996) is characterized by the total range ofExochosphaeridium insigne, with the top of this zonebeing defined by its HO. Exochosphaeridium insigne isan important marker species in our boreholes, its totalrange defining the upper and lower boundaries of zoneGOS2. We consider GOS2 broadly equivalent to theupper part of zone DN2 of de Verteuil and Norris(1996), the presence of Cordosphaeridium cantharellussupporting this contention. The maximum range ofExochosphaeridium insigne is about 20–18.1 Ma (earlythrough early late Burdigalian) in middle to highernorthern latitudes (Jimenez-Moreno et al. 2006;Dybkjær and Piasecki 2008, 2010).

GOS3 is defined by the HO of Exochosphaer-idium insigne at its base, and the HO of Apteodiniumspiridoides at its top, with the HO of Distatodiniumparadoxum used as a substitute for the top of thiszone in the Shukheir-13A borehole. GOS3 comparesfavorably with DN3 and DN4 of de Verteuil and

Norris (1996), as the top of DN4 is also defined bythe HO of Distatodinium paradoxum, and Apteodi-nium spiridoides has a HO within the upper part ofDN4 (de Verteuil and Norris 1996). However, it isnot possible to discriminate between zones DN3 andDN4 in our study because the LO of Labyrinthodi-nium trucatum, which defines the base of DN4, doesnot have a consistent LO in our boreholes: rather aLO in GOS2 in the Kareem-30 borehole, GOS3 inthe Shukheir-1 borehole, and GOS4 in the EastShukheir-1 and Shukheir-13A boreholes. Moreover,because the LO of Labyrinthodinium trucatum else-where is within the uppermost Burdigalian at around16.5 Ma (Louwye et al. 2007; see Section 5.4), thelower occurrences in our study presumably representcaving. An added difficulty in discriminating zoneDN3 in our study is that the eponymous speciesCousteaudinium aubryae, which reaches an acme inDN3 in the eastern USA, was not recorded in ourboreholes.

GOS4 extends from the top of GOS3 to the HOof Cleistosphaeridium placacanthum, except whereCleistosphaeridium diversispinosum is used as a sub-stitute for the top of this zone in the Kareem-30borehole. GOS4 compares most closely with DN5 ofde Verteuil and Norris (1996), as the top of DN5 isalso defined by the HO of Cleistosphaeridiumplacacanthum (as Systematophora placacantha in deVerteuil and Norris 1996). This species has adiachronous HO in the North Atlantic region,varying from ca. 13.5 to ca. 11.6 Ma (lower throughupper Serravallian; Section 5.5). In the present study,the HO of Cleistosphaeridium placacanthum is prob-ably within nannofossil zone NN5 (although there issome uncertainty regarding the upper limit of thiszone in all our boreholes), and the top of GOS4 istherefore late Langhian and possibly early Serraval-lian in age. Surprisingly, Unipontidinium aquaeductum,which is restricted to zone DN5 in the eastern USA(de Verteuil and Norris 1996) and a distinctiveoceanic component of Langhian–Serravallian assem-blages throughout the North Atlantic region (Louwyeet al. 2007), the Mediterranean (Zevenboom 1995),and Central Paratethys (Jimenez-Moreno et al. 2006),has not been reported in the present study. Nor has itbeen reported in previous studies of the Gulf of Suez(Ahmed and Pocknall 1994; El Beialy and Ali 2002),although Mahmoud (1993) recorded Unipontidiniumcf. aquaeductum without illustration. It is unclearwhether biogeographical or ecological factors areresponsible for its absence or scarcity, althoughduring the early Middle Miocene the Gulf of Suezwas narrowly connected to the Mediterranean Sea,and by middle Middle Miocene time it had become arestricted evaporitic basin separated from the


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Mediterranean (Ouda and Masoud 1993; Popov et al.2004).

GOS5 is defined at its lower boundary by the HOof Cleistosphaeridium diversispinosum (upper Langhianand possible lower Serravallian) and extends to the topof the studied boreholes. This zone lacks persistentlyoccurring diagnostic species that might allow compar-ison elsewhere, but evidence from selected dinoflagel-late cyst species suggests an age no younger thanSerravallian. Assuming a Serravallian age, GOS5 isapproximately time-equivalent to zones DN6 and DN7of de Verteuil and Norris (1996). The distinctiveCannosphaeropsis passio, whose total range defineszone DN7, was not reported in this or previous studiesof the Gulf of Suez. Restricted hypersaline marineconditions within the Gulf of Suez and its separationfrom the Mediterranean Sea at this time (Popov et al.2004) are presumably responsible for the sparse andtaxonomically depleted dinoflagellate cyst associationthat characterizes GOS5, and would explain theapparent absence of Cannosphaeropsis passio.

7. Stratigraphic significance of the proposed

zonation

The dinoflagellate cyst and nannofossil distributions ofthe present study help refine the dating of the Nukhul,Rudeis, Kareem and Belayim formations, and of theunderlying Paleogene strata, and clarify the position ofthe Paleogene–Miocene unconformity in the threewells where it is present (Figure 13).

7.1. Paleogene strata

Upper Paleocene through Lower–Middle Eocenenannofossil assemblages characterize the lowermoststrata of the Shukheir-1 (Lower Eocene NP11, andLower–Middle Eocene NP12–14), East Shukheir-1(Lower–Middle Eocene NP12–14), and Shukheir-13A(Upper Paleocene NP9, and Lower–Middle EoceneNP12–14) boreholes. Dinoflagellate cyst assemblagesare broadly consistent with the nannofossil evidence,but appear to contain significant contamination fromcaving. The lowest 100 m of the Shukheir-1 borehole

Figure 13. Correlation of Early and Middle Miocene formations in the studied boreholes based on the calcareous nannofossilzonation of Martini (1971) as recognized in the present study and dinoflagellate cyst zonation proposed herein. The time scale ofLourens et al. (2005) is used.

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were considered to include Miocene deposits of theNukhul Formation as well as underlying Paleoceneand Eocene deposits (GPC 1966), but are now shownto be entirely Eocene in age.

Lower Miocene deposits of the Nukhul and Rudeisformations (below) immediately overlie Paleogenestrata in our boreholes, signifying a hiatus of at least24 myr and testifying to a period of significant erosionor non-deposition prior to the Early Miocene marinetransgression that accompanied Gulf of Suez rifting.

7.2. Nukhul Formation

The Nukhul Formation was deposited during the earlystages of Gulf of Suez rifting and subsidence (Bos-worth et al. 1998). Throughout the Gulf of Suez, thedatable part of the Nukhul Formation predominantlybelongs to Blow’s (1969) early and mid-Aquitanianplanktonic foraminiferal zone N4 (Scott and Govean1985) and may continue into the Burdigalian (Evans1988; Malpas et al. 2005). But, in general, thisformation is poorly dated due to the scarcity ofdiagnostic planktonic foraminifera and calcareousnannoplankton (El-Heiny and Martini 1981).

Dinoflagellate cyst assemblages in the studied wellsindicate an Aquitanian through mid-Burdigalian age(GOS1–GOS2) for this formation; and our nannofossilbiostratigraphy allows assignment to NN1 or NN2(early Aquitanian to mid-Burdigalian) at the base, andlower NN4 (mid- to late Burdigalian) at the top. Thebase of the Nukhul Formation is strongly diachronous,having a mid- or late Burdigalian age in Shukheir-13A(lower NN4; although the lowest samples are barren),and early or mid-Aquitanian in East Shukheir-1 (noolder than NN1, and no younger than mid-Aquitanianbased on the HO of the dinoflagellate cyst Deflandreaphosphoritica).

The lowest 100 m of the Shukheir-11 borehole(Figures 5, 10, 13) were originally assigned to theEocene and Paleocene, with about 20 m of the NukhulFormation unconformably overlying it (GPC 1981).The entire sequence is limestone, with shale at the base.We assign the entire lowest 120 m to zone NN4 (mid-Burdigalian–mid-Langhian), and the upper part todinoflagellate cyst zone GOS2 (early to mid-Burdiga-lian) suggesting that the entire sequence in fact belongsto the Nukhul Formation. We label this interval as the‘Nukhul? Formation’ in the present study.

7.3. Rudeis Formation

An Early Miocene age is widely assigned to the RudeisFormation (NCGS 1976; El Beialy and Ali 2002;Mandur 2009), although Marzouk (2009) proposed anEarly to early Middle Miocene age for Gulf of Suez

borehole GS 148-1, based on nannofossils. Thesepublished observations are consistent with our ownbiostratigraphic results.

The Rudeis Formation is the thickest formationrepresented in our study (619 m in the Shukheir-1borehole) and present in all boreholes. Its base isdiachronous, having a maximum age of late Aquita-nian–early Burdigalian (middle of zone NN2) in theEast Shukheir-1 borehole, and a mid- to early lateBurdigalian minimum age (lower part of zone NN4,and within GOS2) in the Shukheir-11 and Shukheir-13A boreholes. The top of the Rudeis Formation ismid-Langhian in age (within the lower part of zoneNN5 and within GOS4). Zone GOS3 (late Burdigalianto early Langhian) is restricted to the Rudeis Forma-tion in all examined boreholes.

7.4. Kareem Formation

In the Gulf of Suez, the lower boundary of the KareemFormation is identified by the appearance of evaporitesbelonging to the Rahmi Member (Figure 2). In theGulf of Suez, the Kareem Formation is widelyaccepted as Middle Miocene in age (NCGS 1976),and has been dated as Langhian and Serravallian(Salah and Alsharhan 1997; El Beialy and Ali 2002),Langhian (Al-Husseini 2008), and Langhian and earlySerravallian although entirely within nannofossil zoneNN5 (Mandur 2009) which Lourens et al. (2005)assigned to the mid- and upper Langhian.

In the present study, the base of the KareemFormation occurs some distance above the base ofzone NN5. The upper boundary of the KareemFormation occurs within zone NN5 in the Shukheir-11borehole, which is the only borehole where thisboundary is dated conclusively by nannofossils,although in the East Shukheir-1 borehole, it is tenta-tively assigned to NN5. Nannofossil evidence thereforepoints to a late Langhian age for the Kareem Forma-tion. Dinoflagellate cyst biostratigraphy is consistentwith this assignment, the Kareem Formation occurringwithin zone GOS4 (upper Burdigalian, Langhian, andlower Serravallian?) in the East Shukheir-1 and Shu-kheir-11 boreholes, and GOS4 and GOS5 (upperBurdigalian, Langhian and Serravallian?) in the Shu-kheir-13A and Kareem-30 boreholes (Figure 13). Nosamples were available from the Shukheir-1 well.

7.5. Belayim Formation

The Belayim Formation is characterized by thedominance of evaporite facies. It was included withinthe Lower to Middle Miocene succession in the Gulf ofSuez by Ahmed and Pocknall (1994), and to theSerravallian by Al-Husseini (2008) and Mandur (2009).


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In the present study, the Belayim Formation wasdocumented only in the East Shukheir-1 and Shukheir-11 boreholes, its upper boundary not being observedowing to the unavailability of samples. In theShukheir-11 borehole, nannofossils from the lowerpart of the Belayim Formation are assignable to zoneNN5 (upper Langhian). No nannofossils were found inthis formation in the East Shukheir-1 borehole,although dinoflagellate cyst zones GOS4 and GOS5were recognized in the Shukheir-11 borehole, andGOS5 in the East Shukheir-1 borehole. Combiningnannofossil and dinoflagellate cyst evidence, theBelayim Formation is no older than late Langhianand might not be younger than Serravallian, in ourstudy.

7.6. Stratigraphic hiatuses

Evans (1988, figure 6) suggested five stratigraphichiatuses/events in the Gulf of Suez during the Neogene:(1) the pre-Nukhul event spans the Oligocene to theearliest Miocene, (2) the post-Nukhul event separatesthe Nukhul Formation from the shales of the RudeisFormation, (3) the mid-clysmic event within the RudeisFormation, (4) the post-Kareem event separates theKareem Formation from the overlying anhydrites ofthe Belayim Formation, and (5) the post-Zeit eventoccurs at the Miocene–Pliocene boundary.

The missing Upper Eocene and Oligocene strata ofthe pre-Nukhul event are unambiguously evidenced byour nannofossil zonation. However, the post-Nukhuland mid-clysmic events are more difficult to recognize,although the poor representation of zones NN1–3 inall boreholes except East Shukheir-1 may be a mani-festation of the post-Nukhul event. A well-developedzone NN4, the distribution of GOS1–GOS4 markertaxa, and an absence of conclusive sedimentologicalevidence, prevent clear recognition of the putative mid-clysmic event.

8. Summary and conclusions

The Gulf of Suez is the main oil province in Egypt,with Miocene reservoirs being the most prolific, and itsgeological development is strongly linked with riftingand subsidence during this time. This study presentsthe first detailed dinoflagellate cyst biozonation for theEarly and Middle Miocene of the Gulf of Suez, basedon 273 ditch-cutting samples from five onshore bore-holes situated on the western margin of the southernpart of the Gulf of Suez. A calcareous nannofossilbiostratigraphy is documented for the same sample setto calibrate the dinoflagellate cyst bioevents andcomplement the age control on these five boreholes.It should be noted that while calcareous nannofossils

provide a convenient and robust chronostratigraphicframework for the present study, dinoflagellate cystdatums may prove equally useful for the Miocenebiostratigraphy of the Gulf of Suez in the future.

Five dinoflagellate cyst biozones are defined, inascending order: Lingulodinium machaerophorum As-semblage Biozone (GOS1; Aquitanian through mid-Burdigalian), Exochosphaeridium insigne Taxon-rangeBiozone (GOS2; lower through mid-Burdigalian),Apteodinium spiridoides Interval Biozone (GOS3; mid-Burdigalian through lower Langhian), Cleistosphaer-idium placacanthum Interval Biozone (GOS4; upperBurdigalian, Langhian, and lower Serravallian?), andPolysphaeridium zoharyi Assemblage Biozone (GOS5;upper Langhian and Serravallian?). GOS1 has fewdiagnostic species, but the LO of Sumatradiniumsoucouyantiae places the upper part of this zone in themid-Aquitanian or younger. Of particular note is thepresence of Exochosphaeridium insigne, which has notbeen reported previously from the Gulf of Suez anddefines zone GOS2 by its total range. This species isconfirmed as having an early through mid-Burdigalianrange in the Gulf of Suez, its HO being within the lowerpart of nannofossil zone NN4. The LOs of Hystricho-sphaeropsis obscura and Sumatradinium drugii withinGOS2 support a Burdigalian age. The HO of Apteodi-nium spiridoides, which defines the top of zone GOS3,has not been recognized previously as a useful Miocenebioevent in the Gulf of Suez, whereas the HO ofCleistosphaeridium placacanthum, which defines the topof zone GOS4, has. Taxonomically depleted assem-blages characteristic of GOS5 presumably relate torestricted marine conditions as the Gulf of Suez becamean evaporative, hypersaline basin disconnected fromthe Mediterranean. The highest occurrences in this partof our sequence may therefore be influenced by local orregional paleoenvironmental factors.

The Nukhul Formation rests unconformably onstrata of Early to Middle Eocene age (mid-Ypresian toearly Lutetian; zones NP12–14) and the oldestdiagnostic assemblages indicate an Early Miocene(early or mid-Aquitanian) age, signifying a hiatus ofat least 24 myr. The base of the Nukhul Formation isdiachronous, and may be as young as mid- or lateBurdigalian in age. The conformably overlying RudeisFormation also has a diachronous base, ranging fromlate Aquitanian–early Burdigalian to mid- to early lateBurdigalian (late Early Miocene), and its top is mid-Langhian in age (early Middle Miocene). The onset ofextensive evaporite deposition marks the base of theKareem Formation. This formation is early MiddleMiocene (late Langhian) in age, although its upperboundary is well constrained only in one borehole.Evaporite facies dominate the conformably overlyingBelayim Formation, which we estimate as being no

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older than late Langhian and possibly no younger thanSerravallian (late Middle Miocene).

Due to the tectonic complexity of the Gulf of Suez,a scarcity of subsurface data and paucity of strati-graphical and sedimentological studies from the areaof study presently hinder attempts to apply ourproposed biostratigraphy to a sequence stratigraphicframework. Further large-scale integrated studiesbased on the subsurface and the nearby outcrops areneeded to interpret the Miocene sequence stratigraphyin the studied area. However, our quantitative datashould improve the paleoenvironmental characteriza-tion of the Miocene stratigraphy of this area, andhence any sequence stratigraphic interpretation.

Acknowledgements

The presented data are based partly on the first author’sPh.D. thesis. AS thanks OAD, the Austrian ExchangeServices, and the Ministry of Higher Education, Egyptfor providing financial support. Partial funding wasprovided by The Palynological Association – AASP,and OAW, the Austrian Academy of Sciences. MJHacknowledges support from a Natural Sciences andEngineering Research Council of Canada DiscoveryGrant. Our appreciation goes to M. Faris (TantaUniversity, Egypt) for providing samples of the Kar-eem-30 borehole, and the Egyptian General PetroleumCorporation for kindly providing other boreholesamples and releasing basic data. We are grateful to K.Dybkjær (Geological Survey of Denmark and Green-land, Copenhagen) and J.B. Riding (British GeologicalSurvey,Nottingham) for their helpful reviews of theMS.

Notes on contributors

ALI S.A. SOLIMAN graduated in geologyfrom the University of Tanta, Egypt in1995. In 2000, he finished his Mastersstudies on the Jurassic palynostratigraphyof the Western Desert, Egypt with Salah ElBeialy. In October 2002, he received a Ph.D.scholarship funded by the OAD, Austria

and he completed his studies on Miocene dinoflagellatecysts from the Gulf of Suez, Egypt in March 2006 under thesupervision of W.E. Piller and M.J. Head. Since November2006, he has been a post-doc embedded in projects fundedby the OAW and FWF dealing with the taxonomy andstratigraphy of the Miocene dinoflagellates of the CentralParatethys and the ancient Lake Pannon. Ali is also aLecturer in stratigraphy and paleontology at the Universityof Tanta, Egypt.

STJEPAN CORIC received his Ph.D. inpaleontology from Vienna University(2000), following his MSc (1988) in appliedgeology from Tuzla University (Bosnia &Herzegovina). His research interest is in usingcalcareous nannofossils as a tool for bios-tratigraphy, especially for the Central

Paratethys (Central Europe). He also uses these fossils toreconstruct paleoecological conditions in this bioprovinceduring the Miocene. He has participated in internationalprojects studying the Early/Middle Miocene transgressionand the paleogeographic evolution in this part of Europe.Currently he works at the Geological Survey of Austria,Department for Sedimentary Geology, as a mappinggeologist in the Austrian part of the Alpine–CarpathianForedeep. Stjepan contributes to the study of the LowerMiocene in Austria using calcareous nannoplankton for agedeterminations and paleoecological interpretations.

MARTIN J. HEAD is a Professor of EarthSciences at Brock University, a position heldsince 2005, and has just completed a three-year term as Chair of his department.Previously he was a Senior Research Associ-ate and Affiliated Lecturer at the Universityof Cambridge, UK, and before that a

Research Associate and Lecturer at the University ofToronto, Canada where he worked with Geoff Norris. Heholds a BSc from Aston University, UK where he wasintroduced to palynology by the late Mavis Butterworth, andgained a Ph.D. from the University of Aberdeen under theguidance of David Batten. Martin’s research interests spanall aspects of dinoflagellate cysts, particularly of the lateCenozoic, and he has more recently become involved instratigraphic classification.

WERNER E. PILLER graduated in 1975from the University of Vienna with a Ph.D.thesis on foraminifera, carbonate sedimenta-tion, and stratigraphy in the Triassic of theEastern Alps. In the mid-1980s, he switchedto Cenozoic reefs. He has worked on modernreefs and shallow-water carbonate environ-

ments in the Red Sea, the Persian Gulf, Indonesia, Japan,and the Caribbean, and on fossil Paleogene–Neogene reefs ofthe Mediterranean and Western Indopacific as well as theParatethys. The main topics within this research have been(paleo)ecology and (paleo)biogeography. He now also workson fossil, long-lived ancient lakes, including Lake Pannon(Central Europe) and Lake Pebas (Amazonia). Besidesgeneral (paleo)ecological topics, he also deals with funda-mental questions concerning stratigraphy. Since 1997, he hasbeen Full Professor of Paleontology and Historical Geologyat the Department of Earth Sciences of the University ofGraz.

SALAH EL BEIALY is Professor and Chairof the Geology Department at MansouraUniversity, where he has long been activelyinvolved in stratigraphic palynology. Hegained his Ph.D. in 1985 from the Universityof Sheffield, UK, under the late Prof. CharlesDownie, and acquired experience in indus-

trial palynology through work with Paleoservices Ltd, Shell,BP and Gupco, Egypt. In 2006, Salah spent a year as aVisiting International Scholar at Brock University, Canada,collaborating with Martin J. Head on a project funded by theArab Fund for Social and Economic Development, Kuwait,under the ZAMLAT fellowship program. Salah’s maininterests are in the application of palynology in dating,paleoenvironmental interpretation, spore-color maturitydetermination, and hydrocarbon exploration from the sur-face and subsurface Mesozoic–Cenozoic of North Africa andthe Middle East.


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dinoflagellate cyst biostratigraphy and palaeoenvironment of the early - middle miocene of the gulf...

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