Journal of Applied Sciences Research, 5(1): 122-136, 2009 © 2009, INSInet Publication

Palynological Investigation of Some Rock Units from Palaeozoic Mesozoic of the Sheiba-1 Well, Western Desert, Egypt

Sayed Abdou Mohammad Atawy

Explorations Department, Egyptian Petroleum Research Institute, Cairo, Egypt.

Abstract: Palaeozoic – Mesozoic assemblages have been isolated from cutting samples of the Sheiba no. 1 well, Western Desert, Egypt. Preserved and diversified sporomorph assemblages have been analyzed from the U. Silurian to the U. Cretaceous sediments. Over 90 species of palynomorphs have been identified; (66 species of spores and pollen graines and adding 24 species of dinoflagellate cysts). Five formations are described, from base to top; Gabbro, Pre- Khatatba, Khatatba, Masajid and Bahariya formations and fore assemblage zones are suggested. Integration of the biostratigraphy with lithological data suggests within the boundaries, two regional un-conformity surface, the first one between pre Khatatba and Khatatba formations and the second in-between Masajid and Bahariya formation. The present work demonstrate a succession of miospore assemblages zones, which have been dated stratigraphically as Silurian, Jurassic and Upper Cretaceous (Cenomanian). Zonal correlation, Palaeogeography and palaeoecology is done. The suggested palynozones in the present work are correlated with other zones in Egypt and abroad.

Key words: Cretaceous, Jurassic, Silurian, palynology, spore-pollen, assemblages, Correlation, angiosperm, gymnosperm, dinoflagellate and biostratigraphy

INTRODUCTION overlain by sandstones intercalated with streak of siltstones in the lower part. Sandstone is light grey, Condensed analysis is done on 19 cutting samples fine grained hard, siliceous, partly calcareous, with have been chosen from the borehole Sheiba no-1, [Lat. orange sand grains. Shale is grey, micaceous, with 30° 5` N – Long. 28° 40` E], Western Desert, Egypt some shell fragments. Siltstone is white, light, grey (Fig. 1). The cooperative studies permitted the moderately hard, to soft, micaceous with thin shale assignment of reliable ages to the palynologic biozones laminae. that occur in sediments of marine origin. Establishing of these ages could be reflected the extended them into Pre- Khatatba Formation: The main interval is 283 sediments of non-marine origin due to these Ft in thickness and mainly composed of sand stone, palynological biozones. Assignment ages due to siltstone and shale. The sandstone is usually hard, sporomorph assemblage biozones are often relatively micaceous with trace of yellow orange and reddish high degree of provincialism. The palynological study sandstone. Shale is blocky to sub-blocky, dark grey and have been integrated and correlated with other localities slitly with laminae of sandstone medium and hard. in Africa and other localities in the world. Khatatba Formation: The main interval is 1339 Ft Lithlogy: Silurian, Middle Jurassic and U Cretaceous in thickness and composed of sandstone: fine, medium succession of the study well comprises five formations. hard, with streaks of shale, blocky to sub blocky, The lithologic rock units are taken from composite well medium hard siltstone, moderately brown, hard. log, description of the Sheiba no-1. Most of the 19 Masajid Formation: The main interval is 306 Ft in samples processed for palynological analysis yielded thickness and composed of limestone, argillaceous, rich assemblages. Palynological content is rather jackstone to mudstone, medium hard, streaks of shale, uniform across all the section until the formational blocky, medium hard and at the base sandstone is fine boundary (Fig. 2). and medium hard.. The summary descriptions of the Gabbro, Pre- Khatba, Khatba, Masajid and Bahariya formations are Bahariya Formation: The main interval is 568 Ft in given from base to top; as follows: thickness and composed of sandstone. It is very fine Gabbro Formation: The main interval is 314 Ft in rounded to surrounded, medium hard, with streaks of thickness and mainly composed of: gabbro with other shale, medium hard to soft and streaks of siltstone and minerals in the upper part of the formation and shale sandy limestone medium hard to hard.

Corresponding Author: Sayed Atawy, Explorations Department, Egyptian Petroleum Research Institute, Cairo, Egypt.

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Fig. 1: Location map of Sheiba no-1 well.

Fig. 2: Lithologic column of Sheiba no-1 Well, Westen Desert, Egypt.

MATERIALS AND METHODS Washing the residue several times after 12 hours after a few minuets adding Dilute (HCL 10%) and washes, More than 19 cutting samples are prepared to the it three times with distilled water. A heavy liquid study. Dilute hydrochloric acid (HCL 10%) added to (1.8 mg. specific gravity) is prepared to separate the the cutting samples, to remove any carbonates. After 3 light palynological residue by sieving through a 15-µ hours, the residue washes three times with distilled nylon sieve. Two slides or sometimes more investigated water, then adding hydrofluoric acid (HF 49%). depending on the enrichments of the sample (Fig. 2).

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By using a transmitted light Binocular Microscope biostratigraphy of the late Ludlow to early Devonian is with 10X20 U to 10X40 U. magnifications connected poorly documented[43]. with Digital Camera with Computer. Synorisporites libycus? Lophozonotriletes p o ecilo m o rphus, Synorisporites tripapilla tu s, Biostratigraphy: The present work represent an A p icu liretu sisp o ra sp ecu la , E m p h a n isporites attempt to evolve a compiling the palynological micrornatus and Streelispora newportensis, these characteristics for the Silurian, Jurassic and Cretaceous assemblage species have been deccned in the late rock units as detected from the study 19 samples and Silurian and in the earliest Lower Devonian by identify over 90 species of palynomorphs species Richardson and McGregor[42], partially coincide and (66 species of spores and pollen grains adding to them; match with working in this interval. 24 species of dinoflagellate cysts). The previous palynological investigations, of the Age Assignment: Based on the study of samples and study rock units, have approved that they have an due to the main important index assemblages species organic matters and micro floral debris. The identified; the assemblage zone –I, is of the Silurian morphologic and phylitic evolution of the microfloras age. as well as and their durability in sediments may represent some local and regional stratigraphic events, (2) Pre- Khatatba, Khatatba and Masajed these definitions of the suggested palynozones in the Formations - ( Zone – II): present work and the correlation with other zones in Interval: The main interval is 1622 ft. in thickness. Egypt and abroad. The frequency distribution charts of the recovered Disscusion: some palynomorphs from the study well, are shown in Tables (1, 2). The Pre - Khatba Formation: 283 ft. in thickness and Herein the study interval for the U. Silurian – U. mainly composed of sand stone, siltstone and shale. It Cretaceous (Cenomanian) rock units, can be able to is underlies Khatba Formation and they separated by identify fore palynomorphs zones. Most of these zones unconformity surface. Palynomorphs are very boor and coincide and match with the previous workings in such not detected in it. interval. These study from base to top as follow: The Masajid Formation: 306 ft. in thickness mainly (1) Gabbro Formation – (Zone – I): composed of limestone. It overlies the Khatba Interval: The main interval is 314 ft. in thickness Formation. An unconformity surface separated between the Masajed Formation and Bahariya Formation. It is Disscusion: In the recent years, it has been a steadily very boor in palynomorphs. – awareness of the usefulness of Silurian spores for regional and interregional correlation[47]. From this The Khatatba Formation: is 1339 ft. in thickness formation, 4 cutting samples studied for there mainly of sandstone. Five cutting samples are studied palynomorph contents. The upper part of this formation for occurences microfloras contents. Upper limit is rich mainly composed of gabbro with other minerals and it occuerances of species as: Gonyaulacysta jurassica and is barren from miospores content. Epiplosphaera reticulospinosa. The main important From the study of the main important species of palynomorphs assemblage presented; Cicatricosisporites palynomorph assemblages shown on the slides are; pseudoreticulatus, Concavisporties jurienensis, Chelinospora sp., Clivosispora sp,. Convolutispora Concavisporties SP., Concavissimisporites verrucosus, sp., Cymbosporites verrucosus, Dichadogonyaulax D i c t y o p h y l l i d i t e s h a r r i s i i , K l u k i s p o r i t e s sellwoodii, Emphanisporites protophanus, pseudoreticulatus and Syathidites australis. The main Laevolancis divellomedium, Pseudodyadospora species are recorded of pollen grains such as petasus, Quadrisporites variabilis, Retusotriletes Araucariacites australis, Cycadopites carpentieri, m aculatu s, R etu sotriletes sp., Retusotriletes Cycadopites sp., Diad pollen (Cupressacites triangulatus, Scylasporas downiei, Synorisporites axyceroides) and Inaperturopollenites limbatus. papillensis, Tetrad sp., and Tetrahedraletes medinensis. Dinoflagellate cysts are recorded mainly; cf. In Libya, the almost complete Palaeozoic Apteodinium sp., Cribroperidinium edwardsii, subsurface section in western Libya, ranging in age Cribroperidinium SP., Ctenidodinium panneum, from Cambrian to late Carboniferous, is of primary Ctenidodinium sp., G onyaulacysta jurassica, importance for the understanding of the early Korystocysta gochtii, Korystocysta pachyderma, development of miospores of primitive land plants Lithodinium jurassica, Meiourogonyulax sp. And d uring P alaeozoic time and the m io sp o re Systematophora areolata.

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Table 1: Strategraphic frequency distribution of spores and pollen grains from Sheiba-1 well, Western Desert, Egypt.

The species Gonyaulacysta jurassica remains an mentioned that Korystocysta gochtii is characterizing important cosmopolitan in the Oxfordian, in North for Callovian. Dimeter & Smelror[10], in the southern Africa[56,57] and Western Europe. Moreover Urban, et G ermany recorded G onyaulacysta jurassica, al.,[55] proposed Gonyaulacysta jurassica as a marker Ctenidodinium tenellum, Ctenidodinium continuum. species for the Late Jurrassic of the Alamein area in Thusu & Vigran[51] , defined the Late Callovian- Early the north Western Desert of Egypt. The same Oxfordian in the northeast Libya by the presence of conclusion has been proposed by; Abou Ela & El Wanaea acollaris and Korystocysta pachyderma. Shamma[1]. Habib & Drugg[14] reported the stratigraphic The assemblage of Korystocysta pachyderma, importance of Lithodonia jurrassica in the Callovian Sentusidinium villersense, Gonyaulacysta jurassica, sediments of Black – Bahama Basin. This conclusion Korystocysta gochtii, Piloidinium echinatum and is supported by Abou Ela & El Shamma[1], for Wanaea acollaris define the contact between the Late recognizing the Callovian. Woollam & Riding[57], Callovian and Early Oxfordian, Ibrahim, et al.,[30].

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Table 2: Strategraphic distribution of dinofllate cysts in Sheiba-1 well, Western Desert, Egypt.

Age Assignment: Due to the study and previous is remarked by predominant occurrence of discussion of the assemblage zone -II is of the Elaterosporites klaszi and a parallel reduction, of Callovian - Oxfordian age. Afropollis jardinus. Other important associated taxa in this zone are; Perotriletes pannuceus, Elaterocolpites (3) Bahariya Formation: castelainii and Cicatricosisporites minutistriatus. Interval: covers 668 ft. in thickness In Bahariya Angiosperm pollen grains are sporadically Formation two palynomorhs zones: (Zone III and Zone occurring and represented by a few grains of Afropollis IV) they are from base to top: jardinus, Tricolpites sp. and Cretacaeiporites scabratus. Gymnosperm pollen grains are also rare and (a) Elaterosporites klaszi Acme Zone III: (Early represented mainly by Araucariacites australis, Cenomanian): Classopollis sp. and Classopollis brasiliensis. Interval: This zone covers, 400 Ft. in thickness. Dinoflagellate cysts in this assemblage zone include, Florentinia radiculata, Florentinia sp., Disscusion: An influx of Elaterosporites klaszii is a Cleistosphaeridium sp., and Subtilisphaera perlucida. remarkable event indicative for this zone. The Zone III Age assignment:

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Table 3: Strategraphic of range chart spores and pollen grains from Sheiba-1 well, Western Desert, Egypt.

Aboul Ela, et al.[1]; El-Shamma[12]; El-Shaarawy, et Disscusion: From this formation, the chosen and al.; Bassiouni, et al. and El-Shamma, et al.[12] all of studied 13 cutting samples for their plants microfossils them suggested this zone as Early Cenomanian age. content two samples are barren: The Zone – IV defined by the predominance of the angiosperm pollen grains (b) Afropollis jardinus Acme Zone – IV) (Early Afropollis jardinus. Also it is characterized by the Cenomanian): sporadic occurrence and distinctive association of Interval: This zone covers, 268 ft. in thickness. Elateroplicites africaensis, Elaterocolpites castelainii,

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Table 4: Strategraphic range chart of spores, pollen grains and dinoflagellate cysts in Sheiba-1 well, Western Desert, Egypt.

Cryblosporites pannuceous, Cicatricosisporites al. and Bassiouni, et al., referred this biozone to early minutistriatus and Cyathidites / Dictyophilidites. Cenomanian age. The pollen grains are relatively few and So, from the foregoing we can conclude that the represented by Araucariacites australis, Ephedripites Afropollis jardinus assemblage Zone (IV) is of Early sp., Callialasporites dampieri and Classopollis sp. The Cenomanian age. mainly characteristic taxa of angiosperm pollen grains The fluctuation in the percentage of total terrestrial are Afropollis jardinus and Tricolpites sp. components and marine dinocysts of the assemblages Dinocysts are rare in this biozone. The common indicate well the fluctuation in the sea level during occurring taxa include, Subtilisphaera sp., Florentinia deposition of the Bahariya Formation. radiculata, Florentinia berran and Florentinia sp. The range chart of the recovered some palynomorphs from the study well is shown in the Age Assignment: The occurrence of Afropollis jardinus Tables (3, 4). provides a strong evidence for age not younger than the Early Cenomanian. This species first appeared in Correlation: the Aptian and has been consistently encountered till the early Cenomanian[31,27,]. Florentinia berran has (A) - Zonal correlation: From the study, it can be been recorded from the Vraconian to Lower correlated zones and lithologic section of the studied Cenomanian of Morocco[6]. Other author such as El- well section with two wells Bed 8-1 and W. Tiba -1, Shamma[12]; El-Shamma & Baioumi[12]; El-Shaarawy, et in the northern Western Desert, Egypt (Fig. 3).

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Fig. 3: Location and zonel correlation.

(B) - Palaeogeography and Palaeoecology: The Aptian-Albian. one group of angiosperm pollen palynological correlation of the individual taxa of (Afropollis) and a sporomorph group of unknown Egypt with other area in Africa and northern South botanical affinity (Elaterosporites, Elaterocolpites, America shows that the sequence of palynological Galeacornea, . . . etc.) characterize the Cenomanian assemblages in these areas. It is relatively similar time. The dominance occurrence of Afropollis jardinus because they are all part of the same Cretaceous "group" indicates a near shore setting. The fluctuation microfloral province or realm, namely the middle in the percentage of total terrestrial components and Cretaceous North Gondwana Realm[4], the ASA marine dinocysts of the assemblages indicate well the (African-south American province)[22]. fluctuation in the sea level during deposition of the The microfloras of this province are generally Bahariya Formation. This is supported by relative characterizing by the abundance of Classopollis or occurrence of both rich sporomorph and rare dinocyst Araucariacites together with a regular occurrence and components, which may indicate shallow marine great diversity of Ephedripites group. Bisaccate pollen environment grains are rare or absent. Pteridophyte spores are Deep wells in the Western Desert have so far yield present in comparatively low diversity during the Silurian microfloras (phytoplankton and miospores)

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PLATE I: (all figures X400) 1: Matonisporites simplex Deak. 2, 8: Cicatricosisporites sp. 3: Cyathidites australis Couper. 4: Concavissimisporites punctatus (Del&Sprum) Brenner. 5, 6: Elaterosporites klaszii 7: Elateroplicites sp. (Jardiné & Magloire) Jardiné. 9: Crybelosporites sp. 10: Cretacaeiporites scabratus Herngreen. 11: Afropollis jardinus (Brenner) Doyle. 12: Murospora florida (Balme)Pocock. 13: Stellatopollis barghoornii Doyle et al. 14 Tricolpites sp. 16,19: Araucariacites australis Cookson. 15: Inaperturopollenites limbatus (Balme) Dev. 17: Steevisipollenites sp. 18: Spheripollenites sp. 20: : Ephedripites spp. 21:Mudirongea sp. 22, 23, 26: Odontochitina operculata 24: Cribroperidinium orthoceras (Eisenak) Davey. (Wetzel) Deflander & Cookson 25: Florentinia sp. 27: Lithodonia callomonii Sarjean)Gocht. 28: Cribroperidinium sp. 29: Cyclonephelium sp. 30: Oodonadattia sp..

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PLATE II: (all figures X400) 1: Concavissimisporites verrucosus 2 : Concavisporties sp. (Del. & Sprum) Del., Det . & Hughes 3 : Cicatricosisporites pseudoreticulatus 4 : Dictyophyllidites harrisii Couper. Bolkhovittian 5 : Inaperturopollenites limbatus Balme. 6 : Syathidites australis Couper. 7 : Klukisporites pseudoreticulatus Couper. 8 : Concavisporties jurienensis Balme. 9 : Diad pollen (Cupressacites axyceroides Reyre). 10 : Cycadopites carpentieri Singh. 11 : Murospora florida (Bame) Pocock. 12 : Cycadopites sp. 13 : Araucariacites australis Cookson 14 : Callialasporites trilobatus (Balme) Dev. 15 : Korystocysta pachyderma (Deflandre) Woollam. 16 : cf. Apteodinium sp. 17 :Cribroperidinium edwardsii 18 : Cribroperidinium sp. (Cookson& Eisenack) Davey 19: Gonyaulacysta jurassica (Deflandre ) Norris&Sarjeant . 20: Ctenidodinium sp. 21: Lithodonia jurassica (Eisenack) emend. Gocht. 22: Systematophora areolata Klement. 23: Ctenidodinium panneum (Norris ) Lentin & Williams 24: Meiourogonyulax sp. 25: Korystocysta gochtii (Sarjeant) Woollam. 26: Dissiliodinium sp.

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PLATE III: (all figures X400) 1: Scylasporas downiei Burgess and Richardson. 2: Dichadogonyaulax sellwoodii Sarjeant 3,5: Retusotriletes maculatus Gregor and Cam¢eld. 4: Retusotriletes triangulatus Streel. 6: Clivosispora sp. 7: Tetrahedraletes medinensis Strother and Traverse. 8,18: Laevolancis divellomedium Burgess and Richardson. 9: Cymbosporites verrucosus Richardson and Lister. 10: Synorisporites papillensis Gregor. 11: Tetrahedraletes medinensis Strother and Traverse. 12: Quadrisporites variabilis Cramer and Diez. 13: Convolutispora sp. 14: Emphanisporites protophanus Richardson and Ioannides. 15: Chelinospora sp. 16: Retusotriletes sp. 17: Tetrad sp. 19: Pseudodyadospora petasus Wellman and Ricardson. known from Egypt, In addition, existence of subtropical toward the north. The quantitative Carboniferous assemblages has been proven[46], Closely differences assemblages have affected by the comparable to contemporary previously have been differences in sedimentary processes and other described from the subsurface of the Sinai Peninsula[45]. environmental conditions prevailing in the sites of The palynomorphs groups of Egypt show minor deposition. differences in the type of flora than those reported Although the polyporate angiosperm forms from the equatorial regions. They may attribute to the (Cretacaeporites) have early appeared in the equatorial climatic change from hot tropic at the equator to humid region during the Albian - Cenomanian, Tricolpate

132 J. Appl. Sci. Res., 5(1): 122-136, 2009 forms at this region still represented by small primitive environmental control. Dominance usually bears an forms. At the same time, these forms seem to have inverse relationship to diversity, many specimens more morphological diversity in the north area special correlating with few species and vice versa. at the Atlantic sites, as indicated by Kotova[35], and Dinoflagellate cysts assemblages have described and Hochuli and Kelts[29]. illustrated from numerous areas in the world. As An environmental interpretations based on miospores, some species of dinoflagellates are palynomorphs comprise only a small part of the field cosmopolitan where as others have distributed restricted of palaeoecology and have some limitations. Among to certain regions. these limitations is the extinction of the parent plants The combination of these data provide a firm producing sporomorphs and their palaeoecological dinostratigraphic framework for correlation with the relationships led at the end to unsufficient data about Egyptian Cretaceous assemblage and have been used in their ecologic conditions. The paleogeographic situation dating confirmation of the recovered assemblage zones represents another important factor for stratigraphic and in the present work. The sea is gradually shallower climatic interpretation of sporomorph assemblages. toward the Albian and interrupted with minor Some terrestrial palynomorphs seem to have almost successive phases of regression and transgression world, wide distribution, such as some groups of during the early Cenomanian. pteridophyte spores as well as some groups of Most of the available literatures have discussed gymnosperm pollen grains. However, groups of the Mesozoic dinocysts palaeogeography and palynomorphs are restricted to certain climatic belts and confined exclusively to presence or absence of are used to define flora provinces[28]. Environmental data on selected taxa and a little attention has interpretation, of the relatively abundance of the given to the population ratio or sedimentary facies palynomorphs groups can be used in assessing distance control on the assemblage. Norris[37] recorded in a from land. Miospores are commonly more numerous review of Middle Jurassic to Early Cretaceous than microplankton at near-shore deposits, whereas the dinocysts distribution of recognition, three provinces; reverse is often true in beds that accumulated in open Boreal, Tethyan and Anti-Boreal (Austral). The Tethyan marine conditions. The climate type of vegetation province however, is best developed in western north closing the land energy of the depositional Atlantic, Southern Europe and North Africa. It has environment, and may other factories can however been studied by Davey & Verdier[8,9]; Norris[38]; distorted these trends to greater or lesser extend[36]. Below[5,6]; Duxbury[11]; Thusu, et al.[52,53] and According to these upper mentioned concepts the Omran, et al.[41]. ecological and environmental conditions of the upper Cretaceous sediments in the study area discussed as Conclusions: Five formations recorded and discussed following: from the studied section, they are from top to base as Afropollis jardinus dominates the miospore the following: components with elater-bearing sporomorphs (mainly Elaterosporites klaszi) and small psilate tricolpate C Bahariya Formation: The main interval is 568 Ft in pollen and spores of the Gabonisporis group and thickness smooth trilete spores, where as gymnosperm pollen are C Masajid Formation: The main interval is 306 Ft in relatively scarce. Mainly occurrence of Elaterosporites thickness klaszi and other Elater-bearing spores may suggest a C Khatba Formation: The main interval is 1339 Ft colonization of marginal area or barrier complex during in thickness a marked regressive phase. C Pre- Khatba Formation: The main interval is 283 This may supported by less number of other Ft in thickness marine dinoflagellate cysts. These plants prefer the C Gabbro Formation: The main interval is 314 Ft in moist-humid climate and their frequency in the thickness. preparation supported the above conclusion that deposition took place close to shore in the Early About of 90 species of palynomorphs have been Cenomanian. identified; about 66 species spores and pollen grains The ecological control on the distribution of the adding to them 24 species of dinoflagellate cysts. dinocysts has pointed out by Dale[7] who reported Three assemblage zones are established and markedly different assemblages of living dinocysts in correlated with other localities they are: different sedimentary environments. In this aspect, dominance and diversity changes in the taxonomic C III- Zone (Albian - Cenomanian). composition of fossil dinoflagellates can relate to C II- Zone (Jurassic). inshore and offshore trends, there by implying C I- Zone (Silurian).

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Two regional unconformity surface are in-between 11. Duxbury, S., 1983. A study of dinoflagellate cysts pre –Khatatba and Khatatba formations and between and acritarchs from the Lower Creen Sand (Aptian Masajid and Bahariya formation. to Lower Albian) of the Isle Wight, south England. Palaeont. Band., 186: 18-80. ACKNOWLEDGMENT 12. El Shamma, A.E., 1988. Aptian and Albian miozones of Western Desert, Egypt. 9th pet. Conf. The author wishes thank and gratitude to the For Expl. and Prod., EGPC., pp: 1-21. management of, (E.G.P.C.) for providing samples and 13. Evitt, W.R., 1961. Observation of the morphology logs upon which the study were carried out and thanks of fossils dinoflagellates Micropal., New York, 7: to Mr. Walid Ahmad for his effort helping me in 385-420. samples preparation to study. 14. Habib, D and W.S. Drugg, 1983. Dinoflagellate ages of Middle Jurassic – Early Cretaceous REFERENCES sediments in the Blacke- Bahama Basin . Initial Report, DSDP, 76 U. S. Gov. Print, Washington, 1. Aboul Ela, N.M. and A.A. El- Shamma, 1997. 623-638. Palynostratigraphy of the Middle-Upper Jurassic 15. Herngreen, G.F.W., 1973. Palynology of Albian- rocks in El- Giddi borehole, north Sinai, Egypt. Cenomanian strata of Borehole 1-QS-I-MA, Acta Univ.Carolinae, Geol., 41(1): 47-55 State of Maranhao, Brazil. Pollen et Spores, 15: 2. Atawy, S.A.M. and M.M. Mandur, 2006: 515-555. Palynomorphs and calcareous nannoplankton 16. Herngreen, G.F.W., 1974. Middle Cretaceous biostratigraphical study on upper Jurassic - lower palynomorphs from northwestern Brazil. Results of Cretaceous of bed 8-1 well, Western Desert, Egypt. a palynological study of some boreholes and Egypt, J., petrol., 15: 77-102. comparison with Africa and the Middle East. Sci. 3. Batten D.J. et Li Weben, 1987. Aspects of Geol. Bull. Strasbourg, 27: 101-116. palynomorph distri-bution, floral Provines and 17. Herngreen, G.F.W., 1974. Middle Cretaceous chmate during the Cretaceous.Geol. Jb., Ilannover, palynomorphs from northwestern Brazil. Results of A, 96: 219-230. a palynological study of some boreholes and 4. Batten, D.J. and P.J.R. Uwins, 1985. Early-Late comparison with Africa and the Middle East. Sci. Cretaceous (Aptian-Cenomanian) Palynomorphs. J. Geol. Bull. Strasbourg, 27: 101-116. Micropalaeont, 4: 151-168. 18. Herngreen, G.F.W., 1975. Palynology of Middle 5. Below, R., 1981. Dinoflagellate - Zysten aus dem and Upper Creta- ceous strata in Brazil. Meded. oberen Hauterive bis unteren Cenoman Süd West - Rijks geol. Dienst., N.S., 26: 39-91. Markkos: Palaeontographica, Band, 176: 1-45. 19. Herngreen, G.F.W., 1975. Palynology of Middle 6. Below, R., 1982. Aptian to Cenomanian and Upper Creta- ceous strata in Brazil. Meded. dinoflagellates cysts from the Mazagan Plateau, Rijks geol. Dienst., N.S., 26: 39-91. Northwest Africa (sites 545 and 547, Deep Sea 20. Herngreen, G.F.W., 1981. Microfloral relationships Drilling Project, Leg 79). Initial Reports, DSDP, between Africa and South America in Middle and 79: 621-649. Upper Cretaceous time. Proc. Palynol. Conf., 7. Dale, B., 1986. Ecological Boundaries in Lucknow (1976-1977), 3: 406-417. Dinoflagellate palynology in Boundaries and 21. Herngreen, G.F.W., 1981. Microfloral relationships palynology Symposium CIMP / University of between Africa and South America in Middle and Sheffield, Abst. Upper Cretaceous time. Proc. Palynol. Conf., 8. Davey, R.J. and Verdier, 1973. An investigation of Lucknow (1976-1977), 3: 406-417. microplankton assemblages from Latest Albian 22. Herngreen, G.F. and A.F. Chlonova, 1982. (Vraconian) sediments: Rev. Esp. Micropalaeontol., :Cretaceous microfloral provinces. Pollen et Spores 5: 173-212. 23(3-4): 441-555. 9. Davey, R.J. and Verdier, 1974. Dinoflagellat cysts 23. Herngreen, G.F.W. and A.F. Chlonova, 1981. from the Aptian type sections at Garagas and La Cretaceous microfloral province. Pollen et Spores, Bedoule , France : Palaeontology, 17: 623-653. 23: 441-555. 10. Dimeter, A. and Smelror, 1990. Callovian Middle 24. Herngreen, G.F.W. and A.F. Chlonova, 1981. Jurassic marine microplankton from southern Cretaceous microfloral provinces. Pollen Spores, Germany: Biostratigraphy and paleoenvironmental 23(3/4): 441-555. interpretations .- Palaeog., palaeocli., Palaeoecol., 25. Herngreen, G.F.W., 1973. Palynology of Albian- 80: 173-195. Cenomanian strata of borehole 1-QS-1-MA, state

134 J. Appl. Sci. Res., 5(1): 122-136, 2009

of Maranhao, Brazil. Pollen Spores, 15(3/4): 39. Norris, G., D.M. Jarzen and B.V. Awai-Thorne, 515-555. 1975. Evolution of the Cretaceous terrestrial 26. Herngreen, G.F.W., 1974. Middle Cretaceous palynoflora in western Canada. Geol. Ass. Can. palynomorphs from northeastern Brazil. Sci. Geol. Spec. Paper, 13: 333-364. Bull., 27(1/2): 101-116. 40. Omran, A.M., H.A. Soliman and M.S. Mahmoud, 27. Herngreen, G.F.W., 1975. Palynology of Middle 1990. Early Cretaceous palynology of three and Upper Cretaceous strata in Brazil. Meded. boreholes from northern Western Desert (Egypt). Rijks Geol Dienst, 26(3): 39-91. Rev. Palaeobot. Palynol., pp: 66: 293-312. Palynot., 28. HOCHULI P.A., 1981. North Gondwanan floral 35: 337-358. elements in Lowerto Middle Cretaceous sediments 41. Omran, A.M., H.A. Soliman and M.S. Mahmoud, of the Southern Alps. (Sou- thern Switzerland, 1990. Early Cretaceous palynology of three Northern Italy). Rev. Palaeobot.o Paly- nol., 35: boreholes from northern Western Desert (Egypt).- 337-358. Rev.palaeobot. Palynol., 66: 293-312. 29. Hochuli, P.A. and K. Kelts, 1980. Palynology of 42. Richardson and McGregor, 1986. Silurian and Middle Cretaceous black clay facies from DSDP. Devonian spore zones of the Old Red Sandstone Sites (417) and (418) of the western North Atlantic Continent and adjacent region. Geol. Surv. Can. : Init. Reps., (51-53): 897-935. Bull., 364: 1-79. 30. Ibrahim, M.I.A., N.M. Aboul Ela and S.E. Kholeif, 43. Rubinstein, C. and P. Steemans, 2002. Miospore 2002. Dinoflaellate cyst biostratigraphy of Jurassic- assemblages from the Silurian^Devonian boundary, Lower Cretaceous formations of the North Eastern in borehole A1-61, Ghadamis Basin, Libya. Review Desert, Egypt., N.Jb.Geol.Palaont.Abh., 224(2): of Palaeobotany and Palynology, 118: 397-421 255-319. 44. Schrank, E., 1984. Paleozoic and Mesozoic 31. Jardine C.S. and L. Magloire, 1965. Palynologie et palynomorphs from the Foram – 1 well (Western stratigraphie du Cretace des bassins du S6n6gal et Desert, Egypt). N. Jb. Geol. Palaeont Monat. 2: de Cote d'Ivoire. Mem. Bur. Rech. Geol. Min., 32: 95-112. 187-245. 45. Schrank, E., 1987. Paleozoic and Mesozoic 32. Jardine, S. and L. Magloire, 1965. Palynologie et palynomorphs from Africa (Egypt and Sudan) with stratigraphie du Cretace des Bassins du Senegal et special to Late Cretaceous pollen and de Cote d'Ivoire: Mem. B.R.G.M., (32), Coll. Int. dinoflagellates. Berliner Geowiss. Abh., A,75(1): Micropol., 187-245. 249-310. 33. Jardine, S., 1967. Spore a expansions en from 46. Schrank, E., 1984. Paleozoic and Mesozoic d'elateres du Cretace moyen d'Afrique occidentale palynomorphs 168 M.I.A. lbrahim/Review of : Rev. Palaeobot. Palynol., 1: 235-258. Palaeobotany and Palynology 94 (1996) 137-168 34. Jardine, S., 1967. Spores a expansions en forme from the Foram 1 Well (Western Desert, Egypt). d'elateres du Cretace moyen d'Afrique occidentale. Neues Jahrb. Geol. Pal~iontol. Monatsh., 2: Rev. Palaeobot. Palynol. 1: 235-258. 95-112. 35. Kotova, Z., 1978. Spores and pollen of Cretaceous 47. Smith, A.G., A.M. Hurley and J.C. Drewry, 1981. deposits ofEastern North Atlantic Ocean, Deep Sea Palaokontinentale Weltkarten des Phanerozoikums. drilling project, Leg41, sites 367 and 370. Init. Stuttgart (Enke): 102 Rep. D.S.D.P., Washington, 41: 841-881. 48. Srivastava, S.K., 1978. Cretaceous spore-pollen 36. Lister, J.K. and D.J. Batten, 1988. Stratigraphic floras: a global evalu- ation. Bio. Mere. 3: 1-130. and palaeoenvironmental distribution of Early 49. Srivastava, S.K., 1978. Cretaceous spore-pollen Cretaceous dinoflagellates cysts in the Hurlandson floras: a global evalu- ation. Bio. Mere, 3: 1-130. Farm Borehole, West Sussex, England.- Palaeotog. 50. Srivastava, S.K., 1978. Cretaceous spore-pollen Abt. B,(210 91-(3): 9-89. floras : a global evaluation, Mem., 3(1): (1-130). 37. Norris, G., 1968. Microspores from the Purbeck 51. Thusu, B. and J.O. Vigran, 1985. Middle –Late beds and marine Upper Jurassic of southern Jurassic (Late Bathonian-Tithonian) palynomorphs, England : Palaeontolo., 12(4): 574-620. Libya. In Symposium on palynostratigraphy of 38. Norris, G., 1973. Palynologic criteria for northeast Libya (Arabian Gulf Company); Journ. recognition of the Jurassic Cretaceous boundary in Micropalaeont., 4(1): 113-130. Western Europe. In: Chlonova, A.F. (Ed.), 52. Thusu, B., J.G.L.A. Van Der Eem, A. El-Mehdawi Proceedings of 3rd International Palynological and F.B. Argoub, 1988. Jurassic - Early Cretaceous Conference, Palynology of Mesozoic. Publishing palyno-stratigraphy in northeast Libya.-. El Arnauti, House Nauka, Moscow. A. et al. (Eds.).

135 J. Appl. Sci. Res., 5(1): 122-136, 2009

53. Thusu, Van Der Eem, El-Mehdawi and Argoub 56. W illiams, G.L., 1977. Dinocysts, their 1988. Jurassic-Early Cretaceous palynostratigraphy classification, biostratigraphy, and paleoecology. In: in northeast Libya. Subsurface palynostratigraphy RAMSA, A.T.S., Oceanic Micropalaeont., 2: (Eds), pp: 171-214. 1231-1325. 54. Urban , L.L., L.V. Moore and M.L. Allen, 1976. 57. Woollam, R. and J.B. Riding, 1983. Dinofalgellate Palynology, thermal alteration, and source rock cyst zonation of the English Jurassic.- Inst. potential of three wells from Alamein area , Geol. Sci., London, dep., 83(2): 1-42. Western Desert, Egypt: 5th EGPC Explor. Seminer. Phill Pet. Co. Special paper: 3-31. 55. Urban, L.L., L.V. Moore and M.L. Allen, 1976. Palynology, thermal alteration, and source rock potential of three wells from Alamein area, Western Desert, Egypt: 5th EGPC Explor. Seminer. Phill Pet. Co. Special paper, 3-31.

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