M. ÁLL. FÖLDTANI INTÉZET ÉVI JELENTÉSE AZ ÉVRŐL

M. ÁLL. FÖLDTANI INTÉZET ÉVI JELENTÉSE AZ 1973. ÉVRŐL A MICROFACIES STUDY OF THE UPPER CRETACEOUS-PALEOCENE-LOWER EOCENE SEDIMENTS AT DUW I AND GURNAH SECTIONS, SOUTHERN EGYPT by M. G. В a r a k a t and A. S. E l -D a w o o d y Geology Dept., Faculty of Science, Cairo University, Giza/Egypt The Upper Cretaceous-Lower Tertiary Sediments are widespread botli on the surface and in the subsurface of Egypt. They are mainly developed in shale and mari facies with limestone interbeds. By and large, the Upper Cretaceous-Lower Eocéné succession falls intő well defined rock Stratigraphie units. These units are studied in the present work through a profile in Southern Egypt, represented by Gebei Duwi along the Red Sea coast in the east and Gebei Gurnah in the Nile Valley against Luxor to the west (fór location, see Fig. 1). The Classification of the Upper Cretaceous-Lower Tertiary sediments has been the subject of copious literature since the very early days of geological investigation in Egypt. K. A. Z ittel (1883) was the first pioneer who studied the fossiliferous marine succession overlying the Nubia Sandstone of the Western Desert where he advocated the conformable relationship between the Upper Cretaceous and the Lower Tertiary in Southern Egypt. Other eminent authors contributed to the geology of this succession in Upper Egypt. Among those: M. Bla k c k ek h o r n (1900), H. J. L. B e a d n e l l (1905), W. F. H u m e (1911), F. R. S. H en so k (1938), M. I. F aris (1947), S. E. N a k k a d y (1949, 1950, 1951), M. I. Y oussef (1957), M. I. F aris and M. Y. H assak (1959), R. Sa id (1960, 1962), R. Said and H. Sa r b y (1964), V. A. K r a s h e- k ik n ik o v and V. P. P o k ik ar o v (1964), Z. R. E l -N aggar (1966), T. M. A bd E l -R a z ik (1968), V. A. K r a s h e k ik n ik o v and T. M. A bd E l -R a z ik (1969) and last bút not least M. M. I sm ail and T. M. A bd E l -R a zik (1969). Stratigraphy The Upper Cretaceous-Lower Tertiary succession along the studied profile is differentiated intő six major rock Stratigraphie units of mapable character and acquiring regional extent. These are arranged stratigraphically as: Nubia Sandstone and Quseir Variegated Shale, Duwi Phosphate, Dakhla Shale, Tarawan Chalk, Esna Shale and Thebes Formations. The following is a brief account for the different rock units previouslv introduced. It deals mainly with their lithological charaeters, their Stratigraphie relationships and Variation in facies.

3 9 2 M. G. Barakat A. S. E l-daw oody 7. ábra. Helyszínrajz. (7. Vizsgált terület) Fig. 7. Location шар. (2. Investigated section) 1. Nnbia Sandstone and Quseir Variegated Shale The term Nubia Sandstone was first introduced intő the Egyptian stratigraphy by R ussegger (1837) after the type locality Nubia in Southern Egypt. It was later recognized by Y oussef (1957) in the Quseir area and named the Nubia Sandstone. Wherever the base is exposed, the transgressive Nubia Sandstone bed rests unconformably over the basement rocks. The

Két dél-egyiptomi szelvény mikrofácies-vizsg. 3 9 3 sandstones are mainly cross-bedded, variegated, brownish to yellowish white, violet with thin ferruginous bands. They are mostly unfossiliferous, medium to fine grained and well sorted. The thickness of these sandstones amounts to 200 mts. in Duwi section (Suppl. I). They are overlain bv a series of unfossiliferous variegated shales and clays, being multicolored and intercalated by fine grained sandstone bands particularly at the base. These shales were invariably considered by older authors as a part of the Nubia Sandstone rock unit. Ghorab (1956) considered the variegated shales overlying the Nubia Sandstone and underlving the lowermost phosphatic bed in the Quseir area as a separate formation and named it the Quseir Formation. Y oussef (1957) introduced the name Quseir Variegated Shales fór the same formation and assigned it to the Campanian age. The thickness of these shales amounts to 150 mts. at Gebei Duwi. 2. Duwi Phosphate Formation A succession of phosphatic lenticular bands interbedded with shales, maris and limestones о verlies conformably the Quseir Variegated Shales. This formation was named Duwi Formation in Quseir district by Y oussef (1957). The Duwi Phosphate extends in a conspicuous scarp fór about 40 kms. on the western side of Duwi Range, underlving the Dakhla Shale Formation with Ostrea vesiculans Z ittel and Pecten farafrensis Z it t e l. It crops out also to the north, northwest and south of Gebei Duwi, attaining a thickness of about 150 170 mts. 3. Dakhla Shale Formation These shales were first described by Said (1961) at its type locality along the scarp north of Mut, Dakhla Oasis. They are formed of yellowish to greyish shales becoming marly at the base and attaining a thickness of about 130 mts. at the type locality. They are of remarkably constant lithological characters. Sometimes, however, they change laterallv in facies almost entirely or at least in part to chalk or chalky limestones. This Variation was pointed out by K e r d a n y (1969) and he called it as the Khoman Chalk. This formation could be equated with the Sudr Chalk formation of Ghorab (1961). The Dakhla Shale unit assumes a thickness of 150 170 mts. at Gebei Duwi. 4. Tarawan Chalk Formation This formations was described formally by A w ad and G h o br ial (1966) in its type locality at Tarawan block in Kharga Oasis where it attains a thickness of about 45 mts. It is described as a thick bed -o chalk, grading intő chalky limestone or siliceous limestone which is dated back to the Upper Paleocene. It shows great lateral Variation both in lithology and in thickness. To the south of Kharga Oasis, the chalk changes into an ochreous sandy limestone unit previously described by B lanckenhorn (1900) under the term Kurkurstufe and was dated to the Lower Eocéné. To the east in Quseir district, it represents a chalk unit, with few mari intercalations attaining a thickness of about 20 mts. at Gebei Duwi. 5. Esna Shale Formation This rock unit was described fullv by B ead n ell (1905) in its type locality at Gebei Oweina, opposite Esna in Upper Egvpt, where it attains a thickness

394 M. G. B arakat A. S. E l -D aw oody of about 60 mts. It is sometimes referred to as the 'Upper Esna Shale (H ume 1911 and others), but mostly equated with both the Kharga papershale member of G horab (1956) and Upper Oweina Shale member of El- N aggar (1966). This unit has a very wide geographical distribution. It is well developed along the Nile Valley, in the Safaga-Quseir district as well as in Gebei Egna in Central Sinai (Said 1962). These shales were assigned to the Upper Paleocene (Said and K e r d a n y 1961, Said 1962). At Gebei Duwi, this rock unit assumes a thickness of about 50 mts., characterized by its grey to dark grey color, greenish in part, fissile and locally ferruginous. At Gebei Gurnah along the Nile Valley, against Luxor, the section is represented by shales of ±18 mts. thick, the base of which is unexposed. This part of the section rejiresents the uppermost part of the Esna Shale Formation and corresponds to the uppermost part of the same formation at Gebei Duwi (Suppl. I). 6. Tliebes Formations The uppermost succession in the studied section is composed of calcareous shale, shaly limestone and limestone. It is designated by E l -N aggar (1966) as the Thebes Formation. It is further differentiated intő a lower Thebes Calcareous Shale and an upper Thebes Limestone. The former is distinguished from the latter by relative increase in the argillaceous matter. The Thebes Formation was originally described by Said (1960, 1962) as limestone with fiint and maris; basal beds with Operculina libyca Sch w a g e r. Its type locality is at Gebei Gurnah, against Luxor where it attains a thickness of about 300 mts., overlving the Esna Shale. The Thebes Formation is introduced to indicate the open marine facies which is synchronic with the Alveolinid Farafra Limestone Formation representing a reefal facies of Early Eocéné age. This unit crops out along the Nile Valley and Stretches eastwards forming the cliffs of Wadi Qena. It is developed to the east along the Red Sea Range in the Quseir-Safaga district and forming the table-land in Gebei Egma in Central Sinai. To the west of the Nile, this unit forms the plateau land at Kharga Oasis extending further south to the latitude of Aswan. In Duwi Range, Quseir area, the Thebes Formation forms conical hills extending N W SE with dip slopes eastwards. It attains a thickness of about 160 mts., the basal Table 1

Két dél-egyiptomi szelvény 39 5 20 mts. of which are of the Thebes Calcareous Shale. The material upon which this study is based was described in detail by E l-d a w o o d y (1970). The occurrences of the previously mentioned rock Stratigraphie units together with their thicknesses in meters are shown by Table 1. Microfacies and paleoecology A microfacies may be defined as the complex of microscopical features of sedimentary rocks which permit interpretation and correlation of the conditions that prevailed during Sedimentation and diagenesis. This recent method is п о лу gaining importance in the field of local, regional and interregional straf i- graphical correlations. Cu villier and Sacal (1951) introduced this method of study and pointed out its value as a Stratigraphie correlation tool. A series of monographs were published, dealing with the microfacies of many parts of the world (H. H agn 1955, M. R e y and G. N ouet 1958, S. H anzaw^a 1961, A. F ord and J. H oubolt 1963, M. B. Cita 1965, M. M isik 1966 etc.). In Egypt, M. A. G horab and M. M. I smail (1957) were the pioneers in microfacies studies. They described, identified and micro-photographed the different microfacies met with in the Eocéné and Pliocene Sediments to the east of Helwan. This was followed by a series of microfacies studies in many parts of Egypt, of which M. G. B arakat and N. M. T e w f ik (1966), M. M. I smail and Á. A. Selim (1967), M. G. B arakat and S. E. F ah m y (1968) and M. M. I smail and T. M. A bd E l-r a zik (1969) are the most important and very near to the present study. In this study, indurated interbeds were thin sectioned and microscopically examined. The terminology proposed by F olk (1959) in deseribing the different carbonate types is followed. The environmental conditions that jirevailed during Sedimentation were discussed, interpreted and a paleogeographic reconstruction was attempted. 1. Variegated shale (Pl. I, Fig. 1) AJ MICROFACIES Upper Cretaceous The rock is pale greenish yellow to yellowish brown argillaceous matter, microcrystalline, very fine grained, with ferruginous streaks and irregulär patches, slightly arenaceous and poorly micaceous, unfossiliferous. This facies is found in the Variegated Shale unit at Gebei Duwi, sample no. 100. This type reflects an inner neritic environment of relatively shallow water conditions not far from a nearby land-mass. 2. Sandy shale (Pl. I, Fig. 2) Pale to dark brownish, highly siliceous, sand grains being angular to subrounded, ill-sorted, with phosphatic grains highly stained with iron oxides and few glauconitic granules, with no proper Orientation. This association is recorded from Duwi Phosphate Formation, sample no. 3. This type of facies reflects shallow marine environment where the phosphatic material has been accumulated and in which the derived clastics were deposited not far from the nearby land-mass.

3 9 6 M. G. В ARAKAT A. S. E l -Daw oody 3. Fossiliferous micrite (PL II, Fig. 1) Dark grevish with pale brownish staining, cryptocrystalline, exhibiting more or less regulär fine bands with undifferentiated organic remains together with phosphatic (?) grains arranged nearly parallel to the direction of lamination, with very fine quartz grains filling up fine veinlets. This facies is found in Duwi Phosphate formation, sample по. 3a. It is also known in samples 28/D, 29/D and 30/D of the uppermost phosphatic bed, but of rare faunal content together with its lack in banding. They also embrace fine carbonaceous dots haphazardly arranged. Such a type of facies reflects a neritic environment with calm conditions o f Sedimentation low agitated bottom conditions. 4. Phosphatic biosparite (PL II, Fig. 2) Pale yellowish brown, main ly composed of phosphatic remains in the form of plates, granules and rounded bodies embedded in a mátrix of microcrystalline carbonates and in parts it is sparry calcite. Phosphatic granules are mostly well sorted and they exhibit straight extinction with micaceous inclusions. This facies is known in Duwi Phosphate Formation, sample no. 3b just below the uppermost phosphatic bed. Such a type of association reflects an inner neritic environment that have been stronglv affected by high level of energy caused by waves. Secondary crystallization mav have taken place and gave rise to the sparry texture. 5. Phosphatic blomlcrlte (PL III, Fig. 1) The rock is dark grevish, cryptocrystalline, highly fossiliferous, with bentonic fauna and phosphatic remains. Benthonic foraminifers are mainly represented by rotalid forms together with some Clavullna spp.? Phosphatic remains are represented by well preserved vertebrae, ribs and undifferentiated fragments irregularly scattered through the whole facies. This biomicrite is recorded from Gebei Duwi, sample no. 27/D at the base of the Dakhla Shale Formation and just above the uppermost phosphatic bed. Such a type of facies reflects a mixed environment in which marine transgression gentlv overlapped the phosphatic bioherms resulting in this peculiar association. 6. Heterohellx blomlcrlte (PL III, Fig. 2) Pale brownish yellow, microcrystalline, highly fossiliferous, with planktonic and benthonic foraminifers. The planktonic foraminifers are mainly represented by Heterobelix spp., Globotruncana spp., Globigerinas and Globorotalias. Benthonic foraminifers are represented by Bollvlna spp.?, together with some lagenid and rotalid forms. Tvpical biomicrites of the genus Heterohelix are recorded from the Dakhla Shale Formation at Gebei Duwi, samples 23/D, 24/D and 25/D. Such a type of association reflects deep water conditions of warm sea with normal salinitv where planktonic elements are the most abundant and coarser terrigenous materials is completely absent.

Két dél-egyiptomi szelvény mikrofácies-vizsg. 39 7 Paleocene 7. Globorotalia biomicrite ( A ) (Pl. IV, Fig. 1) Pale brownish yellow, with argillaeeous matter, fine grained and cryptocrystalline, highly fossiliferous, with planktonic foraminifers particularly round-keeled Globorotalias together with Globigerina spj>. They are completely replaced by fine grained calcite filling up their interior cavities. Benthonic foraminifers are also common and they are habhazardly distributed in the rock section. This facies in known in the Dakhla Shale Formation at Gebei Duwi, sample no. 21/D. Such a type of facies reflects deep water deposit of at least semi-pelagic character with abundance of planktonic calcareous microfauna. 8. Globorotalia biomicrite ( B ) (Pl. IV, Fig. 2) Pale brownish yellow, with argillaeeous matter, fine grained and cryptocrystalline, highly fossiliferous, with planktonic Foraminifera such as sliarp - keeled Globorotalias together with round-keeled Globorotalias, also with few benthonic foraminifers. This biomicrite represents a transitional phase between the round-keeled and the sharp-keeled Globorotalias which characterize the advent of the Upper Paleocene fauna. It is known in the Dakhla Shale Formation at Gebei Duwi, samples 16/D?, 17/D, 18/D and 19/D. The last three samples are of a relatively poor faunal content. This association reflects an outer neritic to bathyal environment. 9. Globorotalia biomicrite (C) (Pl. V, Fig. 1) Pale yellowish brown, with argillaeeous matter more than those observed in the previous ojder biomierites (A) and (B), fine grained and cryptocrystalline, highly fossiliferous, with planktonic foraminifera particularly sharpkeeled Globorotalias together with few benthonic foraminifers This facies is recorded from the Tarawan Chalk Formation at Gebei Duwi, samples 13/D, 14/D and 15/D. Such an association reflects deep water deposition with predominance of planktonic elements (neritic environment), without contribution of coarser terrigenous material. 10. Marly mierite (Pl. V, Fig. 2) The rock is dark brownish, very fine grained, with dense argillaeeous mátrix. Moderately coarse grained euhedral calcite is scattered allover, stained by iron oxides and devoid of anv organic remains. This association is onlv recorded from sample no. 10/D, intercalating the Esna Shale Formation at Gebei Duwi. It is similar to that recorded by I smail and Selim (1967) from the Cretaceous strata of Gebei Ataqa scarps. This facies indicates deposition under fairly deep marine conditions of the neritic zone récéiving no terrigenous material. 11. Marly foraminiféral biomicrite (Pl. VI, Fig. 1) The rock is pale brownish, stained with iron oxides, microcrystalline and highly fossiliferous, foraminiferal fauna rich in planktonic species together with somé rotalid forms, all embedded in an argillaeeous mátrix. Microfossils

3 9 8 M. G. B arakat A. S. E l-daw oody are completely replaced by fine grained calcite. This biomicrite is known in samples 9/D, 11/D and 12/D at the base of the Esna Shale formation at Gebei Duwi. This association reflects deep water conditions of middle neritic environment in a warm sea with normal salinity where planktonic elements are the most abundant, and coarser terrigenous materials are completely absent. Lower Б] осе ne 12. Foraminiferal biomicrite (Pl. VI, Fig. 2) The rock is dark greyish yellow, cryptocrystalline, fine grained, highly argillaceous, fossiliferous with planktonic species and undifferentiated organic remains. This biomicrite occurs in the Thebes Formation, represented by samples H/GH and I/GH at Gebei Gurnah and sample no. O/D at Gebei Duwi. Such a type of facies reflects an outer neritic environment where no coarser terrigenous material is accumulated. fí) PALEOECOLOGY This study aims to throw more light on the conditions under which Sedimentation took place. The included fossil organisms are good indicators fór their adaptation to conditions that prevailed during their life (H ecker 1965). Since this study is based on two wide spaced Stratigraphie sections, it is preferred to treat each of them separately. Through comparison of these sections, the whole sequence is elucidated. The Duwi section embraces the Stratigraphie interval between the Upper Cretaceous and the Lower Eocéné. The Gurnah section includes the Stratigraphie interval represented by the Lower Eocéné only. Upper Cretaceous: It is composed of multicolored shales, unfossiliferous, slightly to moderatelv sandy and phosphatic in part. These lithological characters indicate deposition in a relatively shallow and stagnant water under toxic bottom conditions during the Campanian time. Shortlv after the outset of the Maestrichtian in Duwi district, further shallowing took place resulting in a lacustrine environment. This was stronglv affected by waves and undertow on a beach and participated in the accumulation of phosphatic remains. Shallowing of the basin continued, and the phosphatic beds were deposited. Next to this, inundation took place and outer neritic conditions prevailed resulting in the formation of fine grained calcareous deposits rich in planktonic elements without contribution of coarse grained material. Paleocene: By the advent of Early Tertiarv in Duwi district, rapid shallowing took place and a slight break is observed. This faunal break between the Upper Cretaceous (Maestrichtian) and the Lowermost Tertiarv (Dánián) is not accompanied by any facies change. Open marine facies dominated in both ages. This is probably attributed to sudden uplift followed by a short period of erosion and abrupt inundation which led to open marine facies in both Maestrichtian and Dánián sediments. Similar sequence of facies, irrespective of aging, was recorded in Ezz El-Orbán area (Bar a k a t and F ah m y 1968).

Két dél-egyiptomi szelvény mikrofácies-vizsg. 3 9 9 The Dánián sediments are characterized by abundant planktonic elements, particularly Globigerinas and round-keeled Globorotalias. This type of outer neritic facies dominated also in the Upper Paleocene (Landenian) with the sharp-keeled Globorotalias embedded in a fine argillaeeous groundmass. Intertonguing of médium grained carbonates were met with, howevérit was found unfossiliferous. Open marine facies persisted throughout the Paleo, cene characterizing the continuously subsiding basin during this epoch. Loiver Eocéné: The Lower Eocéné of both Duwi section in the east and Gurnah outcrop in the west is represented by open marine facies with planktonic fauna, few benthonics and undifferentiated organic remains. This type of facies dominated the vast region extending between the Red Sea and the Nile Basin and probably farther to the west during this lapse of time. Conclusions Through the analyses of microlitho- and microbiofacies assemblages, it was possible to recognize the depositional environments in the different formations. The Upper Cretaceous succession of Duwi Range was accumulafcecj under variable conditions. It commenced with multicoloted shales of shallow and stagnant or toxic bottom conditions. This is followed by lacustrine environment whereby phosphatic remains settled down building up the Duwi Phosphates. Next to this phase, deepening took place and resulted in the formation of fine grained calcareous deposits. The Lower Tertiary of Duwi started with a slight break whereby no change in facies is observed. The Lower Eocéné of both Gebei Duwi and Gebei Gurnah was deposited in an outer neritic environment whereby planktonic elements predominate. This environment is synchronous with the Alveolinid Faraira Limestone Formation representing a reefal facies. ACKNOWLEDGEMENTS: The authors wish to express their gratitude to the authorities of the General Petroleum Company, Egypt fór the facilities offered in the field during the excursion of the Soviet Project 1500. Thanks are also due to Prof. D r. I. M. F a r a g, head of Geology Department, Faculty of Science, Riyadh University/Saudi Arabia fór his enthusiasm, continuous encouragement and valuable leading comments, as well as to D r. J. K o n d a, Director, Geological Survey of Hungary, fór his kindness shown in Publishing this paper.

4 0 0 M. G. В ARAKAT A. S E l-daw oody REFERENCES A b d A l - R a z i k, T. M. 1968: Stratigraphy of the sedimentary cover of Anz-Atshan- South Duwi district. Bull. Fac. Sc., Univ. Cairo, 41:153 179. A w a d, G. H. and G h o b r i a l, M. G. 1966: Zonal stratigraphy of the Kharga Oasis. U.A.R. Geol., Surv., Min. Res. Dept., Cairo, Pap. 34:77 pp. B a r a k a t, M. G. and F a h m y, S. E. 1968: Basinal evolution of Ezz El-Orban area during the Paleogene time. Bull. Fac. Sc., Univ. Cairo, 42:325 339, 5 pls. B a r a k a t, M. G. and T e w f i k, N. M. 1966: Microfaeies of the Upper Cretaceous and older Sediments in Ezz El-Orban exploration well No. 1. J. Geol. U.A.R. Cairo, 10:25-35, 6 pls. B e a d n e l l, H. J. L. 1905: The relations of the Eocéné and Cretaceous Systems in the Esna-Aswan Reach of the Nile Valley. Quart. J. Geol. Soc. London, 61:667 678, fig. 1, 2. B l a n c k e n h o r n, M. 1900: Neues zur Geologie und Palaeontologie Aegyptens. I. Das Carbon und Kreide (Cenoman, Túron und Senon). Z. Deutsch. Geol. Ges., Berlin, 12:21-47. C i t a, M. B. 1965: Jurassic, Cretaceous and Tertiary microfaeies from the Southern Alps. Internat. Sed. Petr. Ser. 8, Leiden. C u v i l l i e r, J. and S a c a l, V. 1951: Correlations stratigraphique par microfaeies en Aquitaine Occidentale. 23. pp., 90 pls. Brill, Leiden. E l -D a w o o d y, A. S. A. 1970: Stratigraphical and paleontological studies on some Cretaceous and Lower Tertiary Sediments in Egypt. Ph. D. Thesis, Univ. Cairo, 559 pp., 70 pls. E l -N a g g a r, Z. R. 1966: Stratigraphy and planktonic Foraminifera of the Upper Cretaceous Lower Tertiary succession in the Esna-Idfu region, Nile Valley, Egypt, U.A.R. - Bull. Brit. Mus. (Nat, Hist.) London, 2:291 pp., 23 pls. F a r i s, M. I. 1947: The contact of the Cretaceous and Eocéné rocks in the Taramsa- Tukh area (Quena, Upper Egypt). Bull. Inst. Egypt., Le Caire, 28:73 85, pls. 1, 2. F a r i s, M. I. and H a s s a n, M. Y. 1959: Report on the stratigraphy and fauna of the Upper Cretaceous Paleocene rocks of Um El-Huetat, Safaga area. Ain Shams Sc. Bull., Cairo, 4:191-207, pls. 1, 2. F o l k, R. L. 1959: Praetical petrographic Classification of limestones. Bull. Amer. Assoc. Petrol. Geol., Tulsa/Oklahoma, 43:1 38. F o r d, A. and H o u b o l t, J. 1963: The microfaeies of the Cretaceous of Western Venezuela. Internat. Sed. Petr. Ser., Leiden 6:1 55. G h o r a b, M. A. 1956: A summary of a proposed rock Stratigraphie Classification of the Upper Cretaceous rocks in Egypt. Read before the Geological Society of Egypt, Cairo, June 12, 1956. G h o r a b, M. A. 1961: Abnormal Stratigraphie features in Ras Gharib oilfield. 3rd Arab. Petrol. Congr., Alexandria: 10 pp. G h o r a b, M. A. and I s m a i l, M. M. 1957: A microfaeies study of the Eocéné and Pliocene east of Helwan. Egypt. J. Geol., Cairo, 1:105 124. H a g n, H. 1955: Fazies und Mikrofauna der Gesteine der Bayerischen Alpen. Internat. Sed. Petr. Ser., Leiden, 1:1 174. H a n z a w a, S. 1961: Facies and micro-organisms of the Paleozoic, Mesozoic and Cenozoic Sediments of Japan and her adjacent island. Internat. Sed. Petr. Ser. 5, Leiden. H e c k e r, R. F. 1965: Introduction to paleoecology. 163 pp., 17 pls. Elsevier, New York. H e n s o n, F. R. S. 1938: Stratigraphical correlation by small Foraminifera in Palestine and adjoining countries. Geol. Mag., London, 75:227 233. H u m e, W. F. 191 l : The effects of secular oseillation in Egypt during the Cretaceous and Eocéné periods. Quart. J. Geol. Soc., London, 67:118 148, pl. 6. I s m a i l, M. M. and A b d E l - R a z i k, T. M. 1969: Stratigraphical microfaeies studies in Gebei Anz area, near Quseir (Eastern Desert, U.A.R.). Bull. Fac. Sc., Univ. Alexandria, 9:365 381, 12 figs.

K ét dél-egyiptomi szelvény mikrofácies-vizsg. 4 0 1 I s m a i l, M. M. and S e l i m, A. A. 1967: A microfacies study of the Cretaceous and Eocéné strata of Gebei Ataqa scarps, Eastern Desert, U.A.R. Ibid., 8:235 257, 15 figs. K e r d a n y, M. T. 1969: Paleontology and regional correlation studies on the Upper Oretaceous and Lower Tertiary rocks of Middle Egypt. Ph. D. Thesis, Ain Shams Univ., Cairo, 177 pp., 18 pls. K r a s h e n i n n i k o v, V. A. and A b d E l - R a z i k, T. M. 1969: Zonal stratigraphy of the Paleocene in Qusseir Red Sea Coast. Proc. 3rd Afr. Micropaleont. Colloq., Cairo, 1968:299-309. K r a s h e n i n n i k o v, V. A. and P o n i k a r o v, V. P. 1964: Stratigraphy of Mesozoic and Cainozoic Sediments in Egypt. Sov. Geol., Moscow, 2:42 71. M i s i k, M. 1966: Microfacies of the Mesozoic and Tertiary limestones of the West Carpathians. Slov. Akad. Vied., Bratislava, 1966:269 pp., 101 pls. N a k k a d y, S. E. 1949: The foraminiferal fauna of the Esna Shales of Egypt. I. Bull. Inst. Egypt., Le Caire, 31:209 247. N a k k a d y, S. E. 1950: A new foraminiferal fauna from the Esna Shales and Upper Cretaceous Chalk of Egypt. J. Paleont., Tulsa/Oklahoma, 24:675 892, pls. 89, 90. N a k k a d y, S. E. 1951: Stratigraphical study of the Mahamid district. Bull. Fac. Se., Univ. Alexandria, 1:17 43. R ey, M. and Notjet, G. 1958: Microfacies de la région Prérifaine et de la Moyenne Moulouya (Maroc Septentrional). Internat. Séd. Petr. Ser., Leiden, 3:1 41, 96 pls. R u s s e g g e r, J. R. 1837: Kreide und Sandstein: Einfluss von Granit auf letzteren. N. Jb. Min., 1837:665-669. S a i d, R. 1960: Planktonic Foraminifera from the Thebes Formation, Luxor, Egypt. Micropaleont., New York, 6:277 286, pl. 1. Sa i d, R. 1961: Tectonic framework of Egypt and its influence on distribution of Foraminifera. Bull. Amer. Assoc. Petrol. Geol., Tulsa/Oklahoma, 45:198 218. S a i d, R. 1962: The Geology of Egypt. XV+377 pp., 10 pls. Elsevier. Amsterdam, London, New York. S a i d, R. and K e r d a n y, M. T. 1961: The geology and micropaleontology of Faraira Oasis, Egypt. Micropaleont., New York, 7:317 336, pls. 1, 2. S a i d, R. and S a b r y, H. 1964: Planktonic Foraminifera from the type locality of the Esna Shale in Egypt. Ibid., 10:375 395, pls. 1 3. Y o u s s e f, M. I. 1957: Upper Cretaceous rocks in Kosseir area. Bull. Inst. Desert Egypte, Cairo, 7:35 54. Z i t t e l, К. A. 1883: Beiträge zur Geologie und Palaeontologie der Libyschen Wüste und der angrenzenden Gebiete von Aegypten. Palaeontographica, Stuttgart, 30:112 pp. 26 MÁFI évi jelentés 1973.

4 0 2 M. G. B arakat A. S. E i -Daw oody Plate I I. Tábla 1. Variegated shale: very fine grained, slightlv arenaceous, with ferruginous streaks and irregulär patches, unfossiliferous. X 60 Environment: inner neritic, with relatively shallow w^ater conditions not far from a nearby land-mass. Campanian, Gebei Duwd, sample no. 100 2. Sandy shale: highly siliceous, sand grains being angular to subrounded, with somé phosphatic grains, unfossiliferous. X 60 Environment: shallow marine, where phosphatic materials have been accumulated. Campanian Maestrichtian, Gebei Duwi, sample no. 3 * * * 1. Tarka pala: nagyon finom szemcséjű, gyengén homokos; vasas erekkel és szabálytalan vasas foltokkal; ősmaradványmentes. 60X Környezet: belső neritikus, viszonylag sekély vízi, partközeli. 2. Homokos pala: erősen kovás; homokszemcséi szögletesek, ill. gyengén koptatottak, néhány foszfátszemcsével; ősmaradvány mentes. 60 X Környezet: sekélytengeri; foszfátos anyagok felhalmozódásához kedvező.

2o* Két dél-egyiptomi szelvény mikrojácies-vizsq. 4 0 3

404 M. G. Barakat A. S. E l-daw oody Plate II - II. Tábla 1. Fossiliferous micrite: very fine grained, exhibiting more or less regulär fine bands, with undifferentiated organic remains together with some phosphatic (?) grains arranged nearly parallel to the direction of lamination. X 100 Environment: neritic, with calm conditions of Sedimentation. Campanian Maestrichtian, Gebei Duwi, sample по. 3a 2. Phosphatic biosparite: medium grained, fossiliferous mainly composed of phosphatic remains in the form of plates, granules and rounded bodies embedded in a sparry calcite mátrix. X 30 Environment: inner neritic, affected by high level of energy caused by waves. Campanian Maestrichtian, Gebei Duwi, sample no. 3b * * * 1. Ősmaradványos mikrit: nagyon finom szemcséjű, többé-kevésbé szabályos finom sávozottsággal, meghatározhatatlan szerves maradványokkal és foszfát-(?) szemcsékkel, amelyek a lemezesség irányával közel párhuzamos elrendeződésűek. 100X Környezet: neritikus; nyugodt üledékképződési viszonyokkal. 2. Foszfátos biopát: közepes szemcséjű, ősmaradványos, főleg foszfátos maradványokból áll, melyek lemezek, szemcsék és gömbölyded testek alakjában pátos kalcit alapanyagba ágyazódnak. 30 X Környezet: belső neritikus; a nagy energiaszintű hullámverés hatókörében.

Két dél-egyiptomi szelvény mikrofácies-vizsg. 4 0 5 2

4 0 6 M. G. B arakat A. S. E l-d aw oody Plate III - III. Tábla 1. Phosphatic biomicrite: fine grained, highly fossiliferous, with benthonic foraminifers mainly represented by rotalid forms, together with well preserved phosphatic remains such as vertebrae and ribs. X 30 Environment: mixed environment in which marine transgression gently overlapped the phosphatic bioherms. Maestrichtian, Gebei Duwi, sample no. 27/D 2. Heterohelix biomicrite: fine grained, highly fossiliferous, with abundant planktonic foraminifers represented by Heterohelix spp., Globotruncana spp., Globigerinas and Globorotalias, loosely packed in a carbonate mátrix. X 100 Environment: outher neritic, no coarser terrigenous material accumulated. Maestrichtian, Gebei Duwi, sample no. 25/D * * * 1. Foszfátos biomikrit: finomszemcséjű, ősmaradvány dús, bentosz Foraminiferákkal (főleg Rotalida alakok), valamint jó megtartású, foszfát anyagú maradványokkal (csigolyák és bordák). 30 X Környezet: vegyes környezet, melyben a tenger transzgressziója kissé túlterjedt a foszfátos bio hermákon. 2. Heterohelixes biomikrit: finomszemcséjű, ősmarad vány dús, sok plankton Foraminiferával, melyek Heterohelix spp., Globotruncana spp., Globigerina és Globorotalia maradványokból állnak és lazán, karbonátos alapanyagba ágyazódnak. 100 X Kö r n у e z e t : külső neritikus; durvább terrigén anyag felhalmozódásától mentes.

Két dél-egyiptomi szelvény mikrofácies-vizsg. 4 0 7 2

408 M. G. В arakat A. S. E l-d aw oody Plate IV - IV. Tábla 1. GloborotaUa biomicrite (A): fine grained, highly fossiliferous, with abundant planktonic foraminifers particularly round-keeled Globorotalias, together with Globigerina spp. Benthonic foraminifers are common. X 100 Environment: deep marine, of at least semi-pelagic character. Lower Paleocene (Dánián), Gebei Duwi, sample no. 21/D 2. Globorotalia biomicrite (В): fine grained, highly fossiliferous, with abundant planktonic foraminifers such as sharp-keeled Globorotalias together with round-keeled Globorotalias. Benthonic foraminifers are rare. X 100 Environment: outer neritic to bathyal. Upper Paleocene (Landenian), Gebei Duwi, sample no. 19/D ^ 1. Globorotalias biomikrit ( A ): finomszemcséjű, ősmaradvány dús, sok plankton Foraminifera maradvánnyal, elsősorban gömbölyded taréjú Globorotaliákkal Globigerina spp. társaságában. Általánosan elterjedtek a bentosz Foraminiferák. 100 X Környezet: mélytengeri, legalábbis hemipelágikus jellegű. 2. Globorotaliás biomikrit ( В): finomszemcséjű, ősmaradvány dús, sok plankton Foraminiferával, nevezetesen éles taréjú Globorotaliákkal és gömbölyded taréjú Globorotaliákkal. Bentosz Foraminifera ritka. 100 X K ö rn y e z e t: külső neritikustól batiálisig.

Két dél-egyiptomi szelvény mikrofácies-vizsg. 4 0 9 2

4 1 0 M. G. Barakat A. S. E l-daw oody Plate V - V. Tábla 1. Globorotalia biomicrite (C): fine grained, highly fossiliferous, with abundant planktonic foraminifers particularly sharp-keeled Globorotalias. Bentonic foraminifers are rare. X 100 Environment: neritic, no coarser terrigenous material accumulated. Upper Paleocene (Landenian), Gebei Duwi, sample no. 13/D 2. Marly micrite: medium grained euhedral crystals of calcite, scattered allover a dense argillaceous mátrix, devoid of any organic remains. X 60 Environment: neritic, no terrigenous material accumulated. Upper Paleocene (Landenian), Gebei Duwi, sample no. 10/D * * * 1. Globorotalms biomikrit (C): finomszemcséjű, ősmaradvány dús, sok plankton Foraminiferával, elsősorban éles taréjú Globorotaliákkal. Bentosz Foraminifera ritka. 100 X Környezet: neritikus; durvább terrigén anyag felhalmozódásától mentes. 2. Márgás mikrit: közepes szemcséjű idiomorf kalcit kristályok tömött, agyagos, szerves maradványtól mentes alapanyagban hintve. 60 X Környezet: neritikus; terrigén anyagfelhalmozódás nélkül.

Két dél-egyiptomi szelvény milcrofácies-vizsg. 411 2

4 1 2 M. G. В arakat A. S. E l-daw oody Plate VI - VI. Tábla 1. Marly foraminiferal biomicrite: fine grained, highly fossiliferous, with abundant planktonic foraminifers together with some rotalid forms embedded in an iron-stained argillaceous mátrix. X 60 Environment: middle neritic, no coarser terrigenous material accumulated. Upper Paleocene (Landenian), Gebei Duwi, sample no. 9/D 2. Foraminiferal biomicrite: fine grained, highly argillaceous, fossiliferous, with planktonic foraminifers and undifft rentiated organic remains. Benthonic foraminifers common. X 60 Environment: outer neritic, no coarser terrigenous material accumulated. Lower Eocéné, Gebei Gurnah, sample no. I/Gh * * * 1. Márgás, foraminiferás biomikrit: finomszemcséjű, ősmaradványdús, sok plankton Foraminiferával néhány Rotalida alak társaságában, amelyek vasas festésű agyagos alapanyagba ágyazódnak. 60 X Kö r n у e z e t : közép-neritikus; durvább terrigén anyagfelhalmozódástól mentes. 2. Foraminiferás biomikrit: finomszemcséjű, erősen agyagos, ősmaradványos; plankton Foraminiferákkal és meghatározhatatlan szerves maradványokkal. Általánosan elterjedtek a bentosz Foraminiferák. 60 X Környezet: külső neritikus; durvább terrigén anyagfelhalmozódástól mentes.

Két dél-egyiptomi szelvény mikrofácies-vizsg. 4 1 3 2

4 1 4 M. G. В ARAKAT А. S. E l-d aw oody KÉT DÉL-EGYIPTOMI FELSŐKRÉTA-PALEOCÉN-ALSÓEOCÉN SZELVÉNY (DUWI ÉS GURNAH) ÜLEDÉKEINEK MIKROFÁCIES-VIZSGÁLATA írta: B a r a k a t, M. G. és E l - D a w o o d y, A. S. Kairói Egyetem, TTK, Földtani Tanszék, Giza, Egyiptom A szerzők által vizsgált két szelvény földrajzi helye az 1. ábrán, rétegoszlopa pedig az I. mellékleten látható. Összesen hat kőzetrétegtani egységet különböztetnek meg. Ezek (alulról felfelé) a következők: 1. a Quseir-i Tarka Pala és Núbiai Homokkő (kampani, részben idősebb?) 2. a Duwi-i Foszfát-Formáció (kampani maastrichti) 3. a Dakhla-i Pala-Formáció (maastrichti paleocén) 4. a Tarawan-i Kréta-Formáció (felsőpaleocén) 5. az Esna-i Pala-Formáció (felsőpaleocén alsóeocén) 6. a Tébai Formáció (alsóeocén) a) tébai meszes pala rétegtagozat b) tébai mészkő rétegtagozat. Ezek vastagságát az 1. táblázat tünteti fel. Mikroszkópos vizsgálattal, a kőzettani és őslénytani jellegek tekintetbevételével, 12 mikrofácies volt megkülönböztethető; ezek leírását a szöveg tartalmazza, fényképei pedig az I VI. táblákon találhatók. A Duwi-hegyvonulat felsőkréta képződményei változó üledékképződési viszonyok között rakódtak le. A Tarka Pala sekély, stagnáló vagy toxikus vízben képződött. Ezt követően a Foszfát-Formáció tavi környezetben rakódott le. Majd mélyülés, neritikus meszes palás plankton-foraminiferás üledékképződés következett. A kréta paleocén határon gyors és rövid kiemelkedés volt, amely után az üledékképződés ugyancsak nyílt neritikus fáciesben folytatódott végig a paleocén és az alsóeocén folyamán, az utóbbiban már a Gurnah-i területen is. I. Melléklet. A Duwi-i és a Gurnah-i szelvény összevont rétegoszlopa. Szerkesztette B a r a k a t, M. G. E l - D a w o o d y, A. S. 1. Mészkő, 2. krétás mészkő, 3. kréta, 4. márgás mészkő, 5. márga, 6. meszes pala, 7. pala, S. foszfát, 9. tarka pala, 10. homokkő.