Calcareous Nannoplankton Biostratigraphy of the Lower and Middle Miocene of the Gulf of Suez, Egypt.

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1 Australian Journal of Basic and Applied Sciences, 3(3): , 2009 ISSN Calcareous Nannoplankton Biostratigraphy of the Lower and Middle Miocene of the Gulf of Suez, Egypt. Medhat M.M. Mandur Egyptian Petroleum Research Institute, Nasser City 11727, Cairo, Egypt. Abstract: The lower and Middle Miocene successions of the Gulf of Suez (Gs well, Gs A well and Gs well) comprise four formations.these formations are Nukhul, Rudeis, Kareem and Belayim. The biostratigraphic zonation of the studied successions is based on the calcareous nannoplankton assemblages. The examination of the studied samples has led to the identification of forty four calcareous nannoplankton species belonging to twelve genera. The calcareous nannoplankton content is used to subdivide the studied succession into six calcareous nannoplankton biozones. The correlation of these biozones with those known from the Gulf of Suez region and from other parts of the world confirms that the present zonation has strong relationships with those recognized in the Mediterranean region. The Lower / Middle Miocene boundary is defined and discussed. It is placed at the Helicosphaera ampliaperta / Sphenolithus heteromrphus zonal boundary. Key words: Calcareous nannoplankton, Miocene, Biostratigraphy INTRODUCTION The present work deals with the lithostratigraphy and biostratigraphy of the Lower and Middle Miocene of the Gulf of Suez, Egypt. The work is based on the study of calcareous nannoplankton assemblages obtained from the Lower and Middle Miocene of three subsurface wells successions of Gulf of Suez. The stratigraphy of the Miocene rock in Egypt has been the focus of attention by many workers for along time. Among these works are Blankenhorn (1901), Barron &Hume (1902), Hume (1916), Macfadyen (1930), Brouwer (1940), Heybrok (1949), Said &Bassiouni (1958), Said (1962&1990), Ansary & Andrawis (1965), Ghorab & Marzouk (1967), El Heiny & Martini (1981), Arafa (1982, 1991), Evans & Maxon (1986), Evans (1988), Haggag et al., (1990), Darwish & El Azabi (1993), Eweda & Zalat (1996), Sadek (2001), Mahran et al (2002), El deeb et al (2004), El Ashwah & Mandur (2006), Michal et al (2008), Helenes, J. et al (2009) and Michael streng et al (2009). MATERIALS AND METHODS The material of the present work includes 95 ditch samples obtained from Gs well, which is located at latitude 28 57' N and Longitude 32 57' E, 79 ditch samples obtained from Gs A well, which is located at Latitude 28 50' N and Longitude 33 6' E and 98 ditch samples obtained from Gs well, which is located at Latitude 28 45' N and Longitude 33 11' E fig. (1). The calcareous nannoplankton fauna, separated from the studied samples, are identified by using an Olympus polarized microscope with x100 oil immersion lens. RESULTS AND DISCUSSION Lithostratigraphy: The Miocene sedimentary rocks of Egypt are economically important; it represents the main oil province in Egypt. Also some commercial deposits such as gypsum, sulphur and claystone are present and extracted from the Miocene rocks. The lithostratigraphy of the Gulf of Suez was the subjected of several studies, the most important of which are: Moon &Sadek (1923), EG.P.C (1964), Ghorab &Marzouk (1967), N.C.G.S( 1974), Garfunkel & Bartov Corresponding Author: Medhat M.M. Mandur, Egyptian Petroleum Research Institute, Nasser City 11727, Cairo, Egypt. Medhatmandur@yahoo.com 2290

2 Fig. 1: Location map of the studied succession. (1977), Hosny et al (1986), Evans (1988), Hamza (1992), El Heiny & Morsi (1992), El- Azabi (1997 and Refaat (2002) According to Issawi et al (1999) the succession of the studied sections is subdivided into four rock units (figs.2, 3, 4), these are arranged chronologically, from base to top, as follows: 1- Nukhul Formation: In the present work at Gs well, the Nukhul Formation is recorded with thickness of about 124 feet Lithologicaly it is composed of sandy shale, argillaceous limestone and shale. At Gs A well, thickness of Nukhul Formation is about 120 feet. This Formation consists of calcareous shale and argillaceous limestone. The Nukhul Formation sediments of the studied successions are characterized by moderate calcareous nannoplankton content. It is unconformably underlain by the Lower Eocene rocks, Issawi et al (1999) and conformably overlain by the Rudeis Formation. The age of this Formation is Early Miocene (Aquitanian). 2-Rudeis Formation: The average thickness of this Formation, in the studied succession is 609 feet 1170 feet, and 1268 feet of Gs well, Gs well, Gs196 1-A well and Gs well respectively.this Formation in the present work conformably overlies the Nukhul Formation and conformably underlies the Kareem Formation. The Rudeis Formation sediments are characterized by a very rich content of calcareous nannoplankton. This Formation is assigned to the Early Miocene (Burdigalian). Lithologically the Rudeis Formation is subdivided into three members. These members are, from base to top, as follow: A- Mhieherrate /Hawara member: it is composed of shale, argillaceous limestone and calcareous sandy marl at Gs well. Where it is about 380 feet thick. At A well successions the Mhieherrate / Hawara member is about 1170 feet thick. Lithologically it is composed of shale, sandstone and argillaceous limestone. 2291

3 Fig. 2: Generalized Lithostratigraphy and biochronology of the early and Middle miocene at Gs well Succession. 2292

4 Fig. 3: Generalized Lithostratigraphy and biochronology of the early and miocene at Gs well Succession. 2293

5 Fig. 4: Generalized Lithostratigraphy and biochronology of the early and Middle miocene at Gs well Succession. 2294

6 At Gs well succession the Mhieherrate / Hawara member is composed generally of shale and argillaceous limestone, where it is about 928 feet thick. B- Asl Member: it is composed of calcareous shale with thickness of 100 feet at Gs well and at Gs well is composed of marl, Limestone and shale with thickness of 190 feet. C- Mreir member: it is composed of dark grey shale with hard thin bands of marl. Its thickness of Gs and Gs are 129 feet and 150 feet respectively. 3-Kareem Formation: The average thickness of this Formation, in the studied succession is 775 feet and 660 feet of Gs and Gs respectively. This Formation is subdivided into two members. The lower one is called Rahmi member which consists of sandstone, gypsum and shale, with average thickness 371 feet of Gs well and 560 feet thickness of Gs well which consists of shale, limestone and gypsum. The upper one is the Shagar member which is composed of limestone and shale of Gs with average thickness of 404 feet. At Gs 216-1, the Shagar member consists of sandy limestone with average thickness of 100 feet. The Kareem formation yielded a considerable content of calcareous nannoplankton associations. It is conformably overlies the Rudeis Formation and conformably underlies the Belayim Formation. The age of this Formation is Middle Miocene (Langhian Early serravallian). 4-Belayim Formation: The Belayim Formation represents the beginning of the main Miocene evaporates cycle Ghorab et al (1964).The Belayim Formation conformably underlies south Gharib Formation and conformably overlies Kareem Formation, Issawi et al (1999). It is assigned to Middle Miocene (serravallian) age. In the studied succession it attains 366 feet. It is subdivided into three members they are as follow from base to top: Baba member (gypsum), Sidri member (hard limestone) and Feiran member (gypsum). Biostratigraphy: Calcareous nannoplankton is an important component of the phytoplankton in the marine realm and has been one of the main open ocean primary producers since Triassic. It was probably an even more important phytoplankton group than today because diatoms only become abundant as late as the campanian (Burnett et al 2000, Mitlehner 2000 and Herrle 2003). The examination of the Miocene successions has led to the identification of 44 calcareous nannoplankton species belonging to 12 genera. The stratigraphic range of the identified species is given in figs. (5, 6, 7). Some selected representative index calcareous nannoplankton species are illustrated in plates (1). The biozonation used in this work based on the standard calcareous nannoplankton zonation of Martini (1971). According to the stratigraphic ranges of the identified calcareous nannoplankton species from the succession under investigation six calcareous nannoplankton zones are established here, from base to top as follows: 1- Triquetrorhabdulus Carinatus Zone (NN1): According to Bramlette & wilcoxon (1967) emended by Matini &Worsley (1970). This zone is defined from the last occurrence of Helicosphaera recta and /or Sphenolithus ciperoensis to the first occurrence of Discoaster drugii. This zone is recorded from the lower part of the Nukhul Formation at Gs well and Gs196-1A well with thickness of about 100 feet and 80 feet, respectively, see figs. (5, 6 ). In the present study the upper boundary of this zone is defined by the last occurrence of Discoaster calculosus and the first occurrence of Discoaster drugii. It is characterized by the following calcareous nannoplankton species : Discoaster calculosus, Reticulofenestra lockeri, Cyclicargolithus abisectus, Sphenolithus moriforms, Discoaster deflandrei, Cyclicargolithus floridanus and Helicosphaera euphratis, see figs. (5, 6 ) This zone is assigned to the Early Miocene (Early Aquitanian). In Egypt it is equivalent to that of Arafa (1991) and El deeb et al (2004). 2-Discoaster drugii Zone (NN2): This zone was originally established by Martini& Worsley (1970), as the interval from the first occurrence of Discoaster drugii to the last occurrence of Triquetrorhabdulus carinatus. In the present work the Discoaster drugii zone is recorded from the uppermost 24 feet of Nukhul Formation and lowermost 130 feet of Rudeis Formation of Gs well and also recorded from the uppermost 40 feet of Nukhul Formation and 2295

7 Fig. 5: Stratigraphic range chart of the calcareous nannoplankton species recognized in Gs well succession. lowermost 150 feet of Rudeis Formation of Gs A well. In the studied successions this zone is defined as the interval from the first occurrence of the Discoaster drugii to the first occurrence of Sphenolithus belemnos, see figs (5, 6). The Discoaster drugii zone is characterized by the following calcareous nannoplankton assemblages: Discoaster deflandrei, Sphenolithus moriforms, Helicosphaera granulata, Helicosphaera euphratis, Helicosphaera intermedia, Helicosphaera kamptneri, Helicosphaera ampliaperta, Helicosphaera scissura, Sphenolithus conicus, Sphenolithus compactus, Cyclicargolithus floridanus, Braarudosphaera bigelowii, Discoasater drugii and Discoaster adamanteus see figs. (5, 6). According to this calcareous nannoplankton association this zone was assigned to the Early Miocene age (Late Aquitanian to the beginning of Burdigalian). In Egypt this zone is equivalent to that of Arafa (1991) and Marzouk (1998). 2296

8 Fig. 6: Stratigraphic range chart of the calcareous nannoplankton species recognized in Gs well succession. 2297

9 Fig. 7: Stratigraphic range chart of the calcareous nannoplankton species recognized in Gs well succession. 2298

10 Explanation of Plate (1) The calcareous nannoplankton species (All Figures X2350) 1Helicosphaera intermedia (Martini, 1965), Discoaster drugii Zone, Gs160-1 Well. 2 Helicosphaera kamptneri (Hay&Mohler in Hay et al., 1967), Helicosphaera Kamptneri Zone, Gs well. 3 Helicosphaera ampliaperta (Bramlette &wilcoxon, 1967), Sphenolithus Belemnos Zone, Gs Well. 4 Helicosphaera rhomba (Bukry, 1971), Sphenolithus heteromrphus Zone, Gs Well. 2299

11 5 Helicosphaera scissura (Miller, 1981), Helicosphaera ampliaperta Zone, Gs A. 6 Helicosphaera euphratis (Haq, 1966), Helicosphaera ampliaperta Zone, Gs A Well 7 Pontosphaera multipora (Kamptner, 1948, Roth, 1970), Sphenolithus Belemnos Zone, Gs160-1 Well. 8, 9 Sphenolithus heteromorphus (Deflandre, 1953), Sphenolithus heteromorphus Zone, Gs Well. 10 Sphenolithus moriformis(bramlette &wilcoxon, 1967), Discoaster drugii Zone, Gs A Well. 11, 12 Sphenolithus belemnos (Bramlette &Wilcoxon, 1967), Sphenolithus belemnos Zone, Gs160-1 Well. 13, 14 Cyclicargolithus floridanus (Roth&Hay inhay et al., 1967), Sphenolithus Heteromorphus Zone, Gs Well. 15 Reticulofenestra pesudoumbilica (Gartner, 1969), Discoaster exilis Zone, Gs160-1 Well. 16 Cyclicargolithus abisecutus (Wise, 1973), Helicosphaera ampliaperta Zone, Gs Well. 17 Braarudosphaera biglowii (Deflandre, 1947), Sphenolithus heteromrphus Zone, Gs Well. 18 Discoaster drugii (Bramlette &wilcoxon, 1967), Discoaster drugii Zone, Gs A Well. 19, 20 Discoaster formosus (Martini &Worsley, 1971), Sphenolithus heteromrphus Zone, Gs Well. 21 Discoaster calculosus (Bukry, 1971), Triquetrorhabdulus carinatus zone, Gs160-1 Well. 22 Discoaster exilis (Martini &Bramlette, 1963), Discoaster exilis Zone, Gs160-1 Well. 23 Discoaster deflandrei (Bramlette &Riedel, 1954), Sphenolithus Belemnos Zone, Gs A Well. 24 Discoaster variabilis (Martini &Bramlette, 1963), Helicosphaera ampliaperta Zone, Gs160-1 Well. 3-Sphenolithus belemnos Zone (NN3): This zone was introduced by Bramlette &Wilcoxon (1967), emended by Martini (1971).It is defined as the interval from the last occurrence of Triquetrorhabdulus carinatus to last occurrence of Sphenolithus belemnos. This zone is recorded from the Rudeis Formation at Gs (250 feet thick), Gs196 1-A (780 feet thick) and Gs (578 feet thick), see figs.(5, 6, 7).In the present study this zone was determined by the first and last occurrence of Sphenolithus belemnos, see fig.(5, 6, 7). The Sphenolithus belemnos zone is characterized by the same assemblage of the previous zone in addition to the following assemblage: Sphenolithus belemnos, Triquetrorhabdulus milowii, Discoaster aulakos, Micrantholithus vesper, Helicosphaera mediterranea, Reticulofenestra gartneri, Helicosphaera rhomba and Calcidiscus macintyrei, see figs.(5, 6, 7). According to very rich content of calcareous nannoplankton, this zone is assigned to Early Miocene (Early Burdigalian) age. In Egypt this zone is recorded by El Heiny &Martini (1981), Arafa (1991), Marzouk (1998), El deeb et al (2004) and El- Ashwah& Mandur(2006). 4-Helicosphaera ampliaperta Zone (NN4): It is defined as the interval of last occurrence of Sphenolithus belemnos to last occurrence of Helicosphaera ampliaperta.this zone was firstly introduced by Bramlette &Wilcoxon (1967).emend.Martini (1971).The upper part of the Rudeis Formation belongs to this zone with thickness of 229 feet, 240 feet and 690 feet of Gs 160-1, Gs A and Gs216-1 respectively.in the studied successions this zone is defined by the last occurrence of Sphenolithus belemnos to the last occurrence of Helicosphaera ampliaperta species, see figs. (5, 6, 7 ). The study of the calcareous nannoplankton content of the sediments of this zone prove that it has the richest one where it contents the same assemblage of the previous zone in addition to the following assemblage: Sphenolithus heteromorphus, Discoaster variabilis, Discoaster petaliformis, pyrocyclus inversus, Discoaster trinidadensis and Scyphosphaera aranta, see figs.(5, 6, 7). 2300

12 According to the very rich content this zone is assigned to Early Miocene (Late Burdigalian) age. In Egypt this zone is equated to that of El- Heiny & Martini (1981), Arafa (1982), Marzouk (1998), El deeb et al (2004) and El Ashwah &Mandur (2006). 5- Sphenolithus heteromorphus Zone (NN5): According to Bramlette &Wilcoxon (1967), this zone is defined from the Last occurrence Helicosphaera ampliaperta to Last occurrence of Sphenolithus heteromorphus. The Sphenolithus heteromorphus zone is recorded from the Kareem Formation at Gs (775 feet thick) and Gs (660 feet thick), see figs. (5, 7). In the investigated area this zone includes the interval from the Last occurrence of Helicosphaera ampliaperta to the Last occurrence of Sphenolithus heteromorphus, see figs (5, 7).The Sphenolithus heteromorphus zone is characterized by the presence of Discoaster deflandrei, Discoaster variabilis, Discoaster exilis, Helicosphaera californiana, Calcidiscus macintyrei, Triquetrorhabdulus rugosus, Sphenolithus heteromorphus, Discoaster formosus, Cyclicargolithus floridanus, Helicosphaera kamptneri, Discoaster signus, Discoaster moorei, Sphenolithus compactus, Discoaster aulakos, Helicosphaera rhomba, Helicosphaera perplexus, Braarudosphaera biglowii, Discoaster drugii, Helicosphaera mediterranea, Discoaster trinidadensis, Micrantholithus vesper, Discoaster musicus, Helicospaera burkei, Pyrocyclus hermosus, Sphenolithus moriformis and Sphenolithus conicus, see figs. (5, 7 ). It is assigned to the Middle Miocene (Langhian to the beginning of serravallian age). In Egypt this zone is equivalent to that of El Heiny & Martini (1981), El deeb et al (2004) and El Ashwah &Mandur (2006) 6-Discoaster exilis Zone (NN6): This zone was originally established by Hay (1970), emended by Martini (1974). It is defined from the Last occurrence of Sphenolithus heteromorphus to the First occurrence of Discoaster kugleri and/or Last occurrence of Cyclicargolithus floridanus. This is recorded in Belayim Formation at Gs well succession with 366 feet thick, see fig. (7). In the studied succession the Lower boundary of this zone is defined by the Last occurrence of the Sphenolithus heteromrphus species, see fig (7).The Discoaster exilis zone characterized by a poor association of calcareous nannoplankton assemblage: Discoaster deflandrei, Discoaster variables, Discoaster braarudii, Cyclicargolithus floridanus, Braarudosphaera biglowii, Discoaster drugii, Reticulofenestra pesudoumbilica, Discoaster trinidadensis and Discoaster exilis see fig. (7). The age of this zone is middle Miocene (serravallian).this zone is equated to that of El deeb et al (2004) and El- Ashwah & Mandur (2006). Early / Middle Miocene Boundary: In term of calcareous nannoplankton the Early /Middle Miocene boundary is given by different authors: Bramlette &wilcoxon (1967), Martini (1971), Muller (1978), Aubry (1993), Sadek (2001) and El deeb et al (2004) delineated the Early / Middle Miocene boundary coincides with the NN4/NN5 zonal boundary at the Last occurrence of Helicosphaera ampliaperta. Shimon&Aline (1980) and Marzouk (1998) placed the Early /Middle Miocene boundary at the top of the Helicosphaera ampliaperta (NN4) Zone. On the present study the Early /Middle Miocene boundary is determined accurately by means of calcareous nannoplankton at the level of the disappearance of Helicosphaera intermedia, Helicosphaera scissura, Pyrocyclus inversus, Helicosphaera euphratis, Helicosphaera ampliaperta, Sphenolithus moriformis, Triquetrorhabdulus milowii, Scyphosphaera aranta and Discoaster petaliformis and the appearance of the following species: Discoaster exilis, Helicosphaera californiana, Triquetrorhabdulus rugosus, Discoaster formosus, Discoaster signus, Discoaster moorei, Helicosphaera rhomba, Helicosphaera burkei, Calcidiscus macintyrei, Pyrocyclus hermosus and Discoaster musicus, see figs.(5, 7). So the Early /Middle Miocene boundary coincides with the Helicosphaera ampliaperta /Sphenolithus heteromorphus zonal boundary. Conclusions: The present study deals with the Lithostratigraphy and Biostratigraphy of the Lower and Middle Miocene successions in the Gulf of Suez area, Egypt. The material of this study consists of 272 samples which were collected from three wells: Gs 160-1, Gs A and Gs Lithostratigraphyically, the studied succession is divided into four formations from base to top as follows: Nukhul, Rudeis, Kareem and Belayim.The Miocene successions of the present study has been subdivided into six biostratigraphic zones, according to the stratigraphic range of the identified calcareous nannoplankton species (44 species belonging to 12 genera ). According to the study of the vertical distribution of the 2301

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