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tocEocene planktonic foraminifera from the north Eastern Desert, Egypt: Biostratigraphic, paleoenvironmental and sequence stratigraphy implications

Yasser Salama, Mostafa Sayed, Shaban Saber, and Ibrahim Abd El-Gaied

Article number: 24.1.a11
Copyright Palaeontological Association, March 2021

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Submission: 19 April 2020. Acceptance: 18 March 2021.


The Eocene succession at Beni Suef–El Zaafarana District in north Eastern Desert is rich in planktonic foraminiferal assemblages. The main objectives of this work are to use the planktonic foraminifera to recognize the biostratigraphy for the Middle-Upper Eocene succession in the study area. Seventy planktonic foraminiferal species belonging to 20 genera and seven families are identified from the Eocene El Fashn and Beni Suef formations. Three planktonic foraminiferal biozones are recognized. These are from older to younger Morozovelloides crassatus Zone (late Middle Eocene) that is recorded from El Fashn Formation, Globigerinatheka semiinvoluta Zone (latest Middle Eocene–Late Eocene) and Globigerinatheka index Zone (Late Eocene age) that are recorded from the Beni Suef Formation while the Maadi Formation is found barren in planktonic foraminifera. These zones are correlated with those from nearby areas in Egypt and the Mediterranean regions. The Middle/Upper Eocene (Bartonian/Priabonian) boundary is discussed here in detail. The percentage of the planktonic foraminifera in the total foraminiferal content (P %) points to a change in water depth. There was a significant decrease in the planktonic/benthic foraminiferal ratio from the late Middle Eocene El Fashn Formation to the Late Eocene Maadi Formation at Beni Suef–El Zaafarana District. This ratio change supports a shallowing upward in paleodepth. Based on the lithology, planktonic/benthic ratio and the obtained water depth, the studied Eocene succession could be subdivided into four depositional sequences. These sequences agree with the global eustatic sea-level and the depositional sequences in nearby areas.

Yasser Salama. Geology Department, Faculty of Science, Beni-Suef University, 65211, Egypt. (Corresponding author)
Mostafa Sayed. Geology Department, Faculty of Science, Beni-Suef University, 65211, Egypt.
Shaban Saber. Geology Department, Faculty of Science, Beni-Suef University, 65211, Egypt.
Ibrahim Abd El-Gaied. Geology Department, Faculty of Science, Beni-Suef University, 65211, Egypt.

Keywords: Foraminifera; Eocene; biostratigraphy; Egypt

Final citation: Salama, Yasser, Sayed, Mostafa, Saber, Shaban, and Abd El-Gaied, Ibrahim. 2021. Eocene planktonic foraminifera from the north Eastern Desert, Egypt: Biostratigraphic, paleoenvironmental and sequence stratigraphy implications. Palaeontologia Electronica, 24(1):a11.

Copyright: March 2021 Palaeontological Association.
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The Eocene Epoch witnessed the development of a carbonate platform covering a huge area of Egypt (Said, 1962; Saber and Salama, 2017; Abd El-Gaied et al., 2019). The foraminiferal contents of the Eocene platform were the target for many previous studies in the Nile Valley and the north Eastern Desert (Bassiouni et al., 1974, 1975; Kenawy et al., 1977; Haggag, 1986, 1989 b; Haggag and Anan, 1987; Haggag and Luterbacher, 1991; Haggag and Bolli, 1995, 1996; Hussein, 1994; Obaidalla and El-Ayyat, 2001; El-Dawy and Dakrory, 2005; Strougo et al., 2013; El Ayyat and Obaidalla, 2016; Abdel-Fattah, 2018). The planktonic foraminifera are a basic group of fossils in the biostratigraphy and depositional environment interpretation. The wide geographical distribution and high species diversity of the planktonic foraminiferal group enabled us to use this group in correlation with the Eocene rocks (BouDagher-Fadel, 2012). The occurrence of planktonic and benthic foraminifera is considered a valuable tool in the determination of the paleobathymetry and paleoecological changes. Their abundance and diversity are related to changes in oceanographic parameters such as temperature, salinity, organic flux, and sea level fluctuations (Leckie et al., 1998; Ernst and Van der Zwaan, 2004; Darabi et al., 2018). Planktonic foraminifera are rare or nearly absent in near shore environments and increase in abundance with increasing depth (van Hinsbergen et al., 2005). The planktonic/benthic foraminifera ratio (P/B) reflects changes in the environmental settings from inner to outer neritic environments (Murray, 2006; Pippèrr and Reichenbacher, 2010; Pippèrr, 2011).

The foraminiferal contents and biostratigraphy of the Middle-Upper Eocene successions are previously studied in the north Eastern Desert, at wadi Bayad El-Arab and Gebel Homret Shaibon (Abd El-Gaied and Abd El-Aziz, 2005; Aly et al. 2011); they identified only two planktonic foraminifera zones including Truncorotaloides (Acarinina) rohri and Turborotalia (ampliapertura) pseudoampliapertura zones, and two benthic foraminifera zones including Palmula ansaryi and Bulimina jacksonensis zones. However, this biostratigraphy result was poorly discussed and the studied sections are suitable to complement the biostratigraphic record of the Middle-Upper Eocene successions in the north Eastern Desert, particularly at the Beni Suef area.

The study area has not been subjected to sufficient studies because of the difficulty in reaching it, but with new asphaltic roads, researchers can easily access the Eocene successions along Beni Suef–El Zaafarana. Recently, Abd El-Gaied et al. (2019) studied in detail the benthic foraminiferal assemblages and paleoenvironment of the Middle-Late Eocene succession in this area. However, the micropaleontological studies of the Eocene sequence by means of planktonic foraminifera in the study area in the north Eastern Desert were not the subject of sufficient previous works. Therefore, the foremost purpose of this study is to develop the biostratigraphic frame of the middle-upper Eocene deposits in the east Beni Suef area, north Eastern Desert.

In this study we report stratigraphical and micropaleontological results for the Middle-Upper Eocene succession by using planktonic foraminifera data. The goals of this work are also to study the biostratigraphic zonation and to determine the paleobathemetry of the studied sequences. Although the Eocene sequence stratigraphy in Eocene successions of north Eastern Desert was subject to few studies, a sequence stratigraphic classification for the Middle-Upper Eocene succession in the studied area is attempted also here for the first time. Although the Eocene sequence stratigraphy of north Eastern Desert was previously studied by a few number of authors (Tawfik et al., 2016; Saber and Salama, 2017; Hussein, 2019), the present study highlight the planktonic foraminifera ratio and sea level changes from the perspective of sequence stratigraphy.


s figure1Three stratigraphic sections in the study area were analysed for planktonic foraminifera. These sections are located along the eastern side of the Nile River, the first section (A) is located at about 15 km east of Beni Suef city between latitude 28° 59′ N and longitude 31° 11′ E; the second (B) is located at about 20 km east of Beni Suef city between latitude 28° 57′ N and longitude 31° 13′ E, while the third section (C) is located at about 135 km west of El Zaafarana between latitude 28° 58′ N and longitude 31° 22′ E (Figure 1). The studied succession was differentiated into three rock units, arranged from base to top: the El Fashn Formation (late Middle Eocene), the Beni Suef Formation (late Middle Eocene-Late Eocene), and the Maadi Formation (Late Eocene) (Figure 2).s figure2 The El Fashn Formation was first described by Bishay (1966) at Wadi El Sheikh southeast of El Fashn City as a sequence of sandy and chalky limestone and sandy shales of 88 m thick. In the study area, the upper part of this formation is exposed and unconformably overlain by the Beni Suef Formation. It attains a thickness of about 35 m consisting of grayish white, hard and burrowed massive limestone, yellowish white marly limestone, and egg yellow marl intercalations (Figure 3).s figure3 This rock unit is highly fossiliferous with benthic and planktonic foraminifera, which are highly abundant in the marl beds and less abundant in the limestone and marly limestone beds. The planktonic foraminiferal assemblages suggest a late Middle Eocene (Bartonian) age for this rock unit.

The Beni Suef Formation was first described by Bishay (1966) to describe the succession exposed at Gebel Homret Shaibon overlying the El Fashn Formation and underlying the Maadi Formation. Mansour et al. (1982) subdivided this formation into the Qurn Member at the base and the Tarbul Member at the top. In the studied area, the Beni Suef Formation exposed at sections B and C and subdivided into two members. The lower Qurn Member which exposes at the lower part of section B, where it measures 54 m and is composed mainly of grayish yellow gypsiferous shale, silty shale, and light green marl. The upper Tarbul Member was recorded at the upper part of section B and measured 24 m (Figure 4).s figure4 It composes of yellowish gray hard marly limestone, greenish yellow shale, and yellowish white marl with a thin bed of hard egg yellow thalassinoid limestone capped by chalky and dolomitic limestone. This member includes the majority of section C, with a thickness of about 63 m. The basal part of the Tarbul Member (8 m thick) in section C consists of fossiliferous egg yellow marls and yellowish white marly limestone. The middle part is about 25 m thick and consists of egg yellow to yellowish white marl. The upper part of this member is 30 m thick and is composed of various colors of marl and fossiliferous limestone. The abundance and diversity of planktonic foraminiferal species in the lower part of the Beni Suef Formation are greater than those in the middle and upper parts. Based on the occurrence of both planktonic and benthic foraminifera, the Beni Suef Formation in the present work is assigned to a late Middle to Late Eocene age.

The Maadi Formation was first described by Said (1962, 1971) as part of the upper Mokattam of Zittel (1883). Its type locality is at east of the Maadi district with a thickness of about 70 m, composed of variegated and gypsiferous shale overlain by limestone, calcareous sandstone, and dolostone. In the study area, the lower part of the Maadi Formation is exposed in section C, with a thickness of about 14 m of shale and egg yellow sandy marls (Figure 5). The marl beds were highly fossiliferous containing large echinoids, gastropods, pelecypods (Carolia placunoides), Nummulites spp., and abundant corals. No planktonic foraminiferal species are found in this formation but it is enriched in large and small benthic foraminifera.


s figure5In order to achieve the aim of the present study, 97 rock samples were collected from the measured three sections at 50 cm to 2 m intervals. At least 250 gm was taken from each sample to extract the microfaunal contents. The samples were soaked in hydrogen peroxide solution. The samples were washed under running water and sieved using a 63 μm sieve. The residue was dried and separated into several fractions to facilitate the picking of different microfossils using a binocular microscope. The picked foraminiferal tests were identified to species-level and photographed by SEM (Scanning Electron Microscope, JSM 5400 LD at Assiut University). The planktonic and benthic foraminiferal species were counted in each sample to calculate the planktonic percentage in the total foraminiferal associations (P%). This percentage could be estimated by applying the following formula: P%= 100*(P/ (P +B–S). Where P is the number of planktonic foraminiferal species, B is the total number of benthic species and S is the number of infaunal benthic species (Bulimina, Bolivina, Lagena, etc.). Paleodepth is obtained by using the equation by van der Zwaan et al (1990):

Depth (m) = e3.58718 + (0.03534*P%)

Where e is the base of the natural logarithm (e = 2.718281825) and P% is the planktonic percentage.


s figure6The planktonic foraminiferal investigation of the studied successions resulted in the identification of seventy planktonic species belonging to seven families and 20 genera. The taxonomy of Pearson et al. (2006) and Pearson and Wade (2015) are followed in this study. The age and stratigraphic distribution of the recorded species were highlighted (Figure 3, Figure 4, Figure 5). The identified species have been examined and photographed using a Scanning Electron Microscope (SEM) and illustrated in Figure 6, Figure 7, and Figure 8. The type specimens of this work were housed in the Geological Department, Faculty of Science, Beni-Suef University. The identified planktonic foraminifera species are summarized in Table 1.


The stratigraphic distribution of the identified planktonic foraminiferal species allowed us to identify four planktonic foraminiferal zones for the upper Middle to Upper Eocene successions (Figure 2Figure 3, Figure 4, Figure 5). These zones were described and correlated with the international standard zones, and with those recorded in Egypt and the Tethyan province (Figure 9). The present zonation followed the most recent Cenozoic planktonic foraminifera scheme of Wade et al. (2011).

E 13. Morozovelloides crassatus Zone

s figure7Category. Highest-Occurrence Zone.

Definition. This zone was defined by Wade et al. (2011) as a highest-occurrence zone including the biostratigraphic interval between the highest occurrence (HO) of Orbulinoides beckmanni to the HO of Morozovelloides crassatus. In this work, the base of the present zone was not found because Orbulinoides beckmanni was absent and no other alternative species were found.

Age. late Middle Eocene (Bartonian).

Assemblages. The most characteristic species are Acarinina rohri, A. topilensis, A. libyaensis, A. matthewsae, A. spinuloinflata, A. bullbrooki, A. primitiva, A. collactea, A. pentacamerata, Igorina broedermanni, Morozovelloides crassatus, M. lehneri, Subbotina minima, Subbotina senni, S. utilisindex, Globorotaloides suteri, Turborotalia cf. ampliapertura, Turborotalia centralis, Globigerinita pera, Globoturborotalita euapertura, Guembelitria oveyi, and Globigerinatheka kugleri.

The most important benthic species recorded in this zone include assemblages of the genera Palmula (P. ansaryi, P. cushmani, P. suturalis, P. toulmin), Lenticulina, Pararotalia (P.audouini, P. spinigera), Anomalinoides (A. fayoumensis), Lagena, Cibicidoides (C. pharaonis, C. proprius), Uvigerina (U. peregrine, U. isidroensis, U. capayana, U. rippensis), Eponides (E. ellisorae, E. lotus) and Planulina (P. cocoaensis).

s figure8Remarks. This zone is occured in sections A and B of the El Fashn Formation (Figure 3) and characterized by high abundance of spinose planktonic foraminifera (Acarinina). In the tropical and subtropical areas, which are characterized by open marine conditions, the upper boundary of this zone marked the Middle / Late Eocene boundary. This boundary is marked by the disappearance of almost all spinose planktonic species (e.g. Morozovelloides and the large Acarinina spp.) (Toumarkine and Luterbacher, 1985; Haggag, 1990; Haggag and Luterbacher, 1991; Berggren and Pearson., 2005 and Wade et al., 2011). Berggren et al. (1995) marked overlap interval between the HO of Acarinina rohri and the LO of Globigerinatheka semiinvoluta, and they considered Globigerinatheka semiinvoluta is slightly older than the HO of Acarinina rohri (Abd El-Shafy et al., 2007). On the other hand, Berggren and Miller (1988) and Berggren et al. (1985) marked the top of Truncorotaloides rohri–Morozovella spinulosa Zones (P14) at the simultaneous extinction of Morozovella spinulosa and LO of Globigerinatheka semiinvoluta. Berggren and Pearson (2005) and Wade et al. (2011) noticed that Morozovelloides crassatus is the senior synonym of Morozovelloides spinulosa, so they defined Morozovelloides crassatus Zone (E13) from the HO of Orbulinoides beckmanni to the HO of Morozovelloides crassatus. In this work, the HO of Morozovelloides crassatus and most of the spinose forms (large Acarininids and Morozovelloides) are synchronous, so the present Zone is coincided with the E13 Zone of Berggren and Pearson (2005) and Wade et al. (2011). In Section A, the species Morozovelloides crassatus and the associated spinose forms are present throughout the section. However, these species and the associated assemblages disappeared after the unconformity between the El Fashn and Beni Suef formations in section B, so the exact location of the top of this zone E13 was not found (Figure 4).

Hantkenina assemblages, especially Hantkenina alabamensis and H. primitive, are usually recorded within this zone and extend to the overlying Late Eocene zones (Toumarkine and Luterbacher, 1985; Al-Hellou, 2000; Smadi, 2002 and others). In the present studied sections the Hantkenina assemblages are not recorded.

s figure9Correlation. This zone was recognized by many authors from the late Middle Eocene of Egypt and the Tehyan Province. Globally, it is correlated with Truncorotaloides (=Acarinina) rohri of Trinidad (Bolli, 1957b; Postuma, 1971), Italy (Bolli, 1972; Toumarkine and Bolli, 1975), Spain (Hillebrandt, 1974), United Arab Emirates (Anan et al., 1992), Israel (Benjamini, 1995), Libya (El-Khoudary, 1980), and Egypt (Bassiouni et al.,1974; Anan, 1979; Samir, 1986; Haggag, 1989b,1990; Selima, 1989; Haggag and Luterbacher, 1991; Abd El-Aziz, 2008; Strougo et al., 2013; Marzouk et al., 2014). It was also equaited with the P.14 Zone (Truncorotaloides rohri / Morozovella spinulosa zone of Berggren et al. (1995) and E.13 Zone (Morozovelloides crassatus zone of Berggren and Pearson (2005); Wade et al. (2011) (Figure 9).

E14. Globigerinatheka semiinvoluta Zone

Category. Highest-Occurrence Zone.

Definition. This zone was defined by Wade et al. (2011) as a highest-occurrence zone that defined by the biostratigraphic interval between the HO of the late Middle Eocene Morozovelloides crassatus to the HO of Globigerinatheka semiinvoluta.

Age. late Middle Eocene–Late Eocene (Bartonian–Priabonian).

Assemblages. The most characteristic assemblages recorded from this zone are Globigerinatheka semiinvoluta, Gk. rubriformis, Gk. tropicalis, Turborotalia cerroazulensis,T. pomeroli, T. cunialensis, T. cocoaensis,T. ampliapertura, Dentoglobigerina venezuelana, D. pseudovenezuelana, D. galavesi, D. tripartita, Chiloguembelina cubensis, Ch. ototara, Pseudohastegerina micra, P. naguawichiensis, P. danvillensis, Subbotina praeturritilina, S. corpulenta, S. eocaena, S. angiporoides, S. hagni, S. yaguaensis, S. tecta, S. linaperta, Parasubbotina inaequispira, Globigerinita africana, G. echinata, Globoturborotalita barbula, G. martini, G. praebulloides, G. occlusa, G. gnauki, Acarinina medizzai, Catapsydrax unicavus, C. howei, C. dissimilis, C. cryptomphala, Paragloborotalia opima, P. nana, Tenuitella angustiumbilicata, T.gemma. The most common benthic species recorded in this zone are assemblages of the genera Cancris (C. auriculus, C. danvillensis, C. subconicus), Baggina (B. bradyi), Laevidentalina (L. soluta), Textularia (T. fahmyi, T. recta), Paralabamina (P. lunata), Neoeponides (N. schreibersi), Pararotalia (P. audouini, P. spinigera), Reussella (R. terquemi), Elphidium, Saracenaria, Planulina, Anomalinoides (A. acutus), Cibicidoides (C. yankaulensis), Discorbis (D. bulla, D. vesicularis), and Rosalina (R. quadrata).

Remarks. The present zone occurs in Section B including the whole thickness of the Qurn Member of Beni Suef Formation and most of the Tarbul Member (samples 30-39). It occurs in Section C and represented by samples 1-34 of the Tarbul Member of Beni Suef Formation. It overlies the Morozovelloides crassatus zone and underlies the Globigerinatheka index zone. The lower boundary of the present zone is marked at the highest occurrence of the Morozovelloides crassatus and its associated spinose forms and located at the base of the Qurn Member. However, the upper boundary was traced at the last occurrence of Globigerinatheka semiinvoluta and the first appearance of Turborotalia cunialensis (Figure 2, Figure 5). Berggren et al. (1995) mentioned that the lowest occurrence of Turborotalia cunialensis defined the top of Globigerinatheka semiinvoluta zone (P 15 Zone) and the base of the planktonic P 16 Zone. The Globigerinatheka semiinvoluta zone occurs above the Turborotalia pseudoampliapertura zone in the Upper Eocene rocks of the Fayum province in Egypt (Haggag 1990, 1992). In western Sinai, Abd El-Shafy et al. (2007) recorded this zone from the Upper Eocene succession at Wadi Bagha. Strougo et al. (2013) and Marzouk et al. (2014) defined the Globigerinatheka semiinvoluta Subzone (P15b) from the Upper Eocene of the Fayum province.

Toumarkine and Luterbacher (1985), Berggren and Miller (1988), and Berggren et al. (1995) reported that the Globigerinatheka semiinvoluta appeared at younger levels than the extinction of the spinose forams. On the other hand, Pearson and Chiasson (1997), Norris et al. (1997), Wade (2004), Berggren and Pearson (2005), and Wade et al. (2011) reported that the LO of Globigerinatheka semiinvoluta is younger than that was previously recorded by Berggren et al. (1995), where the LO of Gk. semiinvoluta was older than the HO of Morozovelloides crassatus. In the tropical and subtropical areas, the present zone is distinguished by the Globigerinatheka semiinvoluta and the advanced forms of Turborotalia cerroazulensis lineage, such as Turborotalia cocoaensis, Turborotalia cerroazulensis together with Turborotalia pomeroli, Globigerinatheka tropicalis, Hantkenina alabamensis, H. primitiva, and numerous large species of Subbotina and Globigerina. On the other hand, in temperate areas, Globigerinatheka luterbacheri and Globigerinatheka index are abundant, and the zonal marker may be absent (Toumarkine and Luterbacher, 1985).

Correlation. Globally, the age of the Globigerinatheka semiinvoluta zone is late Eocene (Bolli, 1957b; Hillerbandt, 1974; Stainforth et al., 1975; Toumarkine and Luterbacher, 1985; Berggren and Miller, 1988). Moreover, Berggren et al., (1995); Berggren and Pearson (2005); Wade et al., 2011, and Karoui-Yaakoubi (2017) assigned a late Bartonian–Early Priabonian age to this zone. This zone was recorded from northeast Libya (Imam, 1999) and Egypt (Bassiouni et al., 1974; Abddel-kireem, 1985; Haggag, 1989a; Haggag and Bolli, 1996; Abul-Nasr, 1993; Shahin 1998; Abdallah et al., 2003; Abd El-Shafy et al., 2007; Strougo et al., 2013; Marzouk et al., 2014 and others) (Figure 9). It could be correlated with the Globigerapsis semiinvoluta zone of Italy (Bolli and Cita, 1960), Syria (Al-Helou, 1996), Spain (Hillebrandt, 1974), Israel (Benjamini, 1980), and Tunisia (Karoui-Yaakoub et al., 2017).

E 15. Globigerinatheka index Zone

Category. Highest-Occurrence Zone.

Definition. The present zone is defined by Wade et al. (2011) as the interval between the highest occurrence (HO) of Globigerinatheka semiinvoluta and the HO of Globigerinatheka index. In the present study the nominate species of this zone (Globigerinatheka index) has not appeared, so the upper boundary of this zone is undefined in the studied section and only contains a part of this zone.

Age. Late Eocene (Priabonian).

Assemblages. Thirteen species are identified from the present zone including Turborotalia cerroazulensis, Turborotalia cunialensis, Turborotalia cocoaensis, Subbotina yaguaensis, Dentoglobigerina tripartita, Pseudohastegerina naguewichiensis, Chiloguembelina cubensis, Catapsydrax dissimilis, Globoturborotalita occlusa, Tenuitella angustiumbilicata, Paragloborotalia opima, Paragloborotalia nana, and Tenuitella gemma. The most important benthic foraminiferal species recorded in this zone include assemblage of the genera Cancris (C. auriculus, C. subconicus), Epistomaroides, Rosalina (R. quadrata), Discorbis (D. vesicularis), Paralabamina (P. lunata), Cibicidoides (C.yankulaensis, C. ocalamus), Pararotalia, Textularia (T. adamsi, T. recta), Lenticulina, Nonionella (N. africana, N. labradorica), and Reussella (R.terquemi).

Remarks. In this study, the Globigerinatheka index zone includes the upper part of the Tarbul Member of the Beni Suef Formation in section C (samples 35-42). The lower boundary of this zone is located at the HO of Globigerinatheka semiinvoluta and the LO of Turborotalia cunialensis. Meanwhile, the upper boundary is undefined due to the absence of the nominate species (Figure 2, Figure 5). In this study, this zone is recorded for the first time from the Late Eocene of the north Eastern Desert of Egypt. This zone is also characterized by the presence of the slightly keeled and flattened Turborotalia cunialensis and the most highly evolved Turborotalia species; Turborotalia cerroazulensis and Turborotalia cocoaensis. The abundance of large species of Globigerina, Dentoglobigerina (Globoguadrina), Paragloborotalia nana, and very small forms of Pseudohastigerina naguewichiensis characterized this zone.

Correlation. This zone is globally matched with the Late Eocene Turborotalia cerroazulensis zone (Bolli, 1957b; Toumarkine and Luterbacher, 1985) and Turborotalia cunialensis/Cribrohantkenina inflata zone P 16 (Berggren et al., 1995; Mukhopadhyay, 2003). It is also correlated with the Late Eocene Turborotalia cocoaensis and Turborotalia cunialensis zones (Mukhopadhyay, 2005); Globigerinatheka index zone E 15 of Berggren and Pearson (2005) and Wade et al., (2011) and with the Turborotalia cerroazulensis zone of northeast Libya (Imam, 1999). In Egypt, this zone could be correlated with the Late Eocene Globorotalia cerroazulensis Zone in central Sinai (Viotti and El-Demerdash, 1969), Globigerinoides index tropicalis zone in west central Sinai (Abul-Nasr, 1993), Turborotalia cocoaensis zone in north Sinai and Nile Valley (Bassiouni et al., 1974 and Farouk, 2007), and also with Turborotalia cerroazulensis zone in west central Sinai (Abd El-Shafy et al., 2007) and the Fayum area (Haggag, 1990) (Figure 9).

The interval overlies the Globigerinatheka index zone in section C includes the exposed lower part of the Maadi Formation. This interval is characterized by an absence of planktonic species. It is equivalent to the benthic foraminiferal Pyrgo elongata zone recorded by Abd El-Gaied et al. (2019) from the studied section. The identified benthic species in this interval includes miliolid, textularid, and nummulitid foraminifera. This interval assigned the Late Eocene age based on its stratigraphic position and the occurrence of the marker small and large benthic foraminifera (Nummulites and Operculina) and macrofossils (Carolia placunoides and other bivalves; large and small size of gastropods, corals and echinoids). The abundance of the miliolids, textularids, and nummulitids with a remarkable extinction of the planktonic foraminifera at this interval of the studied succession was related to fall of the eustatic sea-level that took place at the end of the Late Eocene (Berggren et al., 1985; Keller et al., 1987; Anan 1995, 2007).

Middle / Upper Eocene (Bartonian / Priabonian) Boundary

Up until now, the Global Stratotype Section and Point (GSSP) for the Middle/Upper Eocene (Bartonian/Priabonian) boundary has not been designated. Generally, in Egypt the Middle–Upper Eocene (Bartonian/Priabonian) boundary was traced at the lowest occurrence of Globigerinatheka semiinvoluta (Strougo, 1992 and 2008; Abd El-Shafy et al., 2007; Strougo et al., 2013 and Marzouk et al., 2014). Some authors placed this boundary at the last appearance of Truncorotaloides (Acarinina) rohri and the associated spinose forms (Haggag, 1986, 1989a, 1989b; Haggag and Luterbacher, 1991; Abd El-Aziz, 2002; Abdallah et al., 2003; Abd El-Gaied and Abd El-Aziz, 2005). Haggag (1992a, b) studied the planktonic foraminiferal groups in the Middle and Upper Eocene succession in different localities of Egypt and recognized that the Middle/Upper Eocene (Bartonian / Priabonian) boundary traced at the top of the Turborotalia pseudoampliapertura zone. However, Aly et al. (2011) and Abd El-Gaied et al. (2019) placed this boundary between the benthic foramineferal Palmula ansaryi zone and the Bulimina jacksonensis zone. Some authors (Blow, 1979; Toumarkine and Luterbacher, 1985; Shahin, 1992; Berggren et al., 1995; Haggag and Bolli, 1996; Mukhopadhyay, 2003 and others) considered the extinction of the middle Eocene spinose planktonic foraminifera as a marker for the boundary between the late Middle and the earliest Upper Eocene in the tropical and Mediterranean reagions. Others considered the first appearance of the Globigerinatheka semiinvoluta simultaneously with the disappearance of the Middle Eocene Truncorotaloides, Morozovellids, and the large Acarinina distinguished the Middle/Upper Eocene boundary (Strougo, 1992, 2008). According to the standard chronostratigraphic scale, the Bartonian/Priabonian boundary is located either at the P14/P15 zonal boundary or at the lower part of zone P15 (Toumarkine and Luterbacher, 1985; Berggren et al., 1995). In Egypt and the Middle East, Anan (1994, 2011), Hussein (1998), Helal (2002), Aly et al. (2011), and Abd El-Gaied et al. (2019) placed the Bartonian/Priabonian boundary at the last appearance of the benthic foraminiferal species palmula ansaryi. In the present study, the boundary between the Middle Eocene (Bartonian) and Upper Eocene (Priabonian) was located within the Globigerinatheka semiinvoluta zone (according to the works of Berggren and Pearson (2005), Wade et al., (2011), and Karoui-Yaakoubi (2017). The sedimentary succession at this boundary was characterized by shale and marl intercalations.


Planktonic foraminifera have a great value in constructing the sea level changes (Hart and Bailey, 1979; Leckie, 1987). Saber and Salama (2017) stated that the Eocene succession exposed to the south of our studied area is deposited under alternative transgressive and regressive cycles that related to the sea-level fluctuations. The vertical and lateral lithological changes besides the planktonic and benthonic ratio in the present study show environmental change from deep to shallow marine environments. Paleodepth obtained from the regression equation of Van der Zwaan et al. (1990) allowed us to reconstruct sea level changes that prevailed during deposition of the Eocene succession. Based on the observed facies changes, the Middle-Upper Eocene succession in the study area can be subdivided into four depositional sequences. The absence of lowstand systems tract of these sequences is probably due to erosional events along the sequence boundaries (Saber and Salama, 2017).

1) s figure10Depositional sequence 1 (DS1).This is the older depositional sequence and is of late Middle Eocene (Bartonian) age and is represented by the El Fashn Formation. The age of this sequence was confirmed by its occurrence with the Morozovelloides crassatus Zone. The transgressive systems tract (TST) of sequence 1 was marked by limestone and marl with high P/B ratios (75-89%) that reflect water depth upto 550 m (Figure 10) in the upper bathyal environment and indicated the maximum flooding surface. The upper part of the El Fashn Formation at section A and basal part of section B corresponds to the highstand systems tract (HST) that consists of limestone with P/B ratio 57-68% that indicates shallowing upward in the depositional environments to water depth upto 450 m. This sequence is well correlated with sequence 2 of Saber and Salama (2017). Globally, it was correlated with the third order cycle TA3.6 of Haq et al. (1987) and Bar 1of Hardenbol et al. (1998). The P% decreased to 57 % at the uppermost part of El Fashn Formation, reflected sea level drop and water depth 340 m (Figure 10). Bartonian/Priabonian sea level fall was previously described in Egypt (Strougo, 1992; Peters et al., 2009; Sallam et al., 2015; Wanas et al., 2015; Abdel-Fattah et al., 2016; Saber and Salama, 2017). This boundary was also described from the European basins (Hardenbol et al., 1998), southern Israel, and the southeastern Sirt basin (Guirad and Bosworth, 1999). The global eustatic sea level fall is complement with Bartonian/Priabonian boundary (Vail et al., 1977; Haq et al., 1987).

2) Depositional sequence 2 (DS2). This sequence is represented by the Qurn Member of Beni Suef Formation and the lower part of Globigerinatheka semiinvoluta zone (Figure 9, Figure 10A). It is of latest Bartonian–early Late Priabonian age. It was deposited with P% of 57-45 % and water depth upto 320 m. It is subdivided into transgressive and highstand systems tracts. The TST of sequence 2 was mainly shale corresponding to the outer ramp facies of sequence 3 of Saber and Salama (2017). The lowering of sea level began to deposit the high stand systems tract in the form of shallower marl facies at the upper part of Qurn Member (water depth 270 m), reflected by the lowering of the planktonic foraminifera ratio P% to 40%. These ratios recorded at the middle part of Globigerinatheka semiinvoluta zone.

3) s figure11Depositional sequence 3 (DS3). This sequence corresponds to the topmost part of the Qurn Member and the whole thickness of the Tarbul Member of the Beni Suef Formation, which was represented by the upper part of Globigerinatheka semiinvoluta zone and Globigerinatheka index zone of Priabonian age that coincide with the TST and HST, respectively (Figure 10, Figure 11A-C). The transgressive systems tract is mainly marly facies and characterized with a planktonic ratio P% up to 36% decreasing gradually within the highstand deposits to reach 6% at the boundary with the overlying sequence. This sequence was well correlated with sequence TA4-2 of Haq et al. (1987) and the lower boundary corresponds to Pr2 boundary of Hardenbol et al. (1998) (Figure 10).

4) Depositional sequence 4 (DS4). It is represented by the upper Eocene Maadi Formation (Figure 10 and Figure 11B). The lowering of sea level leads to form a hardground horizon with Thalassinoids at the top of Beni Suef Formation. This horizon is documented in the Fayum area (Abdel-Fattah et al., 2010, 2016). Also, it is described from the European basins as Pr3 boundary (Hardenbol et al., 1998). Globally, this lowering of sea level was documented between 3rd order cycles TA4.2 and TA4.3 of Haq et al. (1987). The boundary between the Beni Suef and Maadi formations is characterized by a complete absence of planktonic foraminifers that reflects paleowater depth of about 36 m, and the deposition took place in inner shelf environment (Pippèrr and Reichenbacher, 2010; Pippèrr, 2011). The transgressive systems tract deposits are mainly marl and shale rich in benthic foraminifera. Moreover, the Maadi Formation is rich in mega-fossils (Bivalves, gastropods, echinoids), algae and benthic foraminifera (Figure 11D) that live in shallow marine environment (Murray and Alve, 1999; Kooistra et al., 2002; James and Bone, 2011; Granier, 2012; Reuter et al., 2012; Sarkar, 2016). Also, the Maadi Formation is distinguished by the first appearance of solitary and colonial corals that were not observed in the underlying Eocene rocks of the studied sequence and some of the neighboring areas. These corals and their faunal associations prevailed as a small patch reef formed during the highstand systems tract of sequence 4. This view shows a great accordance with the observation that was concluded by Scheibner et al. (2000) from the Galala Mountains, north Eastern Desert, Egypt. Morsilli et al. (2012) stated that the Eocene corals are largely found as reef patches. The well-preserved corals were considered as important tool to reflect the past sea level, occupying shallow marine settings with water depth 40 m (Carpenter et al., 2008; Woodroffe and Webster, 2014; Hibbert et al., 2016). Generally, the Middle to late Eocene age was assigned as the time of coral diversity and abundance in the Tethyan area (Fagerstrom, 1987; Budd, 2000; Geel, 2000; Perrin, 2002; Nebelsick et al. 2003, 2005; Morsilli et al., 2012; Król et al., 2017).


The deposition depth of the El Fashn Formation was deeper than the overlying formations, which was indicated by the highest percentage of planktonic foraminifera (P % = 75-89%). The Beni Suef Formation was deposited in inner to middle shelf environment with moderate P % (57-45 % for the Qurn Member and 6-36% for the Tarbul Member). The Maadi Formation was deposited in an elevated area, indicated by a complete disappearance of planktonic foraminifera and the high abundance of carbonate producers of large benthic foraminifera, corals, and algae that need light for photosynthesis process. A significant biotic turnover in the muricate planktonic foraminiferal genera occurred in the late Middle Eocene with a prominent decline in the Acarininids lineage and the extinction of the Morozovellids. This turnover event was associated with the weakening of photosymbiotic partnerships with algae and the increased surface water productivity (Wade, 2004). Barr and Berggren (1980) mentioned that the disappearance of the Truncorotalids and Morozovellids at the end of the late Middle Eocene are due to ecological changes (shallowing) or to preservational conditions. The previous studies on the spinose planktonic foraminiferal genera detected that these genera were prominent surface dwellers for the tropical and subtropical fauna, and their rapid global extinction through the late Middle Eocene was abrupt (Pearson et al., 1993; Toumarkin and Luterbacher, 1985; Wade, 2004;d Cotton et al., 2017). These extinction levels have been widely used in global biostratigraphic schemes (Blow, 1969; Toumarkine and Luterbacher, 1985; Berggren and Pearson, 2005; Wade et al., 2011). The abundance of the miliolids and nummulitids with a remarkable extinction of the planktonic foraminifera may be related to the fall of the eustatic sea level that occurred in the Late Eocene (Berggren et al., 1985; Keller et al., 1987; Anan, 1995, 2007). Abdelghany (2002) mentioned that this global regression may be due to a tectonic disturbance and the drop in sea level.


The stratigraphy and the planktonic foraminifera of the Middle-Upper Eocene successions at Beni Suef–El Zafaarana District, north Eastern Desert, Egypt, were studied in detail in this work. Lithologically, the studied sequence was described well and could be subdivided into three lithostratigraphic units covering a time interval from the late Middle to Late Eocene. These rock units are from base to top: the El Fashn (late Middle Eocene), the Beni Suef (latest Middle-Late Eocene), and the Maadi formations (Late Eocene).

The investigation of the microfaunal content of 97 rock samples collected carefully from three exposed sections resulted in the identification of seventy planktonic foraminiferal species belonging to 20 genera and seven families.

The vertical distribution of the estimated species enabled us to recognize three planktonic biozones arranged from base to top as: Morozovelloides crassatus zone (late Middle Eocene) including the El Fashn Formation, Globigerinatheka semiinvoluta zone (late Middle Eocene–early Late Eocene) and Globigerinatheka index zone (Late Eocene) including the Beni Suef Formation. The examination of the samples of the Maadi Formation yielded common to abundant representation of large and small benthic foraminifera and complete absence of the planktonic species.

Based on the changes in planktonic ratio and the paleowater depth, the studied Eocene successions are subdivided into four depositional sequences.


The authors would like to thank Prof. G. Abdel-Gawad from the Geology Department, Faculty of Sciences (Beni-Suef University) for his help in the field work. We would like to thank our editors A, Elewa, C. Haug, and our reviewers for taking time in this article.


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