Sea-Level Changes in the Paleocene (Danian–Thanetian) Succession At

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Proceedings of the Geologists’ Association 128 (2017) 764–778

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Proceedings of the Geologists’ Association

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Sea-level changes in the Paleocene (Danian–Thanetian) succession at

the Dakhla Oasis, Western Desert, Egypt: implications from benthic foraminifera

a b,

Sherif Farouk , Sreepat Jain *

Exploration Department, Egyptian Petroleum Research Institute, Nasr City, 11727, Egypt

Adama Science and Technology University, School of Applied Natural Sciences, Department of Applied Geology, P.O. Box 1888, Adama, Ethiopia

A R T I C L E I N F O A B S T R A C T

Article history:

–

Received 27 January 2017 The Danian Thanetian benthic foraminiferal assemblages at the Gharb El-Mawohb section in the Dakhla

Received in revised form 22 June 2017 Oasis of Western Desert (Egypt) are inferred in combination with characteristic species, genera

Accepted 26 June 2017 distribution, Benthic Foraminifera Numbers (BFN), species diversity, and abundance of high ﬂux-species

Available online 21 July 2017

to infer prevailing paleoenvironment, paleoproductivity and paleobathymetry vis-à-vis sequence

stratigraphy, regional tectonics, climate and changes in sea-level. The response of benthic foraminiferal

Keywords:

assemblages to sea-level changes during boundary successions, namely the Danian/Selandian (D/S) and

Benthic foraminifera

the Selandian/Thanetian (S/Th) is also analyzed. Data suggests a remarkably highly equitable

Sequence stratigraphy

environment throughout the studied interval. Eighty eight percent of the data plot in the restricted

Western Desert (Egypt)

littoral environment (mostly in brackish and some in normal lagoons) suggesting that the fauna are not

Danian–Thanetian

stressed despite a largely shallow depositional setting (middle to outer neritic, at places upper bathyal).

The dominance of calcareous taxa indicates a largely open marine condition, in a largely oxic and

oligotrophic environment, except in the late Paleocene where high-organic-ﬂux species suggest

increased paleoproductivity possibly due to local upwelling. The end of Zone P2 marks the deepest part of

the studied section (outer neritic to upper bathyal) followed by gradual shallowing across the section

(inner to middle neritic), with intermittent deepening in the middle of Zone P3a and P3b (middle neritic).

There is shallowing at the transitions of Zones P3a, P3b and P4 (inner neritic). The changes in the vertical

facies and benthic foraminiferal assemblage at the D/S and S/Th boundaries are analyzed.

1. Introduction central parts of the Western Desert have received much attention

for stratigraphic, paleontological and sedimentological studies (see

The southern Tethyan margin represents an important area for Luger, 1985; Bassiouni et al., 1991; El-Azabi and El-Araby, 2000;

studying processes on the Paleocene continental margin, as it Tantawy et al., 2001; Hewaidy et al., 2006; El-Azabi and Farouk,

provides numerous well-exposed outcrops, yielding well-pre- 2011; Boukhary et al., 2013; El Nady and Hammad, 2015; Hewaidy

served microfossils and representing a wide variety of paleoenvir- and Ayyad, 2015; Farouk and El-Sorogy, 2015; Farouk, 2016).

onmental settings (Farouk, 2016). Climatically, the Paleogene was a However, benthic foraminiferal paleoenvironmental and paleo-

highly dynamic period, transitioning from a near ice-free world of bathymetric studies in the Dakhla Oasis remain scarce (Schnack,

the Cretaceous to the glacially dominated world of the Neogene, 2000; Hewaidy et al., 2014; Farouk and Jain, 2016).

marked by important biotic and environmental changes (Zachos The present study is an attempt to bridge this gap and uses the

et al., 2001; Speijer, 1994, 2003; Speijer and Schmitz, 1998; Speijer presence and distribution of benthic foraminiferal species, genera

et al., 2000; Arenillas, 2011; Schmitz et al., 2011; Liebrand et al., and assemblage, BFN (Benthic Foraminiferal Number), species

2017). Along the continental margin, Egypt (Fig. 1a) occupies a diversity, and abundance of high ﬂux-species to infer the prevailing

prominent place to study biotic changes, where the southern and paleoenvironment, paleoproductivity, paleooxygenation and pale-

obathymetry of the Danian–Thanetian interval at the Gharb El-

Mawohb section (Dakhla Oasis, Western Desert, Egypt). The study

also attempts to document the response of benthic foraminiferal

* Corresponding author.

assemblages to sea-level changes during boundary successions,

E-mail address: [email protected] (S. Jain).

http://dx.doi.org/10.1016/j.pgeola.2017.06.006

S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778 765

Fig. 1. Location map. (a) Paleobiogeographic map showing the position of Egypt (study area) along the continental margin. (b) Detailed map of the study area (inset: map of

Western Desert, Egypt, mentioning the studied locality).

namely the Danian/Selandian (D/S) and the Selandian/Thanetian Several Recent benthic foraminiferal studies have demonstrat-

(S/Th) of the Dakhla Oasis vis-à-vis sequence stratigraphy, regional ed that some species or assemblages exhibit preferences for

tectonics, climate and sea-level changes. speciﬁc oxygen and/or trophic levels, whereas others are tolerant

The ﬁve proxies are used in this study namely benthic to a wider range of oxygen availability and of many types of food

foraminiferal species, genera and assemblage, Benthic Foraminif- (see Murray, 1991; Gooday, 2003). It has been well demonstrated

eral Number, species diversity and abundance of high ﬂux-species. that benthic foraminiferal distribution is largely limited by a

These are briefed ﬁrst along with a note on the relevance of benthic combination of food availability and oxygenation (the TROX model

foraminifers as a bathymetric proxy. of Jorissen et al.,1995; see Speijer,1994; Jain and Collins, 2007; Jain

766 S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778

et al., 1997; Alegret and Thomas, 2004). The amount of organic Speijer, 2003; Speijer and Schmitz, 1998; Schnack, 2000; Alegret

matter ﬂux to the sea ﬂoor, however, mainly governs the et al., 2003; Ernst et al., 2006; Stassen et al., 2009; Sprong et al.,

occurrence of species within the sediment, if oxygen content of 2012). When inferred in conjunction with % Planktics, the

the bottom-water is not the limiting factor (see Van der Zwaan abundance of some depth-related species, as well as the upper

et al., 1999). But the ecological preferences of shallow water depth-limits of others, changes in paleodepth can be robustly

Cretaceous–Paleocene taxa are less well established as much of the inferred (see also Van der Zwaan et al., 1990, 1999).

information on their ecological preferences are based on deep sea

benthic foraminiferal data (see Speijer, 1994; Alegret and Thomas, 2. Stratigraphic setting

2004) aided by few comparative accounts of fossil and recent

assemblages (see Kaiho, 1994; Van der Zwaan et al., 1999). Hence, The Western Desert is one of the most characteristic landscapes

to appreciate the role of benthic foraminiferal assemblages, of the tectonically stable shelf in Egypt (Said,1962; Farouk, 2016). It

inference from the interaction of benthic foraminifera with other is a plateau desert with big oases; among them being those of Beris,

proxies (BFN, Diversity and P/B ratio) are used here to estimate the Kharga, Dakhla and Farafra found in southern and central parts

0 0

prevailing paleoenvironment, paleoproductivity and plaeooxyge- (Fig. 1b). These oases are outlined by latitudes 24 30 N and 27 30

0 0

nation. N and longitudes 27 00 E and 31 00 E and marked by the

In this context, the benthic foraminiferal number (BFN; the presence of a thick Maastrichtian–Ypresian sedimentary sequen-

number of benthic foraminifera per gram of sediment) is a useful ces that record changes in facies, thickness and fauna with

proxy to estimate past oxygen content and organic matter ﬂux (see regionally traced hiatuses along escarpment faces and plateau

Jorissen et al.,1995; Van der Zwaan et al.,1999). In oxygen depleted surfaces (Figs. 2 and 3).

sediments, BFN generally decreases whereas in environments with At the base of the escarpment faces of Kharga and Dakhla, the

increasing organic matter ﬂux to the seaﬂoor, BFN numbers Duwi Formation is unconformably overlain by the Lower

increase (see Gooday, 1994, 2003; Holbourn et al., 2001; Alegret Maastrichtian–Late Paleocene Dakhla Shale Formation (Fig. 3),

et al., 2005; Reolid et al., 2008; Alegret and Thomas, 2013). comprised of a thick shale with mudstone interbeds. The Dakhla

However, increasing organic matter ﬂux to the seaﬂoor leads to Formation, from base upward, contains the Mawhoob Shale, Beris

higher oxygen consumption, thereby decreasing BFN values, if a Mudstone and Kharga Shale Members, respectively (Awad and

certain threshold is reached (see Murray, 2000). Conversely, in Ghobrial, 1965). An unconformity marks the contact between

seasonally anoxic basins with high primary production, increase in Mawhoob Shale and Beris Mudstone. Further, the Kharga Shale

benthic foraminiferal standing stocks are also noted (see Bernhard, Member is divided into two units (see Luger, 1985), the Lower and

1987). Thus, BFN is controlled by both oxygen content and organic Upper Kharga Shale and is separated by a hiatus marking the

matter ﬂux. To discern the role of each of these factors alone, other Cretaceous/Paleogene (K/Pg) boundary (see also Farouk and Jain,

data (benthic foraminiferal assemblages, species-speciﬁc distribu- 2016).

tion and the distribution of high-ﬂux benthic foraminiferal

species) need to be looked at, in conjunction. We have used Total 3. Biostratigraphy

BFN and % Calcareous BFN as proxies to estimate past oxygen

content and organic matter ﬂux. 3.1. Morozovella angulata Zone (P3a) (see Fig. 4)

Benthic foraminiferal diversity is another indirect parameter to

estimate oxygen content and organic matter flux for ancient This zone is defined as a partial range from the first appearance

bottom waters. In general, assemblages exposed to low oxygen of the M. angulata (White) to the ﬁrst appearance of Igorina albeari

and/or high organic matter ﬂux exhibit low diversity and a (Cushman and Bermudez). It is of early Paleocene (61.0–60.0 Ma,

dominance of a few taxa (see Sen Gupta and Machain-Castillo, according to Berggren and Pearson, 2005). In the present study, it is

1993; Speijer et al., 1996; Den Dulk et al., 1988; Van der Zwaan recorded in the Upper Kharga Shale Member of the Dakhla

et al., 1999; Holbourn et al., 2001). However, low diversity faunas Formation and attains about 22 m thick (samples 248–280) at

also occur under oxygenated conditions if the organic matter ﬂux is Gharb El-Mawohb section. The most important planktonic species

very low (see Schmiedl et al., 1998). Therefore, other parameters recorded from this zone are Chiloguembelina midwayensis (Cush-

such as BFN and benthic foraminiferal assemblages (including the man), Chiloguembelina subtriangularis Beckmann, Eoglobigerina

presence of speciﬁc species and genera) are needed to discern the spiralis (Bolli), Parasubbotina pseudobulloides (Plummer), Para-

role of diversity to estimate organic-matter ﬂux and oxygenation of subbotina varianta (Subbotina), Parasubbotina variospira (Belford),

the bottom-water. Fisher’s alpha (a), Shannon–Weaver informa- Subbotina triangularis (White), Subbotina triloculinoides (Plummer),

tion function (Shannon H), Equitability and Dominance are used Acarinina strabocella (Loeblich and Tappan), M. angulata (White),

here as diversity proxies (see also Hayek and Buzas, 1997). Species Morozovella praeangulata (Blow), Igorina pusilla (Bolli), Praemurica

diversity includes a measure of both species number and inconstans (Subbotina), Praemurica praecursoria (Morozova), and

Equitability (or Evenness), a measure of how equally abundant Praemurica uncinata (Bolli), Globanomalina chapmani (Parr),

species are in a community. The number of species per sample is a Globanomalina compressa (Plummer), Globanomalina ehrenbergi

measure of richness. Evenness is a measure of the relative (Bolli), and Globanomalina imitata (Subbotina).

abundance of the different species making up the richness of an

area. Shannon H, a measure of heterogeneity is used as an index of 3.2. I. albeari Zone (P3b) (see Fig. 4)

diversity. It takes into account the number of species and the

equitability of their distribution within a sample. Fisher’s a is the This zone is deﬁned as a partial range from the ﬁrst appearance

relationship between the number of species and the number of of the I. albeari (Cushman and Bermudez) to the ﬁrst appearance of

individuals in those species. It is independent of sample size and Globanomalina pseudomenardii (Bolli). It is of latest Danian–earliest

can be calculated knowing only species richness (S) and total Selandian (60.0–59.4 Ma, according to Berggren and Pearson,

number of individuals (N). 2005). This zone is recorded in the Upper Kharga Shale Member of

The benthic foraminifera, as outlined above, besides being an the Dakhla Formation and attains about 322 m thick (Samples 281–

important source of information about paleoenvironmental 300) at Gharb El-Mawohb section. The most important planktonic

conditions at the sea ﬂoor, such as ocean productivity and species recorded from this zone are C. midwayensis (Cushman), P.

oxygenation, are also excellent bathymetric markers (see also varianta (Subbotina), P. variospira (Belford), S. triangularis (White),

S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778 767

Fig. 2. Field photographs. (a) Study area showing Maastrichtian–Thanetian succession (Kharga Shale Member and Tarawan Chalk Formation, respectively) at the Dakhla

Oasis, Western Desert. (b) Contact between Kharga Shale Member and Tarawan Chalk Formation. (c) The Selandian–Thanetian boundary and the sequence boundary, ThWD

(see Fig. 3 for details and text for explanation).

S. triloculinoides (Plummer), Morozovella acuta (Toulmin), Morozo- P. uncinata (Bolli), G. chapmani (Parr), G. compressa (Plummer), G.

vella aequa (Cushman and Renz), M. angulata (White), Morozovella ehrenbergi (Bolli), G. imitata (Subbotina), and G. pseudomenardii

conicotruncata (Subbotina), I. pusilla (Bolli), I. albeari (Cushman and (Bolli). Due to the homogeneity and due to the poor preservation of

Bermudez), P. praecursoria (Morozova), P. uncinata (Bolli), and G. foraminiferal tests of the Tarawan Chalk Formation, the P4 cannot

imitata (Subbotina). In the present study, the Danian/Selandian be subdivided into 4a–c subzones.

boundary is placed within the I. albeari Zone (between samples

284 and 285; see Figs. 3 and 4). 4. Sequence stratigraphy

3.3. G. pseudomenardii Zone (P4) (see Fig. 4) Three sequence boundaries are identiﬁed across the Danian/

Selandian (D/S) and Selandian/Thanetian (S/Th) Stage boundaries.

This zone is deﬁned as a total range zone biostratigraphic They are marked by sedimentation and faunal breaks (such as

interval marked by the total range of G. pseudomenardii (Bolli). It is erosional, lack of biozones, facies shifts and sharp changes in

of late Paleocene (59.4–55.9 Ma according to Berggren and biofacies). The inferred sequence boundaries document the

Pearson, 2005). This occupies the upper part of the Dakhla presence of three third-order depositional sequences with each

Formation and the Tarawan Formation and attains about 13.5 m representing a transgressive–regressive systems tract (TST–HST)

thick (samples 301–315) at Gharb El-Mawohb section. The most (see Fig. 4), where the Lowstand Systems Tract (LST) are missing

important planktonic species recorded from this zone are C. due to the deposition in an intra-shelf basin characterized by the

midwayensis (Cushman), C. subtriangularis Beckmann, E. spiralis presence of submerged paleo-structural highs and lows (El-Azabi

(Bolli), P. varianta (Subbotina), S. triangularis (White), S. triloculi- and Farouk, 2011). Each (Sequence and Sequence boundary) are

noides (Plummer), Subbotina velascoensis (Cushman), Acarinina brieﬂy outlined below.

nitida (Martin), A. strabocella (Loeblich and Tappan), M. acuta

(Toulmin), M. aequa (Cushman and Renz), M. angulata (White), 4.1. Sequence DaSQ3

Morozovella apanthesma (Loeblich and Tappan), M. conicotruncata

(Subbotina), Morozovella velascoensis (Cushman), I. pusilla (Bolli), I. This depositional sequence covers an interval from the K/Pg

albeari (Cushman and Bermudez), P. praecursoria (Morozova), and unconformity (Ma/DaWD; Fig. 3) at the base which is

768 S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778

Fig. 3. Stratigraphy and sequence stratigraphy of the studied section. The contained lithology, inferred transgressive system tracts (TST), highstand system tracts (HST),

depositional sequences (such as MSQ1, MSQ2, etc.) and Sequence boundaries (such as L/UMaWD) are also mentioned. The present study is a follow up from a previous

Maastrichtian–Danian benthic foraminiferal study (Farouk and Jain, 2016).

S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778 769

Fig. 4. Biostratigraphy of the studied section based on the distribution of index planktonic foraminifera.

characterized by the lack of planktic zones CF2–P1b (top of Zone upper part of the Kharga Shale Member of the Dakhla Formation at

CF3) falls within the interval of the uppermost part of the P. the Dakhla–Kharga oasis (see Farouk and El-Sorogy, 2015).

uncinata (P2) Zone (Farouk and Jain, 2016; Fig. 3). The present

study deals only with the upper part of this sequence (HST3) (see 4.4. Sequence ThSQ6

Fig. 4).

It covers the interval of the Tarawan Formation and falls within

4.2. Sequence DaSQ4 the interval of the upper Paleocene G. pseudomenardii (P4) Zone

(from samples 306–315) (Figs. 3 and 4).

This depositional sequence falls within the interval of the

uppermost part of the P. uncinata (P2) Zone to the lower part of the 4.4.1. Sequence boundary ThWD

I. albeari (P3b) Subzone (from samples 237–284) (Figs. 3 and 4). This is marked by the presence of an irregular surface of a thin

10 cm thick conglomerate bed consists of a gravelly mudstone bed

4.2.1. Sequence boundary DaWD with an irregular basal surface marks. The latter marks the

It is represented by a vertical facies changes from a ledge of boundary between the Dakhla Shale and the Tarawan Chalk

ferruginous calcareous sandy shale that separates the pale to dark (Fig. 2b). The Tarawan Formation is composed of white, snow white

gray to green calcareous and phosphatic shale below (HST3) and to yellowish white, hard, thickly bedded, and wall forming chalk

the gray to yellowish gray to brown glauconitic shale with and chalky limestone with few marl and shale intercalations. This

sandstone and siltstone intercalations, above (TST4) (Figs. 3 and 4). depositional sequence is represented by a transgressive systems

tract (TST) present only in the studied interval.

4.3. Sequence SeSQ5

5. Material and methods

This depositional sequence falls within the interval of the upper

part of P3b subzone and the lower part of the P4 Zone (Figs. 3 and Seventy-eight benthic foraminiferal Danian–Thanetian samples

4). It covers the upper most part of the Dakhla Formation (from (5490 specimens) were analysed from a section at the Gharb El-

0 00 0 00

samples 285–305). Mawohb at the main escarpment (26 01 02 N, 28 13 18 E;

Dakhla Oasis; Fig. 1). The 125–63 mm fraction from 2 g of

4.3.1. Sequence boundary SeWD sediments was investigated qualitatively and quantitatively under

This sequence boundary is characterized by a faunal break due the binocular zoom stereomicroscope. Diversity measures (Shan-

to the absence of the I. albeari (P3b) Zone, in part (Farouk and El- non H, Fisher’s a, Equitability and Dominance) and species

Sorogy, 2015). Lithologically, the D/S boundary lies within the abundance are used in combination with benthic foraminifera 770

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Fig. 5. Diversity measures, species, BFN (benthic foraminifera numbers), Percentage Planktic (%P), benthic foraminiferal assemblages, proposal sea level curve (in meters) and identiﬁed System Tracts (TST and HST) for the studied – 778 section. S.

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764 – Fig. 6. Benthic foraminiferal species abundance distribution pattern, assemblages, Percentage Planktic (%P), benthic foraminiferal assemblages, proposal sea level curve (in meters) and identiﬁed System Tracts (TST and HST) for the 778 studied section. 771

772 S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778

Fig. 7. Benthic foraminiferal community structure and depositional settings. The plot of Fisher’s a versus Shannon H gives a good idea of the depositional settings (i.e.

restricted vs. open marine) of the studied sequence-based benthic foraminiferal fauna. (a) All data; (b) Sequence stratigraphic-based benthic foraminiferal community

structure; and (c) Benthic foraminiferal assemblage-based distribution.

number (BFN) to infer changes in paleooxygenation and organic (Shannon H, Fisher’s a, Equitability and Dominance) are further

matter ﬂux (Fig. 5). These, when inferred in conjunction with the used to provide a better estimation of the prevailing ecological

BFN of dominant genera (Cibicidoides,Cibicides, Anomalinoides, structure and depositional environment (Fig. 7). Faunal changes

Epistomina and Haplophragmoides) and species (i.e. Cibicides across the D/S and S/Th boundaries are also addressed (Figs. 8 and

farafraensis, Cibicidoides howelli, Epistomina esnahensis, Cibicidoides 9). The distribution of high-organic-ﬂux benthic foraminiferal

phraonis and Anomalinoides acutus) (Fig. 6), they provide a robust species is also analysed for a better understanding of the prevailing

estimation of the prevailing paleoenvironment (see also Bernhard, environment in terms of changes in nutrient availability. All data

1987; Kaiho and Hasegawa, 1994; Jorissen et al., 1995; Van der are interpreted in terms of sequence stratigraphy, regional

Zwaan et al., 1999; Murray, 2000; Holbourn et al., 2001; Herrle tectonics, climate and sea level and summarized (Fig. 10). The

et al., 2003a,b; Farouk and Jain, 2016). Diversity measures inferred sea level is based on the abundance (%) pattern of

S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778 773

Fig. 8. Benthic foraminiferal changes at the Danian–Selandian boundary.

Fig. 9. Benthic foraminiferal changes at the Selandian–Thanetian boundary.

774 S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778

Fig. 10. Summary of events and the inferred sea-level curve of the studied Danian–Thanetian interval. Abbreviations used include: BFN = Benthic foraminifera number; %

P = Percentage Planktic, %HOFS = Percentage high organic-ﬂux species; % Calc. BFN = Percentage calcareous benthic foraminifera number. The paleodepth followed here

includes: Inner Neritic: <50 m; Middle Neritic: 50–100 m.

calcareous benthic foraminifera, species abundance, distribution 6.2. Systems tracts

of characteristic species, lithology and the presence and absence of

planktonic foraminifera (P/B ratio). The paleodepth followed here In general, benthic foraminifera are relatively frequent to

includes: Inner Neritic: <50 m; Middle Neritic: 50–100 m; Outer common with moderate to good preservation within the trans-

Neritic: 100–200 m; and Bathyal >200 m. gressive systems tracts (TST) but exhibit moderate to poor

preservation, with pervasive fragmentation and recrystallization

6. Results within the highstand systems tracts (HST).

6.1. Species diversity, BFN, P/B ratios and depositional setting 6.2.1. Highstand systems tracts

Two highstand systems tracts (HST) are identiﬁed – HST4

A statistically signiﬁcant correlation (Pearson = 0.800 at the 0.01 (samples 281–284; assemblage 16) and HST5 (samples 288–305;

level; 2-tailed) is noted between Fisher’s a and Shannon H, assemblage 18; see Fig. 6). During HST4 all diversity indices and

suggesting that both indexes are good proxies for species diversity BFN are low, and marked by the absence of planktonic foraminifera

(Fig. 11 ) (see also Murray, 1991; Speijer, 1994; Speijer and van (Figs. 3 and 4). Haplophragmoides glabra dominates the assemblage

derZwaan, 1996). Equitability is consistently high throughout the (see Fig. 6). HST5 contrasts HST4 characteristics, displaying

studied section (see Fig. 5). Dominance is consistently low moderate levels of species diversity and BFN values with presence

throughout the studied section but somewhat higher between of planktonic foraminifers that gradually decrease up section; P/B

samples 280–303 (assemblages 15–18; see Fig. 5). All the ratios do not exceed 20%. HST5 is characterized by the abundance

aforementioned proxies are inferred and in terms of systems of C. farafraensis and C. phraonis (see Fig. 6). Both HST4 and

tracts, below. HST5 fauna sit within the restricted brackish lagoonal/littoral

region with a single data point (of HST5) transgressing into the

open marine region.

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Fig. 11. A statistically signiﬁcant correlation is noted between diversity measures, Fisher’s a and Shannon H.

6.2.2. Transgressive systems tracts (samples 267–280). Assemblage 14 contrasts with the other two

Three transgressive systems tracts (TST) are identiﬁed – TST4 assemblages in that it is characterized by the abundance of

(samples 237–280; assemblages 13–15); TST5 (samples 285–287; agglutinated foraminifera H. excavata and H. glabra; both

assemblage 17) and TST6 (samples 301–315; assemblage 19 see Assemblages 13 and 15 are dominated by calcareous foraminifera

Fig. 6). All TSTare marked by higher values of diversity, BFN and the (see Fig. 6). Assemblages 13 is characterized by C. howelli and C.

dominance of C. howelli and C. farafraensis (and E. esnahensis in farafraensis and Assemblage 15 by C. farafraensis and E. esnahensis.

TST5 and TST6; see Fig. 6). TST4 is characterized by high P/B ratios TST5 is also dominated by calcareous foraminifera, E. esnahensis

in the lower section (samples 237–254; between 60–70%) followed and C. farafraensis. TST6 continues the trend with C. farafraensis but

by decreasing values, up section (20%). TST4 exhibits consistently also includes A. aegyptiacus (see Fig. 6). C. farafraensis, the

higher values of diversity, BFN and the dominance of C. howelli, C. dominant calcareous benthic foraminifera, transgress the bound-

farafraensis and E. esnahensis (see Figs. 5 and 6). TST5 is ary as also 34% (11 species) of the 32 recorded species. 14 species

characterized by increasing P/B ratios from 14 to 40% and higher are exclusive to the Thanetian and 7 are for Selandian (see Fig. 9).

values of diversity, BFN with the abundance of E. esnahensis and C. The only major change across the Selandian–Thanetian boundary

farafraensis (Fig. 6). TST6 is characterized by increasing P/B ratios (see Fig. 9) is the abrupt increase in high-ﬂux spices from a modest

from 17 to 50% and higher values of diversity, BFN with the 8.1% to a huge 72% in the Thanetian primarily due to the

abundance of C. farafraensis and Anomalinoides aegyptiacus (Figs. 5 proliferation of the opportunistic species A. aegyptiacus (see

and 6). The data points of TST4 sit within the brackish lagoonal/ Figs. 6 and 10).

littoral region, however those of TST4 and TST6 transgress into the

open marine region. 6.4. High-organic-ﬂux species

6.3. Benthic foraminiferal assemblage The high-organic-ﬂux species considered in this study include

A. aegyptiacus, Bolivina cretosa, Bulimina prolixa, Nonionella

Assemblage 13 (in-part) has been dealt with in Farouk and Jain africana, Nonionella insect, Praebulimina kikapoensis, Praebulimina

(2016 but is now dealt here in its entirety (samples 238–254). This russi, Pyramidulina afﬁnis, Pyramidulina distans, Pyramidulina

and the remaining assemblages are inferred vis-à-vis System semispinosa, Pyramidulina vertebralis, Pyramidulina zippei and

Tracts, below (see Fig. 3). Reussella aegyptiaca (see also Sen Gupta and Machain-Castillo,

1993; Sen Gupta, 1999; Fontanier et al., 2002; Jorissen et al., 2007;

6.3.1. Highstand systems tracts Alegret and Thomas, 2013). On an average the high-organic-ﬂux

HST4 is exclusively characterized by the presence of aggluti- species do not constitute a major portion of the benthic

nated foraminifera H. glabra and H. excavata (Assemblage 16), foraminiferal assemblage (ranging from 0 to 12%) except in TST6

whereas HST5, on the other hand is marked by the abundance of (Assemblage 19) where they make up 27% (see Fig. 6). The TST

calcareous benthic foraminifera C. farafraensis and C. phraonis with values are slightly higher than HST values. TST4 averages 12% of

accessory presence of Haplophragmoides excavata, Rotalia calcar- high-organic-ﬂux species (see Fig. 6). HST4 is marked by the total

iformis and H. glabra (Assemblage 18) (see Fig. 6). Major changes absence of high-organic-ﬂux species and HST5 registers 8.2% value.

are noted between assemblages 16 and 17 that straddle the D/S A summary of all proxies, percent calcareous foraminifera,

boundary (see Fig. 8). The changes at the Danian–Selandian benthic foraminiferal assemblage and inferred bathymetry (rela-

boundary are dramatic (see Fig. 8). There is an abrupt shallowing tive sea level) is given in Fig. 10. Bathymetry (relative sea level) is

(inner neritic depths) before the boundary (Assemblage 16: inferred by using the presence of characteristic species, the

dominated by shallow-water Haplophragmoides and Ammobacu- abundance values of calcareous benthic foraminifers and the

lites), a transitioning from a agglutinated low-salinity marsh presence and abundance of planktonic foraminifers. Taken

setting to a calcareous–foraminifera dominated open marine together, these proxies provide a sound estimate of the relative

setting, from a low-oxygen shallow infaunal benthic foraminiferal sea level (Fig. 10).

assemblage to an epifaunal and well-oxygenated environment in

the Selandian is noted (see Figs. 6, 8 and 10). 6.5. Sea-level curve

6.3.2. Transgressive systems tracts Inferred bathymetry (relative sea level) is based on the presence

TST4 has three assemblages: Assemblage 13 (samples 238– of characteristic benthic species, the abundance values of

254), Assemblage 14 (samples 255–266) and Assemblage 14 calcareous benthic foraminifers and the presence and abundance

776 S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778

of planktonic foraminifers (Fig. 10). There is no potential inﬂuence 1997) throughout the section suggests a scenario of moderate

of downslope transport affecting the composition of assemblages oligotrophy (reduced paleoproductivity) with moderately well-

as they are bathymetrically well-deﬁned. The end of Zone P2 marks oxygenated conditions (Fig. 6) (see also Alegret and Thomas, 2001;

the deepest part of the studied section (outer neritic to upper Galazzo et al., 2015). This scenario is also corroborated by reduced

bathyal) followed by gradual shallowing across the section (inner percentages of high-ﬂux species throughout the studied section

to middle neritic), with intermittent deepening in the middle of (<12%) of the total benthic foraminiferal assemblage (see Fig. 6)

Zone P3a and P3b (middle neritic). There is shallowing at the except for Assemblage 18 that records a somewhat higher

transitions of Zones P3a, P3b and P4 (inner neritic) (see Fig. 10). percentage (27%) but then then so does the aforementioned

A minor hiatus terminated sequence SeWD (between HST4/ epibenthic taxa (35%) (Fig. 6). Interestingly, there is a strong

TST5) within the P3b Zone closed to the D/S boundary (see). This positive and signiﬁcant correlation (Pearson = 0.345 at the 0.01

hiatus is attributed to a brief global sea-level fall. During Selandian, level; 2-tailed; N = 78) between the abundances of Cibicides/

increasing rates of sea-level rise resulted in the ﬂooding of the Cibicidoides and Anomalinoides with %P suggesting deeper paleo-

Western Desert and the subsequent deposition of a retrograda- depths (see also Van Morkhoven et al., 1986; Thomas, 1990); these

tional parasequence marked by foraminiferal calcareous shale with abundances also corresponds with TST intervals (see Fig. 5).

medium diversity benthic foraminifera. Afterwards, as the rate of Cibicides/Cibicidoides have been considered as proxy for bottom

relative sea-level rise slowed, during the lower part of Zone P4, a water ventilation (improved oxygenated conditions) (see Haug and

progradational shallow subtidal shale of the Lower Kharga Shale Tiedemann, 1998; Bickert et al., 2004; Jain and Collins, 2007).

unit was deposited (HST5). A vertical facies changes matches well Hence, moderately well-oxygenated conditions are inferred for

with the Se/Th boundary, as observed in the present study and in intervals at the end of Assemblages 14–15 and 17 (Fig. 5).

most parts of Egypt suggesting eustatic changes associated with Data also suggests that the Early Danian (Zone P2) sediments

tectonic event marked by accelerated uplift of the Mediterranean were deposited in an outer neritic to the uppermost bathyal

coast, with the emergence and erosion of several elevated environment at 100 m paleodepth. During the mid of subzone P3a

structures and increased subsidence in the internal depocenters and at the transition of subzones P3a–P3b, fall of sea-level is noted

(the so-called “Velascoensis Event” by Strougo, 1986). (Fig. 10). A similar sea-level ﬂuctuation has been noted during

subzone P3a at different locations in Egypt (Lüning et al., 1998;

7. Discussion Speijer, 2003) and also in Western Europe (see Hardenbol et al.,

1998). The Selandian (largely Zone 3b; see Figs. 5 and 10) is marked

The most characteristics feature of this Danian–Thanetian by low sea level. The succeeding Thanetian Zone P4 benthic

succession is the dominance of calcareous benthic foraminifers foraminiferal assemblage (19; Figs. 5 and 10) is typical of a highly

(Cibicides, Cibicidoides and Epistomina) and the minor role of productive middle to outer neritic environments (quite characteris-

agglutinated foraminifers (Fig. 6) which contrasts with the tic of the southern Tethyan region), possibly as a result of trade wind

Maastrichtian–Danian (in-part only) succession, where aggluti- induced upwelling (see also Speijer et al., 1996). Modeling studies

nated foraminifers proliferated (notably Ammobaculites, Haplo- suggest that the North African margin was probably affected by

phragmoides and Trochammina). However, the present study (the north-eastern winds during the Paleogene (Huber and Sloan, 2000).

D–Th succession) has fewer species (66) as opposed to the hugely These were driven by strong tropical–subtropical temperature

proliﬁc Maastrichtian–Danian (in part) (156 species; see Farouk gradients and are held responsible for a southeast to west coastal

and Jain, 2016). Additionally, another striking feature is bathyme- currentwith signiﬁcant upwellingalongthe North coastofAfricaas a

try – the D–Th succession is much deeper, at parts touching upper consequence (Huber and Sloan, 2000; Huber et al., 2003). During the

bathyal, but largely remaining within the middle to outer neritic late Paleocene, intensiﬁed upwelling is inferred to explain increased

depths (). productivity (27% of high-ﬂux-species in Assemblage 19; see

There is, however, two striking similarities also – (1) both Figs. 6 and 10), leading to eutrophication of the water column and

studies (samples 1–247) and this one (samples 238–315) plot oxygen deﬁciency on the sea ﬂoor. Increasing productivity is also

largely in the restricted lagoonal/littoral environment (mostly reﬂected by the benthic taxa: buliminids (highﬂux species), and of A.

brackish and some in normal marine lagoon region), rather than in aegyptiacus (Speijer et al., 1996; Kouwenhoven et al., 1997) (see

the normal marine environment (Fig. 7), as would be expected Figs. 6 and 10). Opportunistic middle-outer neritic A. aegyptiacus

with high species diversity and deeper bathymetry () (see also assemblages invaded the sea ﬂoor (Speijer et al., 2000) in response

Murray, 1991). Interestingly, the present data also largely plot in to eutrophic conditions and poor and variable oxygenation. This

the restricted region (88%, see Fig. 7; except 9 data points from taxon exhibits a similar opportunistic strategy towards dysoxic to

TST4 and TST6; 84% of the present data falls below <5, Fisher’s a, anoxic conditions noted during the PETM (see also Speijer and

see Fig. 7). Increased runoff and concomitant shallowing would Wagner, 2002).

also explain the intermittent presence/dominance of agglutinated

foraminifera in Assemblages 14 and 16 (Haplophragmoides and

8. Conclusion

Ammobaculites) within the studied section (Fig. 6). Haplophrag-

moides have been well documented from inner neritic and coastal

The Danian–Thanetian benthic foraminiferal assemblages are

environments (Le Roy, 1953; Luger, 1985; Speijer and Schmitz,

analyzed with respect to sequence stratigraphy (in terms of HST

1998). (2) A remarkably highly equitable environment with only

and TST). Overall, data suggest a remarkably highly equitable

few episodic intervals of species Dominance is noted in both

environment with low dominance. Eighty eight percent of the data

studies (see Fig. 5) suggesting a lack of stressed environment.

plot in the restricted littoral environment (mostly brackish and

Data also indicate that the environment evolved from an initially

some in normal marine lagoons) suggesting that the fauna are not

oligotrophic, open marine, outer neritic to upper bathyal (Assem-

stressed despite a largely shallow depositional setting (middle to

blage 13; see Fig. 10) setting towards a more eutrophic inner to

outer neritic, at places upper bathyal). The dominance of

middle neritic setting (Assemblage 19; see Fig. 10), possibly

calcareous taxa indicates a largely open marine conditions, in a

inﬂuenced by coastal upwelling by the end of the Paleocene.

largely oxic environment, except in the Thanetian where high-

The dominance of epibenthic taxa Cibicides/Cibicidoides and

organic-ﬂux species suggest high paleoproductivity possibly due

Anomalinoides (except A. aegyptiacus which has been considered as

to local upwelling.

a high-ﬂux species; see Speijer et al., 1996; Kouwenhoven et al.,

S. Farouk, S. Jain / Proceedings of the Geologists’ Association 128 (2017) 764–778 777

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