Hamad, Paleocene

Egypt. Jour. Paleontol., Vol. 9, 2009, p. 1-29 ISSN 1687 - 4986
BIOSTRATIGRAPHY OF THE LATE
PALEOCENE / EARLY EOCENE DEPOSITS OF GEBEL EL BRUK
AREA, NORTH- CENTRAL SINAI, EGYPT
Mansour. M. HAMAD
Geological institute, P.O. Box 41821, Madinah, Saudi Arabia.
ABSTRACT
The planktonic foraminiferal assemblage of the interval spanning the late Paleocene / early
Eocene boundary at Gebel El Bruk area, north – central Sinai, Egypt, have been studied and
analyzed in detail to deduce the main planktonic foraminiferal biostratigraphic zones.
Lithostratigraphically, three rock units were recognized from base to top: Tarawan , Esna and
Thebes formations. The planktionc foraminifera is well to moderately diversified and relatively
well preserved in most of the studied samples except in the Thebes Formation. The
stratigraphic distribution of the planktionc foraminifera allowed to recognize the following
biozones, from base to top: 1) Globanomalina pseudomenardii Zone (P4), 2) Morozovella
velascoensis Zone (Globanomalina pseudomenardii / Acarinina sibaiyaensis Interval Subzone
(P5a) and Acarinina sibaiyaensis / Morozovella velascoensis Interval subzone (P5b) of the late
Paleocene age (Thanetian) and 3) Morozovella edgari / M. subbotinae (P6a), 4) Morozovella
subbotinae (P6b), 5) Morozovella formosa formosa (P7), and 6) Morozovella aragonensis (P8)
zones of the early Eocene (Ypresian) age. The Paleocene / Eocene boundary at Gebel El Bruk
is located within the Morozovella velascoensis Zone and coincides with the boundary between
the Globanomalina pseudomenardii / Acarinina sibaiyaensis Interval Subzone (P5a) and
Acarinina sibaiyaensis / Morozovella velascoensis Interval subzone (P5b) (in the upper part of
the Esna Formation). This boundary is in coincidence with the small benthic foraminiferal mass
extinction (BEE). Compartive study of these zones with those of various sections in Egypt and
from western and eastern Tethyan realms revealed regional characteristics of the Paleocene –
Eocene boundary with the studied section.
The study of the planktonic foraminifera around the late Paleocene – early Eocene
boundary in the study area reflected the presence of a global planktonic foraminiferal faunal
turnover event. This turnover event is characterized by extinction and orginiation of some index
planktonic foraminiferal species (e.g. the first occurrence of the Acarinina berggerni, A.
sibaiyaensis and A. africana in Acarinina sibaiyaensis / Morozovella velascoensis Interval
subzone (P5b), just above the P / E boundary (sapropelic dissolution clay layer). It is also
emphasized by the sudden changes in the planktonic / benthonic ratio, relative abundance of
morozovillds,, acarininds and subbotinids that showed an increasing in the warm water planktic
species (Morozovella and Acarinina) in relative to the cooler water species that represented by
the Subbotina spp.,
Key words: Paleocene, Eocene, Planktonic foraminifera, biostratigraphy, Egypt.
INTRODUCTION
The Paleocene / Eocene deposits of Egypt have been the subject of numerous
stratigraphical and paleontological investigations. These sediments are represented
by different marine facies (hale, chalk, marl and limestone interbeds). Any
investigation of the Paleocene / Eocene boundary must include a detailed study of
the planktonic foraminifera as cornerstone for correlation. The distribution of
planktonic foraminifera in the Paleocene/ Eocene boundary in the study area let
the present author to carry out this problem. Gebel El Bruk area is laocated in north
central Sinai, and lies between Lat. 29° and 30° 25' N and Long. 33° 15' and 24° E
(Fig. 1). The southern border of the area reaches Nakhl Village and represented by
elevated plateau of Tertiary rocks. While its northern parts are formed of anticlinal

Hamad2
structures trending in northeast – southwest direction and occupied the low lands.
The previous stratigraphic investigations on the surface and subsurface geology of
this area were carried out by Moon & Sadek (1921), Beadnell (1926), Moustafa &
Khalil (1989), and Said (1990). These studies were conducted primarily to
determine the different stratigraphic units and their ages. From the
micropaleontological point of view, the calcareous nannoplanktons are investigated
by Faris & Zahran (2002) who studied the calcareous nannoplanktonic assembage
of Gebel El Bruk, and recognized different nannofossil zones arranged from base
to top as follows: Fascicultus tympniformis Zone (NP5), Discoaster mohleri Zone
(NP7 / NP8), Discoaster multiradiatus Zone (NP9) and Tribarchitus contortus Zone
(NP10) of late Paleocene age and Discoaster binodosus Zone (NP11),
Tribarachitus orthostylus Zone (NP12) of early Eocene age. Moreover, they placed
the Paleocene / Eocene boundary between the NP9 and NP10 zonal boundary.
More recently, El Nady (2006) studied the Paleocene / Eocene boundary at Gabal
Kshkoul, east–central Sinai and recognized five planktonic foraminiferal zones from
base to top:P3b,P4,P5,P6a, and P6b. He also showed that the Paleocene/ Eocene
boundary lies within the Morozovella velascoensis (P5) Zone of Paleocene age.
Abu Zenima
WadiAlArish
S i n a iS i n a i
P e n i n s u l aP e n i n s u l a
Al Tor
Dahab
W
adi Sudr
Ayun Mousa
Suez
Great Bitter
Lake
Ayn Sukhnah
Wadi Araba
Gulf
of
Suez
Ras Gharib
GulfofAqaba
Red SeaRed Sea
Al Arish
M e d i t e r r a n e a n S e aPort Said
Ras Muhamed
Taba
Eastern
Desert
Wadi Gharandal
Study area
Gabal El Bruk
W
adi El Bruk
Ismalia
N
0 40Km
G. Maghara
G. Halal
G. Minsherah
35°34°33°32°
31°
30°
29°
Cairo - Suez Road
G. Sarbut El Gamal
G. Sant Katrin
Al QusimaG. Gharra
Rafah
Abu Rudies
Fig. 1: Location map showing the studied Gabal El Bruk area, north- central Sinai, Egypt

Biostratigraphy of late Paleocene-early Eocene in Sinai 3
The aim of the present work is to define and evaluate as precisely as the planktonic
foraminiferal biozones in Gabal El Bruk, north – central Siani, Egypt. Moreover, to
locate the Paleocene / Eocene boundary and recognize the main bioevents across
the Paleocene / Eocene boundary transition using planktonic and benthonic
foraminiferal analysis. Correlation of the recoded planktonic foraminifera with their
Tethyan sections is also refered. The second aim is to deduce the main
paleoenvironmental conditions that were flourished during the deposition of the
different rock units. The planktonic foraminiferal turnover across the Paleocene/
Eocene transition boundary is also investigated besides the rough analysis of the
benthonic foraminiferal association to deduce the benthonic foraminiferal extinction
event (BEE). No carbon or oxygen isotopic analysis were carried out, so the
citation of the Paleocene / Eocene boundary is tentative.
MATERIAL & METHODS
About forty-five samples covering the stratigraphic interval of the late
Paleocene / early Eocene in Gebel El Bruk, north - central Sinai, Egypt, have been
collected and analyzed for their planktic foraminiferal content with little reference to
their benthic ones. The sampling process started as usual from the base of the
Tarawan Formation at base, up to the exposed part of the Thebes Formation and
denoted as GB1 to GB 45, using sampling interval of 1m. For the more precise
micropaleontological analysis especially around the Paleocene / Eocene boundary
the sampling interval become 50cm and sometimes 20cm and 10cm. The samples
are treated here according to their hardness. The soft samples are prepared by
taking a suitable weight of sample and was dried and heated in an oven below
50°C for about 1.5 hours, then soaked in 10% hydrogen peroxide solution for
disintegration. The disintegrated samples were then washed using different types
of sieves ranging from 63µm, 125µm, 250µm to 595µm. But for the hard samples,
they were crushed into smaller fragments and heated in an oven below 50°C, then
soaked in kerosene for 24 hours till the disintegration process was completed. After
that, the previous procedure with the soft samples was repeated in the same
manner. After that the washed residue sieved through set of sieve ranging from
500μm to 63 μm screen. The realtives abundance data of the planktonic foraminifra
are presented in figure 3. Scanning Electron Microscpic photomicrographs of these
taxa are shown in one plate.
LITHOSTRATIGRAPHY
The Paleocene – Eocene deposits are well exposed in the central and northern
parts of Sinai forming the main bulk of the anticline ridges in many places. The
stratigraphic section exposed in Gebel El Bruk area could be divided into the
following rock units from base to top:
Tarawan Formation:
This rock unit was originally described by Awad and Ghobrial (1965) in Gebel
Tarawan, Kharga Oasis and Nile Valley area. It is represented in the study area by
yellowish to grayish white, indurated chalky to marly limestone that is easily
identified in the field showing close affinity to that described in Nile Valley area.
This formation grades upward into yellowish marly limestone and brownish white

Hamad4
cherty limestone with scattered brownish chert bands and nodules at top. The
contact between this unit and the Esna Formation is gradtional. The Tarawan
Formation is recorded at the base of the studied section attaining 27m in
thickness, (Fig. 2)
Esna Formation:
This rock unit was originally described and introduced by Beadnell (1905) as
Esna Shale (green to grayish green shales) that underlying the “Eocene
Operculina limestone”, in Gebel Oweina, southeast of Esna region, attaining 60 m
in thickness. Later on, Said (1960) studied the shale - marl succession at Gebel
Oweina, southeast Esna and showed that it overlies the Tarawan Formation and
underlies the Thebes Formation and assigned it to late Paleocene / early Eocene
age. Subsequently, Said (1962) raised this shale unit to formational rank and
named it as Esna Formation. In central Sinai, especially along the scarp face of El
Tih – Egma plateau and other localities, this rock unit was introduced to describe
the Paleocene shale - marl sequence overlying the Late Cretaceous Sudr
Formation.
The Esna Formation is represented mainly by monotonous grayish to greenish
gray laminated shale and marl beds that intercalated with ledges of argillaceous
limestone and chalk. Closer field examination of the Esna Formation revealed a
prominent sapropelic dissolution dark reddish gray laminated clay layer (sample
no. 24 of 2m in thickness) barren of both planktonic and benthonic foraminiferal
species and recorded at the middle part of this formation. This sapropelic layer may
be suitable level for recognition of the Paleocene – Eocene boundary and it may
tentatively coincide with interval of the Carbon Isotope Excursion (CIE) recoreded
in other regional sections. This layer was recorded from several sections in the
Tethyan realm (4m thick at Possagno, Italy; 3.5 thick at Zumaya section, 2m at
Caravaca, and 40 cm at Alamedilla, Spain (Canudo & Molina, 1992; Arenillas et al.,
1999). Speijer (1994) recorded this sapropelic layer (partly laminated shale layer
indiacting low oxygen deficiency) also at Wadi Nukhul, west central Siani, Egypt.
Speiger & Wagner (2000 & 2001) recoreded similar but black shale bed (dark
brown laminated marl) in the late Paleocene thermal maximum at three sections In
souther Israel and Egypt. The Esna Formation is well developed in the studied
section, attaining a thickness of about 60m. It conformably overlain by the early
Eocene Thebes Formation and underlain by the upper Paleocene Tarawan
Formation.
Thebes Formation:
This formational name was originally proposed and described by Said (1960)
who described this rock unit at its type locality at Gebel Gurnah (opposite Luxor),
Nile Valley, as massive limestone beds with flint bands and nodules conformably
overlying the Esna Formation with gradational boundary. The Eocene rocks have
widely distributed in central and northern parts of Sinai and they conformably
overlie the Esna Formation and in other places unconformably overlie the
Cretaceous rocks. In north - central Sinai, this formation is well exposed in the vast
synclinal areas between Gebel Yelleg and Gebel Halal. Sometimes the Thebes
Formation is referred at other localities with different names as at Gebel Egma in
central Sinai, this flinty limestone, known locally as the Egma Limestone covering
the extensive table land of the Egma plateau.

At Gebel El Bruk area, the Thebes Formation is lithologically represented by
massive, hard limestones with chert bands and nodules, interbedded with marly
limestone (Fig. 2). On the basis of the absence or presence of the chert bands and
nodules, this formation could be subdivided in the field into three units, from base
to top: 1- Lower cherty limestone unit, 2- middle chalky limestone unit moderately
rich with Nummulites, Operculina and Assilina sp. as well as other macrofossils
and 3- an upper cherty limestone unit fossiliferous with Alveolina spp. The
formation attains a thickness of about 34 meters in the studied area. The Thebes
Formation has been dated as early Eocene age as proofed by different authors as;
Youssef 1954; Said 1960 & 1962 & 1990; El Naggar, 1966; and Lűger, 1988; as
well as Berggren & Ouda, 2003.
PLANKTONIC FORAMINIFERAL BIOSTRATIGRAPHY
The global Paleogene foraminiferal biozonation and their subdivision scheme
was previously tackled by different authors. The first pionner work was conducted
by Bolli (1957a, b) in Trinidad, at the Caribbean Sea. In fact, Bolli’s zonation was
accepted and applied by different authors and became base for the other
numerous palnktonic foraminiferal zonation that many authors had followed such
as Blow (1969), Premoli Silva & Bolli (1973), Berggren & Van Couvering (1974),
Stainforth et al. (1975), Toumarkine & Luterbacher (1985), Bolli et al. ,1985;
Berggren & Miller (1988), Aubry (1996 & 1999); Molina et al, (1999); Monechi et al.,
(1999 & 2000); Luterbacher (2004) and others. Later on, some modifications was
carried out on this zonal scheme that proposed by Bolli (op.cit), for example
Berggren & Norris (1997) who studied some locations in the Atlantic, Indian and
Pacific oceans and presented some revised Paleogene zonal scheme that adopted
in this study with some modification. The biozonation used in this study is that
Berggren et al. (1995) with reference to the work of Salis et al. (1998) and
Berggren & Ouda (2003) in Egypt. Recently, Berggren & Pearson (2005) revised
the trpoical and subtropical Eocene planktonic foraminiferal zonation and
introduced sixteen biozones and showed that the Paleocene – Eocene boundary is
correlated with the first occurrence of the Acarinina sibaiyaensis (base of zone E1)
at the top of the truncated and redefiend (former) Zone P5. Table 1 shows some
comparisons and correlation between these different planktonic foraminiferal
subdivisions carried out by different authors.
Several authors have studied the biostratigraphic interval that straddles the
Paleocene – Eocene boundary in Egypt and studied the biostratigraphical and
geochemical changes that influenced this transitional interval. Among these
authors are El Naggar (1966); Hewaidy (1983), Haggag (1991); Sprijer et al.,
(1995), Schimtz et al., (1996) and Salis, et al., (1998), Speijer et al., (1998) Sprijer
et al., (1997) and Samir (2002), respectively. Recently, intensive studies carried out
by Ouda (2003); Ouda et al., (2003); Berggren & Ouda (2003a, b, c) on the
Paleocene – Eocene boundary in some sections in the area of Nile Valley. Most of
these authors showed that the Paleocene – Eocene boundary lies within the Esna
Formation at the level of last appearance of Morozovella velascoensis or first
appearance of Acarinina wilcoxensis and / or Pseudohastigerina wilcoxensis that
matching the P5 / P6a zonal boundary.

Hamad6
The study of the vertical stratigraphic distribution of the planktonic foraminifera
allowed to recognize six palnktonic foraminiferal zones spanning the time interval
form late Paleocene (Thanetian) to early Eocene (Ypresian), they are from base to
top: 1) Globanomalina pseudomenardii (P4), 2) Morozovella velascoensis Zone of
the late Paleocene age (Thanetian) (P5) and 3) Morozovella subbotinae Zone, 4)
Morozovella aragonensis zones of the early Eocene age (Ypresian). The
biostratigraphic results of the planktonic foraminifera at Gebel ElBruk in conjunction
with the biostratigraphic work of calcareous nannofossils of Faris & Zahran (2001)
confirmed that no unconformity could be recorded in the late Paleocene / early
Eocene interval at Gebel El Bruk sequence. From the chemostratigraphical point of
view, it observed that the Paleocene / Eocene boundary coincides with the base of
the Carbon Isotopic Excursion (CIE) that now is accepted and became strong
criterion for the determination of the Paleocene / Eocene boundary (Berggren et al.
1998). This CIE boundary is related to major prominent climatic global changes
and evolutionary turnovers and extinction of biota all over the world and marked by
global warming that called and defined as Paleocene – Eocene Thermal Maximum
(PETM). In the present work, more detailed planktonic foraminiferal analysis
around this boundary was carried out as well as some remakes on the benthonic
foraminiferal association distributed in the section will be refereed.
1- Globanomalina pseudomenardii Zone (P4):
Category: Total range zone.
Author: Bolli (1957a) as Globorotalia pseudomenardii Zone.
Definition: Total range of the nominate taxon Globanomalina pseudomenardii.
Remarks and discussion: In the studied section this zone spans the total
range interval of the Globanomalina pseudomenardii. It is recorded in the whole
Tarawan Chalk and lowermost part of the Esna Shale, covering the stratgraphic
interval from sample no. 1 to sample no. 17. The nominated taxon has sometimes-
erratic and sporadic distribution that may be attributed partial dissolution in some
levels in this interval. This zone conformably underlies the Morozovella
velascoensis Zone at Gebel El Bruk section and assigned to the late Paleocene
(Thanetian) age.
Berggren & Norris (1997) subdivided this zone on the basis of the first
occurrence of Acarinina nitida and Ac. subsphaerica that coincides with the first
occurrence of Globanomalina pseudomenardii into the following subzones from
base to top: (1) Globanomalina pseudomenardii / Acarinina subsphaerica
concurrent range subzone (P4a), (2) Acarinina subsphaerica / Muricoglobigerina
soldadoensis interval subzone (P4b) and (3) Muricoglobigerina (Acarinina)
soldadoensis / Globanomalina pseudomenardii interval subzone (P4c). This
tripartite subdivision is well recognized and easily to trace in this study. In the
following are the main features recognized in these subzones.
2- Globanomalina pseudomenardii / Acarinina subsphaerica concurrent
range Subzone (P4a):
Category: Concurrent range zone
Author: Berggren & Norris (1997)

Definition: Concurrent Interval of the two nominate taxa between the first
occurrence of Globanomalina pseudomenardii and the last occurrence of Acarinina
subsphaerica.
Remarks: This subzone is recorded in the lowermost part of the Tarawan
Formation, covering the stratigraphic interval from sample no. 1 to 5 and attining
thickness of 6m. It is characterized by great diversity and frequency of planktonic
foraminifera, among the recorded angular morozovillids are Morozovella angulata,
M. acuta, M. conicotruncata. Acrininids are rarely recorded and represented by
Acarinina primitiva, where Muricoglobigerinids; Muricoglobigerina mckannai. The
Subbotinids are recorded in the form of Subbotina triloculinoides and S.
velascoensis as well as Globanomalina pseudomenardii and Igorina albeari (Fig.2).
3- Acarinina subsphaerica / Muricoglobigerina (Acarinina) soldadoensis
interval Subzone (P4b):
Category: Interval Subzone
Definition: Biosstratigraphic interval from the last occurrence of Acarinina
subsphaerica to the first occurrence of Muricoglobigerina (Acarinina) soldadoensis.
Author: Berggren & Norris (1997).
Remarks: This subzone is recorded in the upperrmost part of the Tarawan and
the lowermost part of the Esna Formations at Gaba El Bruk, covering the
stratigraphic interval from sample no. 6 to 12, attining 6m in thickness and
characterized by the following planktonic foraminifera: Igorina pusilla, Ig. albeari,
Acarinina nitida, Muricoglobigerina (Acarinina) mckannai, Morozovella
velascoensis, angulata, M. aequa (That makes it first occurrence at the upper
bounary of this subzone), M. acuta, Globanomalina pseudomenardii, Subbotina
triangularis and S. velascoensis.
4- Muricoglobigerina (Acarinina) soldadoensis/Globanomalina
pseudomenardii interval Subzone (P4c):
Definition: Biosstratigraphic interval from the first occurrence of
Muricoglobigerina (Acarinina) soldadoensis to the last occurrence of
Globanomalina pseudomenardii. and the last occurrence of Acarinina mckannai as
well as the first occurrence of Morozovella subbotinae.
Author: Berggren & Norris (1997).
Remarks: This subzone is approximately recorded in the lowermost to middle
part of the Esna Formation at Gaba El Bruk, covering the stratigraphic interval from
sample no. 13 to 17, attaining 5m in thickness and characterized by the following
planktonic foraminifera: Acarinina nitida, Mg. Mckannai (makes its last occurrence
at the top of this zone), Morozovella velascoensis, M. angulata, M. subbotinae
(That makes it first occurrence at the upper boundary of this subzone),
Globanomalina pseudomenardii, and Subbotina velascoensis. Regarding the
benthonic foraminifera association, this zone is dominated with mixed Midway

Hamad8
Gl.pseudomenardii
M.angulata
Ac.subsphaerica
Ac..primitiva
M.gracilis
M.subbotinae
Ac.whitei
Mg.senni
M.acuta
Ig.albeari
Ac.wilcoxensis
M.conicotruncana
Ac.nitida
Mg.mckannai
Mg.soldadoensis
S.triangularis
M.aragonensis
M.acuta
M.marginodenta
Mg.esnehensis
Ac.sibaiyaenis
Ac.africana
Ig.brodermanni
Ps.wilcoxensis
M.lensiformis
M.edgari
Stratigraphic Distribution of the planktonic foraminifera
Gr= Globorotalia
Pl= Planorotalites
M= Morozovella
Mg.=Muricoglobigerina
Ig= Igorina
S= Subbotina
Ac= Acarinina
Gl= Globanomalina
Sandy Limestone
Dissolution clay layer
Chalky Limestone
Dolomitic Limestone
Argillaceous Limestone
Calcareous Shale
Ac.pentacamerata
M.querta
Ac.acarinata
CIE Interval
.
.
Limestone
S.velascoensis
Ig.pusilla
M.velascoensis
M.formosagracilis
.
.
.
(outer neritic conditions) and Velasco – types (upper bathyal environments),
among the benthonic foraminifera recorded in this zone are: Siphogenerinoieds
eleganata, Bulimina qaudrata, Spiroplectinella dentata, Alabamina wilcoxensis,
Lenticulina midwayensis (Tarawan Formation), Vlavulinerina scrobiculata,
Angulogavelinella avnimelechi, Neofalbellina jarvisi, Cibicidoides pseudoacutus,
Tritaxia midwayensis, Loxostomum applinae, Cibicidoides hyphalus, Gavelinella
beccariformis and Nuttalides truempyi that recored in the basal part of the Esna
Formation.
On the global scale the Globanomalina pseudomenardii Zone (totally from P4a
to P4c) at Gabal El Bruk could be correlated with Globorotalia pseudomenardii
Zone of Bolli (1957 &1966), Premoli Silva & Bolli (1973), Stainforth et al. (1975),
Blow (1979) and equated with Planorotalites pseudomenardii Zone of Toumarkine
& Luterbacher (1985), Berggren et al (1995); Canudo & Molina (1993); Arenillas &
Molina, (1996); Pardo et al., 1999 , Arenillas et al., 1999 as well as to P4 Zone of
and Olsson et. al. (1999) and Berggren & Ouda (2003). In Egypt, this zone could
equated with Globorotalia pseudomenardii Zone of Beckmann et al. (1969), to
Planorotalites pseudomenardii Zone of Aref et al. (1988) and to the Globanomalina
pseudomenardii Zone of Aref & Youssef (2001), Salis et al. (1998) and El Nady &
Shahin (2001) and Samir (2002) as well as El Nady (2006) (Table.1).
Paleocene
ThanetianYpresian
c
ThebesFormation
NP12NP11NP5
M.formosa
formosaP7
Gl.pseudomenardii(P4)
Eoene
45
44
43
42
41
40
39
38
37
36
36
35
34
33
32
31
30
29
28
27
26
25
24
23
22
21
20
19
18
17
16
15
14
13
12
11
10
9
8
7
6
5
4
3
2
1
M.aragonensis
P8
SampleNo.
Plank.
zones
Age
Age
Rock
unit
NP4
Tarawan
Formation
Stratigraphic distribution of planktonic foraminifera
.
.
..
.
.
..
..
P4aP4b
M.aequa
M.formosaformosa
Mg.soldadoensisangulosa
EsnaFormation
NP10NP9NP7/8
M.velascoensisM.
subbotinae
P6b
~ ~ ~ ~
P4cP5a
M.edgari
P6aP5b
EsnaFormation
NP10NP9NP7/8
M.velascoensisM.
subbotinae
P6b
~ ~ ~ ~
P4cP5a
M.edgari
P6aP5b
Ac.pseuedotopilensis
S.linaperta
M.caucasica
S.finlayi
M.occlusa
... ..
0
12m
6
Cherty Limestone .. ..
CIE Interval
Fig.2: Planktonic foraminiferal distribution chart of Gabal El Bruk, north-central Sinai,
Egypt

5- Morozovella velascoensis Zone (P5):
Category: Partial range zone.
Author: Bolli (1957).
Definition: This zone represents the biostratigraphic interval of the partial
range of Morozovella velascoensis, where its lower boundary is defined by the last
occurrence of Globanomalina pseudomenardii and its upper boundary is
delineated by to the last occurrence of Morozovella velascoensis.
Remarks and discussion: In the present study this partial range zone has
different notations and is defined as interval from the last occurrence of
Globanomalina pseudomenardii at base to the last occurrence of Morozovella
velascoensis at top or from the first occurrence of Morozovella subbotinae to the
last occurrence of the nominated taxon. This zone is recorded in the middle part of
the Esna Formation, covering the stratigraphic interval form sample no.18 to
sample no. 26, measuring a thickness of 20 meters. It conformably overlies the
Globanomalina pseudomenardii Zone (P4) and underlies conformably the
Morozovella edgari Zone and assigned to the late Paleocene (Thanetian) to early
Eocene age. It is noteworthy of mention that this zone is characterized by distinct
turnover in the planktonic foraminiferal turnover in the diversity and relative
abundance of the planktonic taxa. Moreover, the Paleocene / Eocene boundary is
located within it. The most characteristic planktonic foraminiferal species that make
their first appearance in this zone are the following: Igorina brodermanni, M.
subbotinae, M. velascoensis, M. gracilis, M. marginodetata, M. edgari, M. primitiva,
Subbotina triloculinoides, S. velascoensis, S. linaperta, Muricoglobigerina
(Acarinina) esnahensis, Mg. soldadoensis, Acarinina africana, A. sibaiyaensis,
Acarinina nitida, A. whitei, A. wilcoxensis.
Correlating the nominated zone with the other world wide planktonic
foraminiferal zones, it corresponds to the Globorotalia velascoensis Zone of Bolli
(1957&1966), and coeval with the Morozovella velascoensis Zone recorded by
Toumarkine & Luterbacher (1985) and also could be matched with Morozovella
velascoensis Zone of Premoli Silva & Bolli (1973), Canudo et al., (1995); Molina et
al. (1999), Pardo et al., (1999). Moreover, this zone could be equated to the
combined P5 and P6a Zones of Berggren & Miller (1988) It also equivalent to the
Morozovella velascoensis Zone (P5) of Berggren et al. (1995), and to the Igorina
laevigata and Morozovella velascoensis Zones of Arenillas & Molina (1996). In
Egypt this zone could be correlated with the Morozovella velascoensis of Salis et
al. (1998) in Nile Valley, Egypt as well as equivalent to M. velascoensis Zone of El
Nady & Shahin (2001) and Samir (2002) in Gebel Samra, West - Central Sinai, and
to the Morozovella velascoensis Zone (P5) of Berggren & Ouda (2003) in the
Dababyia section, Upper Nile Valley, Egypt.
It is noteworthy of mention that the M. velascoensis Zone (P5) has been
subjected to different attempts of subdivisions. Arenillas & Molina (1996) studied
the Paleocene / Eocene transition in Alamedilla, Spain and showed that the long
ranging of the M. velascoensis and stated that M. velascoensis could be extended
beyond the Paleocene / Eocene boundary as well as the extinction of the Igorina
laevigata coincides with the BEE event. They also considered that the last
occurrence of Igorina laevigata as criterion for the determination of the Paleocene /

Hamad10
Eocene boundary and subdivided the P / E transition in Alamedilla into two
subzones, from base to top: 1) Igorina laevigata late Paleocene) and 2) M.
velascoensis zone (early Eocene) Berggren & Norris (1997) considered that Igorina
laevigata may be junior synonym of Igorina albeari. Tantawy (1998) in the Nile
Valley of Egypt emended the Igorina laevigata Zone of Arenillas & Molina (op.cit).
Pardo et al. (1999) subdivided the Morozovella velascoensis zone (P5) on the
basis of the first occurrence of Acarinina sibaiyaensis into two subzones form base
to top: (1) Luterbacher pseudomenardii / Acarinina sibaiyaensis (P5a) and (2)
Acarinina sibaiyaensis / Morozovella velascoensis subzone (P5b). Molina et. al.
(1999) and Arenillas & Molina (2000) studied the P/ E transition at Zumaya, Spain
and suggested five subzones for the Morozovella velascoensis Zone (P5), from
base to top are: 1- Morozovella aequa 2- Morozovella gracilis 3- Acarinina
berggerni 4- Acarinina sibaiyensis 5- Pseudohastigerina wilcoxensis. Speijer et al.
(2000) proposed three – fold subdivision of the Zone P5 as follows (from base): 1-
Globanomalina chapmani 2- Morozovella allisonensis 3- Globanomalina luxorensis
subzones. In Egypt, especially in the Nile Valley region Salis et al. (1998) and Aref
& Yousef (2000) subdivided the P5 Zone into two zones: a lower Igorina laevigata
and an upper Globanomalina luxorensis. Berggren & Ouda (2003a) considered
that Igorina laevigata might be a junior synonym of Igorina albeari and studied the
P/ E boundaery the in Dababyia section, Upper Nile Valley, Egypt, and emended
the Morozovella velascoensis Interval Zone. They subdivided it into three subzones
from base to top: 1- Globanomalina pseudomenardii / Acarinina sibaiyaensis
Subzone, 2- Acarinina sibaiyaensis / Pseudohastigerina wilcoxensis Subzone and
3- Pseudohastigerina wilcoxensis / Morozovella velascoensis Subzone. More
recently Berggren & Pearson (2005) correlated the Paleocene – Eocene boundary
with the first occurrence of Acarinina sibaiyaensis. In the studied area of Gabal El
Bruk, due to the absence of Glaboanomalina luxorensis, the present author
subdivided the Morozovella velascoensis Zone into two subzones, on the basis of
the appearance and disappearance of Acarinina sibaiyaensis, from base to top: 1-
Globanomalina pseudomenardii / Acarinina sibaiyaensis Subzone (P5a) and 2-
Acarinina sibaiyaensis / Morozovella velascoensis Subzone (P5b). In the following
are the main faunal features of these subzones.
6- Globanomalina pseudomenardii / Acarinina sibaiyaensis Interval Subzone
(P5a):
Category: Interval subzone
Author: Berggren & Ouda (2003)
Definition: This subzone represents the biostratigraphic interval from the last
occurrence of the Globanomalina pseudomenardii to the first occurrence of the
Acarinina sibaiyaensis.
Remarks: This subzone is approximately occurred in the middle part of the
Esna Formation, covering the stratigraphic interval from sample no. 18 to 24,
attaining 13m in thickness. It is characterized by occurrence the following
planktonic foraminifera taxa: Acarinina nitida, Ac. esnahensis, Ac. mckannai, Ac.
wilcoxensis, Ac. primitiva, Morozovella velascoensis, M. gracilis, M. occlusa, M.
subbotinae, M. edgari, M. acuta, and Subbotina velascoensis. The nominated
subzone could be correlated with the lower part of Morozovella (Globorotalia)

velascoensis Zone of Bolli (1957) and Toumarkine & Luterbacher (1985) as well as
Berggren et al. (1995). It equivalent to Igorina laevigata Zone of Arenillas & Moilna
(1996) and equated to Globanomalina pseudomenardii / Acarinina sibaiyaensis of
Pardo et al. (1999). And to Globanomalina pseudomenardii / Acarinina sibaiyaensis
of Berggren & Ouda (2003).
It is worthy of mention that the typical late Paleocene benthonic foraminiferal
species that recorded in the Esna Formation and corresponding to subzone (P5a),
contains some cosmopolitian taxa. Among them are: Gavelinella beccariformis,
Angulgavelinella avnimelechi, Coryphostoma midwayensis, Neoflabellina jarvisi,
Bulimina midwayensis, Osangularia velascoensis, Stilostomella midwayensis,
Gyroidinoides quadratus, Alabamina wilcoxensis, Aragonia velascoensis. The
occurrence of these taxa in the Globanomalina pseudomenardii / Acarinina
sibaiyaensis subzone (P5a) indiacte a predominance of outer neritic shallow
marine environments. The extinction of these benthonic taxa toward the top of this
subzone (sample 23) confirm the location of the Paleocene – Eocene boundary in
the Esna Formation and strongly reflect regressive phase in the uppermost part of
this subzone. This phase could be related to tectonic activity during the Paleocene
time (Velascoensis event) of Strougo (1986) and may be correlated with the
eustatic sea - level fluctuation change of Haq et al. (1987)
7- Acarinina sibaiyaensis / Morozovella velascoensis Interval Subzone (P5b):
Author: Berggren & Ouda (2003) emended here as Acarinina sibaiyaensis /
Morozovella velascoensis Subzone.
Definition: This subzone represents the biostratigraphic interval from the first
occurrence of the Acarinina sibaiyaensis to the last occurrence of the Morozovella
velascoensis.
Remarks: This subzone is approximately recorded in the topmost of the middle
part of the Esna Formation at Gabal El Bruk, covering the stratigraphic interval
from sample no. 24 to 27, attaining 4m in thickness and characterized by
occurrence of the following planktonic foraminiferal assemblage: Acarinina
africana, Ac. acarinata, Ac. wilcoxensis, Ac. triplex, Ac. soldadoensis, Ac.
sibaiyaensis, Morozovella velascoensis, M. gracilis, M. subbotinae, M. edgari, and
S. triangularis. The nominated subzone could be correlated with the upper part of
Morozovella (Globorotalia) velascoensis Zone of Bolli (1957) and Toumarkine &
Luterbacher (1985) as well as Berggren et al. (1995). It is equivalent to
Morozovella velascoensis Zone of Arenillas & Moilna (1996) and equated to
Acarinina sibaiyaensis / Morozovella velascoensis of Pardo et al. (1999). And to
Pseudohastigerina wilcoxensis/ Acarinina sibaiyaensisand Pseudohastigerina
wilcoxensis/ Morozovella velascoensis of Berggren & Ouda (2003).
It is noted that large number of the late plaeocene benthonic foraminiferal taxa
that previously recorded in Globanomalina pseudomenardii / Acarinina sibaiyaensis
Subzone (P5a) became extinct in this subzone (Acarinina sibaiyaensis /
Morozovella velascoensis Subzone) and replaced by newly appearing taxa such as
Aragonia aragonensis, Bulimina tuxpamensis and Globocassidulina subglobosa
(sample 25). This makes our results in accordance with those of Ortiz (1995).

Hamad12
Table 1 . Correlation of the late Paleocene / early Eocene planktonic foraminiferal biozones with biozonation
used in this study
EoceneEocenePaleocenePaleocene
YpresianYpresianThanetianThanetian
Gr.
velascoensis
Gr.
subbotinae
Gr.
formosa
Gr.
pseudomenardii
Bolli
(1957
& 1966)
M.
formosa
M.
subbotinae
M. edgari
M.
velascoensis
Pl..
pseudomenardii
Toumarkine&
Luterbacher
(1985)
Gr.wilcoxensis
berggreni
P7
Gr.subbotinae
Gr. velascoensis
acuta
P6
Gr.soldadoensis/
Gr.pasionensis
P5Blow
(1979)
M.
aequaPs.wilcoxensis
Canudo &
Molina
(1992)
Pl.
pseudomenardii
P4
M.subbotinae
P6
M.
formosa
M.velascoensis
M.fromosa
P6a
Berggren
et al.
(1995)
M.
velascoensis
P5
Gl.pseudomenardii
Ig.
laevigata
M.
subbotinae
Arenillas
&
Molina
(1996)
Gl.pseudomenardii
Ps. wilcoxensis
M.velascoensis
M. formosa
Gl.pseudomenardii
P4
M. formosa
formosa P7
Present
study
Age
Age
Gr.
aragonensis
Gr.
aragonensis
Gl.(Pl.)
pseudomenardii
M.
velascoensis
P5
M.
formosa
Mg.
soldandoensis
Pardo
et al.
(1999)
M.subbotinae
P6
M.
formosa
M.velascoensis
M.fromosa
P6a
M.velascoensis
P5
A.sibaiyensis/
M.velascoensis
P5b
P.pseuodomenardii
A.sibaiyensis/
P5a
Gl.pseudomenardii
P4
Molina
et al.
(1999)
M.subbotinae
M.
edgari
M.
formosa
M.subbotinae
M.velascoensis
Ps.
wilcoxensis
Ac.
sibaiyensis
M.
gracilis
M.
aequa
Mg.soldandoensis
M.
aragonensis
M.
aragonensis
M.
aragonensis
M.
subbotinae
P6b
M. edgari
P6a
M.velascoensis
P5
M.
subbotinae
M.
aragonensis
P8
M.
edgari
Ps. wilcoxensis
Ac. sibaiyensis
Gl.pseudomenardii
Ac.sibaiyensis
Ac.
berggerni
Gl.pseudomenardii
Ac.sibaiyensis
M.velascoensis
Ac.sibaiyensis
Berggren
& Ouda
(2003)
M.
aragonensis
P8
Gl.pseudomenardii
Ac.subspherica
Ac.subspherica
Ac.soldadoensis
Ac.soldadoensis
Gl.pseudomenardii
Ac.soldadoensis
Gl.Pseudomenardii
P4c
M.
formosa
Gr= Globorotalia Pl= Planorotalites M= Morozovella Mg.=Muricoglobigerina
Ig= Igorina S= Subbotina Ac= Acarinina Gl= Globanomalina

8- Morozovella edgari Zone (P6a):
Category: Interval zone.
Author: Premoli Silva & Bolli (1973) and Toumarkine & Luterbacher (1985)
Definition: Biostratigraphic interval between the last occurrence of
Morozovella velascoensis to the last occurrence of the nominate taxon.
Remarks: In the study area, this zone is recorded in upper part of the Esna
Formation, covering the startigraphic interval from sample no. 27 to sample no. 30,
spanning a thickness of 10 m. It is assigned in this study to the early early Eocene
(early Ypresian) age. Faunaistically, thiz zone is characterized by distinct planktic
foraminiferal association and the first appearance of the following taxa:
Morozovella formosa gracilis, M. lensiformis, Acarinina pseudotoplensis,
Pseudohastigerina wilcoxensis, Acarinina soldadoensis angulosa, together with the
common occurrence of the following taxa: Morozovella edgari (that makes its last
occurrence at the top of this zone), M. maginodentata, M. aequa, M. subbotinae,
M. acuta (disappaered in the middle of this zone), M. quetra, M. gracilis, Subbotina
linaperta, Acarinina esnahensis, Ac. wilcoxensis, Ac. nitida and others (Fig. 2).
This zone could equated with the lower part of Globorotalia subbotinae Zone of
Bolli (1957 & 1966), to the lower part of Morozovella subbotinae Zone of Arenillas
& Molina (1996). It is equivalent to Globorotalia aequa Zone of Luterbacher (1964),
to the lower part of the Globorotalia subbotinae Zone of Stainforth et al. (1975) and
the lower part of the Subzone P6b (Globorotalia subbotinae / Pseudohastigerina
wilcoxensis) of Berggren & Van Couvering (1974). Moreover, It could be matched
with the lower part of P6a Subzone of Berggren et al. (1995) and to Morozovella
edgari zone of Molina et al. (1999) and Berggren & Ouda (2003). In the
Mediterranean relam. It is equivalent to the Morozovella edgari Zone of
Toumarkine & Luterbacher (1985). Locally in Egypt this zone corresponds to the
Morozovella edgari Zone of Salis et al. (1998) in Nile valley, South Egypt. It could
be matched with Morozovella edagri Zone of Aref et al. (1988) and Aref & youssef
(2001) as well as the lower part of Morozovella subbotinae Zone of Samir (2002) in
south - western Sinai, Egypt. It could be matched with Morozovella edgari Zone of
El Nady & Shahin (2001) and El Nady (2005).
9- Morozovella subbotinae Zone (P6b):
Category: Partial range zone
Author: Luterbacher & Premoli Silva (1975).
Definition: Berggren & Noris (1997) defined this zone as interval characterized
by the partial range of the nominate taxon between the last occurrence of
Morozovella velascoensis to the first occurrence of Morozovella aragoensis. But in
the present work it is represented by the biostratigraphic interval between the last
occurrence of the Morozovella edgari and first occurrence of Morozovella
aragonensis or Morozovella formosa formosa.
Remarks: This zone is located in the uppermost part of Esna Formation and
covering the stratigraphic interval from sample no. 30 to 34, attaining a thickness of
12 m. It conformably overlies the Morozovella edgari Zone and underlies the
Morozovella formosa formosa Zone (Fig. 2). This zone is characterized by
occurrence of the following planktic foraminifera species: Morozovella subbotinae,
M. formosa gracilis, M. marginodentata, M. aequa, M. acuta, M. lensiformis,

Hamad14
Acarinina wilcoxensis, Ac. soldadoensis soldadoensis, Ac. pseudotoplensis, Ac.
triplex, Subbotina velascoensis, S. eocanica and Ac. acarinata. Due to the
forementioned palnktonic foraminiferal assemblage, this zone is assigned here to
the early Eocene (Ypresian).
Based on the planktonic foraminiferal assemblage, the Morozovella subbotinae
Zone could be correlated with the upper part of Globorotalia rex (synonym of
Morozovella subbotinae) Zone of Bolli (1957 &1966), to Globorotalia subbotinae
Zone of Premoli Silva & Bolli (1973) and Toumarkine & Luterbacher (1985), to
upper part of Globorotalia wilcoxensis berggerni Zone of Blow (1979). It could be
matched with middle part of Morozovella subbotinae Zone (Morozovella
velascoensis / Morozovella formosa subzone) of Berggren et al. (1995), to the
Morozovella subbotinae Zone of Molina et al. (1999) and Berggren & Ouda (2003).
to the Morozovella subbotinae Zone of Salis et al. (1998). In Egypt, the nominated
zone could be equivalent to the upper part of Globorotalia subbotinae Zone of
Beckmann et al. (1969), to the Morozovella subbotinae Zone of Aref et al. (1988),
Aref & Youssef (2001) and to the M. subbotinae Zone of Salis et al. (1998) as well
as upper part of the M. subbotinae Zone of Samir (2002). It could be matched also
with M. subbotinae Zone of Obaidallah (2000), El Nady & Shahin (2001) and El
Nady (2005)
Pre - CIE
Interval
Clay bed
Calcareous
Shale/
marl bed
Post - CIE
Interval
CIE Interval
(1m)
P5aP5b
MorozovellavelascoensisZone
Esna
Shale
Shale layer rich
in pellets
Esna
Shale
27.1
27.0
26.9
26.8
26.7
26.5
26.4
26.3
26.2
26.1
25.0
24.9
24.8
24.7
24.6
24.5
24.4
24.3
24.2
24.1
24
23.9
23.8
23
23.6
23.5
23.4
23.3
23.2
Unfossiliferous clay
bed with
slightly benthonic
Fossiliferous
shale/
marl bed
with low
oxygen
fossiliferous
Shale with
planktonic
forams
fossiliferous
Shale with
planktonic
forams
Morozovellavelascoensis
Ac.sibaiyaensis
Mg.esnahensis
M.gracilis
Ac.africana
Mg.soldadoensis
Marly bed Unfossiliferous clay
P6a
Morozovellaedgari
S.velascoensis
Ps.wilcoxensis
Ig.lodoensis
M.quetra
M.edgari
Fig. 3. Diagrammatic section showing the location of CIE interval at Gabal El Bruk,
north - central Sinai, Egypt

10- Morozovella formosa formosa Zone (P7):
Author: Bolli (1957a)
Definition: This zone is biostratigraphically, but not nomenclaturally,
equivalent to the Morozovella formosa-Morozovella lensiformis Subzone (P8a) of
Blow (1979). It has also been recognized as the Morozovella formosa-Morozovella
lensiformis Partial- range Subzone (P6c) of Berggren and Miller, 1988; the Morozo
vella formosa formosa/Morozovella lensiformis-Morozovella aragonensis Interval
Zone (P6b) of Berggren and others (1995) In the present work it represented by
biostratigraphic interval from the first occurrence of the Morozovella aragoensis to
the first occurrence of Acarinina pentacamerata.
Remarks: This zone is recorded in the lower part of the Thebes Formation,
attaining a thickness of 16 meters and covering the stratigraphic interval from
sample no. 34 to sample no. 40. This zone conformably overlies the Morozovella
subbotinae Zone and conformably underlies the Morozovella aragonensis Zone
(Fig. 2). It is assigned to the early Eocene (Ypresian). This zone is characterized by
abunadnce of planktonic forams: Morozovella subbotinae, M. aquea, M. formosa
formosa, M. marginodentata, M. lensiformis, M. formosa gracilis, M. aragoensis.
The Acarinindes are represented by: Acarinina nitida, Ac. primitiva, while
Muricoglobigerinids are presented by: Mg. soldadoensis soldadoensis, Mg.
soldadoensis angulosa and the subotininds by: Subbotina linaperta, along with the
last occurrence of the following taxa: Mg. esnahensis, A. wilcoxensis, M.
lensiformis, Ac. pseudotoplensis.
The Morozovella formosa formosa Zone could be correlated with Globorotalia
formosa Zone of Bolli (1957 & 1966) & Blow (1979), to the Morozovella formosa
Zone of Toumarkine & Luterbacher (1985). Moreover, it could be equated with the
M. formosa (P7) Zone of Berggren et al. (1995); Arenillas & Molina (1996); Pardo
et al., (1999) and Molina et al., (1999). In Egypt, it coincides with Globorotalia
formosa Zone of Beckmann et al. (1969), to the Morozovella formosa Zone of Aref
et al. (1988), Aref & Youssef (2001) and Salis et al. (1998) as well as M. formosa
Zone of El Nady & Shahin (2001) in Central and Northern Sinai.
11- Morozovella aragonensis Zone (P8):
Author: Bolli (1957a)
Definition: Biostratigraphic interval from the first occurrence of the Acarinina
pentacamerata to the last appearance of the Eocene planktonic foraminifera in the
studied section.
Remarks: In the present study this zone is recorded in the uppermost part of
the Thebes Formation, attaining a thickness of 12 meters and covering the
stratigraphic interval from sample no. 40 to sample no. 45. This zone conformably
overlies the M. formosa formosa Zone (Fig. 2). It is assigned here to the early
Eocene (Ypresian) age. Among the recorded planktonic foraminifera taxa in this
zone are Morozovella aragonensis, M. subbotinae, M. quetra, M. formosa formosa,
Subbotina linaperta, Acarinina pentacamerata, Ac. acarinata, Igorina brodermanni,
Muricoglobigerina soldadoensis soldadoensis, Mg. soldadoensis angulosa.
On the worldwide correlation and on the basis of the planktonic foraminiferal
association, the Morozovella aragonensis Zone could be matched with Globorotalia

Hamad16
aragonensis Zone of Bolli (1957a), and Premoli Silva & Bolli (1973), to Globorotalia
aragonensis (P9) Zone of Blow (1979), to the Morozovella aragonensis Zone of
Toumarkine & Luterbacher (1985). Moreover, it could be equated with the P8 Zone
of Berggren et al. (1995) and Molina et al., (1999). In Egypt, this zone could be
equivalent to the Globorotalia aragonensis Zone of Beckmann et al. (1969), It could
be equated with the Morozovella aragonensis Zone Aref et al. (1988); Salis et al.
(1998), Aref & Youssef (2001) and to M. aragonensis Zone of El Nady & Shahin
(2001) (see Table. 1).
THE PALEOCENE / EOCENE PLANKTONIC FORAMINIFERAL
TURNOVER EVENT IN THE STUDY AREA
The end of the Paleocene and starting of Eocene (~55.5 Ma) was distiguished
by one of the most significant periods of global change during the Cenozoic, where
sudden global warming events recorded in geologic history, currently being
identified as the 'Paleocene-Eocene Thermal Maximum’ PETM), which upset
oceanic and atmospheric circulation and led to the extinction of numerous deep-
sea benthonic foraminifera (Haq et al., 1988; Zachos et al. 1993; Berggren et al,
1995;) .
The Paleocene – Eocene boundary transition and their most relvant events
have been studied by numerous workers. Some of them such as Bolli, 1957; Bolli &
Premoli Silva, 1975; Stainforth et al., 1975; Toumarkine & Luterbacher, 1985; and
Luterbacher, 2000, identified the P / E boundary on the basis of the last occurrence
of the Morozovella velascoensis. Others assumed to be coincident with the first
occurrence of the Pseudohastigerina wilcoxensis (Berggern et al., 1967; Berggren
& Miller, 1980, Olsson et al., 1999) but later on, both datums appeared to be
diachronous (Molina et al., 1992, Lu & Keller, 1993; Pardo et al., 1994, 1995;
Speijer, 1994) . According to Berggren et al., (1995) the P / E boundary is
bracketed by the Benthonic Extinction Event (BEE) and the last occurrence of
Morozovella velascoensis. The planktonic foraminiferal turnover across the P / E
boundary has been recently studied by different authors (Canudo et al., 1995;
Molina et al., 1997, Lu &Keller, 1995; Berggren & Abury 1996; Aubry et al. 1996
and Berggren et al., 2003) and most of them proposed a number of global
changes or distinct bioevents that have been occurred across or bracketed this
boundary in the world, reflecting drastic sea level changes during this time interval.
The working Group Committee (Aubry, 2000), later accepted these bioevnets.
Among these criteria for denotation of this interval are the following:
1- Occurrence of planktonic foraminiferal turnover that accompanied by
appearance and disappearance of some planktonic foraminiferal species e.g. the
last occurrence of the Morozovella velascoensis, that makes the P5/P6 zonal
boundary Berggren et al., (1995).
2- The NP9 / NP10 of the calcareous nannoplankton zonal boundary that
equivalent to the first occurrence of Tribarchitus bramlettei (index species for the
base of Zone NP10) and last occurrence of Discoaster multiradiatus (Aubry et al.,
1996 & 1998).
3- The δ C13
excursion or Carbon Isotopic Excrusion (CIE) that means
negative excursion in the isotopic composition of the total dissolved inorganic
carbon (Stott & Kenneett, 1990, 1991; Schmitz et al., 1997).

4- The Benthonic Foraminiferal Extinction Event (BEE), a major tunover in
bathyal and abyssal benthonic foraminiferal fauna (Miller et al. 1987, Thomas
1990, Speijer et al., 1996; Pardo et al., 1997) and coorelative with the last
occurrence of the Stensionia beccariiforms assemblage.
In Egypt, the Paleocene – Eocene boundary has been traditionally placed by
the planktonic foraminiferal specialists at the level of the last occurrence of
Morozovella velascoensis or the first occurrence of the Pseudohastigerina
wilcoxensis (El Naggar, 1966;Hewaidy, 1983; Masters, 1984; Strougo, 1986;
Haggag, 1993; El Heiny & Morsi, 1995; Shahin, 1998; Tantawy, 1998; Marzouk &
Luning, 1998; Obedaillah, 1999 & 2000; ; El Nady & Shahin, 2001; Saad, 2001; El
Nady & Shahin, 2001; Scheibner et al., 2001 & 2002; Samir, 2002; El Nady 1995 &
2005 & 2006). Others studied the P – E boundary such as: Salis et al., (1998);
Speijer et al., (1995); Aref & Youssef, (2000) and placed this boundary between
the Igorina laevigata Zone at base (late Paleocene, Thanetian) and the
Globanomlina luxorensis Zone at top (early Eocene,Ypresian). Berggren & Ouda
(2003b) emended the Morozovella velascoensis Zone in the Dababyia section, Nile
Valley, Egypt, and subdivided it into three subzones on the basis of the last
occurrence of Globanomalina pseudomenardii and Morozovella velascoensis and
the first occurrence of Acarinina sibaiyaensis.
The P / E boundary in the studied area is gradational (could be correled with
the P5 / P6a zonal boundary by planktonic foraminiferal specialists). Detailed
investigations at Gabal El Bruk section revealed occurrence of prominent 2m,
yellowish gray marl bed contaning a reddish gray dissolution clay bed of 30cm in
thickness (it is usually of phosphatic composition and is poorly fossiliferous in
planktonic and benthonic foraminiferal taxa). This sapropelic dissolution clay bed
may represent the P / E boundary event in Gabal El Bruk section. In the studied
section the Paleocene – Eocene boundary is located within the Esna Formation
and placed within the Morozovella velascoensis Zone, more precisely between the
Globanomalina pseudomeanradii / Acarinina sibaiyaensis and Acarinina
sibaiyaensis / Morozovella velascoensis subzonal boundary (Fig.2). The Paleocene
- Eocene boundary herein is characterized by palnktonic foraminiferal turnover
event, including the extinction and appearance or origination of species and also
distinct gradual change in their relative abundance and diversity. The planktonic
foraminiferal faunal turnover that recorded in Gabal El Bruk section shows great
resemblances to that of Alamedilla (Molina et al., 1996) and Zumaya, Carvaca
(Canudo et al., 1995) in southern Spain and also of that Shain & El Nady (2001)
from Egypt. Figure 4 shows that the quantititaive analysis of the planktonic
foraminiferal association across the P / E boundary and indicate significant
environmental changes acroos it. The planktonic foraminiferal tunover is
distinguished by a major increase in the low / high latitude ratio (low latitude warm
water species / high latitude cool water species) that reflect warm water
environments. This paleoecological inference is also indicated by the high species
richness and high abundance of morozovilles and low latitiude, compressed
tropical to subtropical acarininides (55%) that increased just below the P/E
boundary transition and reached its maximum just above the clay bed (P/E
boundary). This may termed as acrininid incrusion (acrininids maximum diversity
that coincides with the benthonic mass extinction, BEE). This analysis also showed

Hamad18
low richness of the low abundance of high latitudes cooler water subbotinides
(20%) and muricoglobigeinids (5%) that suggests warm water environments in the
studied section.
The dominant components at the studied section that noticed within the
Paleocene - Eocene planktonic foraminiferal turnover are the great existence of the
genus Morozovella (both large and small morozovilleds) with total combined
relative abundance of 50% and this well depicted in the realtive abundance
besides the species diversity. This relative abundance of low latitudes surface
dewellers decrease above the P / E boundary (Sapropleic clay bed), definitly above
the Acarinina sibaiyaensis / Morozovella velascoensis Interval subzone (in P5a
Subzone), where it reaches 30% in the late Paleocene and 50% in the begining
early Eocene. This decreasing upwards could be related to the declination of the
large morozovellids (Morozovella acuta, M. velascoensis, M. occlusa, M. parva).
On the other hand the small morozovellids (Morozovella subbotinae, M. aequa, M.
gracilis, M. marginodetata, M. edgari and M. lensiformis) that become more
abundant in the early Eocene (P6a and P6b). Figure 4 also shows the gradual
dissappearence (extinction) and orginination of some morozovilleds across the P /
E boundary such as extinction of late Paleocene taxa: Morozovella angulata, M.
conicotruncata, M. acutispira Acarinina mckannai, Igorina pusilla pusilla and
Globanomalina pseudomenardii., Acarinina subspherica,. Some are therived and
persisted through the P/ E boundary as Morozovella subbotinae, M. aequa,
M.edgari and survived in the P6a zone. Other morozovilleds are evolved and
therived in P7 and P8, but in relatively low abundance such as Morozovella
formosa formosa, M. lensiformis, M. aragonensis, M. marginodentata, Acarinina
sibyaiensis, Ac. africana.
The Acarininids are fairly common and the quantitative analysis of its relative
abundance showed great significant changes across the P / E boundary, especially
around the Morozovella velascoensis (P5a and P5b) Zone. These tropical to
subtropical, low latitude taxa indicate major increase in both of the number and
diversity (appearance of new speices). The acarininids relative abundance begins
just below the boundary clay bed, the P / E transition boundary (ranged from 10% -
25% in Globoanomalina pseudomenadrii Zone (P4) and increased approximately
to 25% - 40% in the base of the Morozovella velascoensis Zone (P5a) of the late
Paleocene and exhibits maximum abundnace and diversity above the P / E
transition boundary (sapropelic dissolution clay bed) reaching 48% - 55% in
Acarinina sibaiyaensis / Morozovella velascoensis Interval subzone P5b and
Morozovella edgari Zone (P6a). The maximum diversity of the acarininids
coincides also with the boundary clay bed or the BEE and reached its peak
(Acarininids incrusion). The planktonic foramniferal extinctions and origination
occurred gradually (relative gradual changes between the extinction of typical late
Paleocene taxa and origination of typical early Eocene taxa). Some Acarininds
totally dissappeared below the the P / E transition boundary such as Acarinina
mckanni, Ac. nitida, Ac. subsphaerica and M. acutispira. others appeared or
originated for the first time just above the bounadry clay bed in the early Eocene
such as the compressed tropical acarininids spp e.g. Acarinina africana, Ac.
sibaiyensis, Ac. qutera, A. Wilcoxensis, A. broedermani (Fig. 4) suggesting warm
water environments in the Tethys region during the P/ E boundary transition.

Hamad20
This foraminiferal turnover is followed upwards in the P7 and 8 Zones by
cooling conditions (Fig. 4) as suggested from the increased abundance and
appearance of the cooler water subbotinids. Although the subbotinids spp. is rather
dominant but their diversity is low and number of taxa except the extinction of some
taxa before the P / E boundary such as Subbotina triloculinoides and S. finlayi.
Other subbotinids thervied without any change except in their relative abundance
e.g. Subbotina linaperta, S. triangularis, S. eocaenica, S. inaequispira, S.
hornibrooki) and further reduction of morozovellids.
In the present study, the paleoecological inference are based on the
information recorded in the previous studies, so it could be deduced that gradual
warming have been started in the end of P4 Zone (where great abundance of such
warm fauna are recorded) and this warming event reached its maximum magnitude
during the Paleocene / Eocene boundary event (P5 Zone, as major increase in the
low latitudes warm water morozovelids and compressed tropical acarininids
(Acarinina sibaiyaensis, A. africana, A. berggreni). Moreover the Morozovellids that
considered also low latitudes warm taxa show increase in the relative abunce just
above the P / E boundary that coeval with the clay sapropel bed. This global
maximum warming continued above the P / E boundary (boundary clay bed)
through the early Eocene zones.
__________________________________________________________________
Explanation of Plate 1
(All the figured specimens are photographed with Scanning Electron
Microscope and magnified as x150 µm except for figure 6 magnified as x 200 µm)
Fig. 1: Morozovella velascoensis (Cushman), sample 22, Esna Formation.
Figs. 2: Morozovella formosa (Bolli), sample 35, Thebes Formation
Figs. 3: Morozovella aragonensis (Nattall), sample 26, Thebes Formation.
Figs. 4: Morozovella conicotruncana , sample 3, Tarawan Formation.
Figs.5&6: Morozovella subbotinae (Morozova), sample 31, Esna Formation.
Fig. 7: Globanomlina pseudomenadrii (Bolli), sample 3, Tarawan Formation.
Fig. 8: Acarinina subsphaerica Subbotina, sample 5, Tarawan Formation.
Fig. 9: Subbotina triloculinoides (Plummer), sample 10, Tarawan Formation.
Fig. 10: Morozovella edgari (Premoli Silva & Bolli), sample 28, Esna Formation.
Figs. 11: Muricoglobigerina soldadoensis (Bronnimann), sample 15, Esna Formation.
Fig. 12: Acarinina sibaiyaensis (El Naggar), sample 21, Esna Formation.
Fig. 13: Subbotina triangularis (White), sample 11, Esna Formation.
Fig. 14: Subbotina triloculinoides (Plummer), texture of surface, sample 10, Tarawan
Formation.

EsnaFormation
Paleocene
ThanetianYpresian
Eocene
ThebesFormation
NP12NP11NP10NP9NP7/8NP5
M.velascoensisM.aragonensis/
formosaP7
Gl.Pseudomenardii(P4)
45
44
43
42
41
40
39
38
37
36
36
35
34
33
32
31
30
29
28
27
26
25
24
23
22
21
20
19
18
17
16
15
14
13
12
11
10
9
8
7
6
5
4
3
2
1
M.subbotinae
M.
aragonensis
SampleNo.
Biozone
Age
Age
Rock
unit
NP4
Tarawan
Formation
.
.
..
.
.
..
..
o oo
~ ~ ~ ~
P4aP4bP4cP5aP5bP6aP6b
Abundance ofAbundance of
AcarininaAcarinina
sppspp.%.%
smallsmall
MorozovellaMorozovella sppspp..
largelarge
MorozovellaMorozovella sppspp..
5030
Benthonicforaminifera
20 40 4020
Planktonicforaminifera
PaleotempPaleotemp..
curvecurve
coldcold
PaleodepthPaleodepth
curvecurve
warmwarmNeriticNeritic bassyalbassyal
Deep / ShallowDeep / Shallow
morphotypesmorphotypes
50%
Fig. 4: Quantitative foraminiferal analysis, inferred paleodepth and paleotemperatures
curves at Gabal El Bruk , north - central Sinai, Egypt
CONCLUSIONS
1- The time interval spanning the late Paleocene – early Eocene sequence
exposed at Gebel El Bruk, north - central Siani, Egypt has been analyzed for its
planktonic forminiferal assemblage. One composite stratigraphic surface section
from this area is described and investigated. Three rock units were recorded in this
area from base to top: Tarawan Chalk, Esna Formation (late Paleocene) and
Thebes Formation (early Eocene). The biozonation of Berggren et al. (1995) has
been modified on the basis of the first occurrence of Acarinina sibaiyaensis,
subdividing Morozovella velascoensis zone (P5) into two subzones (P5a, P5b).
2- Based on the vertical stratigraphic distribution of the planktonic foraminifera
in the studied section, the late Paleocene / early Eocene transition could be
subdivided into six planktonic foraminiferal zones, arranged from base to top: 1)
Globanomalina pseudomenardii (total range Zone P4), 2) Morozovella
velascoensis Zone (P5): a- (Globanomalina pseudomenardii / Acarinina
sibaiyaensis Interval Subzone (P5a) and Acarinina sibaiyaensis / Morozovella

Hamad22
velascoensis Interval subzone (P5b) of the late Paleocene age (Thanetian) and 3)
Morozovella edgari subbotinae (P6a), 4) Morozovella subbotinae (P6b), 5)
Morozovella formosa formosa (P7), and 6) Morozovella aragonensis (P8) zones of
the early Eocene (Ypresian) age.
3- The Paleocene / Eocene boundary at Gebel El Bruk has located to within
the Morozovella velascoensis Zone and coincides with the subzonal boundary
between the Globanomalina pseudomenardii / Acarinina sibaiyaensis Interval
Subzone (P5a) and Acarinina sibaiyaensis / Morozovella velascoensis Interval
subzone (P5b) (in the upper part of the Esna Formation). This boundary is also in
coincidence with the level of benthonic foraminiferal mass extinction (BEE). It is
noteworthy of mention that a closar examination of the Esna Shale revealed a bed
of 2m thickness containing a unique sapropelic dissolution clay layer (30cm) that
could be a result of a global rise in the lysocline and calcite compensation depth.
This sapropelic dissolution clay layer coincides with sample no. 24, and also situate
the Paleocene – Eocene boundary.
4- The quantitative analysis of the planktonic foraminifera indicate a significant
gradual change in response of the environmental or climatic conditions and is
characterized by the abundance of morozovellids and acarininids populations in
response to the subbotinids. The planktonic foraminiferal tunover across the late
Paleocene – early Eocene boundary interval is marked by a major increase in the
low latitude / high latitude ratio (warm / cool ratio) that indicate surface water
warming attributed to the global maximum warming event. Also the quantitative
analysis showed an increase in the low latitiude , warm water species of both
small and larger morozovellids just above the Paleocene / Eocene boundary,
where some morozovellids have been disappeared or extincted e.g. Morozovella
angulata, M. conicotruncata, M. acuta, M. parva, M. velascoensis and others are
originated or evolved e.g. Morozovella subbotinae, M. formosa formosa, M.
lensiformis, M. aragonensis, M. marginodentata). Also the low latitude, warm water,
compressed tropical to subtropical acarininids such as Acarinina sibaiyensis, Ac.
africana, A. wilcoxensis , A. quetra, showed an increase also just below the P/ E
boundary but it reached its climax above the P/E boundary (dissolution clay layer)
indiacting warm water conditions that related to the 'Paleocene-Eocene Thermal
Maximum’ PETM), and prevailled during the early Eocene but decreased later on
the upper levels of this time interval, where the cooler water subbotinids and
rounded acarininds begun to realtively increase in P7 Zone and continued through
P8 zone.
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