02-faris.indd


Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt
139

�
AB STRA CT
Integration of the calcareous nannofossil and planktonic foraminiferal biostratigraphies has been performed for the 
Upper Maastrichtian – Palaeocene successions at Gebel Umm Khushayb and west El-Hassana sections (north-central 
Sinai, Egypt). The studied successions include the uppermost part of the Sudr, Dakhla, and Tarawan formations and 
their lateral coeval Beida Formation. Biostratigraphic analysis has allowed recognition from Zone CF2 to Zone P4 
in terms of planktonic foraminifera and from Zone CC26c to Zone NP7/8 in terms of calcareous nannofossils. The 
Maastrichtian/Palaeogene (K/Pg) boundary is characterized by an erosional surface that marks a hiatus between the 
Sudr/Dakhla or Sudr/Beida formation boundaries, as confi rmed by the absence of the planktonic foraminiferal CF1 
to P1a zones and their equivalent nannofossil zones (top part of CC26c to lowest part of Zone NP3). The Danian/
Selandian (Da/Se) boundary lies in the upper part of the Dakhla Formation within the top of nannofossil Zone NP4, 
and within planktonic foraminiferal Zone P3b, similar to that of the Global Standard Stratotype-section and Point 
(GSSP) of the D/S boundary which has recently been chosen at the Zumaia section, northern Spain. A minor hiatus 
was observed across the Selandian/Thanetian boundary as indicated by a lithological change and a very condensed 
Zone NP6, corresponding to the Dakhla and Tarawan formation boundary in the west El-Hassana section.

Keywords: biostratigraphy, calcareous nannofossils, Danian/Selandian boundary, planktonic foraminifera, north-
central Sinai

Integrated biostratigraphy of two
Upper Maastrichtian – Palaeocene
successions in north-central Sinai, 

Egypt

�
Mahmoud Faris1 and Sherif Farouk2 

1 Geology Department, Faculty of Science, Tanta University, Egypt; (mhmfaris@yahoo.com)
2 Egyptian Petroleum Research Institute, Nasr City, 11727, Egypt; (geo.sherif@hotmail.com)

doi: 104154/gc.2012.10 

Geologia Croatica 65/2 139–160 3 Figs. 4 Tabs. 3 Pls. Zagreb 2012

Geologia CroaticaGeologia Croatica

1. INTRODUCTION

The Palaeocene successions in Egypt are marked by widely 
distributed, condensed successions rich in calcareous plank-
tonic faunal assemblages with distinct vertical and lateral 
facies changes. A considerable number of previous papers 
deal with the biostratigraphy of the Palaeocene of Sinai (e.g. 
LÜNING et al., 1998; MARZOUK & LÜNING, 1998; EL-
NADY & SHAHIN, 2001; SAMIR, 2002; AYYAD et al., 

2003; SPEIJER, 2003; AL-WOSABI & ABU SHAMA, 
2007; FARIS & SALEM, 2007; FARIS & ABU SHAMA, 
2007; FAROUK & FARIS, 2008). The present study pro-
vides the fi rst information on the biostratigraphy at Gebel 
Umm Khushayb and only a few small works have been un-
dertaken on the El-Hassana area (EL-DEEB et al., 2000 & 
FARIS et al., 2000). These authors placed the Palaeocene 
stage boundaries according to older concepts (before defi ni-



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specimen /2–5 fov), R= rare (one specimen/6–10 fov) and 
VR=very rare (one specimen/ more than 10 fov).

For the planktonic foraminifera, about 200g of dry rock 
samples were disaggregated in water and washed through a 
63μm sieve. The relative abundance of planktonic foraminif-
eral taxa are defi ned as follows: abundant, >26%; common, 
16–25%; few, 6–15%; rare, 2–5%; very rare, <2%.

3. GEOLOGICAL SETTING AND 
LITHOSTRATIGRAPHY

Tectonically, SAID (1962) divided Egypt into two major 
provinces, the deformed Unstable Shelf to the north, and the 
nearly horizontal and less deformed Stable Shelf to the south 
(Fig. 1). The Syrian Arc Fold Belt is one of the best-known 
structural features in the Unstable Shelf, and it played an im-
portant role in controlling the confi guration of the deposi-
tional sequences and the great complexity of changes both 
in facies and thickness (FAROUK & FARIS, 2008). The 
study area lies in north-central Sinai of the Unstable Shelf 
and is characterized by complex uplifts and domal anticlines 
of the Syrian Arc Fold Belt, that were formed during the clo-
sure of Neo-Tethys during the convergence of the African-
Arabian Craton (STAMPFLI et al., 1995).

Maastrichtian – Palaeocene siliciclastic/carbonate out-
crops are widely distributed in north-central Sinai, where the 
Campanian-Maastrichtian Sudr Formation overlies uncon-
formably the Palaeocene sediments, which correspond to four 
well-defi ned formations from oldest to youngest are; Dakhla 
Formation, Tarawan Formation and lowermost part of the 
Esna Formation and their lateral coeval Beida Formation. 
The following is a detailed lithostratigraphic description of 
the detected Upper Maastrichtian – Palaeocene formations 
in the study area, given from older to younger (Fig, 2).

Sudr Formation- Campanian-Maastrichtian

The Campanian-Maastrichtian Sudr Formation (GHORAB, 
1961) is widespread throughout the foot slopes of Sinai. It 
unconformably overlies the Dakhla or Bedia formations with 
a sharp lithological contact. The Sudr Formation is subdi-
vided from base to top into the Markha and Abu Zenima 
members. The study measured part of the Sudr Formation 
deals only with the uppermost part of Abu Zenima Member 
(Upper Maastrichtian). It consists of argillaceous li me stone 
with a measured thickness of about 2–2.5 m in the study sec-
tions (Fig. 2).

Dakhla Formation- Danian-Selandian

The term Dakhla Formation was fi rstly used by SAID (1961) 
to describe the Maastrichtian-Palaeocene siliciclastics and 
carbonate deposits in Dakhla Oasis, Western Desert. In 
northern latitudes 26º30’ in Egypt, the lower part of the Da-
khla Formation is generally laterally equivalent to carbonate 
facies (the Sudr and Khoman formations).

Therefore in the Sinai Peninsula, the Dakhla Formation 
belongs to the Palaeocene and it overlies unconformably the 

tion of the global stratotypes of the Danian/Selandian and 
Selandian/Thanetian boundaries). In the two study sections, 
the K/Pg, De/Se and Se/Th remain unclear and not been pre-
cisely identifi ed.

However, many discrepancies in the Palaeocene bio-
events could not be clarifi ed because either taxonomically 
different concepts caused uncertainties in correlation of the 
Palaeocene zones, especially in the southern Tethyan realm, 
(ORUE-ETXEBARRIA et al., 2007; ARENILAS, 2012), or 
these marker bio-events are recorded from different palaeo-
latitudes showing considerable variations in age (FAROUK 
& FARIS, 2011).

The main purpose of this research was to accurately cor-
relate the Palaeocene bio-events with the standard biostrati-
graphic scales, using both calcareous nannofossils and plank-
tonic foraminifera, for two Upper Maastrichtian – Palaeocene 
successions in north-central Sinai, and to discuss in details 
the Cretaceous/Palaeogene (K/Pg), the Danian/Selandian 
(Da/Se) and the Selandian/Thanetian (Se/Th) boundaries in 
the studied successions.

2. MATERIALS AND METHODS

Seventy-six rock samples were collected, approximately ev-
ery. 25–50 cm from the two studied sections at Gebel Umm 
Khushayb (30º14’27”N and 33º13’33”E) and west El-Has-
sana (30º25’40”N and 33º46’41”E), (Fig. 1).

Calcareous nannofossils were analyzed using standard 
smear slides, which were examined using a light photomi-
croscope at 1250X magnifi cation. A qualitative estimation 
of the abundance of calcareous nannofossil taxa are noted as 
follows: A= abundant (more than 5 specimens /fi eld of view, 
fov), C=common (1–5 specimens/fov), F=frequent (one 

Figure 1: Location map of the study area.



Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt Geologia Croatica
141

Maastrichtian Sudr Formation and also underlies the Tarawan 
Formation, with very clear contact, and can be easily recog-
nized in the fi eld. It consists mainly of moderately hard, 
greenish grey monotonous pelagic calcareous mudstone with 
fl ooded well-diversifi ed calcareous planktonic assemblages 
with thicknesses ranging from 20 to 25 m in the west El-
Hassana section.

Tarawan Formation- Thanetian

The Tarawan Formation (AWAD & GHOBRIAL, 1965) is 
composed of hard to moderately hard, massive yellowish 
white argillaceous limestone, partly limonitic with a thick-
ness of 2 to 4 m in the west El-Hassana section. The partly 
resistant, light-coloured limestone of this unit is clearly dis-
tinguished from the overlying and underlying dark-colored 

Figure 2: Stratigraphic correlation of the studied sections in the north-central Sinai. Calcareous nannofossil schemes are after MARTINI (NP, 1971) and 
VAROL (NTp, 1989) and SISSIGH (CC, 1977). Planktonic foraminiferal schemes are after BERGGREN & PEARSON (P, 2005).



Geologia Croatica 65/2Geologia Croatica
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soft shales. In Egypt, the Dakhla Formation is overlain by the 
Tarawan Formation which includes, at its upper part, the so-
called “Velascoensis Event” with notable changes in the pat-
terns of sedimentation in late Palaeocene time. The event that 
produced those changes is believed to be primarily tectonic 
coupled with global sea-level fall (STROUGO, 1986).

Beida Formation- Palaeocene

The term Beida Formation was fi rstly used by ALLAM & 
KHALIL (1988) based upon predominant carbonate depos-
its at Wadi Beida, north of Gebel Arif El-Naqa. It is equiva-
lent to the Palaeocene siliciclastic/carbonate of the Esna For-
mation, which is recorded in different parts of Egypt.

In the study area, the Beida Formation has a wide dis-
tribution in the submerged palaeo-high areas around central 
Sinai, extending from Gebel Umm Khushayb to Ras Sudr. 
It unconformably overlies and underlies the Sudr and Thebes 
formations, respectively. The Beida Formation attains a total 
thickness of 40 m and is composed of greenish gray marl, 
argillaceous limestone, and well-bedded chalky limestone 
with chert bands in the Gebel Gebel Umm Khushayb section.

4. BIOSTRATIGRAPHY

The biostratigraphy is evaluated here based on the Creta-
ceous Foraminiferal (CF) Zonal Scheme of LI & KELLER 
(1998) and on the Palaeocene (P) Zonal Scheme of BERG-
GERN & PEARSON (2005). These zonal schemes are ap-
plied in the present study to provide a much improved bio-
stratigraphic framework.

For the calcareous nannofossil zonation, the Cretaceous 
Zonal Scheme of SISSINGH (1977) and the Palaeogene 
Zonal Scheme of MARTINI (NP, 1971) and VAROL (NTp, 
1989) have been applied. The distribution of the calcareous 
nannofossils and planktonic foraminifera in the two studied 
sections are shown in Tables 1–4. The most important fo-
raminifera and calcareous nannofossil taxa are fi gured in 
three plates (1–3). Abbreviations used FO= First Occurrence, 

LO= Last Occurrence; FCO= First Common Occurrence; 
FRO= First Rare Occurrence. The following is the descrip-
tion of the established calcareous nannofossil and planktonic 
foraminiferal biozones arranged from older to younger.

4.1. Calcareous nannofossils

4.1.1. Micula prinsii Subzone (CC26c)

Defi nition: The Micula prinsii Subzone is defi ned as the in-
terval from the FO of Micula prinsii Perch-Nielsen to the 
increased frequency of Thoracosphaera operculata Bram-
lette & Martini.

Occurrence: This zone occupied the upper most part of 
the Sudr Formation and is represented by samples 220–221 
(2 m thick) in Umm Khushayb; and samples 1–6 in west El-
Hassana (2.5 m thick).

Characteristic species: The most important taxa also 
identifi ed from this subzone are: Ahmuellerella octoradiata 
(GORKA), Arkhangelskiella cymbiformis VEKSHINA, Ch-
iastozygus amphipons (BRAMLETTE & MARTINI), Strad-
neria crenulala (BRAMLETTE & MARTINI), Cribrospha-
erella ehrenbergii (ARKHANGELSKY), Cyclagelosphaera 
reinhardtii (PERCH-NIELSEN), Eiffellithus gorkae Rein-
hardt, Lithraphidites quadratus BRAMLETTE & MAR-
TINI, Lucianorhabdus cayeuxii DEFLANDRE, Manivitella 
pemmatoidea (DEFLANDRE in MANIVIT), Microrhabdu-
lus decoratus DEFLANDRE, Micula decussata VEKSHI NA, 
Zygolithus crux (DEFLANDRE & PERT), and others (Ta-
bles 1 & 2). Rare specimens of M. murus (MARTINI) and 
M. prinsii PERCH-NIELSEN are recorded in the topmost 
part of the Sudr Formation in the studied sections.

Remarks: The Micula prinsii Subzone was informally 
defi ned by PERCH-NIELSEN (1979) and corresponds to the 
upper part of Zone CC26 of SISSINGH (1977). This sub-
zone is a correlative of the latest Maastrichtian. However, its 
upper limit cannot be determined with accuracy in the two 
studied sections due to a large hiatus observed at the base of 
the Palaeocene.

Plate 1

1–2 Arkhangelskiella cymbiformis VEKSHINA, 1959, sample 2, west El-Hassana section.
3 Watznaueria barnesae (BLACK in BLACK & BARNES, 1959), sample 221, Gebel Umm Khushayb section.
4 Chiastozygus amphipons (BRAMLETTE & MARTINI, 1964), sample 4, west El Hassana section.
5 Braarudosphaera bigelowii (GRAN & BRAARUD, 1935), sample 3, west El Hassana section.
6–7 Microrhabdulus decoratus DEFLANDRE, 1959, sample 221, Gebel Umm Khushayb section.
8 Lithraphidites carniolensis DEFLANDRE, 1963, sample No.5, west El-Hassana section.
9–10 Placozygus sigmoides (BRAMLETTE & SULLIVAN, 1961), sample 32, west El-Hassana section.
11 Eiff ellithus gorkae REINHARDT (1965), sample 220, Gebel Umm Khushayb section.
12 Zeugrhabdotus pseudanthophorus (BRAMLETTE & MARTINI, 1964), sample 3, west El-Hassana section.
13 Thoracosphaera operculata BRAMLETTE & MARTINI, 1964, sample 228, Gebel Umm Khushayb section.
14 Thoracosphaera saxea STRADNER, 1961, sample 12, west El-Hassana section.
15 Lucianorhabdus cayeuxii DEFLANDRE, 1959, sample 220, Gebel Umm Khushayb sectio.
16–17 Micula prinsii PERCH-NIELSEN, 1979, sample1, west El-Hassana section.
18–19 Micula murus (MARTINI, 1961), sample 2, west El-Hassana section.
20 Cribrosphaerella ehrenbergii (ARKHANGELSKY, 1912), sample 221, Gebel Umm Khushayb section.
21–22 Micula decussata VEKSHINA, 1959, sample 222, Gebel Umm Khushayb section.
23 Zygodiscus spiralis BRAMLETTE & MARTINI, 1964, sample 4, west El-Hassana section.
24 Manivitella pemmatoidea (DEFLANDRE in MANIVIT, 1965), sample 221, Gebel Umm Khushayb section.
25 Tetrapodorhabdus decorus (DEFLANDER in DEFLANDER & FERT, 1954), sample 5, west El-Hassana section.



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143

Micula murus is one of the rare Maastrichtian species and 
clearly restricted to low latitudes (WORSLEY AND MAR-
TINI, 1970; THIERSTEIN, 1981; GARDIN, 2002; LEES, 

2002). It was used for recognition of the uppermost Maastric-
tian (LAMOLDA & GOROSTIDI, 1992; POSPICAL, 1994; 
BERNAOLA & MONECHI, 2007 and many others).



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Plate 2

1–2 Ellipsolithus macellus (BRAMLETTE & SULLIVAN, 1961), sample 9, west El-Hassana section.
3 Chiasmolithus edentulus VAN HECK & PRINS, 1987, sample 22, west El-Hassana section.
4 Neochiastozygus perfectus PERCH-NIELSEN, 1971, sample 247, Gebel Umm Khushayb section.
5 Neochiastozygus junctus (BRAMLETTE & SULLIVAN, 1961), sample 242, Gebel Umm Khushayb section.
6 Fasciculithus tympaniformis HAY & MOHLER in HAY et al., 1967, sample 40, west El-Hassana section.
7 Fasciculithus billii PERCH-NIELSEN, 1971, sample 42, west El-Hassana section.
8 Fasciculithus janii PERCH-NIELSEN, 1971, sample 36, west El-Hassana section.
9 Fasciculithus pileatus BUKRY, 1973, sample 242, Gebel Umm Khushayb section.
10 Fasciculithus involutus BRAMLETTE & SULLIVAN, 1961, sample No.40, west El-Hassana section.
11 Fasciculithus alanii PERCH-NIELSEN, 1971, sample 45, west El-Hassana section.
12–13 Sphenolithus primus PERCH-NIELSEN, 1971, sample 245, Gebel Umm Khushayb section.
14 Toweius eminens (BRAMLETTE & SULLIVAN, 1961), sample 247, Gebel Umm Khushayb section.
15 Cruciplacolithus primus PERCH-NIELSEN, 1977, sample No.224, Gebel Umm Khushayb section.
16 Chiasmolithus danicus (BROTZEN, 1959), sample 7, west El-Hassana section.
17 Cruciplacolithus tenuis (STRADNER, 1961), sample 10, west El-Hassana section.
18 Chiasmolithus bidens (BRAMLETTE & SULLIVAN, 1961), sample 248, Gebel Umm Khushayb section.
19 Markalius inversus (DEFLANDRE in DEFLANDRE & FERT, 1954), sample No.6, west El-Hassana section.
20–21 Ericsonia subpertusa HAY & MOHLER, 1967, sample No.20, west El Hassana section.
22 Heliolithus kleinpellii SULLIVAN, 1964, sample No.42, west El-Hassana section.
23 Discoaster mohleri BUKRY & PERCIVAL, 1971, sample No. 45, west El-Hassana section.

4.1.2. Chiasmolithus danicus Zone (NP3)
Defi nition: The Chiasmolithus danicus Zone is defi ned as 
the interval from the FO of Chiasmolithus danicus (BROT-
ZEN) to the FO of Ellipsolithus macellus (BRAMLETTE & 
SULLIVAN).

Occurrence: This zone occupied the lowermost part of 
the Dakhla and Bedia formations and is represented by sam-
ples 222–227 (2.5 m thick) in Umm Khushayb; and samples 
7–8 in west El-Hassana (0.2 m thick).

Characteristic species: The most characteristic species 
of this zone are: Cruciplacolithus tenuis (STRADNER), C. 
primus PERCH-NIELSEN, Ericsonia subpertusa HAY & 
MOHLER, E. cava (HAY & MOHLER) and Coccolithus 
pelagicus (WALLICH).

Remarks: The vanishing Cretaceous species are those 
extinct at the K/Pg boundary, and the Cretaceous persistent 
species are those calcareous nannofossil genera and species 
that are known to occur in the Cretaceous and survive into 
the Palaeocene (PERCH-NIELSEN, 1985b). The NP3 Zone 
is characterized by a decrease of Cretaceous vanishing spe-
cies. In the two studied sections, Cretaceous persistent spe-
cies are very rare in this zone and only a few specimens of 
Thoracosphaera operculata BRAMLETTE & MARTINI, 
Placozygus sigmoides (BRAMLETTE & SULLIVAN) and 
Cyclagelosphaera reinhardtii (PERCH-NIELSEN) domi-
nate the assemblage. This zone has a reduced thickness in 
both the studied sections. Cruciplacolithus edwardsii RO-
MEIN fi rst appears simultaneously with the FO of Ch. dan-
icus (base NP3).

The identifi ed Zone NP3 is equivalent to Zone NP3 of 
MARTINI (1971), the upper part of the Cruciplacolithus 
tenuis Zone of ROMEIN (1979), the CP2 Zone of OKADA 
& BUKRY (1980), FARIS & ABU SHAMA (2007) and 
FARIS & SALEM (2007).

4.1.3. Ellipsolithus macellus Zone (NP4)

Defi nition: The FO of Ellipsolithus macellus (BRAMLE-
TTE & SULLIVAN) is used to defi ne the base of Zone NP4, 
and the FO of Fasciculithus tympaniformis HAY & MOH-
LER defi ned its top (MARTINI, 1971).

Occurrence: This zone occupied the middle part of the 
Dakhla and Bedia formations, represented by samples 228–
244 (14.5m thick) in Umm Khushayb; and samples 9–39 in 
West El-Hassana (19 m thick).

Characteristic species: The FOs of Fasciculithus ulii 
PERCH-NIELSEN, F. billii PERCH-NIELSEN, F. bitectus 
ROMEIN, F. pileatus BUKRY, F. involutus BRAMLETTE 
& SULLIVAN and F. janii PERCH-NIELSEN occur within 
the Zone NP4 in the two study sections.

Remarks: According to the Palaeocene zonation of VA-
ROL (1989), the Zone NP4 in west El-Hassana and Umm 
Khushayb sections can be divided into three subzones, 
NTp6, NTp7 and NTp8. VAROL (1989) subdivided Zone 
NTp7 and NTp8 into several subzones. In the present study, 
it was so diffi cult to subdivide these two biozones into sev-
eral subzones due to the extreme condensation of this inter-
val. On the other hand, Zone NP4 could be divided into two 
subzones; NP4a, Ellipsolithus macellus-Sphenolithus primus 
Subzone, it is defi ned from the FO of E. macellus (BRAM-
LETTE & SULLIVAN) to the FO of Sphenolithus primus 
PERCH-NIELSEN and NP4b, Sphenolithus primus -Fas-
ciculithus tympaniformis defi nes from the FO of Spheno-
lithus primus to the FO of Fasciculithus tympaniformis 
(QUILLÉVÉRÉ et al., 2002 and FARIS et al., 2005). This 
subdivision was applied in the current study.

A small hiatus is suggested at the NP3/NP4 zonal 
boundary in the two studied sections, based on the absence 
of the uppermost part of Zone NP3 and the basal part of 



Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt Geologia Croatica
145

Zone NP4 (absence of Subzone NTp5B and NTp5C and 
most probably the lowermost of Zone NTp6 of VAROL, 
1989). Also a minor hiatus is detected at the NP3/NP4 zonal 
boundary of the northern scarp of the Farafra Oasis (TAN-

TAWY et al., 2003). The NTp6 Subzone is defi ned as the 
interval from the FO of Ellipsolithus macellus to the LO of 
Neochiastozygus imbriei HAQ & LOHMANN and N. 
eosaepes PERCH-NIELSEN.



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Plate 3

1 Heterohelix globulosa (EHRENBERG, 1840), sample 3, west El-Hassana section.
2 Heterohelix navarroensis LOEBLICH, 1951, sample 6, west El-Hassana section.
3 Heterohelix labellosa NEDERBAGT, 1991, sample 220, Umm Khyushab section.
4 Pseudoguembelina costulata (CUSHMAN, 1938), sample 221, Umm Khyushab section.
5–6 Globanomalina compressa (PLUMMER, 1926), sample 229, Umm Khyushab section.
7 Globanomalina pseudomenardii (BOLLI, 1957), sample 247, Umm Khyushab section.
8–10 Praemurica inconstans (SUBBOTINA, 1953), sample 25, west El-Hassana section.
11–13 Morozovella trinidadensis (BOLLI, 1957), sample 25, west El-Hassana section.
14–15 Igorina albeari (CUSHMAN & BERMUDEZ, 1949), sample 36, west El -Hassana section.
16–18 Morozovella angulata (WHITE, 1928), sample 34, west El-Hassana section.
19 Morozovella conicotruncata (SUBBOTINA, 1947), sample 240, Umm Khyushab section.
20–21 Morozovella occlusa (LOEBLICH & TAPPAN, 1957), sample 240, Umm Khyushab section.
22 Morozovella pasionensis (BERMÚDEZ, 1961), sample 34, west El-Hassana section.
23 Acarinina strabocella (LOEBLICH & TAPPAN, 1957), sample 34, west El-Hassana section.
24–25 Parasubbotina pseudobulloides (PLUMMER, 1926), sample 224, Umm Khyushab section.
26–27 Parasubbotina varianta (SUBBOTINA, 1953), sample 246, Umm Khyushab section.
28 Subbotina triangularis (WHITE, 1928), sample 34, west El-Hassana section.
29 Subbotina triloculinoides (PLUMMER, 1926), sample 25, west El-Hassana section.
30 Subbotina velascoensis (CUSHMAN, 1925), sample 252, Umm Khyushab section. scale bar=100 μm in all fi gures.

The distribution of Ellipsolithus macellus is considered 
as being controlled by preservation (dissolution) (MON-
ECHI et al., 1985) or different palaeoecological conditions 
(BACKMAN, 1986, MONECHI et al., 1985).

In the study sections, E. macellus, shows a rare and spo-
radic presence throughout the study interval which may be 
a result of dissolution and /or the effect of diagenesis.

The subzone NTp7 defi nes the stratigraphic interval 
from the LOs of Neochiastozygus imbriei and N. eosaepes 
to the FCO (First Common Occurrence) of Sphenolithus 
primus. The FO of Chiasmolithus edentulus marks the base 
of Subzone NTp7B of VAROL (1989) and occurs within 
Zone NTp7 in the west El-Hassana and Umm Khushayb sec-
tions. According to VAROL (1989), the FO of this taxon can 
be used to directly correlate Tethys and the type area across 
the D/S boundary. The fi rst occurrence of Ch. edentulus in 
the study sections is easily correlated with the type area of 
the Danian/Selandian boundary.

The NTp8 has been defi ned to include the interval from 
the FO of Sphenolithus primus to the FO of Fasciculithus 
tympaniformis. Previous studies have indicated that the oc-
currences of Sphenolithus and Fasciculithus (Palaeocene 
taxa) are closely related. It is generally believed that the ge-
nus Sphenolithus appears just below the genus Fasciculithus 
(e.g. ROMEIN, 1979; BACKMAN, 1986; BERGGREN et 
al., 1995), although other authors observed a reverse setting 
in the relative stratigraphic position of the two biohorizons 
(VAROL, 1989; BERGGREN et al., 2000).

The onset of the fi rst radiation of Fasciculithus species 
occurs in samples 24 and 240 in the west El-Hassana and 
Umm Khushayb sections, respectively. The onset of the sec-
ond radiation of Fasciculithus taxa occurs in samples 36 in 
the west El-Hassana section and in sample 242 in the Umm 
Khushayb section. Radiation of Fasciculithus (F. pileatus, 
F. bitectus, F. involutus, F. janii, and F. ulii) fi rst occurred in 
higher levels above the FO of S. primus in the study area.

As proposed by PERCH-NIELSEN (1985b) the FO of 
Neochiastozygus perfectus PERCH-NIELSEN was used for 
delineating the base of Zone NP5 in North Sea area. In the 
Zumaia section, the FO of this taxon occurs above the First 
Common Occurrence (FCO) of S. primus and immediately 
below the LCO of Braarudosphaera (DINARES-TURELL 
et al., 2007). In the two studied sections, N. perfectus fi rst 
appears within Zone NP4 (Zone NTp7).

The FO of N. perfectus in Zone NP4 in the study sec-
tions is considered to be earlier than reported in the North 
Sea area, and it is therefore apparently a diachronous event 
and must be used with caution for long distance corre lation.

4.1.4. Fasciculithus tympaniformis Zone (NP5)

Defi nition: The fi rst occurrence (FO) of Fasciculithus 
tympaniformis is used to defi ne the base of Zone NP5 and 
the FO of Heliolithus kleinpellii SULLIVAN defi nes its 
top.

Occurrence: This zone occupied the interval from the 
upper part of the Dakhla and Bedia formations, samples 245–
249 (3 m thick) in the Umm Khushayb section, and samples 
40–41 in the west El-Hassana section (1.5 m thick).

Characteristic species: The most characteristic species 
of this zone include those of Zone NP4 in addition to Fas-
ciculithus tympaniformis.

Remarks: According to PERCH-NIELSEN (1985b), 
Toweius eminens (BRAMLETTE & SULLIVAN) fi rst ap-
pears within Zone NP5. In the Zumaia section, the lowest 
occurrence of Toweius eminens occurs in the middle part of 
NP5 (DINARÈS-TURELL et al., 2007). At Umm Khushayb, 
this species (Toweius eminens) fi rst occurs within NP5, while 
in the west El-Hassana section, T. eminens is fi rst recorded 
within the upper part of Zone NP4.

In the study sections,Zone NP5 corresponds to NP5 Zo-
ne of MARTINI (1971), the Fasciculithus tympaniformis 



Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt Geologia Croatica
147



Geologia Croatica 65/2Geologia Croatica
148

Ta
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45 F G

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                                              VR            

44 F G                                               VR            

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39 B

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38 F M                                               R           VR

37 F M                                               F           R

36 F M                                               VR           VR

D
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33 C G

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32 C G

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30 A G                                               R           F

29 C G

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                                              VR           R

28 F M                                               VR           VR

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22 R M                                               F           VR

21 B                                                            

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18 C M VR VR VR                                         F VR         R

17 C M                                               VR VR         R

16 F M         VR                                     VR           VR

15 F M VR VR VR                                         VR           VR

14 F M

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12 C M VR VR VR VR VR                                 VR   VR     VR     VR

11 C M                                               VR VR   VR      

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2 F M F R R VR VR       VR       VR         VR VR VR R     R VR VR   R    

1 C M C F R R R R VR VR VR VR VR VR VR VR VR VR VR VR VR VR R     R VR VR VR      



Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt Geologia Croatica
149

Ta
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e 
1:

 c
on

tin
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Incoming Paleocene Taxa
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ru
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      R       R   V
R F   R         V
R   F     VR R     F     F     R     VR VR   VR

      F R     F   V
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R           VR R             R     F         VR   VR    

      F F     F     R   V
R           VR F     R VR R VR R     F           VR VR VR  

      VR VR     VR     R             V
R   R     V
R             R       VR R        

      F       R     F V
R             V
R R   R R VR   VR VR VR   F   R VR VR          

    V
R   R     R   V
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R

V
R         F F F   VR R R VR R VR VR VR F VR                

                                                                             

      F F     R VR VR R VR VR     VR VR R R R R VR     R R VR                        

    VR R       R VR VR F R       R R           R   F                            

      R R     R   R F VR VR     R VR F F R F F F R VR F                          

    R F R     R VR R F VR       R                 R                            

      R F     R   R VR         R             F R                              

    R F C     R VR VR VR VR   VR   R             F R                              

    R F C     R   F   VR VR     R             F                                

    R F C     F   F           VR R           F                                

    R F C     F VR F     VR     VR R VR   VR     R                                

    R F C     F   R   VR       VR R     VR                                      

    R F R     F   VR   VR       VR                                              

    R F F     F   R   VR VR     VR                                              

      F F     F       R VR                                                    

    VR F R     F   R   R VR     VR VR VR   VR                                      

      F R     R VR   R R VR VR     R F F F R R                                  

    R F R     R   VR   R       R VR                                            

      R R     R       R                                                      

                                                                             

      F F     R   VR VR                                                        

    C F F     R VR VR R   VR   VR                                                

    R F R     R   VR   VR                                                      

    F R R     R   VR   VR   VR                                                  

    R R R     R   VR R VR VR                                                    

    R R R     R   R                                                          

  VR R R   VR VR VR   VR R                                                        

  VR   F F VR VR R VR VR                                                          

    F F F     R   R                                                          

R VR C F   VR   R VR VR R                                                       

R VR C F   VR VR F VR R R                                                        

R VR F F R VR VR R VR F                                                          

VR VR F F R   VR F                                                              

  VR R R R VR VR                                                                

VR                                                                            

                                                                             

                                                                             

                                                                             

                                                                             

A
bu

nd
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ce
 

Pr
es

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va

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n

A
: A

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 P

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r

R:
 R

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VR
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re

 
* 

M
ar

ke
r s

pe
ci

es



Geologia Croatica 65/2Geologia Croatica
150

Ta
bl

e2
 : 

St
ra

tig
ra

ph
ic

 d
is

tr
ib

ut
io

n 
of

 th
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w

ii 

Se
la

nd
ia

n

Be
id

a

251 C G

N
P6

P4

                                        F          

250 C M                                         F R        

249 R M

N
P5

                                          R        

248 C M                                         F R        

247 F G                                           R        

246 C M                                           F        

245 C G                                           F        

244 F M

N
P4

N
Tp

8

P3
b

                                                   

243 C G                                         R       R  

242 C G                                         R R        

D
an

ia
n

241 C M                                         R R        

240 C M                                         R R        

239 B

N
Tp

7

P3
a

                                                R  

238 C M               R                           R        

237 F M               R       R                   R       R

236 F G

P2

                                        R R       V
R

235 A G                                         R R       V
R

234 C G

N
Tp

6

                                        R F     R  
233 R M                                         R R        

232 F M       R                                 R          

231 F M               R       R                 R R        

230 C M                       V
R                 R   F      

229 C M

P1
c

              V
R       V
R                 F F F      

228 A M               V
R       V
R     R   R       F   F      

227 R M

N
P3

              V
R   R   V
R                 F   R      

226 R P   R   R                                 F          

225 C G       R       V
R   R   R                 F F     R  

224 F G

P1
b

R   R F       V
R   R R R                 F F        

223 R M R     R R     R R     R R               R R        

222 F M R R   R R     R   R   F               R R R        

M
aa

s.

Su
dr

221 C M

CC
26

c

CF
2 R F R F R R   R R R   F   R R R R R R R R R       VR

220 C M R R R F R R R R R R R F R R R           R R R R R VR



Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt Geologia Croatica
151

Ta
bl

e 
2:

 c
on

tin
ue

Incoming Paleocene Taxa
N

eo
ch

ia
st

oz
yg

us
 p

er
fe

ct
us

 

Cr
uc

ip
la

co
lit

hu
s t

en
ui

s*

Ch
ia

sm
ol

ith
us

 d
an

ic
us

*

Cr
uc

ip
la

co
lit

hu
s p

rim
us

Co
cc

ol
ith

us
 p

el
ag

ic
us

Er
ic

so
ni

a 
su

bp
er

tu
sa

Cr
uc

ip
la

co
lit

hu
s e

dw
ar

ds
ii 

N
eo

ch
ia

st
oz

yg
us

 m
od

es
tu

s 

N
eo

ch
ia

st
oz

yg
us

 im
br

ie
i 

N
eo

ch
ia

st
oz

yg
us

 e
os

ae
pe

s 

El
lip

so
lit

hu
s m

ac
el

lu
s

Sp
he

no
lit

hu
s p

rim
us

Ch
ia

sm
ol

ith
us

 e
de

nt
ul

us

Fa
sc

ic
ul

ith
us

 b
ite

ct
us

 

Fa
sc

ic
ul

ith
us

 p
ile

at
us

Er
ic

so
ni

a 
un

iv
er

sa

N
eo

ch
ia

st
oz

yg
us

 ju
nc

tu
s 

Fa
sc

ic
ul

ith
us

 p
ile

at
us

Er
ic

so
ni

a 
un

iv
er

sa

Fa
sc

ic
ul

ith
us

 b
ob

ii 

Fa
sc

ic
ul

ith
us

 ty
m

pa
ni

fo
rm

is*

Ch
ia

sm
ol

ith
us

 co
ns

ue
tu

s 

Ch
ia

sm
ol

ith
us

 b
id

en
s 

To
w

ei
us

 e
m

in
en

s 

H
el

io
lit

hu
s c

an
ta

br
ia

e 

Bo
m

ol
ith

us
 co

ni
cu

s 

H
el

io
lit

hu
s k

le
in

pe
lli

i 

Fa
sc

ic
ul

ith
us

 a
la

ni
i 

D
isc

oa
st

er
 b

ra
m

le
tt

ei

R   R   F R           F       R R     R R     R     R R R

R         F           F       F R R   R F     F   F R R R

R       R                         R           R R        

R   F   F F           R           R     R R R F          

R       F             F       F   R   R F F   F          

R   R   F     R     R F       R R R   R R R R            

R   F   F F         R F       R   R   F R R              

R     F R     R       R     R                            

R R R   F F   R         R R F R   R R R                  

R       F     R       F   F F   R F R F                  

    F   F             R R   R F                          

  R R   R F   R       R   R                              

                        R                                

    R   R R   R                                          

    R   R F             R                                

  R R R R R         R                                    

  R R   F C           R                                  

  R R R F F     VR VR                                      

        F F   R R R R                                    

        F F     R R                                      

  R R R F F     R R                                      

    R   F R R R R   R R                                  

  R R   F F R R R                                        

  F R R F F R   R R R                                    

  R   R R R                                              

        R R                                              

  F R R R F R                                            

  F   F F F   R                                          

    R       R                                            

  V
R R V
R

V
R R R                                            

                                                         

                                                         

A
bu

nd
an

ce
 

Pr
es

er
va

tio
n

A
: A

bu
nd

an
t 

G
: G

oo
d

C:
 C

om
m

on
 

M
: M

od
er

at
e

F:
 F

re
qu

an
t 

P:
 P

oo
r

R:
 R

ar
e

VR
: V

er
y 

ra
re

 
* 

M
ar

ke
r s

pe
ci

es



Geologia Croatica 65/2Geologia Croatica
152

zo ne of ROMEIN (1979), and the CP4 Zone of OKADA & 
BUKRY (1980), FARIS & ABU SHAMA (2007) and FARIS 
& SALEM (2007).

4.1.5. Heliolithus kleinpellii Zone (NP6)

Defi nition: The FO of Heliolithus kleinpellii defi nes the base 
of Zone NP6 and the FO of Discoaster mohleri BUKRY & 
PERCIVAL defi nes its top.

Occurrence: Zone NP6 occupies the interval from the 
upper part of the Dakhla and Bedia formations and is repre-
sented by samples 250–251 (2.5 m thick) in the Umm Khu-
shayb section and occurs only in sample 42 (0.4 m thick) in 
the west El-Hassana section.

Characteristic species: In addition to the fl oral as-
semblage, which characterizes Zone NP5, the following 
species are recorded in this zone: Heliolithus kleinpellii, 
Fasciculithus alanii PERCH-NIELSEN, Discoaster bram-
lettei MARTINI, and Bomolithus conicus (PERCH-
NIELSEN).

Remarks: The FO of Heliolithus cantabriae PERCH-
NIELSEN predates the FO of H. kleinpellii in the Umm 
Khushayb and west El-Hassana sections, and occurs at the 
top of Zone NP5, in agreement with the observations of 
PERCH-NIELSEN (1985b) and TANTAWY et al. (2003). 
In the Umm Khushayb section, Discoaster bramlettei occurs 
at the base of Zone NP6 and is considered here to be a reli-
able marker for the base of Zone NP6 in this section.

4.1.6. Discoaster mohleri Zone (NP7/8)

Defi nition: The FO of Discoaster mohleri BUKRY & PER-
CIVAL is used to defi ne the base of Zone NP7/8 and the ap-
pearance of Discoaster multiradiatus BRAMLETTE & RE-
IDEL delineates its top.

Occurrence: This zone is only represented by the Tara-
wan Formation in the west El-Hassana section (samples 43–
45, 1m thick).

Characteristic species: In addition to the identifi ed nan-
nofossils that have been recorded in the Zone NP6; Dis-
coaster mohleri, Fasciculithus schaubii HAY & MOHLER, 
and F. richardii PERCH-NIELSEN have their fi rst appear-
ance in this zone.

Remarks: The zonal scheme of MARTINI (1971) can-
not be applied to this interval because the marker species 
which defi nes the NP7/NP8 zonal boundary (Heliolithus rie-
delii BRAMLETTE & SULLIVAN) is absent in the west 
El-Hassana section. The Discoaster mohleri Zone of RO-
MEIN (1979) is used here. In the Umm Khushayb section, 
the FO of Fasciculithus alanii PERCH-NIELSEN occurs at 
the base of Zone NP6, while this species fi rst appears at the 
base of Zone NP7/8 in the west El-Hassana section.

The recorded Zone NP7/8 is equivalent to the combined 
NP7 and NP8 Zones of MARTINI (1971), the combined CP6 
and CP7 Zones of OKADA & BUKRY (1980), and to the 
NP7/8 Zone of FARIS & ABU SHAMA (2007) and FARIS 
& SALEM (2007).

4.2. Planktonic foraminifera

4.2.1. Pseudoguembelina palpebra partial range 
Zone (CF2)

Defi nition: This zone is defi ned as the biostratigraphic in-
terval from the last occurrence (LO) of Gansserina gansseri 
(BOLLI) to the fi rst occurrence (FO) of Plummerita hant-
keninoides (BRÖNNIMANN).

Occurrence: This zone occupies the upper part of the 
Sudr Formation in the study area. It’s true thickness is not 
defi ned because the base of the Sudr Formation is unexposed 
in the two studied sections.

Characteristic species. The most dominant planktonic 
species recorded in this zone yields a relative high abundance 
of biserial heterohelicids, while pseudoguembelinids, trise-
rial and globotruncanid species are generally very rare (Ta-
bles 3 & 4).

Remarks: The Micula prinsii Subzone coincides with 
part of the Pseudoguembelina palpebra and the whole Plum-
merita hantkeninoides zones (TANTAWY & KELLER, 
2000; KELLER et al., 2007; FAROUK & FARIS, 2008). The 
absence of Plummerita hantkeninoides and Gansserina gan-
sseri zones; in addition to the recognition of Micula prinsii 
confi rms the presence of the CF2 in the upper part of the 
Sudr Formation (Fig. 3).

4.2.2. Eoglobigerina edita Partial-range Zone

Defi nition: This zone is defi ned as the biostratigraphic inter-
val between the LO of Parvularugoglobigerina eugubina 
(LUTERBACHER & PREMOLI SILVA) and the FO of 
Praemurica uncinata (BOLLI).

Remarks: BERGGREN & PEARSON (2005) subdi-
vided the Eoglobigerina edita (P1) Zone from older to 
younger into the: 1) Parasubbotina pseudobulloides (P1a), 
2) Subbotina triloculinoides (P1b) and 3) Globanomalina 
compressa/Praemurica inconstans (P1c) subzones. In the 
present study, the P1b Subzone occurs directly on the Maas-
trichtian (CF2 Zone) (Fig. 3).

Subbotina triloculinoides Lowest-occurrence 
Subzone (P1b)

Defi nition: This subzone represents the biostratigraphic in-
terval from the FO of Subbotina triloculinoides (PLUM-
MER) to the FO of Globanomalina compressa (PLUM-
MER) and/or Praemurica inconstans (SUBBOTINA).

Occurrence: The zone is recorded from the basal part 
of the Beida Formation and only from the Gebel Umm 
Khushayb section. It is represented by samples 222–224 (0.5 
m thick). This subzone is missing in the west El-Hassana 
section due to the larger amplitude of the unconformity in 
this section.

Characteristic species. Characteristic taxa are frequent, 
moderately well preserved and include Globoconusa daub-
jergensis (BRÖNNIMANN), Globanomalina archeocom-
pressa (BLOW), Parasubbotina pseudobulloides (PLUM-



Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt Geologia Croatica
153

MER), Parasubbotina trivalis (SUBBOTINA), Subbotina 
triloculinoides, Praemurica pseudoinconstans (BLOW), 
Chi loguembelina midwayensis (CUSHMAN) and Ch. mor-
sei (KLINE) (Tables 3 & 4).

Remarks: At the K/Pg boundary, several changes are 
observed in the planktonic foraminiferal assemblages, in-
cluding the extinction of virtually all Cretaceous species 
(tropical-subtropical and cosmopolitan), and the fi rst appear-
ance of the Danian species. The Cretaceous species present 
at the base of a transgression of lower Danian sediments are 
reworked, and are represented by small cosmopolitan surface 
water dwellers such as Heterohelix and Pseudoguembelina 
with very rare Rugoglobigerina and Globotruncana spp..

The FOs of Globanomalina compressa and/or Praemu-
rica inconstans have been used to determine the base of Sub-
zone P1c (OLSSON et al., 1999; BERGGREN & PEAR-
SON, 2005). The authors believe that the FO of Glo ba no malina 
compressa predates that of the FO of Praemurica inconstans, 
and occurs within Zone P1b. A similar occurrence in Sub-
zone P1b was also reported by KELLER (2002). According 
to BERGGREN & PEARSON (2005), Zone P1b falls be-
tween the top part of the Cruciplacolithus tenuis (NP2) Zone, 
and the basal part of the Chiasmolithus danicus (NP3) Zone. 
Therefore, the authors believe that the base of Zone P1b 

should be absent in the Gebel Umm Khushayb due to ab-
sences of the Cruciplacolithus tenuis Zone NP2.

Globanomalina compressa/Praemurica inconstans 
Lowest-occurrence Subzone (P1c)

Defi nition: The biostratigraphic interval from the FO of 
Globanomalina compressa and/or Praemurica inconstans 
and the FO of Praemurica uncinata.

Occurrence: This zone is recorded from the lower part 
of the Dakhla Formation and represented only by samples 
7–8 (2.0 m thick) from the west El-Hassana section and it 
encompasses, samples 224–230 (3.0 m thick) at the Gebel 
Umm Khushayb section.

Characteristic species. In this interval the species are 
highly abundant and well preserved. The assemblage of this 
interval is similar to that of the underlying Subzone P1c with 
the addition of four more species Praemurica inconstans, 
Globanomalina compressa and Parasubbotina varianta 

(SUBBOTINA), Morozovella trinidadensis (BOLLI).
Remarks: KELLER (2002) subdivided Subzone P1c 

into two subzones, P1c (1) and P1c (2) based on the fi rst ap-
pearance of Praemurica inconstans. In the present study, the 
FOs of Praemurica inconstans, Globanomalina compressa 

Figure 3: Standard and alternative planktonic foraminiferal and calcareous nannofossil biozonations for the Palaeocene interval. 



Geologia Croatica 65/2Geologia Croatica
154

Table 3: Stratigraphic distribution of planktonic foraminiferal taxa identifi ed in the west El-Hassana section.

Ag
e

Fo
rm

at
io

n

Sa
m

pl
e 

N
o.

 

N
an

no
fo

ss
il 

Zo
ne

Pl
an

kt
on

ic
 fo

ra
m

. Z
on

e
G

lo
bo

tr
un

ca
na

 a
eg

yp
tia

ca
G

lo
bo

tr
un

ca
na

 ro
se

tt
a

Ru
go

gl
ob

ig
er

in
a 

he
xa

ca
m

er
at

a
Ru

go
gl

ob
ig

er
in

a 
m

ac
ro

ce
ph

al
a

Ru
go

gl
ob

ig
er

in
a 

ru
go

sa
H

et
er

oh
el

ix
 g

lo
bu

lo
sa

H
et

er
oh

el
ix

 d
en

ta
ta

H
et

er
oh

el
ix

 n
av

ar
ro

en
sis

H
et

er
oh

el
ix

 st
ria

ta
Ps

eu
do

gu
em

be
lin

a 
ha

ria
en

sis
Ps

eu
do

gu
em

be
lin

a 
co

st
ul

at
a

Ps
eu

do
te

xt
ul

ar
ia

 e
le

ga
ns

G
lo

bo
tr

un
ca

ne
lla

 su
bc

ar
in

at
us

.
Su

bb
ot

in
a 

tr
ilo

cu
lin

oi
se

s*
Su

bb
ot

in
a 

tr
iv

ia
lis

Su
bb

ot
in

a 
tr

ia
ng

ul
ar

is
Su

bb
ot

in
a 

co
nc

el
la

ta
Su

bb
ot

in
a 

ve
la

sc
oe

ns
is

Pa
ra

su
bb

ot
in

a 
ps

eu
do

bu
llo

id
es

Pa
ra

su
bb

ot
in

a 
va

ria
nt

a
Pa

ra
su

bb
ot

in
a 

va
rio

sp
ira

 
Pr

ae
m

ur
ic

a 
in

co
ns

ta
ns

*
Pr

ae
m

ur
ic

a 
un

ci
na

ta
*

G
lo

ba
no

m
al

in
a 

co
m

pr
es

sa
G

lo
ba

no
m

al
in

a 
eh

re
nb

er
gi

 
G

lo
ba

no
m

al
in

a 
ps

eu
do

m
en

ar
di

i*
Ch

ilo
gu

em
be

lin
a 

m
id

w
ay

en
sis

 
Ch

ilo
gu

em
be

lin
a 

m
or

se
i 

Ig
or

in
a 

pu
sil

la
Ig

or
in

a 
al

be
ar

i*
M

or
oz

ov
el

la
 p

ra
ea

ng
ul

at
a

M
or

oz
ov

el
la

 a
ng

ul
at

a*
M

or
oz

ov
el

la
 co

ni
co

tr
un

ca
ta

M
or

oz
ov

el
la

 a
pa

nt
he

sm
a

M
or

oz
ov

el
la

 p
as

io
ne

ns
is

M
or

oz
ov

el
la

  v
el

as
co

en
sis

 *
M

or
oz

ov
el

la
 a

cu
ta

 
M

or
oz

ov
el

la
 p

re
ae

qu
a 

M
or

oz
ov

el
la

 a
eq

ua
 

M
or

oz
ov

el
la

 o
cc

lu
sa

Ac
ar

in
in

a 
st

ra
bo

ce
lla

 
Ac

ar
in

in
a 

m
ck

an
na

i 

Th
an

et
ia

n
Ta

ra
w

an

45

N
P7

/8

P4
b

  R R R R R R R R

44   F R R F R R R R

43   F R R F R R R R

Se
la

nd
ia

n
D

   
   

 a
   

   
 k

   
   

  h
   

   
   

 l 
   

  a

42 NP6

P4
a

  C R R R F R R R R

41

N
P5

  F R R R F R R R  

40   C R R R R R R R R  

39

N
P4

N
Tp

8 P3
b

  R  

38   R R R VR R R R  

37   R R R R  

36   R R R R R R R R  

D
   

  a
   

  n
   

  i
   

a 
   

n

35   R R R R R R R F C R R R R  

34   R R R R R A R R R  

33

P3
a

  R R C R A R  

32

N
Tp

7

  C R R C C R A  

31   A R R R C R R R A  

30   A R R C A R C R F A  

29

P2

  A R R A R A C  

28   C R R R C C A R C  

27   C R C C C A R R  

26   A R C F C A R R  

25   A R C F C A R  

24   C R C F C A R  

23   C C F C A R  

22   C C R C A R  

21    

20   C A F R C R R  

19   C A R R C R R  

18   C A F F C R R  

17   R A F F A F R  

16   R R A F F A F R  

15   C R A C F C C R  

14

N
Tp

6

  C A C C C C  

13   C A C C C C  

12   C A A C R R  

11 C A A C  

10 C R R A C C C VR  

9 r r R R A C F R VR  

8
NP3 P1

c r r r C R A F R R VR  

7 r r r r F R A F R R VR  

La
te

st
 M

aa
s.

Su
dr

6

M
. p

rin
si

CF
2

A F C R      

5 A F R C R F VR    

4 VR VR A F R C F              

3 VR VR VR VR R A F VR C R C F R  

2 A F VR C R  

1 R   R R R A F VR C   R VR                                                            

A= Abundant
C= Common
F= Frequent
VR= Very Rare
R= Rare
r=reworked
*marker species



Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt Geologia Croatica
155

Table 4: Stratigraphic distribution of planktonic foraminiferal taxa identifi ed  in the Gebel Umm Khushayb section.

Ag
e

Fo
rm

at
io

n

Sa
m

pl
e 

N
o.

 

N
an

no
fo

ss
il 

Zo
ne

Pl
an

kt
on

ic
 fo

ra
m

. Z
on

e
G

lo
bo

tr
un

ca
na

 a
eg

yp
tia

ca
Ru

go
gl

ob
ig

er
in

a 
he

xa
ca

m
er

at
a

Ru
go

gl
ob

ig
er

in
a 

m
ac

ro
ce

ph
al

a
Ru

go
gl

ob
ig

er
in

a 
ru

go
sa

H
et

er
oh

el
ix

 g
lo

bu
lo

sa
H

et
er

oh
el

ix
 la

be
llo

sa
H

et
er

oh
el

ix
 n

av
ar

ro
en

sis
H

et
er

oh
el

ix
 st

ria
ta

Ps
eu

do
gu

em
be

lin
a 

ha
ria

en
sis

Ps
eu

do
gu

em
be

lin
a 

pa
lp

eb
ra

Ps
eu

do
gu

em
be

lin
a 

co
st

ul
at

a
Ps

eu
do

te
xt

ul
ar

ia
 e

le
ga

ns
G

lo
bo

tr
un

ca
ne

lla
 su

bc
ar

in
at

us
Su

bb
ot

in
a 

tr
ilo

cu
lin

oi
se

s
Su

bb
ot

in
a 

tr
iv

ia
lis

Su
bb

ot
in

a 
tr

ia
ng

ul
ar

is
Su

bb
ot

in
a 

ve
la

sc
oe

ns
is

Pa
ra

su
bb

ot
in

a 
ps

eu
do

bu
llo

id
es

Pa
ra

su
bb

ot
in

a 
va

ria
nt

a
Pa

ra
su

bb
ot

in
a 

va
rio

sp
ira

Pr
ae

m
ur

ic
a 

in
co

ns
ta

ns
*

Pr
ae

m
ur

ic
a 

un
ci

na
ta

*
G

lo
ba

no
m

al
in

a 
ar

ch
eo

co
m

pr
es

sa
 

G
lo

ba
no

m
al

in
a 

co
m

pr
es

sa
*

G
lo

ba
no

m
al

in
a 

eh
re

nb
er

gi
 

G
lo

ba
no

m
al

in
a 

ps
eu

do
m

en
ar

di
i*

Ch
ilo

gu
em

be
lin

a 
m

id
w

ay
en

sis
 

Ch
ilo

gu
em

be
lin

a 
m

or
se

i 
Ig

or
in

a 
pu

sil
la

Ig
or

in
a 

al
be

ar
i*

M
or

oz
ov

el
la

 p
ra

ea
ng

ul
at

a
M

or
oz

ov
el

la
 a

ng
ul

at
a*

M
or

oz
ov

el
la

 co
ni

co
tr

un
ca

ta
M

or
oz

ov
el

la
 a

pa
nt

he
sm

a
M

or
oz

ov
el

la
 V

el
as

co
en

sis
* 

M
or

oz
ov

el
la

 a
cu

ta
 

M
or

oz
ov

el
la

 p
re

ae
qu

a 
M

or
oz

ov
el

la
 a

eq
ua

 
M

or
oz

ov
el

la
 o

cc
lu

sa
Ac

ar
in

in
a 

st
ra

bo
ce

lla
 

Ac
ar

in
in

a 
m

ck
an

na
i 

Se
la

nd
ia

n
B 

   
   

 e
   

   
 I 

   
 d

   
   

a

251

N
P6

P4
a

R R R R R R R R R R

250 R R R R R R R R

249

N
P5

R R R R R R R R R R

248 R R R R R R R R  

247 R R R R R R  

246 F R R R C F A R C R  

245 R R R R R R R R R  

244

N
P4

N
Tp

8

R R F R F R R  

243

P3
b

R R R VR R R R R R R R  

242 C R VR A R R  

D
  a

  n
  i

   
a 

   
n

241 C R VR A F F R  

240 R R C R F VR R A C R  

239

N
Tp

7
P3

a

 

238 R F R R VR R F  

237 C VR R R R F F R C  

236

P2

R A R  

235 C C R  

234

N
Tp

6

C F  

233 C F  

232 C F  

231 C F      

230 A VR A C F F    

229

P1
c

R R A C F C A  

228 C R F C R F    

227

N
P3

C C F C R F  

226 F R C C C C  

225 F R A F F C VR  

224

P1
b

R R A F R VR VR  

223 C VR A F R  

222 r r R VR A F R  

M
aa

s.
Su

dr 221

C 
 C

26

CF
2 VR VR F F A R R A VR R R R VR  

220   R F F A C R A VR R R C VR                                                        

A = Abundant 
C = Common
F = Frequent
VR = Very Rare
R = Rare
r = reworked
*marker species

and Parasubbotina varianta occur directly above Zone CF2 
in the west El-Hassana section, indicating that the oldest Da-
nian sediments belong to the P1c (2) Subzone.

4.2.3. Praemurica uncinata Lowest-Occurrence 
Zone (P2)

Defi nition: This is the Biostratigraphic interval between the 
FO of Praemurica uncinata to the FO of Morozovella angu-
lata (WHITE).

Occurrence: The zone encompasses the middle part of 
the Dakhla Formation at the west El-Hassana section and is 
represented by samples 9–29 (15 m thick). In the Gebel Umm 
Khushayb section it is recorded from the middle part of the 
Beida Formation and is represented by samples 229–236 (8 
m thick).

Characteristic species. The Praemurica uncinata Zone 
is rich in its faunal content. The most dominant planktonic 
species recorded in this zone include: Globanomalina com-



Geologia Croatica 65/2Geologia Croatica
156

Characteristic species. Morozovella angulata, M. con-
icotruncata, Parasubbotina varianta, M. velascoensis (CU-
SHMAN), M. occlusa (LOEBLICH & TAPPAN), M. acuta 
(TOULMIN), M. aequa (CUSHMAN & RENZ), Subbotina 
velascoensis (CUSHMAN), Subbotina triloculinoides Igo-
rina albeari and I. pusillla (BOLLI) are the dominant plank-
tonic species in the P 3 b Subzone.

Remarks. Morozovella conicotruncata and M. pasion-
ensis fi rst appeared within the lower part of this subzone, 
while M. velascoensis, M. occlusa, M. acuta, M. preaequa 
and Subbotina velascoensis fi rst occurred within the upper 
part of the subzone (Tables 3 & 4).

4.2.5. Globanomalina pseudomenardii Total 
Range Zone (P4)

Defi nition: This zone is defi ned as the interval of the total 
range of the nominated taxon.

Occurrence: The zone occupies about 5.5 m of the up-
permost part of the measured Beida Formation at Gebel 
Umm Khushayb and is represented by samples 244–251. It 
also occurs in the topmost part of the Dakhla Formation, as 
well as the whole Tarawan Formation at the west El-Hassana 
section (samples 40–45).

Characteristic species. The dominant species in this 
subzone include angular morozovellids such as Morozovella 
acuta, M. aequa, M. velascoensis, M. occlusa, Acarinina 
mckannai (WHITE), A. strabocella (LOEBLICH & TAP-
PAN) and Subbotina velascoensis.

Remarks. BERGGREN AND PEARSON (2005) sub-
divided the P4 Zone into three subzones; Globanomalina 
pseudomenardii/Parasubbotina variospira (P4a) concurrent-
range Subzone; Acarinina subsphaerica (P4b) Partial-range 
Subzone and Acarinina soldadoensis/Globanomalina pseu-
domenardii (P4c) concurrent-range Subzone. In the current 
study, it was also diffi cult to subdivide the P4 into these bio-
zones due to the poor preservation of foraminiferal tests as 
a result of carbonate dissolution.

OLSSON et al. (1999) reported that the FO of Morozo-
vella aequa occurs at the lower boundary of the P4c Zone. 
In the present study, the FO of Morozovella aequa is recog-
nized at the top part of P3b Zone, which is equivalent to the 
top part of the calcareous nannofossil NP4 Zone. A similar 
occurrence in the P3b Zone was also reported by ARENI-
LAS (2012) in the Caravaca section of Spain.

5. STAGE BOUNDARIES

5.1. The Cretaceous/Palaeogene (K/Pg) boundary

The K/Pg boundary is marked by an abrupt lithological 
change that corresponds to the boundary between the Sudr 
and Dakhla formations at the west El-Hassana section or to 
the Sudr / Beida formation at Umm Khushayb. Biostrati-
graphic analysis (planktonic foraminifera, calcareous nan-
nofossils) confi rms that the studied sections are incomplete 
and discontinuous across the K/P boundary. A small hiatus 
is suggested by the absence of the Plummerita hantkeni-

pressa, Parasubbotina pseudobulloides, Parasubbotina va-
rian ta, Subbotina concellata (BLOW), S. trinagularis 
(WHI TE), S. triloculinoides, S. trivialis, Praemurica unci-
nata, P. inconstans and Morozovella praeangulata (BLOW) 
(Tables 3 & 4).

Remarks: Subbotina triangularis and S. concellata fi rst 
appear within the upper part of this biozone (Tables 3 & 4). 
STEURBAUT & SZTRÁKOS (2008), mentioned that the 
Praemurica uncinata Zone falls within the top part of the 
calcareous nannofossil Zone NTp6 in south-west France. In 
the present study, it falls within Zone NTp6 and the lower 
part of Zone NTp7. A similar occurrence was also reported 
by STEURBAUT et al. (2000) in the Kalaat Senan section, 
central Tunisia.

4.2.4. Morozovella angulata-Globanomalina 
pseudomenardii Interval Zone (P3)

Defi nition: This includes the interval from the FO of Moro-
zovella angulata to the FO of Globanomalina pseudomen-
ardii (BOLLI).

Occurrence: The biozone is represented by samples 30–
39 (4.5 m thick) in west El-Hassana, and sample 237–243 
(7 m thick) from Gebel Umm Khushayb. Various authors 
have observed that Zone P3 is condensed in this area (e.g. 
SAMIR, 2002; AL-WOSABI & ABU SHAMA, 2007 in 
Egypt; VAN ITTERBEEK et al., 2007 in Tunisia).

Remarks: BERGGREN et al. (1995), BERGGREN & 
NORRIS (1997) and OLSSON et al. (1999) re-subdivided 
P3 Zone into two subzones: the Morozovella angulata-Igo-
rina albeari Interval Subzone (P3a) and the Igorina albeari–
Globanomalina pseudomenardii Interval Subzone (P3b). In 
the present study the P3 Zone can also be divided into two 
subzones.

Morozovella angulata-Igorina albeari Interval 
Subzone (P3a)

Defi nition: interval from the FO of the Morozovella angu-
lata to the FO of Igorina albeari (CUSHMAN & BERMU-
DEZ).

Characteristic species. The planktonic assemblage of 
this subzone is dominated by morozovellids with angular 
conical chambers throughout their youngest whorl, such as 
Morozovella conicotruncata (Subbotina), M. Praeangulata, 
M. angulata (WHITE), and M. praecursoria (MOROZO VA). 
In addition, other taxa are also present: Subbotina triloculi-
noides, Globanomalina compressa, Igorina pusilla and Pra-
emurica uncinata (Tables 3 & 4).

Remarks: Globanomalina compressa, Praemurica un-
cinata, and P. inconstans disappeared in the lower part of 
this subzone.

Igorina albeari/Globanomalina pseudomenardii 
Interval Subzone (P3b)

Defi nition: This represents the Interval between the FO 
of Igorina albeari and the FO of Globanomalina pseudom-
enardii (BOLLI).



Faris and Farouk: Integrated biostratigraphy of two Upper Maastrichtian – Palaeocene successions in north-central Sinai, Egypt Geologia Croatica
157

noides, Guembelitria cretacea, Parvularugoglobigerina eu-
gubina Zones and Parasubbotina pseudobulloides Subzone. 
In the west El-Hassana section, the Subbotina triloculinoides 
Subzone is also missing. Moreover, the upper part of the cal-
careous nannofossil Micula prinsii Subzone and the earliest 
Danian Zones (NP1 and NP2) are missing. This hiatus may 
be linked to tectonic activity and irregular palaeotopography 
associated with low sedimentation rates as suggested by FA-
ROUK & FARIS (2008).

The K/Pg boundary is characterized by the extinction of 
Cretaceous tropical planktonic foraminifera, and an abrupt 
change in species richness. However, most of the Cretaceous 
calcareous nannofossil vanishing species progressively de-
crease in abundance within Zone NP4; only the most disso-
lution-resistant Cretaceous species (Micula decussata, Watz-
naueria barnesae) are still present near the top of Zone NP4. 
The Cretaceous persistent species progressively increase in 
abundance above the K/Pg boundary. Cyclagelosphaera re-
inhardtii is the most common Cretaceous persistent species 
in the Palaeocene.

5.2. The Danian/Selandian boundary

The global stratotype section and point (GSSP) across the 
Danian/Selandian (Da/Se) boundary has been defi ned in the 
Zumaia section, northern Spain close to the FO of F. tym-
paniformis, just below the NP4/NP5 boundary and within 
the planktonic foraminiferal P3b Zone (BERNOALA et al., 
2009). Based on calcareous nannofossils, the Danian/Se-
landian (Da/Se) boundary is delineated at a level close to the 
FO of Fasciculithus tympaniformis, just below the NP4/NP5 
boundary and it coincides with the End Acme of Braarudo-
sphaera bigelowii (BERNOALA et al., 2009). The Lowest 
Common Occurrence (LCO) of Braarudosphaera, which 
marked the lithological change at the D/S boundary at the 
type area in Denmark, can be directly correlated with the 
abrupt transition from the Danian limestones to the marly 
Itzurun Fm. at Zumaia (SCHMITZ et al., 1998; BERNAOLA 
et al., 2009). This event is not applicable to the Tethyan sec-
tions because Braarudosphaera was not recorded there 
(BER NAOLA et al., 2009). The Last Common Occurrence 
(LCO) of Braarudosphaera seems applicable for placing the 
base of the Selandian in Denmark, but it is an unreliable 
event for de lineating the Danian/Selandian boundary in the 
study sections.

Previously in Egypt, the Danian/Selandian was marked 
as a prominent organic-rich layer with a short-term sea-level 
fall coinciding with the P3a/P3b boundary, by using the low-
est occurrence of the slightly keeled Igorina as a zonal boun-
dary criterion (SPEIJER, 2003; OBAIDALLA et al., 2009; 
SPRONG et al., 2009). In the Qreiya section, the organic-
rich layer occurs approximately 1 m above the FOs of Chi-
asmolithus edentulus and small fasciculiths (SPRONG et al., 
2009). This event bed at the D/S boundary, situated at the 
base of the Subzone NTp7B, and the equivalent planktonic 
foraminiferal P3a/P3b zonal boundary, is now considered 
latest Danian in age (BERNOALA et al., 2009; YOUSSEF, 
2009).

On the other hand, FARIS & ABU SHAMA (2007) put 
the Danian/Selandian boundary at the base of Zone NP5. In 
the present study, it is bracketed within the Zone NTp8 (top-
most NP4 equivalent to top part of the planktonic foraminif-
era P3b Subzone), at a level close to the First Occurrence 
(FO) of Morozovella velascoensis, M. occulsa, M. aquea and 
M. acuta (below) and the FO of Fasciculithus tympaniformis 
(above) just below the NP4/NP5 boundary in west El-Has-
sana and Umm Khushayb sections, is similar to that of the 
Global Standard Stratotype-section and Point (GSSP) of the 
Da/Se boundary which has recently been selected at the Zu-
maia section.

An important global nannofossil event is the onset of the 
second radiation of Fasciculithus (F. bitectus, F. involutus, 
F. janii, F. billii and F. ulii). It starts within Zone NTp8 (top-
most NP4 and P3b) at a level close to the FO of F. tympani-
formis and just below the NP4/NP5 boundary in the study 
sections.

The fi rst continuous occurrence (FCO) of Sphenolithus 
primus, the marker taxon for the base of Subzone NTp8A of 
VAROL (1989), is a reliable marker for delineating the Da-
nian/Selandian transition (FARIS et al., 2005, QUILLE-
VERE et al., 2002). In the present study, the FRO (First Rare 
Occurrence) of Sphenolithus primus is not a useful global 
marker because it occurs rarely and sporadically. STEUR-
BAUT & SZTRÁKOS (2008) and BERNAOLA et al. (2009) 
also reported a similar occurrence for the FRO of Spheno-
lithus primus.

5.3. The Selandian/Thanetian boundary

The base of the Thanetian in its original type area, has been 
correlated within the upper part of the nannofossil Zone NP6 
(AUBRY, 1994; KNOX, 1994). The base of Chron C26n at 
Zumaian, as a continuous, deep marine and cyclic sequence, 
offers the possibility of establishing a potential Thanetian 
Unit Stratotype (DINARÈS-TURELL et al., 2007). It is po-
sitioned 30.5 m above the base of the Itzrun Formation, very 
close to the base of Chron C26N (SCHMITZ et al., 1998).

A minor hiatus is proposed at the Selandian/Thanetian 
boundary as indicated by a condensed interval that marks a 
lithological change from the calcareous shales of the Dakhla 
Formation to the limestones of the Tarawan Formation. 
Therefore, the Selandian/Thanetian boundary in the present 
study is located at the top of Zone NP6 and within the lower 
part of the Globanomalina pseudomenardii Zone. No great 
changes in the nannofossil assemblages have been observed 
in the west El Hassana section, except for the FO of Dis-
coaster mohleri. The Heliolithus kleinpellii Zone (NP6) is 
not recorded in several localities in Egypt (e.g. BASSIOUNI 
et al., 1991; FARIS et al., 1999; FARIS & ZAHRAN, 2002; 
AYYAD et al., 2003).

6. CONCLUSIONS

The results obtained can be summarized as follows:
1. An integrated calcareous nannofossil and planktonic fo-

raminiferal biostratigraphy has been achieved for the 



Geologia Croatica 65/2Geologia Croatica
158

Upper Maastrichtian-Palaeocene successions on the 
west El-Hassana and Umm Khushayb sections, north-
central Sinai. The Maastrichtian – Palaeocene material 
studied in this work consists of siliciclastic/carbonate 
deposits belonging to four formations: The Sudr, Dakhla, 
Tarawan formations, and their lateral coeval Beida For-
mation.

2. 44 calcareous nannofossil and 31 planktonic foraminif-
eral taxa are identifi ed with moderate to good preserva-
tion and relatively high diversity. These microfossil as-
semblages allowed subdivision of the study sections into 
one subzone and fi ve calcareous nannofossil zones: Mic-
ula prinsii Subzone (CC26c), Chiasmolithus danicus 
Zone (NP3), Ellipsolithus macellus Zone (NP4), Fas-
ciculithus tympaniformis Zone (NP5), Heliolithus klein-
pellii Zone (NP6), Discoaster mohleri Zone (NP7/8); 
and fi ve planktonic foraminiferal zones and four sub-
zones; Pseudoguembelina palpebra Zone (CF2), Eoglo-
bigerina edita (P1) Zone, Praemurica uncinata Zone 
(P2), Morozovella angulata-Globanomalina pseudom-
enardii Zone (P3), Globanomalina pseudomenardii 
Zone (P4). Zone P1 can be subdivided into the Subbotina 
triloculinoides Subzone (P1b), and the Globanomalina 
compressa/Praemurica inconstans Subzone (P1c). Zone 
P3 is subdivided into the Morozovella angulata-Igorina 
albeari Subzone (P3a), and the Igorina albeari/Globa-
nomalina pseudomenardii Subzone (P3b).

3. Biostratographic analyses of the two studied sections 
based on planktonic foraminifera and calcareous nan-
nofossils, indicate that deposition of the Latest Maas-
trichtian to Early Danian sediments was interrupted by 
erosion and or non-deposition related to tectonic activ-
ity. As a result, some planktonic foraminifera (Plummer-
ita hantkeninoides, Guembelitria cretacea, Parvularu-
goglobigerina eugubina biozones and, Parasubbotina 
pseudobulloides Subzone and their equivalent calcare-
ous nannofossils (top part of CC26c, NP1 and NP2 
zones) are missing.

4. The new-Palaeocene calcareous nannfossil taxa fi rst ap-
pear at the base of Zone NP3 of early Danian age. They 
progressively increase upwards and are more common 
than the Cretaceous vanishing species in Zone NP3 and 
NP4.

5. According to the Palaeocene Zonal Scheme of VAROL 
(1989); the nannofossil Zone NP4 of MARTINI (1971), 
can be divided into three subzones; NTp6, NTp7 and 
NTp8 in the west El-Hassana and Umm Khushayb sec-
tions. A small hiatus is observed at the NP3/NP4 zonal 
boundary as suggested by the absence of the NTp5B 
Subzone and NTp5C and most probably the lowermost 
part of Zone NTp6.

6. The onset of a second diversifi cation of the genus Fas-
ciculithus, represented by F. bitectus, F. involutus, F. ja-
nii, F. billii and F. ulii, begins within Zone NTp8 and 
just below the NP4/NP5 boundary in El Hassana and 
Umm Khushayb sections. This radiation marks the Da-
nian/Selandian boundary. Based on planktonic fora mi-

nifera, the Danian/Selandian boundary lies with the ba-
sal part of the P3b Subzone.

7. The Selandian/Thanetian boundary is placed at the con-
tact between the Dakhla and Tarawan formations at west 
El-Hassana, approximately at the top of calcareous na-
nofossil Zone NP6 within the equivalent planktonic fo-
raminiferal Zone P4. A minor hiatus was observed at this 
boundary as indicated by the prominent lithological 
chan ge from the calcareous shale of the Dakhla Forma-
tion to the limestones of the Tarawan Formation and the 
very condensed calcareous nannofossil Zone NP6.

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Manuscript received June 22, 2011
Revised manuscript accepted March 04, 2012

Available online June 29, 2012