GeolCarp_Vol62_No3_233

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, JUNE 2011, 62, 3, 233—249 doi: 10.2478/v10096-011-0019-6

Biostratigraphy and paleoecology of the Burdigalian—

Serravallian sediments in Wadi Sudr (Gulf of Suez, Egypt):

comparison with the Central Paratethys evolution

IBRAHIM M.

IED

, KATARÍNA HOLCOVÁ

and EZZAT ABD-ELSHAFY

Geology Department, Faculty of Science, Zagazig University, Zagazig, Egypt; ied_i_m@yahoo.com

Institute of Geology and Paleontology, Charles University, Prague, Albertov 6, CZ-128 43 Praha 2, Czech Republic;

holcova@natur.cuni.cz

(Manuscript received June 7, 2010; accepted in revised form

October 13, 2010)

Abstract: Two main Miocene facies were recorded in the Gulf of Suez area: a deep marine and a coastal facies. The
analysed sections in the Wadi Sudr area belong to the marine facies. The Lower Miocene (Burdigalian) is represented
by coastal, shallow marine sediments, rich in coral, algae, gastropods and large pectinids followed by Langhian open
marine sediments and Serravallian lagoonal carbonates. The open marine sediments contain well preserved planktonic
and benthic foraminifers and abundant ostracods. The parts of the sections containing foraminifers have been correlated
with three planktonic foraminiferal zones (Praeorbulina glomerosa Zone, Orbulina Zone and Globorotalia praemenardii—
Globorotalia peripheroronda Zone). Two benthic ecozones were defined (Heterolepa dutemplei—Laevidentalina elegans
Zone and Bolivina compressa—Elphidium spp. Zone). Two cycles of sea-level changes can be distinguished and corre-
lated with global sea-level cycles Bur5/Lan1 and Ser1. The first (Langhian) cycle culminated in open marine sublittoral
to upper bathyal well aerated sediments. The second (Serravallian) cycle was shallower, littoral suboxic sediments were
overlaid by euryhaline carbonates. The studied foraminifera-bearing sediments can be correlated with the lower and
Middle Badenian of the Central Paratethys. Though the area of the Gulf of Suez and the Central Paratethys were situated
in different climatic zones, and influenced by different tectonic events, the main paleoenvironmental events (sea-level
changes, oxygen decrease, salinity changes) are comparable. This correspondence shows that the decisive factors trig-
gering these events were global climatic events.

Key words: Miocene, Paratethys, Egypt, Gulf of Suez, paleoecology, biostratigraphy, foraminifers.

Introduction

Due to the importance of the Miocene sediments in the Gulf
of Suez as oil producing reservoirs, they have attracted the
attention of geologists since the 1930s. From the paleonto-

Fig. 1. Location of the studied sections.

logical  view  (including  Miocene  microbiostratigraphy),  the
sequences were studied by several authors, namely Macfadyen
(1931),  Stainforth  (1949),  Tromp  (1949),  Said  &  Bassiouni
(1958), Souaya (1965, 1966a,b), Ansary & Andrawis (1965),
Said  &  El  Heiny  (1967),  Kerdany  (1968),  Wasfi  (1969),

Cherif (1972), El Heiny & Martini (1981),
Andrawis  &  Abdel  Malik  (1981),  Sallam
(1987), Rateb (1988), Szczechura & Abd-
Elshafy  (1988),  Haggag  et  al.  (1990),
Abd-Elshafy  &  Abd-Elmoneim  (1992),
Cherif  et  al.  (1993),  Phillip  et  al.  (1997)
Abul-Naser  &  Salama  (1999),  Ibrahim  &
Mansour (2002) and Strougo et al. (2006).

The present study deals with the Miocene

exposures  lying  in  the  eastern  part  of  the
Gulf  of  Suez  in  the  area  located  15—20 km
southeast from Sudr city at the entrance of
Wadi  Sudr  from  the  west  (Fig. 1)  where
the  Miocene  deposits  overlie  Cretaceous—
Eocene sediments.

Though

many

micropaleontological

studies  have  been  done  on  this  area,  this
work  presents  biostratigraphical  correla-
tion  with  global  planktonic  foraminiferal
bioevents  and  the  first  quantitative  paleo-
ecological study.

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About 200—300 specimens of foramini-

fers from each sample were determined
(Fig. 5) and the relative abundances of taxa
were calculated. The recorded foraminifers
were studied and documented using a scan-
ning electron microscope in the Department
of Geology and Paleontology, Charles
University of Prague.

Benthic

foraminiferal

faunas

were

grouped  using  Q-mode  cluster  analysis  by
the  software  STATISTICA  (Tree  Cluster-
ing;  Euclidean  distance).  To  verify  results,
three algorithms were used: the single link-
age,  Ward’s  method  and  weighted  pair-
group average.

The following quantitative data were

used for paleoenvironmental interpretations:

(i) Abundance of foraminiferal tests in

1 g of dry sediment.

(ii) Diversity expressed as number of

foraminiferal species.

(iii) Relative abundances of lagenids.
(iv) Relative abundances of infaunal spe-

cies (Murray 1991, 2006; Spezzaferri et al.
2002; Báldi 2006).

(v) Relative abundances of cibicidoids.
(vi) Relative abundances of euryhaline

species (Ammonia spp., Elphidium spp.,
miliolids; Murray 1991, 2006), their abun-
dant occurrence may indicate oscillations of
salinity.

(vii) Oxygen contents were estimated us-

ing BFOI = Benthic Foraminiferal Oxygen
Index (Kaiho 1994, 1999):

BFOI = O/(O+D)*100,

where O is the number of oxic indicators
and D is the number of dysoxic indicators.
Oxic and dysoxic indicators were classified
according to Kaiho (1994, 1999), den Dulk
et al. (2000); Spezzaferri et al. (2002) and
Báldi (2006).

(viii) Paleodepth was estimated using the

relationship  between  bathymetry  and  rela-
tive  abundance  of  planktonic  foraminifers
as proposed by van der Zwaan et al. (1990).
This relationship between plankton/benthos-
ratio  (P/B-ratio)  and  depth  is  based  on  the
fact that availability of nutrients on the sea
floor depends on depth:

Depth [m]= e

3.58718+(0.03534 Pc)

where Pc is the corrected ratio of plankton-
ic/benthic foraminifers:

Pc = (P 100)/[P + (Bt—Bi)],

where P is the number of planktonic fora-
minifers, Bt is the total number of benthic
foraminifers and Bi is the number of deep

Fig. 3. Lithostratigraphy of the Lower/Middle Miocene rocks in the north Wadi Sudr
area (section II).

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infaunal species (van der Zwaan et al. 1990; van Hinsbergen
et  al.  2005;  Báldi  2006)  which  are  excluded  from  analysis
because they are not directly dependent on the flux of organ-
ic  matter  to  the  sea  floor.  The  P/B-ratio  is  not  only  influ-
enced  by  depth,  but  also  by  changes  in  the  oxygenation  of
bottom waters (Sen-Gupta & Machain-Castillo 1993; Joris-
sen  et  al.  1995)  which  may  fluctuate  (Kouwenhoven  et  al.
2003).  A  discrepancy  between  calculated  paleodepths  and
sedimentological record has been pointed out for the Middle
Miocene  of  the  Central  Paratethys  (Hohenegger  2005).
Therefore,  calculated  paleodepths  were  compared  with
paleodepths  estimated  from  the  depth  ranges  of  some  fora-
miniferal  genera  and  species  (Murray  1991,  2006;  Ho-
henegger 2005).

Results and discussion

Lithology

Since Moon & Sadek (1923, 1925), the lithologies of the

Miocene rocks in the Gulf of Suez have been studied by many
authors,  including  Stainforth  (1949),  Sadek  (1959),  and
Ghorab & Marzouk (1967), Said & El Heiny (1967), the Na-
tional Stratigraphic Sub-Committee (1976), Grafunkel & Bar-
tov  (1977),  El  Heiny  (1982),  Hamza  (1988),  Saber  (1991),
Abd-Elmoneim  (1992),  Darwish  &  El-Azabi  (1993),  Abd-
Elshafy  &  Eweda  &  Zalat  (1996),  Refaat  (2002),  El-Azabi
(2004) and others.

According to the National Stratigraphic Sub-Committee

(1976), the Miocene rocks in the Gulf of Suez are represented
by two different facies:

(1) A deep marine facies, which is divided into:

(i) The lower mainly clastic Gharandal Group with its

Nukhul, Rudeis and Kareem Formations; in the studied
east Sudr area, Saber (1991) distinguished this group as
Gharandal Formation with the lower clastic unit consist-
ing of conglomerates, sandstones, marls and limestones;
and the upper carbonate unit consisting of limestones,
marls and sandstones. Mandur (2009) correlated the up-
per part of the Rudeis Formation with the NN4 calcare-
ous nanoplankton Zone (17.95—14.91 Ma, Lourens et al.
2004) and the Kareem Formation with the NN5 Zone
(14.91—13.65 Ma, Lourens et al. 2004).

(ii) The upper Ras Malaab Group is mainly evaporite

with  the  Belayim,  South  Gharib  and  Zeit  Formations.
From  the  Wadi  Sudr  area,  Saber  (1991)  described  this
group  as  the  Ras  Malaab  Formation  consisting  of
evaporites with thin claystone interbeds.

(2) A non-marine (coastal) facies which includes the Abu

Gerfan, Gharamul, Gemsa and Sarbut El Gamal Formations
(Ghorab  &  Marzouk  1967).  In  the  study  area  (Wadi  Sudr),
Eweda  &  Zalat  (1996)  restudied  the  stratigraphy  of  the
coastal facies and divided them into (i) the Abu Gerfan For-
mation:  coarse,  calcareous  conglomerate  alternating  with
gritty, coralline limestone and sandy, fossiliferous limestone
interbeds  and  (ii)  the  Gharamul  Formation:  limestone  se-
quence  –  algal  coralline  limestone  with  rare  marl,  sand-
stone and claystone intercalations.

Fig. 5.

Biostratigraphical

correlation

the

studied

sections

based

planktonic

foraminiferal

events.

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Due to the occurrence of open marine fauna such as fora-

minifers, ostracods and calcareous nannoplankton, the studied
Miocene  exposures  in  Wadi  Sudr  can  be  correlated  with  the
marine facies (Gharandal Group). Following the classification
of the National Stratigraphic Sub-Committee (N.S.S.C. 1976)
suggested  for  the  eastern  coast  of  the  Gulf  of  Suez,  the
section I  in  Wadi  Sudr  belongs  to  the  Early  Miocene  Rudeis
Formation  (samples 1—26).  The  upper  part  of  section I  (sam-
ples 27—38) and the whole of section II can be correlated with
the Kareem Formation (Figs. 2, 3).

The Rudeis Formation consists mainly of pale yellow,

moderately  compact,  massive,  argillaceous  limestone  with
yellow  to  grey,  massive,  calcareous,  argillaceous  sandstone
and  yellow,  moderately  compact,  massive  claystone  fol-
lowed  by  white,  massive,  argillaceous  coralline  limestone
with  yellowish  grey,  bedded,  calcareous  claystone  contain-
ing  banks  of  pelecypods  (Chlamys  zitteli  etc.)  and  gastro-
pods;  the  proportion  of  the  claystone  increases  toward  the
top with two main marl beds (Fig. 2).

In the lower part, the Kareem Formation consists of pale yel-

low to yellowish grey, soft, highly fossiliferous marls with fis-
sile shale intercalated, upwards sporadically slightly dolomitic
or sandy. Rich foraminifers, ostracods and calcareous nanno-
plankton assemblages were recorded here. In the upper part, the
marls are followed by yellow to brown, compact, massive, do-
lomitic limestones, slightly argillaceous and sandy (Fig. 3).

Fossil associations

The studied Miocene sections contain three fossiliferous

horizons:  (1)  The  lower  part  of  section I  (samples 1—26,
Fig. 2)  is  rich  in  macrofossils  such  as  algae,  corals,  gastro-
pods and pelecypods (Chlamys zitteli) and does not contain
microfossils; (2) The upper part of section I (samples 26—38,
Fig. 2) and the lower part of section II (samples 1—13, Fig. 4)
is rich in foraminifers and ostracods. The highest abundanc-
es of both planktonic and benthic foraminifers were recorded
at  the  base  of  the  second  section  (section II,  samples 1—6,
Fig. 4);  (3)  In  the  upper  part  of  section II  (samples 15—19)
foraminifers and ostracods are common (Fig. 4).

In both sections, sixteen planktonic and fifty nine benthic

foraminiferal species were identified (Figs. 2, 4, 10, 11). Good
preservation of foraminiferal tests without abrasions, no size
sorting, occurrence of both juvenile and adult specimens in
samples 1—6, 11—13, 15—21 show that these assemblages are
autochthonous (Holcová 1996). Rare, small and recrystal-
lized tests in samples 7—10 are very probably reworked.

Foraminiferal biostratigraphy

The Miocene sea in the Wadi Sudr area represented a mar-

ginal, periodically isolated basin of the Mediterranean.
Therefore, some biostratigraphical events may not have been
isochronous to the Mediterranean ones.

In the upper part of section I and lower part of section II,

the succession of the following important planktonic fora-
miniferal events were recorded (Fig. 5):

(1) The FO ( = first occurrence) of Praeorbulina sicana

(sample 27, section I; below the base of section II) which is

correlated  with  boundary  of  M4/M5  and  N7/N8  Zones.  This
event was dated to 17.0 Ma in the world ocean (Lourens et al.
2004).  In  the  Mediterranean  area,  this  event,  as  proposed  by
Bicchi  et  al.  (1994),  indicated  the  upper  boundary  of  the  G.
trilobus  interval  Zone;  Mancin  et  al.  (2003)  considered  the
event reliable for the definition of Mediterranean zonal bound-
aries;  Fornaciari  &  Rio  (1996)  dated  it  to  about  16.6 Ma.  In
the  studied  sections,  the  FO  of  Praeorbulina  sicana  corre-
sponds to a new transgression (the base of Kareem Formation)
correlatable  with  the  Bur5/Lan1  boundary  (Hardenbol  et  al.
1998).  Therefore,  the  event  may  be  isochronous  in  the  Wadi
Sudr area and in the “Central” Mediterranean.

(2) The LO ( = last occurrence) of Catapsydrax dissimilis (sam-

ple 1, section II; Fig. 11.27—28) is dated at 17.54 Ma (Lourens et
al. 2004). This species is very rare and occurs in the sample
together with Praeorbulina glomerosa. It is probably reworked
and cannot be used as a zonal marker in the studied sections.

(3 & 4) The FO and LO of Praeorbulina glomerosa were

recorded in sample 34 of section I and sample 3 of section II
(Fig. 11.24). Dating of this event differs for the oceanic realm
(16.1 Ma, Berggren et al. 1995; 16.27 Ma Lourens et al. 2004)
and for the Mediterranean (15.1 Ma, Abdul Aziz et al. 2008).
Mancin et al. (2003) consider this event to be weakly reliable
in the Mediterranean area which agrees with its later appear-
ance in the Mediterranean (see above). The LO of Praeorbuli-
na glomerosa is dated at 14.8 Ma (Lourens et al. 2004).
Because the species was recorded only rarely in one sample,
these events must be evaluated critically.

(5) The FO of Orbulina suturalis (sample 4 of section II; Fig.

11.25) is dated to 15.1 Ma (Berggren et al. 1995) or 14.74 Ma
(Lourens et al. 2004, as Orbulina spp.) in the world oceans. For
the Mediterranean it was dated to 14.7 Ma (Foresi et al. 1998)
or 14.56—14.58 Ma (Abdul Aziz et al. 2008). This event is used
in Mediterranean Zonation as a very good zonal marker (Forna-
ciari et al. 1997). In the Wadi Sudr area, the event occurred in
the interval of outer shelf-upper bathyal setting in which good
communication with the “central” Mediterranean could be ex-
pected. Therefore isochronity of these events in the “central”
Mediterranean and the Wadi Sudr area is supposed.

(6 & 7) The LOs of Praeorbulina sicana and Globorotalia

peripheroronda  (sample 6  of  section II)  are  heterochronous
events in the world oceans. The LO of Praeorbulina sicana
is dated to 14.53 Ma (Lourens et al. 2004) while the LO of
Globorotalia peripheroronda is dated 13.80 Ma and can ap-
proximately mark the Langhian/Serravallian boundary (Lou-
rens  et  al.  2004).  In  the  Mediterranean,  the  event  was
recorded to 13.34—13.41 Ma (Abdul Aziz et al. 2008). Earli-
er disappearance of the species in the section studied might
have  been  caused  by  deterioration  of  environment,  because
in this level more planktonic taxa (G. bisphericus, O. sutura-
lis) also disappear.

(8) The FO of Orbulina universa (sample 13 of section II) de-

fines the boundary of Zones N8/N9 or M5/M6 at 14.74 Ma
(Lourens et al. 2004). In the Mediterranean, it is recorded later
(about 14.3 Ma, Foresi et al. 1998; 14.3 Ma, Abdul Aziz et al.
2008) and may occur diachronously (Casolari et al. 2000). This
and the following events were related to the beginning of new
cycles and the probable restoration of good communication be-
tween the Wadi Sudr area and the “central” Mediterranean.

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Therefore these events might occur in the Wadi Sudr area in the
same time or later than in the other parts of the Mediterranean.

(9) The FO of Globorotalia praemenardii (sample 15,

section II; Fig. 11.36—37) was recorded above a hiatus interpret-
ed from the sedimentary record (Fig. 3). In the Mediterranean
area, this event is dated to 13.90—13.92 Ma (Abdul Azis et al.
2008) or about 14.1 Ma (Foresi et al. 1998) and was recorded
both above and below the FO of Orbulina universa (Mancin et
al. 2003) which impeaches the reliability of this event.

The above mentioned bioevents and their reliability discussed

above were used for correlation of the studied sections (parts with
planktonic  foraminifers:  section I,  samples  26—38;  section II,
samples 1—19) with the Mediterranean zonal schemes of Cita &
Premoli  Silva  (1960),  Cita  &  Blow  (1969),  Bizon  &  Bizon
(1972),  Cita  (1975,  1976),  Bizon  (1979),  Borseti  et  al.  (1979),
Iaccarino (1985), Bicchi et al. (1994), Sprovieri et al. (2002a,b),
Mancin  et  al.  (2003),  Iaccarino  et  al.  (2004)  and  the  Miocene
foraminiferal  zones  from  Egypt  of  Kerdany  (1968),  Wasfi
(1969), El-Heiny & Martini (1981), Rateb (1988), Haggag et
al. (1990), Ibrahim & Mansour (2002) (Fig. 6).

The following Mediterranean planktonic foraminiferal bio-

zones were recognized (Fig. 5):

IFN5 Praeorbulina glomerosa Interval Zone ( = M5 Zone of

Berggren et al. 1995)

Authors of the zone: Bizon & Bizon (1972); amended by

Mancin et al. (2003); upper Burdigalian – lower part of
Langhian.

The lower boundary (FO of Praeorbulina sicana; originally

Praeorbulina glomerosa s.l. which also includes Praeorbuli-
na sicana (Iaccarino 1985)) was recorded in the sample 27,
section I. The upper boundary is represented by the FO of Or-
bulina suturalis (sample 4 of section I).

Because Praeorbulina glomerosa s.str. is rare in the studied

material (in section II it occurs only in one sample), we do not
use its FO for subdividing Zone M5 into the M5a and M5b
Subzones (Bergreen et al. 1995).

In the Gulf of Suez area, the Praeorbulina glomerosa Zone

was described by Kerdany (1968), El Heiny & Martini (1981)
and Haggag et al. (1990).

Besides the index species, in the studied sections this zone

is characterized by occurrence of the following planktonic
foraminiferal species: Globigerinella obesa, Globigerinoides
sicanus and G. quadrilobatus.

Fig. 6. Biostratigraphical correlation of studied sections with local (Gulf of Suez) planktonic foraminiferal biostratigraphy.

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IFN6 Orbulina Interval Zone

The base of this zone can be well correlated with the base of

the M6 Zone of Berggren et al. 1995 ( = FO Orbulina spp.).
Because the succession of the FOs of Orbulina spp. was re-
corded in the study material, they were used to subdivide the
IFN6 Zone into two subzones.

IFN6a Orbulina suturalis Subzone ( = ± M6 Zone of Berg-

gren et al. 1995)

Authors: Iaccarino & Salvatorini (1982); upper Langhian.
The boundaries of this subzone are defined by the FO of Or-

bulina suturalis (sample 4 of section II) to the FO of Orbulina
universa (sample 13, section II).

In the Mediterranean area, the zone is equivalent to the

Globorotalia peripheroronda/Orbulina suturalis Zone of Bizon
& Bizon (1972), the Orbulina suturalis Zone of Borsetti et al.
(1979) and the Orbulina suturalis Subzone of Iaccarino (1985).

In the Gulf of Suez, the Zone is equivalent to the Orbulina

suturalis Zone which was recorded from the Gulf of Suez by
Haggag et al. (1990), the lower part of the Orbulina suturalis/
Globorotalia fohsi peripheroronda Zone of El Heiny & Marti-
ni (1981), the Globorotalia fohsi peripheroronda Zone of
Wasfi (1969) and to the Globoquadrina altispira/Globorota-
lia fohsi peripheroronda Zone of Kerdany (1968).

The interval started with a turnover in the planktonic fora-

miniferal assemblages: Globigerinella spp. disappeared, while
Orbulina suturalis (with its morphotype O. bilobata) ap-
peared together with Globorotalia peripheroronda and Globi-
gerinoides immaturus.

IFN6b Orbulina universa Subzone ( = ± uppermost part of

M6 Zone and lower part of M7 Zone of Berggren et al. 1995)

Authors: Iaccarino & Salvatorini (1982).
Although Iaccarino & Salvatorini (1982) and Iaccarino

(1985) correlated this zone with the Serravallian, a recent dat-
ing of the FO of Orbulina universa in the Mediterranean area
(Abdul Azis et al. 2008) points out that the age of uppermost
Langian for the subzone is more probable.

In the studied sections, only the lower boundary ( = the FO

of Orbulina universa) was recorded. This zone ends at the hia-
tus below the sample 14 in section II.

This zone can be approximately correlated with the Orbuli-

na universa Zone, which was recorded from the Gulf of Suez
by Haggag et al. (1990). It is equivalent to the upper part of
the Orbulina suturalis/Globorotalia fohsi peripheroronda
Zone of El Heiny & Martini (1981); Globigerinoides sicanus/
G. transitoria Zone of Wasfi (1969) and Orbulina suturalis
Zone of Kerdany (1968).

(?)Globorotalia praemenardii—Globorotalia peripheroronda

Subzone ( = ± upper part of M7 Zone of Berggren et al. 1995)

Authors: Iaccarino & Salvatorini (1982); Serravallian.
This zone begins with the FO of the Globorotalia praeme-

nardii and ends with the LO of Globorotalia peripheroron-
da. The samples 15—19 of section II could be correlated with

this zone, though only very rare planktonic foraminifers
occur in this interval.

In Egypt, the zone is equivalent to the Globorotalia kugleri/

Globoquadrina  altiaperta  globosa  Zone  (Said  &  El  Heiny
1967) in Abu Rudeis well No. 2, the Globoquadrina altiaper-
ta/Globorotalia  fohsi  peripheroronda  Zone  (Kerdany  1968)
and  the  Globorotalia  mayeri  Zone  described  in  the  Gulf  of
Suez (Haggag et al. 1990) and in North Western Desert (Ibra-
him & Mansour 2002).

Benthic foraminiferal ecozones

The distribution of the recorded benthic foraminiferal asso-

ciations revealed the presence of two local ecozones which are
defined  and  described  for  the  first  time  in  the  present  work.
The  boundary  between  the  zones  (sample 14,  section II)  re-
flects a clear ecological change documented by a turnover in
benthic foraminiferal faunas. At this turnover, 19 benthic fora-
miniferal  species  disappeared,  and  about  30  species  disap-
peared successively below the boundary. This change is also
reflected  in  cluster  analysis  (Fig. 9).  Possible  ecological  fac-
tors that may have caused this faunal turnover are interpreted
in the following subchapter.

Heterolepa dutemplei—Laevidentalina elegans Assemblage

Zone (samples 1—13, section II)

In addition to the nominate species, this zone is character-

ized by Nodosaria badensis, N. longiscata, Stilostomella con-
sobrina,  St.  adolphina,  Lenticulina  calcar,  L.  melvilli,  L.
inoronata,  Gyroidina  danvillensis,  G.  zelandica,  Textularia
gramen, Riminopsis boueanus, Uvigerina bellicostata, Uvige-
rina  semiornata,  Uvigerina  pudica,  Uvigerina  moravia,  Bo-
livina  digitalis,  Fursenkoina  schreibersiana  and  Lenticulina
vortex.  This  zone  can  be  correlated  with  the  Praeorbulina
glomerosa,  Orbulina  suturalis  and  Orbulina  universa  plank-
tonic foraminiferal Zones.

Bolivina compressa—Elphidium spp. Assemblage Zone

(samples 15—19, section II)

This zone is characterized by Elphidium flexuosum, Elphi-

dium crispum,  Paragaudryinella  interjuncta,  Siphonodosaria
advena, Pappina parkeri, Praeglobobulimina pyrula and Bo-
livina  compressa.  This  zone  can  be  correlated  with  the
Globorotalia  praemenardii—Globorotalia  peripheroronda
Subzone (planktonic Foraminifera).

The zones are local and cannot be correlated with the zona-

tion of Souaya (1966a,b) based on samples from the southern
part of the Gulf of Suez.

Burdigalian/Langhian and Langhian/Serravallian bound-
aries

The Burdigalian/Langhian boundary is dated to 15.974 Ma

and lies in the M5 planktonic foraminiferal Zone above the
FO of Praeorbulina glomerosa s.str. (Gradstein et al. 2004).

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The data from Mediterranean showed a later FO of Praeor-

bulina glomerosa glomerosa (Abdul Azis et al. 2008) in com-
parison with the data of Lourens et al. (2004) from the oceanic
realm. It agrees with the description of the succession of bio-
events in the historical Langhian stratotype (Odin et al. 1997)
where the Burdigalian/Langhian boundary is situated between
the FOs of Praeorbulina sicana and Praeorbulina glomerosa.
Because  more  accurate  biomarkers  were  not  recorded  in  the
studied sections, biostratigraphically the boundary could have
been determined only approximately (similarly to the histori-
cal Langhian stratotype) between the FOs of Praeorbulina si-
cana  and  Praeorbulina  glomerosa  (in  the  intervals  of
samples 27—34  of  section I  and  1—3  of  section II).  The  litho-
logical  or  ecological  turnover  and  hiatus  between  the  sam-
ples 25/26 (section I), which can be correlated with the Bur5/
Lan1 boundary, is situated below the biostratigraphically de-
termined Burdigalian/Langhian boundary. It agrees with cor-

relation of the Bur5/Lan1 with the uppermost Burdigalian
(Gradstein et al. 2004).

The Langhian/Serravallian boundary is dated to 13.654 Ma

in the M7 planktonic foraminiferal Zone and can be correlated
with  the  Lan2/Ser1  boundary  (Lourens  et  al.  2004).  In  the
Mediterranean  area,  the  boundary  is  close  to  the  FO  of
Globorotalia  praemenardii  (13.90—13.92 Ma;  Abdul  Azis  et
al.  2008).  In  the  studied  sections,  the  boundary  is  correlated
with the beginning of the new sea-level cycle with planktonic
foraminifers  Globorotalia  praemenardii  (between  sam-
ples 13/14 of the section II).

Paleoenvironmental analysis

The paleoecological analysis is based on a detailed quantita-

tive study of the rich foraminiferal assemblages from
section II and from the uppermost part of section I. Using

Fig. 7. Quantitative characteristics of foraminiferal assemblages from section II used for paleoecological interpretation. For explanation of
calculation of the BFOI and the paleodepth see chapter Methods.

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changes  of  quantitative  characteristics  of
foraminiferal assemblages as well as clus-
ter analysis and taphonomical analysis of
assemblages  together  with  lithological
characteristics  (Figs. 2,  3,  7,  8),  two  cy-
cles were distinguished:

(1) The lower cycle can be subdivided

into two intervals:

(i) The late Burdigalian/Langh-

ian interval started with shallow-
water

assemblages

(section I,

samples 35—37)  followed  by  rich
and  diversified  foraminiferal  as-
semblages  dominated  by  lagenids
and  cibicidoids  in  samples 1—6,
section II. The foraminifera indicate
normal  marine  environment  and
high oxic conditions (Fig. 7). Paleo-
depth  estimations  from  the  P/B-ra-
tio  and  from  the  depth  distribution
of  taxa  (Figs. 7,  8)  are  comparable
and indicate depths of 50—100 m in
the lower and upper parts of this in-
terval and 100—300 m in the middle
part  (sample 4,  section II).  Charac-
teristics of foraminiferal assemblage
in sample 4 correspond to character-
istics  of  high-stand  assemblages
summarized  by  Armentrout  et  al.
(1990).  Decreasing  abundance  and
diversity  of  foraminiferal  assem-
blages  in  samples 6—8  (section II),
occurrence of reworked tests in sam-
ples 7—10  (section II)  as  well  as  ap-
pearance  of  euryhaline  species  may
indicate a shallower environment. It
can  be  corroborated  by  paleodepth
20—50 m  estimated  from  depth  dis-
tribution of species (Fig. 8).

(ii) The late Langhian interval

starts  between  the  samples 10/11,
where  diversity,  abundance  and
P/B-ratio  of  foraminifer  increase
and  reworked  tests  disappear.
Paleodepth resulted from the depth
distribution  of  recorded  species
has  been  estimated  at  50—100 m,
although  calculated  paleodepths
from  the  P/B-ratio  are  higher  but
less probable (Fig. 7).

assemblages  of  Serravallian  age  indicate  suboxic  conditions
and  probably  much  shallower  conditions  than  the  calculated
paleodepth  from  the  P/B-ratio  (Fig. 7).  The  paleodepth  esti-
mated  from  the  depth  distribution  of  foraminiferal  taxa  indi-
cates  values  of  20—50 m  (Fig. 8).  Suboxic  stenohaline
conditions are gradually changed to very shallow euryhaline
environment at the beginning with dominance of euryhaline
foraminiferal  species.  Later  foraminifers  disappear.  Bio-
stratigraphical correlation based on the FO of planktonic fo-

Fig. 8. Benthic foraminiferal species from section II with known depth distribution
(Murray 1991; Hohenegger 2005). Grey rectangles illustrate intersection of depth ranges
of foraminifers and estimation of paleodepth for separate intervals of the section.

Biostratigraphical correlation using planktonic for-

aminifers enables us to correlate the lower boundary of
this interval (section I, sample 35) with the Bur5/Lan1
boundary (Hardenbol et al. 1998) and upper boundary
(section II, sample 13) with the Ser1 boundary
(Hardenbol et al. 1998).

(2) The Serravallian cycle starts with conglomeratic sand-

stone (sample 14, section II). Samples 15—19 are clearly dis-
tinguished using cluster analysis (Fig. 9). New foraminiferal

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Fig. 9. Results of cluster analysis for samples from section II.
Fig. A—C compares dendrograms obtained by different clustering
techniques.

raminifers Globorotalia praemenardii enables us to correlate
the base of the cycle with the Ser1 boundary (Hardenbol et
al. 1998).

Comparison of the Middle Miocene evolution of the Gulf of
Suez and the Central Paratethys

During the study period the Gulf of Suez formed a marginal

part of the Mediterranean, while the Central Paratethys area

was a chain of basins connected with the Mediterranean (e.g.
Popov et al. 2004). Though these areas were separated by
about 4000 km in the south-north direction (according to the
paleogeographical reconstruction of Popov et al. 2004) in dif-
ferent climatic zones, and influenced by different tectonic
events (Kováč et al. 2007), there are some similarities between
the Middle Miocene evolution of these areas.

According to planktonic foraminiferal bioevents, the Langh-

ian sediments from the Wadi Sudr area can be correlated with
the  Badenian  sediments  of  the  Lower  and  Upper  Lagenidae
Zones  including  the  sediments  of  the  Grund  Formation  of
Austria and Moravia (Ćorić & Rögl 2004; Tomanová Petrová
& Švábenická 2007; Rögl et al. 2007, 2008; Hohenegger et al.
2009a,b).  In  the  Central  Paratethys,  the  Lower/Middle  Mio-
cene boundary is strongly influenced by a local tectonic event:
the  Styrian  Tectonic  Phase  of  Stille  (1924).  Sedimentation
gaps  named  the  “Styrian  Unconformity”  characterized  this
boundary interval (Rögl et al. 2007; Hohenegger et al. 2009b).
After  this  gap,  a  first  Badenian  transgression  was  recorded
within nannoplankton Zone NN4 with rare Praeorbulina sica-
na (Hohenegger et al. 2009b). The main Badenian transgres-
sion covering all the Central Paratethys followed in the NN5
Zone with occurrence of Praeorbulina circularis and Orbuli-
na  suturalis.  This  large  marine  transgression  occurred  in  the
entire  circum-Mediterranean  area  (Rögl  &  Steininger  1983;
Rögl  1998,  1999;  Kováč  et  al.  2007;  Rögl  et  al.  2008;  Ho-
henegger et al. 2009a,b).

In the Wadi Sudr area, sediments with Praeorbulina also

correspond to the new transgression (the base of Kareem For-
mation). However, a hiatus, correlatable in both areas with the
Bur5/Lan1  boundary  of  Hardenbol  (1998),  is  not  so  pro-
nounced as in the Central Paratethys influenced by local tec-
tonics. In both areas, the following marine paleoenvironment
is the deepest in the whole Middle Miocene and contains open
marine  planktonic  foraminifera.  The  interval  corresponds  to
the  Middle  Miocene  Climatic  Optimum  (Gonera  et  al.  2000;
Bicchi et al. 2003; Böhme 2003).

During the Middle Badenian (the interval corresponds ap-

proximately to the Langhian/Serravallian transition), commu-
nication  between  the  Mediterranean  and  the  Paratethys
continued.  A  warm-temperate  climate  in  the  Early  Badenian
was followed by a temperature decline (Middle Miocene Cli-
matic  Transition:  Gonera  et  al.  2000;  Bicchi  et  al.  2003;
Böhme  2003;  Harzhauser  &  Piller  2007)  and  the  global  sea-
level fall around 14.8 Ma can be correlated with the Mi3-event
(Billups & Schrag 2002; Abels et al. 2005). This sea-level fall
has  been  recorded  in  both  areas:  in  the  Central  Paratethys
(Filipescu & Girbacea 1997; Rögl 1998; Báldi et al. 2002) as
well  as  in  the  Wadi  Sudr  area.  Foraminiferal  assemblages  in
the  Pannonian  Basin  of  the  Central  Paratethys  suggest  that
during the Middle Badenian increasing food supply, decreas-
ing oxygen level and growing stress on the sea floor occurred
(Báldi  2006).  These  changes  may  be  characteristic  not  only
for  the  Central  Paratethys:  foraminiferal  assemblages  enable
us to interpret an oxygen decrease also in Wadi Sudr area.

The following evaporite event can also be recorded in both

areas. The “Wielician” Central Paratethys event is character-
ized by deposition of mostly sulphate facies in shallow littoral
parts of the foredeep, while chloride-sulphate facies developed

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in the deepest part of the basin (Oszczypko & Ślączka 1989;
Ghergari  et  al.  1991;  Oszczypko  1997;  Petrichenko  et  al.
1997; Andreyeva-Grigorovich et al. 1999, 2003; Bąbel 2004,
2005; Oszczypko et al. 2006). In the study area the evaporite
event  started  with  suboxic  conditions  gradually  changing  to
very  shallow  euryhaline  environment  with  disappearance  of
foraminifers.

Conclusions

The present biostratigraphical and paleoecological study of

two sections in the Wadi Sudr area enriches the information
about the Miocene history of the joined Gulf of Suez area. De-
tailed quantitative paleoecological analysis was applied in this
area which enables more precisely interpretation of the paleo-
ecological evolution of marine Middle Miocene sediments.

The following sea-level cycles have been distinguished:
(1) The Burdigalian cycle without microfauna which cannot

be  accurately  dated  biostratigraphically.  During  this  cycle,
sandstones,  claystones  and  limestones  were  deposited  in  the
lower  part  and  coralline  algal  limestones  in  the  upper  part
(Rudeis Formation). The limestones rich in pectinid and gas-
tropod  shells  with  coral  colonies  indicate  shallow  marine
environments.

(2) The uppermost Burdigalian-Langhian cycle followed af-

ter a hiatus which can be correlated with the global Bur5/Lan1
sequence  boundary  of  Hardenbol  et  al.  (1998).  In  this  cycle,
clastic  sedimentation  dominates,  it  is  represented  by  clay-
stones, marls and sandy marls (lower part of Kareem Forma-
tion). Biostratigraphically, this cycle is bounded by the FO of
Praeorbulina  sicana  and  the  LO  of  Globorotalia  periphero-
ronda. The Langhian/Burdigalian boundary lies in the lower-
most  part  of  the  cycle,  upwards  the  cycle  can  be  correlated
with  the  planktonic  foraminiferal  zone  of  Praeorbulina
glomerosa and the subzones of Orbulina suturalis and Orbuli-
na universa. A benthic ecozone Heterolepa dutemplei—Laevi-
dentalina  elegans  was  defined  in  this  interval.  Rich  and
diversified  foraminiferal  assemblages  dominated  by  lagenids
and cibicidoids in samples 1—6 in section II indicate a normal
marine,  oxic  environment  with  a  maximum  of  paleodepth
100—300 m for the lower interval of the cycle. The upper inter-
val is shallower (50—100 m) but a normal marine environment
is expected.

(3) The hiatus which can be correlated with global Ser1 se-

quence  boundary  of  Hardenbol  et  al.  (1998)  bounded  Ser-
ravallian  cycle  starting  with  conglomeratic  sandstones
containing few foraminifers. The sandstones are followed by
shales  and  marls  containing  less  diversified  and  abundant
microfauna  with  rare  planktonic  foraminifers  (Zone  Globo-
rotalia praemenardii—Globorotalia peripheroronda). The cycle

ends with dolomitic and argillaceous limestones (upper part of
Kareem  Formation)  without  biostratigraphical  markers.  A
benthic  ecozone  Bolivina  compressa—Elphidium  spp.  was
defined  in  this  cycle.  A  shallow  (20—50 m)  littoral,  suboxic
environment has been interpreted for the lower part of cycle.
Section  upwards,  these  normal  marine  sediments  were  re-
placed by euryhaline limestones.

The studied foraminifera-bearing interval can be correlated

with the early and middle part of the Badenian of the Central
Paratethys.  Though  the  area  of  the  Gulf  of  Suez  and  the
Central  Paratethys  were  situated  in  different  climatic  zones,
and influenced by different tectonic events, the main paleoen-
vironmental  events  (sea-level  changes,  oxygen  decrease,
salinity  changes)  are  comparable.  It  shows  that  the  decisive
factors triggering these events were global climatic events (the
Middle  Miocene  Climatic  Optimum  followed  by  the  Middle
Miocene Climatic Transition).

Acknowledgments:  This  research  was  supported  by  Grants
No. MSM0021620855  and  GAČR  205/09/0103.  We  thank
Sorin  Filipescu  (Cluj),  Janina  Szczechura  (Warszawa)  and
Christian Rupp (Vienna) for their comments and corrections,
which improved the quality of this manuscript.

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