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Maastrichtian-Early Eocene litho-biostratigraphy and palægeography of the northern Gulf of Suez region, Egypt
Journal
of Almacan Earth Soences,
Pergamon Pll:S0889-8382(00)00038-7
Vol
32,
No
2. PP. 223-255. 2001 Elsewer Science Lfd All rights reserved. Prmted I” Great Brlta~n 0899.5362101 S- see front matter
o 2001
Maastrichtian-Early Eocene litho-biostratigraphy and palaeogeography of the northern Gulf of Suez region, Egypt C. SCHEIBNER’,*, A.M. MARZOUK2 and J. KUSS’ ‘UniversitM Bremen, FB5, PO Box 330440, 28334 Bremen 2Geology Department, Faculty of Science, Tanta University, Tanta 31527,
Egypt
ABSTRACT-The Maastrichtian-Lower Eocene sediments on both sides of the northern Gulf of Suez can be subdivided into eight formal formations (including one group) and one informal formation that are described in detail. These lithostratigraphic units reflect three different environmental regimes of deposition or non-deposition. The first regime is characterised by uplift and erosion or non-deposition resulting mostly from the uplift of the Northern Galalal Wadi Araba structure, a branch of the Syrian Arc Foldbelt. The shallow water carbonate platform and slope deposits of the Late Campanian-Maastrichtian St Anthony Formation and the Paleocene-Lower Eocene Southern Galala and Garra Formations represent the second regime and are found north and south of the Northern Galala/Wadi Araba High. The third regime is represented by basinal chalks, marls and shales of the Maastrichtian Sudr Formation and of the Paleocene-Eocene Dakhla, Tarawan and Esna Formations, the Dakhla/Tarawan/ Esna informal formation and the Thebes Group. The distribution and lateral interfingering of the above mentioned environmental regimes reflect different vertical movements, changing basin morphology, sea level changes and progradation of shallow water sediments and is illustrated on 11 palaeogeographic maps. o 2001 Elsevier Science Limited. All rights reserved. RESUME-Les sediments du Maastrichtien et Eocene inferieur, affleurant de part et d’autre au nord du Golfe de Suez, peuvent dtre subdivises en huit unites bien definies (incluant un groupe) et une unite plus informelle qui sont d&rites en detail. Ces unites lithostratigraphiques temoignent de trois environnements sedimentaires differents. Le premier est caracterise par une surrection et une erosion ou une absence de depots qui resulte pour I’essentiel de la surrection de la structure du Northern Galala/Wadi Arabia, une branche de la ceinture plissee de I’arc Syrien. Un environnement de plateforme carbonatee peu profond, avec des depots de pentes, correspondant a la formation de St Anthony du Campanien superieur-Maastrichtien, et aux formations Paleocene-Eocene inferieur du Southern Galala et du Garra, represente le second regime de depot; il est observe au Nord et au Sud du Northern Galala/Wadi Arabia High. Le troisieme regime est constitue par des craies de bassin, des marnes et des shales de la formation maastrichtienne de Sudr, des formations Paleocene-Eocene de Dakla, Tarawan et Esna, la formation informelle de Dakla/Tarawan/Esna et le groupe Thebes. La distribution des milieux de depots precedents et leurs passages lateraux, temoignent de mouvements verticaux, de variations de la morphologie des bassins et du niveau marin, et de la progradation de sediments d’eaux peu profondes. Ils sont illustres par 11 cartes paleogeographiques. o 2001 Elsevier Science Limited. All rights reserved. (Received 27/l /OO: accepted 20/2/01)
*Corresponding author [email protected],
[email protected]
Journal of African Earth Sciences 223
C. SCHEIBNER et al. INTRODUCTION During the last decades, many authors investigated the stratigraphic subdivision of the Upper CretaceousPalaeogene strata in the Galala Mountains and west central Sinai (Fig. I). Most of these studies were focused on the bio- and lithostratigraphical interpretation of isolated sections. Only a few authors, such as Masters (I 984) and Said (I 9901, concentrated on regional comparisons. In this work, the stratigraphic results from the Galala Mountains and neighbouring areas are combined with literature data from numerous isolated sections (especially in west central Sinai). The authors concentrated on questions of lateral facies transitions and their stratigraphical synchroneity or diachroneity. Special emphasis is put on the interfingering of shallow water limestones over swells and tectonically induced uplifts, and basinal marls and shales. The results of the facies investigation, in combination with the different types of hiatuses observed in the area, led to a detailed palaaogeography of the Maastrichtian to Early Eocene that is documented in 11 maps.
GEOLOGICAL SETTING The investigated area represents a segment of the northern passive margin of the Afro-Arabian Plate. This passive margin formed during the Late Triassic/ Jurassic opening of the Neotethys. The extensional tectonic processes resulted in the formation of eastwest-striking northward-deepening half-grabens that were mostly covered by the Late Triassic-Early Cretaceous seas, depending on, among others, sea level fluctuations. Beginning with the initial stages of the collision between the African and European Plates during Turonian times, a dextral transpressive reactivating of the half-grabens took place along the North African-Arabian Plate boundary (e.g. Moustafa and Khalil, 1995). As a consequence, a system of inverted, uplifted and folded grabens was formed along the Syrian Arc System (Fig. I). This area is also known in Egypt as the ‘unstable shelf’ (Krenkel, 1925; Said, 1960). It contrasts with the tectonically unaffected area further south (‘stable shelf’). While the latter is characterised by lithologically uniform marine strata, formed on a gently north-dipping shelf, small-scaled facies variations are obvious within the basin-swellmorphologies of the unstable shelf area (Kuss et al., 2000). The Galala Mountains in the Eastern Desert, together with areas in western Sinai, represent a southern branch of the Syrian Arc called the Northern Galala/Wadi Araba (NGWA) High (Kuss et a/., 2000) (Fig. 2). The Upper Cretaceous-Palaaogene carbonate dominated successions of a south- and north-dipping carbonate ramp prograde from the Northern Galala/
Wadi Araba High. Facies transitions between the Paleocene shallow water ramp carbonates and deeper water intrashelf marls of the Southern Galala Subbasin (Fig. 2) farther south have been studied in sections along the dip direction. Mass transport deposits like slides, slumps and debris flows occur (Scheibner et al., 2000).
METHODS The study area is exposed around the northern parts of the Gulf of Suez. Eight Upper Cretaceous-Palaeogene sections of the Northern and Southern Galala on the western side of the Gulf of Suez were investigated in detail (Fig. 31, including the northern and southern forelands of the Galalas. Additionally, data of west central Sinai, opposite to the working area, was reviewed. Facies interpretations are based on fine-scale logging of stratigraphic sections in and along the Northern Galala/Wadi Araba High. Studies of 169 thin sections of the Maastrichtian-Early Eocene interval are supplemented by 479 marl samples that formed the base for a high-resolution biostratigraphic frame based on planktic and benthic foraminifers and calcareous nannoplankton.
BIOSTRATIGRAPHY For the Maastrichtian, the biostratigraphic scheme given by Perch-Nielsen (1985) and Norris et al. (I 998) (Fig. 4) was followed. The biostratigraphic schemes of Berggren et a/. (I 995) for planktic foraminifers (Pzones), of Martini (I 971) for calcareous nannolankton (NP-zones) and of Serra-Kiel et a/. (I 998) for shallow benthic foraminifers (SB-zones) are used for the Paleocene and Early Eocene. The calibration of planktic foraminifers and calcareous nannoplankton is from Norris et al. (I 998) for the Cretaceous and from Berggren et al. [I 995) for the Palaeogene (Fig. 4). In section T2 (Fig. 4a), NPI 0 could be divided into four sub-zones, named NPI Oa, NPI Ob, NPl Oc and NPI Cd, following Aubry (I 995). In sections Tl, D2 and D3 (Fig. 4a), NPI 0 can only be subdivided into two subzones (NPI Oa-c and NPl Od) because T. digtiabs could not be found. Faris and Strougo (I 998) and Aubry et a/. (I 999) also used this subdivision in their description of the Esna Shales of Egypt. In addition to Berggren et a/. (I 9951, Speijer et al. (2000) was followed in subdividing the planktic foraminiferal biozone P5 into P5a, P5b and P5c. The very short sub-zone P5b is characterised by the total range of M. allisonensis marking the Late Paleocene thermal maximum. All sections presented in Fig. 4 were recalibrated to the above mentioned schemes. If planktic foraminifers,
Maastrichtian-Early
Eocene litho-biostratigraph
AREA 1
I.
AREA 2
AREA 3
7. The two (see inset).
Galala Plateaus at the western Gulf 1: Palmyrid Fold Belt; 2: Negev-Sinai
5: Bahariya Uplift/Western transitions IT-zoneJ were figure),
AREA 4
T-z
. . . .SGS . .>,
Figure Desert
y and pakogeograph
the boundanes
Desert. During formed roughly
of areas
1-6
y of the northern Gulf of Suez region
AREA 5
1 AREA 6
( NGWA 1 of Suez forming part of a Syrian Arc Fold in the Eastern Fold; 3: Northern Galala/Wadi Araba High; 4: Abu Roash;
Late Cretaceous-Palmogene times, the platform (NGWAI parallel with the strike of the Galalas. In transect A-B
to basin ISGSI (bottom of the
are indicated.
Journal of African Earth Sciences 225
C. SCHEIBNER et al.
Figure
2.
Latest
Maastrichtian
pakeogeographic
map
of the circum-tethyan
The area of investigation is around the Northern Galala/Wadi south. The Southern Galala Sub-basin is part of the Eastern
as well
as calcareous
bio-stratigraphy. given used
nannofossils,
The calcareous
were
used for
nannoplankton
priority. The biostratigraphic scheme (planktic foraminifers or calcareous
plankton)
is indicated
which is nanno-
in the figures.
Luger et al. (I 998) foraminiferal biozonation areas in which
was
presented a new for the Maastrichtian
the Late Maastrichtian
planktic for those
index fossil A.
mayaroensis is very rare or absent. Marzouk and Ltining (1998) described a strong variability of planktic foraminifers
and calcareous
nannoplankton
correlations
realm
(modified
after
Araba and reaches to the Southern Desert lntrashelf Basin.
Camoin Galala
et al., 19931.
Sub-basin
in the
(1883) (Fig. 51, the lithostratigraphic subdivision of the Upper Cretaceous-Eocene successions in Egypt has been the subject
of many discussions,
especially
during the 195Os-1960s
(Nakkady,
Naggar, 1966a, 1966b, today, lithostratigraphic
1968; Sabry 1968). Even terminology is used non-
uniformly Formation terminology,
(Issawi
et a/., 1999),
especially
(Herrnina and Lindenberg, the authors used Hermina
as a basis, especially stratigraphic
1950,
with
subdivision.
respect
1957;
El-
the Esna
1989). For era/. (I 989)
to usage of litho-
In accordance
with recom-
on Sinai, especially in the lower Paleocene, whereas in the upper Paleocene the different zonal correlations are
mendations (Salvador,
in good agreement.
units by a geographic term combined with a unit term instead of a geographic term combined with a litho-
El-Dawoody
Boukhary and Abdelmalik
(1992) reviewed
Late Paleocene-Eocene
succession
LITHOSTRATIGRAPHY
(1983) and
the biostratigraphy
of the
in Egypt.
OF MAASTRICHTIAN-
EARLY EOCENE STRATA Ever since the first description of the Maastrichtian to Eocene sediments in the Western Desert by Zittel
226
Journal of African Earth Sciences
of the International Stratigraphic Guide 19941, they describe lithostratigraphic
logical term to allow for lithological variability (e.g. Esna Formation instead of Esna Shale, as has been used frequently in the past). In the following paragraph, commonly used formations
a short summary of the and their regional dis-
tribution of the Upper Cretaceous-Palasogene lithostratigraphic units for northern Egypt and Sinai is given,
Maastrichtian-Early
Figure 3. Section
Eocene litho-biostratigraph
map of the northern
y and pakogeograph
part of the Gulf of Suez.
y of the northern Gulf of Suez region
The nine rectangles
represent
depositional history. The sections in areas 1-6, on the western side of the Gulf of Suez are based on new and literature data; whereas the sections of areas 7-9, on the eastern Suez
including
(Sinai),
some
are based
additional
on literature
suggestions
data
to Lower
(Fig. 5). A
Eocene sediments
Western Desert 51, the following
(Farafra, Dakhla lithostratigraphic
bottom
Overwegi
to top:
layers;
in the
and Kharga) (Fig. units occur from ash-grey
of different
only.
detailed historical overview can be found in El-Naggar (1966a, 1966b) and lssawi (1972). According to the description of Zittel (I 883) of the Upper Cretaceous
areas
(Galala Mountains), side of the Gulf of
shales
(‘aschgraue
Blatterthone’);
snow-white
layered
lime-
stone or chalk with Ananchytes ovata; green shales (‘grtinliche Blatterthone’); and Operculina limestone (Unterlibysche Stufe). Near Esna, Zittel (18831, miscorrelated the green shales underlying the Operculina limestone Western fusion
with
the Danian
‘ash-grey
shales’
Desert. With this miscorrelation, of
lithostratigraphic
terminology
of the
a long constarted.
Journal of African Earth Sciences 227
Section, author and area g
3r
cy
Tim
P
(Ma.
*
50
zone mneta
%95)
P8 P7
7
b P6
-
-
a
P5 -
:k a C
-_EF
s
11
zi -_ ---DF ----
P4 a iT P3
'HG-
+I - -iF -- -
55 .
SO -
THG
a
0 2 --DF---
r
i
C
?
-
Pl
n.e.
b 3
B&P 6
-
Northern Galala
a
PZOM
Td Ibathom.
mayaro. Uacami. ~cticosa Gans. yanaseri
+ -
Planktonic foraminifera data Nannoplanktondata
+ .
+ +
+ +
+ + + + l&L + -
Formations: THG EF SGF TF GF DF DTE SAF SF
sectrons Eocene
The biostratigraphy taken from kterature.
boundary.
+ .
+ -
+ _
+ +
Lithologies:
Thebes Group Esna Formation Southern Galala Formation Tarawan Formation Garra Formation Dakhla Formation DakhWTarawaMEsna Formation St. Anthony Formation Sudr Formation
Figure 4.
;_
0
cherl I--_-I
hiatus
shale
, I ,
I[
sandstone
LCI
debris flow
[fl
chalk
slides
1 ,‘/I
dolomite
I22
limestone
and lithology of newly measured Maastrichtian-Palseogene secttons, including The broad grey band reflects the current opinion on the position of the Paleocene-
The biozonations
of planktonic
forammifers
fP zones),
calcareous
nannoplankton
INP zones
for
Palsaogene and CC zones for Maastrtchttanl and shallow benthic forammifers LS6.Z~ are listed. In the Maastrichtian, the first and last occurences of calcareous nannoplankton index forms are Indicated. The drfferent biozonal schemes used are indicated with + lusedl and (not used). Other biozonal schemes such as shallow benthic forammifers, macrofossils and ammonites are rarely used here and are not listed. The black areas indicate hiatuses, due to erosion or non-deposmon. Question marks indicate uncertain stratigraphical ranges. (a) Sections of areas together
7-6, wtth
on the western side of the Gulf of Suez sections from literature.
(Galala
Mountamsl,
are mostly
newly
measured
sections
Figure 4. continued. including secttons Paleocene-Eocene
The btostratigraphy
and lithology
of newly
taken from kterature. The broad grey band boundary. The biozonanons of planktomc
measured
Maastrichtian-Palaaogene
INP zones for Palaaogene and CC zones for Maastnchttanl and shallow benthtc the Maastnchtian, the hrst and last occurences of calcareous nannoplankton different shallow areas
secttons,
reflects the current opinion on the position of the forammifers (P zones), calcareous nannoplankton foraminifers index forms
fSBZ) are listed. In are indtcated. The
biozonal schemes used are indicated with + fused) and (not used). Other biozonal schemes such as benthic foramtntfers, macrofosstls and ammonites are rarely used here and are not Itsted. The black
mdtcate
hiatuses,
ranges. lbl Sections of Unfortunately, It IS not section. Because of the 119921 belongs to area
due
to erosion
or non-deposnion.
Question
marks
indicate
uncertain
strattgraphical
areas 7-9, on the eastern side of the Gulf of Suez (Sinail, are entirely from ltterature. clear from which part of Gebel Qabeliat Marzouk and Abou-El-Enein (19971 took their htatus, thts section was attributed to area 8, whereas section Gebel Qabeliat of lsmail 7.
C. SCHEIBNER et al.
I-
Formstions in the Western Desert l--
Zlltd,
IBeadnell,
1905
1888 western
-
ium
*M
1961 1911 vestefl routhem Egypt
southern Egypt
Awadand Gob&l, 1866 southern
Harmin * 81., 1989
El Wv, l@S%a western
southern
Egypt
Egypt
l-
a
!!
Thebes
Y presian
Thebes
:hebes
w
grijnlichs Blatterthone
-
isna Shales Passage B&S
Chalk
, ____( Danian
aschgraue ) BWterthone
k! 6 j
-i!
Upper Esna Chalk
Danian Shales
Lower Esna
i
Formations in the Eastern DesertBinai
Sinai
S. Galala zaafarana
AbdHermina et al., ildmfy, 19( 1 1088 r4. Eastern Sinai r( ; Galalc!_ Desert
S. Galala -S-N-
thimwork N. Eastem _N_
.S_
Serai
Sinai
Desert
Thebes
Thebes
I
Naot Esna
Esna
> Brawan-_ -?/--Esna
1
I
Dahklal Tarawanl Esna
Dakhla
Sudr
Esna
II Maastrichtian Shareb
Gebel Thelmet
Figure
5. Lithostratrgraphtcal
schemes
Sudr Gebel Thelme in the
Western
St. Paul
Desert
and in the Eastern
Desert/Sinai.
Today,
Sudr
in southern
Egypt,
the
lithological subdivison of Said 11961) is accepted. in northern Egypt, this subdivision is not applicable due to the thin or even absent Tarawan Formation (TF). Most authors ignore that fact and just expand the Esna Formation down to the Maastrichtian, but this leads to misinterpretations. SAF: St Anthony Formation; SGF:
230 Journal
of African
Earth Sciences
Therefore, rn this study, Southern Galala Formation.
the informal
Dahkla/Tarawan/Esna
Formation
was
Introduced.
Maastrichtian-Early Beadnell
(1905)
Eocene litho-biostratigraph
described,
y and palzeogeograph y of the northern Gulf of Suez region
for the first time, an ‘Esna
Shale’ unit above the chalk (Tarawan)
and the Danian
shales as passage beds between the Cretaceous the Eocene. Hume (1912) mentioned the Lower
and and
the Upper Esna Shales below and above the chalk (Tarawan), respectively. Later, Said (1961) introduced the Dakhla Shale as a new formation, replacing the Danian shales of Beadnell (1905) and the Lower Esna of Hume (1912). The chalk between the Dakhla and Esna Formations was named the Tarawan Chalk by Awad and Ghobrial (1965). Since then, the terms Dakhla Formation (DF), Tarawan Formation (TF) and Esna Formation (EF) have been generally accepted for the lithostratigraphic (Hermina 1966b)
subdivision
introduced
Middle
in southern
and Lindenberg, Oweina
the Tertiary Formations,
the terms
Chalk
and western
1989).
El-Naggar
Lower
and Upper
Oweina
Oweina
Egypt
(1966a, Shale,
Shale for
part of the Dakhla, Tarawan and Esna but this lithostratigraphic scheme found
little acceptance The subdivision
in the scientific community. of Awad and Ghobrial (1965)
not be applied to the Late Cretaceous-Palaaogene of northern Tarawan Although
Egypt
and Sinai, however,
can-
to Early Eocene
from
referred
to as Esna Formation
Formation
Paleocene
(e.g. Bartov
together
because
and Steinitz,
of their
logical similarities. from Maastrichtian located
Desert
9) (Fig. 4b). The transition Thebes
Sudr Formation,
and underlies the Lower
Eocene limestone (Thebes).” a stratigraphic miscorrelation
This usage has lead to of the Esna Formation
certain.
All sections
studied
stratigraphical the various
correlations lithologies
Therefore,
the authors
Esna Formation unit for Upper
as the latest
Ltining et al., 1998a).
propose
the Dakhla/Tarawan/
(DTE) as an informal Maastrichtian-Lower
lithostratigraphic Eocene
shales
Sudr Formation
(Lower
range:
The contact
Formation
usually
coincides
latest Maastrichtian 4a, b).
however,
the Maastrichtian-Eocene
sions were also subdivided
according
succes-
to the schemes
for southern Israel. There, the synonyms for the Sudr, Tarawan and Esna Formations and Thebes Group are Ghareb Formation, Hafir Member, Taqiye Formation and Mor Formation (Bartov and Steinitz, 1977; Romein, 1979; Benjamini, 1992), the chalky Tarawan Formation
respectively. Where (Hafir Member) is
missing on Sinai, the entire shaley to marly formation,
time,
are given
distribution
of
pala.?ogeographic
Ghorab
(1961);
for 11
Wadi Sudr
Campanian-Maastrichtian
of the Sudr Formation
Dakhla
tiated
Sinai,
the changing
Paleocene?)
boundary,
The Dakhla, Tarawan and Esna Formations and their earlier denotations are widely used in Egypt. On
and litho-
of most sections
(SF) (Figs 4a. b and 7c. e)
and marls in those parts of northern Egypt and Sinai where the Tarawan Formation cannot be differen(Fig. 5).
literature)
maps of the investigated area are presented Maastrichtian to Early Eocene time slices.
Stratigraphical
as early
(and additional
with
ern Egypt
(e.g. Said, 1990;
area is not
1, the biostratigraphical
Author and type section: (west central Sinai)
and Sinai it starts
(SGF) to the deeper
a subject of the study. Therefore, the attribution of these sediments to one or the other formation is less
that ranges in southern and western Egypt only from Upper Paleocene to Lower Eocene, whereas in northMaastrichtian
(area 6)
side of the Gulf
Group (THG) in the working
in Fig. 4a, b. To illustrate
the Esna Formation which overlies the Maastrichtian-
of the Gulf of
of the Early Eocene shallow
Galala Formation
Paleocene
Paleocene
west
of Suez (west central Sinai), the areas 7-9 are also orientated from the south (area 7) to the north (area
water
Wadi Qena and on Sinai b y
and litho-
(area I) to north
(Figs 1, 3, 4a and 6). On the eastern
are listed in Table
in northern
1977).
stratigraphical
from south
mation, they mentioned that “the upperpart of the Dakhla, the Tarawan and the Esna which range from represented
is
The stratigraphic intervals range to Lower Eocene. Areas 1-6 are
in the Eastern
Suez, oriented
the
to Early Eocene age in southern Egypt are
times
1-6) and east (areas 7-9) of the Gulf of Suez (Fig. 3). The sections within the single areas are grouped
Southern
age to the Esna For-
Eocene
(Said, 1990) or Taqiye
Discussed below are the eight formal formations (including one group) and one informal formation and their distributions within the nine areas west (areas
water
because
to Early
FORMATIONS AND THEIR DISTRIBUTION WITHIN THE STUDY AREA
strata
Formation is partly absent or very thin. Hermina and Lindenberg (1989) attributed a
Late Paleocene
ranging
is either with
sharp,
to the overlying in which
or is more gradual,
7, 8) the Sudr Formation
in which
terminates
biozone
or CC26
Massive
limestone
beds with thin intercalations shales
white
case (areas 2, within
CC25
Liihology: calcareous
case it
the Cretaceous/Palasogene late or (Fig.
and cream chalk and chalky
and argillaceous
of light grey
crystalline
lime-
stones. The Sudr Formation was studied in areas 1, 2 and 3 (sections Tl , D2,D3 and Sl-9) where it is composed of alternating beds of white chalk (up to 1.20 m) and thin grey marls (up to 0.10 m). In St Paul (area 3), a 1.3 m thick shaley unit is intercalated in the upper part of biozone CC25c, for transitional beds on Sinai.
which is also typical
Journal of African Earth Sciences 23 1
1 Nadi Tarfa
Area
2 Bir Dahkl
THG THG
1-S-
-N-
Eastern Desert
4 6 5 8 St. Anthony1 i. Not-then J. Northern Bas ihari Abu Zanimal jebel Thelme Galala Galaia b Wadi Feiran
3 St.Paul
THG
THG
-N-
Western Sinai
T
T
I
9 NW. Sinai
THG THG
THG
THG
THG
;GF
b
EF
I
EF
EF
SGF
SGF
TF
EF
I
SGF SGF
SGF
DF DF DF
3 t
SF
3
SF
DF
SF
r” :ormations: THG !F SGF
Thebes Group Esna Formation Southern Galala Formation
Figure 6. Distribution deposition.
In area
of the rock
units
TF GF DF
and age of formations 9, on northwestern
within
Tarawan Formation Gana Formation Dakhla Formation
in the nine investigated
Sinai,
the stratigraphical
The black
is uncertain
units are hiatuses because
Profile/Location
Coordinates exact locatron
Kassab and Keheila,
1994
WTSlWadr
Tarfa
wrthout exact locatron
Kassab and Keheila,
1994
140 km east of El Sherkh fad1
El-Dawy,
1999 1999
SlWadr Hawashiya
151 km east of El Sherkh fad1
El-Dawy,
Tl /Wad1 Hawashiya
N28’13.52’;
E32O13,64’
Thus work
T2lWadi
N28”27,31
‘, E32”13,73’
This work
Tarfa
Nrshi et al ., 1994
Sectron 11 /Wad1 Tarfa
wrthout exact locatron
Sectron U/Wadi
wrthout exact location
Bandel et al ., 1987
Wadi Tarfa
without
Tantawy
DB/Brr Dakhl
N28’36.43
‘; E32=‘23,77
D2/8rr
N28’39.61
‘; E32O23.59’
Dakhl
ranges
Author
wrthout
Dakhl
or non-
stratigraphical
or taken from literature
Hawashiya
WDiWadr
due to erosion
of varying
WHSlWadi
O/Wad1 Hawashrya
2
areas. range
DakhlalTarawanlEsna Formation St. Anthony Formation Sudr Formation
this area.
Table 1. Sections that were newly measured Area 1
DTE SAF SF
Tarfa
exact locatron
wrthout exact
locatron
Abu Rimth l-3
N28O43 ‘; E32O.30
Brr Dakhl
without
If coordmates are grven m the Irterature, geographical pomts, but rather geographical
’
exact location
’
et al ., 2000
This work This work Strougo and Faris, 1993 Gretl, 1998 Metwally
then they are mentroned here. ranges given by the authors.
and Abd El Azeam, Coordmates
wrth
1997 a star
do not
indicate
1
Table 1. continued.
3
SSISt.
N28°50.37’;
Paul
Sl -S8/St.
Author
Coordinates
Profile/Location
Area
E32”31,53’
N28O50.72’;
Paul
St. Paul
N28O50.63
St. Paul
N28O50.63’;
St. Paul
wrthout
Scherbner
E32O31,29’ ‘; E32O32.62
’
E32’32.62’
2000
et a I., 2000
Strougo
et al ., 1992
Haggag
(1991)
lsmail and Abdallah,
exact locatton
Mazhar
4
,
Kuss et al
’
et a/.,
Kuss. 1987,
Grrgrs, 1987;
Faris, 1997:
Kulbrok,
N28O56.72’;
E32O25.14’
without
exact location
Selrma and Askalany,
St. Anthony
wrthout
exact
Zrttel,
1883;
1986;
Bandel and Kuss, 1987:
1989;
Malchus,
Thelmet
location
20/2/S
North Galala
ADlAbu
Darag
Camp/S
North Galala
Several/S
North Galala
wrthout
exact locatron
Abdel-Krreem
without
exact location
Hottrnger,
Awad
1998
this work
1996
1990;
Kuss et al.
and Abdou.
1960;
1979;
wrthout
exact location
Abd-Elazeam
without
exact locatron
Gretl, 1998
wrthout
exact locatron
Abd-ElshafY
2000
1971;
Abdallah Mazhar
1996
Kuss and Lepprg, 1989:
Thus work
,
et a/ ., 1970;
Abdel-Krreem,
Kulbrok,
Kuss,
1979
Abdallah
exact locatron
E32’11.24’
1966;
Kuss and Malchus.
Malchus,
and Metwally,
and Atta,
1993
and Atta,
1993
1990
1998
without
exact
locatron
Gretl, 1998
without
exact
location
Abd-Elshafy
EEOlEzz El-Orban
wrthout exact
location
Ansary and Fahmy.
Qabelrat
wrthout exact
locatron
Marzouk
and Abou-El-Enern,
without
exact locatron
Masters,
1984
(Kerdany
and Abdel Salam,
1970)
of Suez
without
exact locatron
Masters,
1984
(Kerdany
and Abdel Salam,
1970)
E/Gulf of Suez
wrthout
exact locatron
Masters,
1984
(Kerdany
and Abdel Salam,
1970)
of Suez
without
exact locatron
Masters,
1984
(Kerdany
and Abdel Salam,
1970)
Araba
without
exact location
Masters,
1984
without
exact locatron
Anan,
wrthout
exact locatron
Shahin,
Wadr Nooz Wadr NoatlWadr
Nooz
Barakat
JliGulf
of Suez
Alef Well/Gulf Morgan H-l
Well/Gulf
G. ArabalGebel AZlAbu
Zenima
Matulla
locatron
1969
and Fahmy,
1969
Shahin,
1992;
Ismarl, 1992,
and Hussern,
Nezzazat
wrthout exact
Nuhkl
wrthout
exact location
Marzouk
BEM/Brr El-Markha
wrthout
exact locatron
Abdelmalik,
and Hussern, 1978a.
1994
location
Ismarl, 1992
wrthout exact
locabon
Shahrn,
Wadi Ferran
without
exact locabon
Marzouk
and Abou-ECEnern,
Wadi Feiran
without
exact locatron
Masters,
1984
without
exact location
Shahin,
wrthout
exact locatron
Masters,
1984
Masters,
1984
E-Ferran
wrthout exact
Wadi Ferran
locatron
1992
(Kerdany
and Abdel Salam.
1970)
(Kerdany
and Abdel Salam,
1970)
wrthout exact
locatron
Masters,
1984
exact
location
Masters,
1984
without
exact
location
Faris et al.,
without
exact
location
Cherif et a/ ., 1989
wrthout
exact
location
Arafa
without
exact
location
El Sheikh and El Beshtawy,
without
exact
location
El-Deeb and El-Gammal.
Wadr Nukhl
without
exact
locatron
Monechi
Wadi Feiran
‘N28”40’-50’;
of Suez
Gebel Qabelrat 4 SectronslAbu
Ruders
Gebel Nezzazat SE Nezzazat/Wadr some secttonsiwadi
GindrlGebel
Gindi
Ferran Feiran
E33°20’-30’
1986;
Ismail, 1992;
Gebel Urn Makhasa
without
exact location
Kulbrok,
1996
Gebel Gindi
without
exact location
Kulbrok,
1996
Wadi Sudr
N29’50.34’;
Wadi Sudr
without
exact
locatron
1992
1997
et a/ ., 1999
Eweda and El-Sorogy,
exact location
If coordmates are given m the literature, geographrcal points, but rather geographrcal
Allam and Khalrl, 1989
1991
without
E33°05,08’
1997
1990
wrthout
E. GhariblGulf
1999
1978b
wrthout exact
1 /Gulf of Suez
IObaidalla,
1992
Qabeliat
E-Bakr Manne
1996;
1994;
Wadi Fetran
Gebel Ekma
1997
1992
Marzouk
9
1996;
and Abdallah,
wrthout
N29O31.86’;
Nl /Wad1 Nooz
1989;
et a/.,
this work
ef a/.,
8
Kulbrok,
Wadi Askhar
Anthony
Bandel and
Boukhary
A3/E of St. Anthony
Al/St.
and Erssa, 1970;
7
1996;
Kuss and Lepprg. 1989;
1986;
Kuss and Leppig,
E32O21,21
Gebel Thelmet
6
Abdou et a/ ., 1969;
Strougo,
N28’54.95’;
GTlGebel
5
1966:
1979;
1999
Ismarl, 1996
Gretl. 1998 Youssef
then they are mentioned here. ranges given by the authors.
and Shrnnawr, Coordinates
1954; wrth
El-Shrnnawr,
a star
do not
1967 rndrcate
C. SCHEIBNER et al.
234 Journal of African Earth Soences
Maastrichtian-Early
Eocene litho-biostratigraphy
andpalazogeography
of the Sudr Formation,
Synonymy: Synonymous with the St Paul Formation of Kuss (1986), Bandel et a/. (1987) and Bandel and Kuss (1987) (Fig. 5). Regional distribution: The Sudr Formation
of the northern Gulf of Suez region
and El-Shinnawi which correlate Late Maastrichtian
is only found
Youssef
and Shinnawi
(I 954)
(1967) found Exogyra cf. overwegi, in area 4 (St Anthony) to the Middle/ St Anthony
Formation.
in northern Egypt and Sinai. At St Anthony (area 41, the chalks of the Sudr Formation have a Late Campanian age. They are dis-
Depositional setting: The Sudr Formation was deposited as basinal chalks with no shallow water
conformably overlain with an erosional surface by the units of the St Anthony Formation (SAF) (Fig. 7d). The stratigraphical range of the Sudr Formation
depositional environment of the chalks of the Sudr Formation on eastern Sinai in greater detail.
at Abu Zenima/Wadi Feiran (area 8) is not clear. Most authors agree that it terminates in the Upper
(19701, Abdallah et al. (I 970) and Abu Khadrah et al. (19871, erroneously included dolomitic limestones of
Maastrichtian;
the
however,
the Sudr Formation
some authors
continues
indicate
influences.
Paleocene,
that
seems
Leppig
(sediments
of the
and Eissa
Southern
above the cave of St Anthony.
(I 989)
indicated
a Late
Galala Kuss and
Paleocene
age by
Formation. St Anthony Formation (SAF) (section Al in Fig. 4a and Fig. 7d) Authors and type section: Bandel and Kuss (1987);
Hamam Faraoun are of Maastrichtian age (Gansserina gansseri Zone). Both sections in Wadi Nooz (area 6) start with 25 m dolomites,
such as Abdallah
the
at Ain Sudr
(area 9) are of Upper Campanian age (Globotruncana aegyptiaca Zone) and those of Gebel Gindi and
thick bedded
cliff
discussed
means of planktic and benthic foraminifers for these strata and attributed them to the Southern Galala
to depend
on how transitional beds are classified. The chalks Kulbrok (1996) described
massive
white
Formation)
up to the Cretaceous/
which
et a/. (1998b)
Discussion: Other authors,
Palasogene boundary (Fig. 4b). Only lsmail (I 992) extended its stratigraphical range at Gebel Qabeliat to the Lower
Lining
which
Monastery of St Anthony (Eastern Desert) Stratigraphical range: Upper Campanian-Upper Maastrichtian
may be attri-
buted to the Sudr Formation. However, dolomitisation has prohibited a conclusive stratigraphical assignment.
The mainly carbonate lithologies of the St Anthony Formation in the Southern Galala disconformably
Similar
overlie
lithologies
were
described
Formation
of Sinai (Youssef
Shinnawi,
1967).
be attributed
from
the
and Shinnawi,
Alternatively,
Sudr
1954;
these dolomites
to the underlying
Turonian
Strata
chalks of the Sudr Formation
may
overwegiis
(Abd-
present.
Age-equivalent
Elshafy and Atta, 1993). In northwestern Sinai (area 91, Youssef and Shinnawi
Exogyra overwegiwere Desert
in the ‘Overwegi
(1954)
known
as the Beris Oyster
and El-Shinnawi
pinkish-white
bedded
(I 967) described chalks
and chalky
175 m of
Late Campanian
were thought to contain rare Maastrichtian foraminifers and Subbotina triloculinoides of Paleocene age
Selima and Askalany, biostratigraphic data
(El-Shinnawi,
sandy-dolomitic
1967).
The scarcity
of the foraminifers
assignment
into doubt,
possible explanation.
and the poor pre-
strongly
although
Forty-five
indicated
puts the latter
reworking
the
sediments
first described Layers’
(Zittel,
Mudstone
with
in the Western 1883),
Member
now of the
Dakhla Formation (Awad and Ghobrial, 1965; Luger, 1985). The base of the St Anthony Formation is of
limestones
that change to yellowish-white hard dolomitic limestone in its upper part. Samples of the upper part
servation
and underlie
carbonates of the Southern Galala Formation. In the upper part of the St Anthony Formation, Exogyra
El-
age (Kuss,
upper units,
by thin sections.
(I 979) described
may be a
minifers
metres below the base
1986;
Kulbrok,
1996). Although is available from
1996;
only poor the mainly
a Maastrichtian
Abdel-Kireem
Upper Maastrichtian
of the Abathomphalus
age is
and Abdou planktic
mayaroensis
fora-
Zone at
Figure 7. The Late Cretaceous-Palaeogene sediments of the western la-d) and eastern lel side of the Gulf of Suez. la1 Section Tl, the southernmost section tn area 1: the chalks of the Tarawan Formation ITFI are intercalated between the marls and shales
of the
limestones Formation
Dakhla
Formation
of the Serai
are overlatn
Formatton
IDFl
below
of the
by the ltmestones
and
Thebes
the
Esna
Group
Formation
ITHG).
of the Southern
Galala
(EFI
161 Section Formatton
02
above. in area
(SGFI
The cliff
at the
2: the marls
with a gradual
top
is built
and shales
contact.
of chalky
of the Dakhla
The fault at the top
is of younger age and was the result of Red Sea graben tectonics. The section continues left of the picture with the rest of the sediments of the Southern Galala and the Esna Formations and the Thebes Group. (cl Section S9 (Kuss et al., 2000) in area 3: the marls and shales of the Dakhla Formation are sandwiched between chalks of the Sudr Formation (SF) below and shallow
water
influenced
sedtments
of the Southern
Galala
Formation
above.
Idl Section
A 1 in area
4: the marls
and sandy
marls of the St Anthony Formation ISAFI are overlain by the shallow water limestones of the Southern Galala Formation. The Southern Galala Formation forms a steep white cliff along the northern rim of the Southern Galala. fel Wadi Nukhl on Sinai: similar courtesy
to section of R.P.
Tl
(al,
Spetjerl.
the thin
Tarawan
The scales
are
Formation
IS sandwiched
only approximattons
due
between
the Dakhla
to a distorted
and the Esna Formations
(picture
perspective.
Journal of African Earth Sciences 235
C. SCHEBNER Gebel Thelmet
(GT; Fig. 4a). A possible hiatus between
et al.
occurs
within
NP7/8,
where
the Dakhla
Formation
the Late Cretaceous and the Early Tertiary sediments in section Al is assumed but could not be substan-
underlies the Tarawan Formation. The latter or even absent in northern Egypt and Sinai.
tiated in the studied sections by means of planktic foraminifers or calcareous nannoplankton. Lithology: Chalky limestones, marls and sandstones Synonymy: The St Anthony Formation corresponds to the Gebel Thelmet Formation of Abdallah and
Lithology: In the studied area, the Dakhla Formation consists of chalky marls in the uppermost Maastrichtian and of softer shaley grey-green marls in the Paleocene (Fig. 8). The thickness of the Dakhla
Eissa (1970) (Fig. 5). Although their term is older, the authors followed Bandel and Kuss (I 987) because Abdallah and Eissa (I 970) and Abdallah et a/. (1970) were apparently confused by the Cretaceous-Eocene lithologies (see the discussion the Sudr Formation). Other reasons for using
of the
term
and
the
St Anthony thickness
Whereas
Formation
are the accessibility
differences
the section
of the
type
in Gebel Thelmet
sections.
is dangerous
is thin
Formation varies from 6.5 m (D3) to 23.5 m (Tl). Synonymy: The Dakhla Formation is synonymous with the ‘aschgraue Blgtterthone of Zittel (18831, the Lower Esna of Hume (I 912) and the Lower Oweina Shale of El-Naggar (I 966a) (Fig. 5). Regional distribution: The Dakhla Formation in all areas except tigraphical results
is present
areas 4, 5 and 7, where
gap occurs
of this study
and Faris (I 993)
a stra-
(Fig. 6). In contrast
in Bir Dakhl
attributed
to the
(area 21, Strougo
the whole
succession,
to access (due to possible mine occurrences) and has a reduced section thickness, the section at monastery of St Anthony is easily accessible and has a much
which is sandwiched between the top of the Sudr Formation and the base of the Thebes Group, to the Southern Galala Formation. However, they subdivided
larger thickness. Regional distribution:
the Southern Galala Formation a lower light green argillaceous
deposits
The shallow
of St Anthony
along the northern equivalent
Formation
formation
in northern
only
Galala. A time
Egypt
and Sinai is
of the St Anthony
are slope sediments of a shallow water platform. In the lower part of the St Anthony
Formation, exposed.
influenced
are mapped
rim of the Southern
the Sudr Formation (Fig. 6). Depositional setting: The sediments Formation carbonate
water
large slumping structures
occur and are well
In the middle part, limestones
and reworked
shallow
water
with slumping
biota, such as Orbitoides
and Omphalocyclus, occur. In the upper part of section A3 (7 km east of St Anthony; Fig. I), the shallow water
prominent
harder
foraminifers
bioclastic
and thick
green-grey
calcareous
into three main units: limestone; a middle limestone
with
chert
bands;
shale.
In the present
large
and an upper study,
the authors correlated this tripartition, which is evident also in neighbouring sections, to the Dakhla, Southern
Galala and Esna Formations
(from base to
top) (Fig. 8). In the Northern Galala (area 61, the Dakhla Formation has a thickness of 10 m and is composed of papershales and marly limestones, planktic
foraminifers
the latter with abundant
(morozovellids)
in thin sections,
bivalve Pinna and teeth of bony fishes were found that
indicating an age of P3 or younger (section Nl ; Fig. 4a). In the present study, the authors attributed these
thrived
zones of reefs (C. Werner, pers.
sediments
to the Dakhla
comm.). Kulbrok (I 996) assigned the deposits of the St Anthony Formation to a distally steepened ramp, and
lithological
and stratigraphical setting:
The
Selima and Kerdany
deposited
as basinal
marls
influences.
Speijer and Schmitz
in calm water
(1996)
assigned them to shallow
marine environments. Dakhla Formation (DF) (Figs 4a, b and 7a-c, e) Author and type section: Said (1961); Dakhla, north of Mut (Western Desert) Stratigraphical range: Maastrichtian to Upper Paleocene The lowermost occurrence of the Dakhla Formation
Depositional
Formation
because
of their
similarities. Dakhla with
Formation no shallow
(I 998) reported
was water from
Gebel Aweina (300 km to the south), for most of the Dakhla Formation, a pala?owater depth of 200 m. The pala?owater only within (1990)
depth decreases to lower than 100 m the planktic foraminifer zone P3. Shahin
described
bathyal
environments
for the shales
in the Paleocene is at St Paul (area 3), within the middle to upper foraminiferal Parvularugoglobigerina
of the Dakhla Formation. Discussion: In the Western Desert, the Dakhla Formation was subdivided by Awad and Ghobrial (1965)
eugubina Zone (Pcx) (Strougo et a/., 1992) and, respectively, the middle NP 1 calcareous nannofossil zone (Girgis, 1987; Faris, 1997). The top of the Dakhla
into three members: the Mawhoob Shale Member; the Beris Oyster Mudstone Member; and the Kharga Shale Member. The Cretaceous/Palaogene boundary
Formation lies in Bir Dakhl (area 21, St Paul (area 3) and northern Northern Galala (area 6) within NP5, where it underlies the Southern Galala Formation. At Wadi
lies within
Tarfa
(area
I) and in western
236 Journal of African Earth Sciences
Sinai
(areas
8, 91, it
the upper part of the Kharga Shale Member
(Awad and Ghobrial, 1965). In contrast to southern and western Egypt where the base of the Dakhla Formation lies in the Lower Maastrichtian and exhibits
8. Bio- and lithostratigraphic
correlation
of six sections
from areas
1-4
on the western
the shallow water sediments of the St Anthony Formation m the Maastricht/an-Paleocene rectangle in sections 03 and 02 indicates the range of the detailed correlation of F/g. 9.
Figure
of the
Southern
Paleocene-Eocene.
of The black
Best visible is the progradation in the
Desertl. FormatIon
(Eastern Galala
side of the Gulf of Suez and
C. SCHEIBNER et al. the complete succession of all three members, in northern Egypt and Sinai only the equivalent of the younger Kharga Shale Member is present (Fig. 5). Here, the Sudr Formation and St Anthony Formation correlate with the Mawhoob Shale Member and the Beris Oyster Mudstone Member, respectively. In
P4. The Tarawan
Formation
in Ezz El-Orban
thickness
of more
than
20 m in the nearby
northern Egypt and Sinai, the base of the Dakhla Formation lies usually at the Cretaceous/Palaeogene
western
boundary
study area was deposited as basinal stones with no shallow water influences.
and the top within
P4/NP6
(Fig. 4a, b).
is very
thick in comparison to the sections of the Tarawan Formation on Sinai and in the Wadi Tarfa area. These sediments may, more appropriately, be assigned to the Southern Galala Formation, which reaches a north-
Bir Dakhl area.
Depositional
setting: The Tarawan
Formation
in the
chalks/limeAnan (1992)
and Lijning et a/. (I 998a) concluded that the Tarawan Formation on Sinai was deposited during a period of
Tarawan Formation (TF) (Figs 4a, b and 7a. e) Authors and type section: Awad and Ghobrial (1965); Gebel Tarawan, Kharga Oasis (Western Desert).
low sea levels. Luger (1985)
and Speijer and Schmitz
Stratigraphical
(19981,
reported
range: Upper Paleocene
The base lies within within lower the Tarawan
NP7/8/(P4)
NP9/(P5). Formation
and the top lies
The stratigraphical range of comprises biozones P4/NP6
on the other
hand,
Egypt that the sediments
from southern
of the Tarawan
Formation
were deposited during sea level highstands. Discussion: In northern Egypt and Sinai, the Tarawan
to P5/NP9. Kassab and Keheila (19941, however, gave a range from zones P3/mid-NP4 to P4c/lower
Formation has a reduced thickness or is absent (Fig. 5). However, even where the Tarawan Formation is
NP9. It overlies
present
the Dakhla
Formation
and underlies
the Esna Formation. Lithology: In the study is characterised 2.10 m (section
area, the Tarawan
Formation
by a 1.80 m (area 1, section Tl) to T2) thick chalk bed with flint, similar
to the underlying
Sudr Formation.
In the Kharga area,
(thin chalks
interval),
it was
authors,
although
profiles
(northeastern
Matulla:
Obaidalla, of the
siliceous
authors.
The Tarawan
Formation
was described
by earlier authors as Chalk (Zittel, 1883), (Beadnell, 1905) or Middle Oweina Naggar, 1966a, 1966b3 (Fig. 5).
Danian Chalk
Chalk Member
(El-
(WTS)
of Kassab
and Keheila
(1994)
crepancies
with respect to lithology
In section
WHS
these
authors
extending Formation, this
(near to section described
the
exhibit
dis-
and stratigraphy. Tl
the
Tarawan
Dakhla
Formation
Consequently,
Maastrichtian Shafik (1996)
1999;
Tarawan
7e).
misled
The some
attributed
even
Formation
(e.g.
and Stradner, 1971). Selima and Askalany attributed chalky limestones in Wadi Askhar
km east abundant
Formation.
In section
Al
(7
of Wadi Askhar), these chalks contain shallow water biota (corals, coralline algae)
and are attributed
in the present study to the Southern
Galala Formation
(Figs 5 and 6).
Garra Formation
Formation
rests
uncon-
(GF) (Fig. 4b)
Author and type locality: Issawi, 1969; South of Gebel Garra, south Western Desert Stratigraphical range: Upper
overlies
the Sudr Formation
overlain
by the Egma Formation
range with the base lying within
P3 (NP4-
from the observations
in the neighbouring
and
they wrongly
graphical this study)
Matulla:
chalks to the Tarawan
Eocene In northwestern
markedly
1987;
Figs 4b Formation
formably over Late Campanian sediments (Fig. 4a). Moreover, its thickness of 30-50 m and stratiNP 5) differs
by various
the respective
in this study),
down to the Maastrichtian and no Sudr whereas in WTS (near to section T2 in
study)
within
Sinai: Hewaidy,
(area 4) to the Tarawan
Regional distribution: In area 1, sections Wadi Hawashiya section (WHS) and Wadi Tarfa section
at the NP6-NP9
discussed
Ismail, 1992; Wadi Nukhl: Marzouk and Hussein, 1994; Wadi Feiran: Marzouk and Abou-El-Enein, 1997; absence
limestone.
not
it is visible
it is represented by a 3-45 m thick chalk unit, which in places changes into chalky limestone, limestone or Synonymy:
or limestones
often
sections.
(from
Similar
to
within
Sinai,
Paleocene
its base
to Lower
disconformably
and lies within
P3a. It is
of the Thebes Group
P6a.
the hiatuses, these discrepancies may be the result of very local highs and lows controlling deposition of these different lithologies.
Liihology: In area 9, the Garra Formation is composed of a basal white argillaceous limestone with chert near its top, overlain by massive limestones and thus
In section Ezz El-Orban Fahmy (1969), the Tarawan
(area 7) of Ansary and Formation is represented
shows similarities with the Southern Galala Formation at Bir Dakhl (area 2). In Kala ‘t al-Gindi, the Garra For-
m layer of mainly argillaceous limestone, which chalky in its lower part (Fig. 4b). The authors it Middle Oweina Chalk after El-Naggar (1966a, and assigned its stratigraphical range to within
mation has a maximum thickness of 49 m (Fig. 4b). At the type locality, the Garra Formation is composed of well-bedded white limestone and chalk with minor shale and marl intercalations.
by a 43 is partly named 1966b)
238 Journal of Afncan Earth Snences
Maastrichtian-Early Regional distribution:
Eocene litho-biostratigraphy The Garra Formation
cribed only by Hamza et a/. (1997)
andpalazogeograph
was des-
from northwestern
and north central Sinai. Depositional setting: In southern Egypt, the Garra Formation was deposited in the middle to inner shelf (Luger, 19851,
whereas
on Sinai deeper marine set-
tings are assumed (see the discussion of the Southern Galala Formation below). Discussion: In northwestern Sinai (area 91, Hamza et a/., (1997) described limestones of the Garra Formation (mid-P3b-mid-PGa), sandwiched between the chalks of the Sudr Formation and the limestones of the Thebes Group (Fig. 4b). Said and Kenawy (I 956) identified a bathyal fauna in the chalky sediments. Whether these deposits are synonym with the Southern Galala Formation remains uncertain. However, at least the introduction
of the Garra Formation
in this part of Egypt may explain earlier discrepancies in lithological
description
and dating
of the Sudr
Formation and Thebes Group. Hermina and Lindenberg (I 989) described the Garra Formation from the southern Western Desert. It disconformably overlies the Kurkur Formation and underlies the Dungul Formation. The Garra Formation,
y of the northern Gulf of Suez region
Abu Darag (Abd-Elazeam and Metwally, 1998). Malchus (1990) described a hiatus ranging from Late Cenomanian
to Maastrichtian
Formation
limestones with flint. Synonymy: Abu Khadrah et a/. (1987) Galala Formation. NP9/10)
The whole Palaeogene part (P5/6;
of section Wadi Naot (limestones and clayey
siltstones)
in the Northern
Abd-Elshafy
Galala was attributed
and Atta (1993)
which was introduced by Abd-Elshafy (1988)
Galala Formation (Fig. 5). distribution:
In sections
D2 and D3 (area
Galala Formation
starts with the
bed and is characterised
limestones
dant chert layers or nodules
c. d) Authors and locality: Abdallah et a/. (1970);
to 0.7 m thick). The hard limestones
of St Anthony Eocene
Data from this study indicate that the base of the Southern
Galala Formation
lies within the Glomal-
veolina levis Zone (Upper Thanetian,
P4c/NP8)
and
the top lies within the Alveolina dainelliZone (Cuisian, PS/NP13). In Bir Dakhl and St Paul, the Southern Galala Formation
is overlying the Paleocene
Formation (Fig. 4a) with a stratigraphical
Dakhla
range from
and shaley marls (up are partly com-
posed of bioclastic wackestones, and chalky and dolomitic limestones. Figure 9 shows the interfingering of the Southern partly overlying D2 and 03).
Stratigraphical range: Upper Paleocene-Lower
by
(up to 1 m thick) with abun-
Southern Galala Formation (SGF) (Figs 4a. b and 7b,
of monastery
in Wadi
Naot Formation in this study because it is possible to differentiate the Dakhla Formation and Southern
alternating
The reference section 18/2 (Kuss and Leppig, 1989) is situated in a north-south-trending wadi, 6 km west
by
to the Naot Formation,
Naot (Wadi Naot is a synonym of Wadi Nooz used by the authors). The authors did not employ the term
first hard limestone
by Kuss and Leppig (I 989)
introduced the
Useit Formation as a junior synonym of the Southern
2), the Southern
redefined
(alveolina,
thickness of about 250 m. In the southern parts, it is
Regional
(Fig. 5).
sandy fossiliferous
numulitids, coralline algae) limestones and limestone/ sandstone intercalations often conglomeratic with a
parts of the Dakhla,
and Esna Formations
In the
(section Nl of Fig. 4a) and underlies the
Thebes Group. Lithology: Massive
in southern Egypt, is a lateral equivalent of the upper Tarawan
in section 20/2.
northern areas of the Northern Galala, the Southern Galala Formation overlies the Paleocene Dakhla
show
Galala Formation
Esna Formation
In section
abundant
and the
in detail (sections
D2, three limestone
bioturbation
beds and
Thalassinoides.
The
Galala Formation
unit A in sections D2 and D3 (Fig.
9) has a thickness Although
main
of Zoophycos
part of the Southern
of 17 m and 20 m, respectively.
the Southern
Galala Formation
has more
or less the same thickness in these sections, the thickness of the different biozones varies (e.g. NP6 and NP7/8;
Fig. 9).
mid-NP5/(P3/4) to mid-NP9/(P4/5). In section D2, the Southern Galala Formation interfingers with the
is composed
with
locally abundant
Esna Formation,
quartz grains that were deposited
as gravity flows,
and the top lies within
NPI O/P6
At St Paul (area 31, the Southern Galala Formation of limestones
(Figs 6,8 and 9). At St Paul, the top of the Southern Galala Formation lies within SBZlO (NPI 2/P7)
such as glides, slumps and debris flows. A few thin
(Gietl, 1998). In St Anthony, the Southern Galala Formation overlies the Late Campanian-Maastrichtian St Anthony Formation, while farther north it is
lower part (Scheibner et a/. , 2000). The steep white cliff at St Anthony and Gebel Thelmet (area 4) is composed of dolomitic limestones
unconformably
of the Southern Galala Formation (Fig. 7d). Because
underlain by Turonian strata in section
20/2 (Kuss and Leppig, 1989) and other parts of the Northern Galala (Abd-Elshafy and Atta, 1993), and by Campanian limestones of the Matulla Formation in
(maximum
20 cm) marl beds are intercalated
in the
of its white colour and its chalky appearance, which is due to diagenetic alternations, several authors (Abdallah and Eissa. 1970; Abdallah et a/. , 1970; Abu
Journal of African Earth Snences 239
C. SCHEIBNER et a I.
Figure 9. Detailed bio- and lithostratlgraphic units described in the text.
240
Journal
of African
Earth Snences
correlation
of sections
03
and 02
m area
2.
The letters
A-F
indicate
different
Maastrichtian-Early Khadrah strata
Eocene litho-biostratigraph
et a/. , 1987) previously
as chalks
misinterpreted
of the Sudr Formation
y and pal;eogeograph
these
(Fig. 5) or of
the Tarawan Formation (Selima and Askalany, 1996). However, the basal conglomeratic debris flow type deposits of O-2 m thickness are overlain by white diagenetically overprinted limestones with abundant corals in the lower 15 m. In the middle part of the nearly 70 m high cliff, Hottingerina lukasi(SBZ4/P4c) was found, indicating a latest Paleocene age. In section 20/2 (area 5) (Kuss and Leppig, 19891, the Late Paleocene-Early Eocene Southern Galala Formation is build of massive sandy limestones, limestone-sandstone
intercalations
and debris flows.
In Wadi Nooz (area 61, it is formed and
chaotically
lithologic mation the
bedded
similarities
of debris
limestones.
flows
Because
to the Southern
Galala
For-
of area 3 (St Paul), this unit is attributed
Southern
Galala
Formation.
lying Dakhla Formation, found, indicating again Hamam (1998)
Faraoun
to
As in the under-
only morozovellids were an age of P3 or younger. In
in the very
described
of
south
debris flows
of area 9, Gietl
up to 6 m thick
with
Galala
y of the northern Gulf of Suez region
Formation,
overlying
Thebes
or whether
it forms
part of the
Group (Fig. 5).
Esna Formation (EF) (Figs ba, b and 7a, e) Author and type section: Beadnell (1905); Aweina near Esna Stratigraphical range: Late Paleocene
Gebel
to Early Eocene
Its stratigraphical range has been discussed intensively (El-Naggar, 1966a, 1966b, 1968; Sabry, 1968; Issawi, 1972). Today, it is accepted in Egypt, except Sinai, that the Esna Formation is intercalated between two, more or less, chalky limestone units. These units are, the Tarawan Formation below and the Thebes Group above,
and thus represent
Early Ypresian
(P4c/lower
6). On Sinai, quite
often
however,
the term
used to describe
shales sandwiched
Late Thanetian
to
NP9 to mid-P7/NP12;
between
Fig.
Esna Formation
the whole
is
Paleocene
the Sudr Formation
below
and the Thebes Group above (Liining et al., 1998a; Marzouk and Lining, 1998; see discussion below). Liihology: The Esna Formation
is composed
grey shales and marls with planktic
of green-
foraminifers
and
siliciclastic sand and larger foraminifers and shallow water limestones with larger foraminifers of Early
calcareous
Eocene age (SBZ7-9, 9 (Wadi Sudr), Gietl
the ‘grtinliche Blatterthone’ of Zittel (18831, the upper Esna of Hume (1912) and the Upper Oweina Shale of
beds with slumps, minifers. In Gebel described with
chalky
larger
NPI O-l 2). In the north of area (1998) found limestone/marl debris flows Urn Makhasa,
limestones
foraminifers
and larger foraKulbrok (1996)
of SBZ4-6
and corals,
which
(NP8/9) may be
nannoplankton.
Synonymy:
El-Naggar
The Esna Formation
(1966a,
1966b)
is synonymous
with
(Fig. 5).
Regional distribution: In Wadi Tarfa (area l), the Esna Formation
is 10.50
is composed
m (Tl ) to 17.10
of the same
m (T2) thick and
lithology
as the
Dakhla
attributed to the Southern Galala Formation. Depositional setting: The sediments of the Southern
Formation. Nishi et al. (1994) described a section south of the Ras Gharib to El-Sheikh Fadl Road with
Galala Formation
only 5 m of the Esna Formation
are sediments
of a carbonate
plat-
form and slope, which were deposited on and around the Northern Galala/Wadi Araba High. They interfinger with
basinal
sediments
of the Southern
Galala Sub-
basin in area 2 (Bir Dakhl). Kulbrok (I 9961, Gietl (1998) and Scheibner
et al. (2000)
described
platform and slope deposits Formation in more detail. Discussion:
In this study,
the carbonate
of the Southern the classification
Galala of Abu
Khadrah eta/ (1987) and Selima and Askalany (1996) are not followed. The Useit Formation described by
the Thebes Group, whereas
overlain
El-Dawy
21 m of Esna Formation in a section Gharib to El-Sheikh Fadl Road. Strougo section
and Faris (19931, (area
21, described
in their Wadi El-Dakhl
is characterised abundant These
by green-grey
shaley
sandstones
are partly
as Dakhla
Formation
(see the discussion
with layers.
cross-laminated
parts
interpreted
marls
thin (up to 0.22 m thick) sandstone
ever, is of Early Paleocene be regarded
calcareous
shales and cream to light grey laminated argillaceous limestones. In section D3 (area 21, the Esna Formation
have rip-up clasts. The sicliciclastic
should
reported
south of the Ras
green-grey
Abu Khadrah et al. (I 987) was thought to overlie a unit termed Esna Formation In St Paul; which, howage and, therefore,
by chalks of
(1999)
intercalations
and were
as distal fan lobes, of which more proximal
at St Paul were
discussed
in Scheibner
et al.
(2000). In Bir Dakhl (area 21, the Southern Galala Formation grades laterally into shales of the Esna
of the Abu Rimth Formation below). Moreover, the same authors correlated the Zaafarana Formation
Formation,
with the originally Formation
Useit Formation, although the first was described to overlie the Southern Galala and is of middle Eocene age (Abdallah et
section D3 (Fig. 9). In section D2, the intimate interfingering of the Esna Formation with the Southern Galala Formation is evident (Figs 8 and 9). As a con-
al., 1970). It is not clear by the above whether the Zaafarana Formation should be attributed to the Useit
sequence, this part of the section can be subdivided into five units. From the bottom to the top, the following
Formation
five units can be distinguished
and, hence, represent
part of the Southern
best visible in section
Journal
D2 and less clear in
(Fig. 9) as follows:
of African
Earth Sciences
24 1
C. SCHEIBNER et al. i) A: alternating
limestones
layers (see Southern
with
abundant
Galala Formation
chert
above);
iii B: 2.5 m grey-green marl; iii) C: 1.9 m alternation of silty marls and dolomitic limestone with laminations and channel structures; iv) D: 4.4 m grey-green marl at the base silty; v) E: 6 m alternation of shaley, partly silty, marls and dolomitic limestones with laminations, channel structures
and rip-up layers;
Paleocene shales or only Lower Paleocene shales were exposed or where they were separated by the Tarawan Formation. If the shales range from the Lower to the Upper Paleocene, the authors suggest the usage of the Dakhla/Tarawan/Esna Formation (Figs 5 and 6). Snavely et al. (1979) stated that most authors agree with the upper portion of the Esna Formation being assigned to the Ypresian Morozovella subbotinae Zone
and
(PG/NPl O/l 1 of Berggren
the transitional
vi) F: 5.2 m of silty marls.
marly beds typical
et a/. , 19951,
of the conformable
Within this profile, units (A), (C) and (E) exhibit characteristics of the Southern Galala Formation,
Esna-Thebes contact were assigned to the Morozovet/a aragonensis Subzone (P7/NP12 of Berggren et
whereas units (B), (D) and (F) could be attributed to the Esna Formation (Fig. 9). In northern Northern Galala (area 61, the 15 m of the
a/., 1995). However, in this study, it was found that the Esna-Thebes contact in the Eastern Desert was
Esna Formation are of Lower Eocene age (NPI 1 /12/P6), indicated by presence of calcareous nannofossils and planktic
foraminifers.
In contrast,
Gietl (1998)
des-
cribed alveolinids of SBZ5 (NP9/P5) from limestones overlying the Esna Formation; which, however, may have been reworked
from older carbonates.
Depositional setting: The Esna Formation deposited as basinal marls with no shallow influences. in areas
Shallow that
Formation. depth
water
interfinger
deposits with
curve
from
were found
the Southern
Speijer and Schmitz
was water only
Galala
(I 998) gave a palseo-
Gebel Aweina
(ca 300 km to the
usually within NPI 1. In the upper Formation as well as in the Thebes
part of the Esna Group, Nummu-
lites deserti was found (LeRoy, 1953; Hermina and Lindenberg, 19891, indicating an Ypresian age (NPl lNPI 21, which contrasts of that species
with the stratigraphical
mentioned
by Serra-Kiel
as SBZ4 and SBZ5 and which corresponds This discrepancy led to some confusion stratigra-phical example,
range
Gietl (1998)
of the
Thebes
correlated
Group.
(SBZ5 or NP9), which the strati-graphical
would
be in disagreement
Dakhla/Tarawan/Esna
the shales of the Esna Formation
Eocene.
Formation
was given
to Beadnell
of the Esna
(I 905),
although
shales in the vicinity of Esna were mentioned earlier by Zittel (1883) and others (see El-Naggar, 1966a, 1966b). In northern shales
Egypt and on Sinai, the whole Paleocene
and marls
Formation
are often
in areas
where
attributed no Tarawan
to the Esna Formation
exists (Said, 1990) and thus have a stratigraphical range from Upper Maastrichtian to Lower Ypresian (see the discussion of the Dakhla/Tarawan/Esna Formation below). Even if only the lower part of the Paleocene
shales are exposed
(e.g. Abu Khadrah
al., 19871, they were quite often referred Formation, which makes lithostratigraphic
et
to as Esna correlation
very confusing (Abu Khadrah et al., 1987; Hewaidy, 1987; Said, 1990; Cherif and Ismail, 1991; Marzouk and Hussein,
1994)
suggest attributing the Esna Formation, would belong to the is only possible in
(Fig. 5). The authors,
therefore,
only Upper Paleocene shales to whereas Lower Paleocene shales Dakhla Formation. This bipartition areas where either only Upper
242 Journal of African Earth Sciences
Because
Maastrichtian
with
range of our samples.
Stratigraphy: The stratigraphical range formal formation is Upper Maastrichtian
on
For
part of
the Thebes Group to the Alveolina cucumifom?is Zone
depth decreases to 100 m only in the uppermost part of the Esna Formation. According to Shahin (19901, were deposited
to NP9. of the
the lower
south) and reported palaaowater depths of about 200 m for most of the Esna Formation. The palseowater
Sinai in bathyal environments. Discussion: The credit for the introduction
range
et a/. (1998)
Formation (DTE) (Fig. 441)
of the gradual
transition
chalk to the Paleocene
of this into Lower from the
shales, the onset
of the DakhlaTTarawan/Esna Formation in Abu Zenimal Wadi Feiran (area 8) is not clearly fixed lithologically. It varies from a level within
the Upper Maastrichtian
to one at the Cretaceous/Palaeogene A small (Shahin,
hiatus 1992).
(K/Pg) boundary.
at the K/Pg boundary is probable As with the lower stratigraphic boun-
dary, the upper boundary is not well constrained. The transition from the Dakhla/Tarawan/Esna Formation to the Thebes overlies Group.
Group
lies around
the Sudr Formation
Liihology: Green-grey Esna Formation Regional Formation
P6/7,
and underlies
NPl l/l 2. It the Thebes
shales and marls, similar to the
distribution: The Dakhla/Tarawan/Esna is only present on Sinai.
Depositional
setting:
The
Dakhla/Tarawan/Esna
Formation was deposited as basinal the Esna Formation (Shahin, 1990). Discussion: an informal
marls similar to
The Dakhla/Tarawan/Esna formation for the latest
Formation is Cretaceous-
Palseogene grey-green shales in northern Egypt and Sinai, where the Tarawan Formation cannot be
Maastrichtian-Early identified.
Eocene litho-biostratigraph
In most
Tarawan/Esna
sections
within
the
y and pakeogeograph y of the northern Gulf of Suez region
Dakhla/
Formation at around upper P4/5, one
quartz grains. The base lies in lower NP12. sediments
may belong to the Southern
These
Galala For-
mation as well but, again, were not subject of this
or more limestones might be attributed to the Tarawan Formation. Masters (1984) indicated two limestone
study. The Thebes Group in area 8 is composed
beds in Wadi Feiran East, which could be attributed
sequence
to the Tarawan
intercalated
tectonic
Formation
duplication
Because probably
and probably represent a
(R.P.
Speijer,
pers.
comm.).
of the reduced thickness of the beds, not all authors indicated these layers as
1992)
of well-bedded
of a
limestones
with
chert bands (El Sheikh and El Beshtawy,
or of yellowish
limestones
chalky
sandy limestones
with chert bands (Shahin,
followed 1990,
by
1992).
In Wadi Feiran (area 81, Eweda and El-Sorogy (I 999)
Tarawan Formation. The varying ages of the top of the Dakhla/Tarawan/Esna Formation are due not to transitional lithologies but to the different biozonations
divided the Thebes Formation into a lower 180-I 90 m thick cherty chalky limestone member and an upper
used. Authors who have worked with the calcareous
Depositional setting: Only the lower part of the Thebes
nannoplankton bio-zonation gave older (NPI 1 = P6) ages than authors who used the planktic foraminifer
sediments were deposited in a basinal setting without
zonation from
(P6/7).
This discrepancy
the variability
calcareous
in the
nannoplankton
probably
planktic
correlation
results
foraminifers(Marzouk and
50-60
m thick calcareous
claystone
member.
Group in area 1 (Wadi Tarfa) was studied. Here, the any shallow water influences. In areas 2-6, the transition from the Southern Galala Formation to the above
lying Thebes
Shahin (1990)
Group
was not investigated.
and Lining et al. (I 998a)
suggested
Lining, 1998). Another explanation may be the usage of different planktic foraminifer biozonations, which
that the Thebes Group on Sinai was deposited during
were revised in time or different taxonomic
a time of a lowered
concepts
of the authors.
sea level. Snavely et a/. (1979)
proposed the following three-stage
depositional
his-
tory for the Thebes Group: Thebes Group (THG) (Figs 4a, b and 7a. e) Authors: Hermina and Lindenberg (1989) Stratigraphical formations
range: Lower Eocene (see different
below) below)
(see different formations
Regional distribution:
Discussion:
below)
Hermina
At Wadi Tarfa, the base of the
Thebes Group lies within NPI 1 /P6. It is composed of chalky limestones alternating with chalky marls. Some of the chalks have layers or nodules of flint incorporated.
and
The Thebes
by chalky limestones
with abundant
chert layers or
nodules, marly intercalations and sandstones with cross-bedding, lamination and rip-ups. They may alternations
Group was introduced
and Lindenberg
(1989).
It replaces
by the
Thebes Formation of Said (1960) and is equivalent to the ‘Libysche Stufe’ of Zittel(18831, excluding the Esna Shales (Fig. 5). The Thebes Group includes the following formations (Fig. 5): i) Farafra
In Bir Dakhl (area 21, the Thebes Group is formed
contain
iii gradual shallowing;
fi) abrupt lowering of sea level.
Liihology: (see different formations Synonymy:
i) basin-wide pelagic carbonate deposition with thin shallow water facies near the basin margins;
Formation,
Formation,
El-Rufuf
Formation,
Serai
Drunka Formation and Dungul Formation
in the scarps and plateau areas south of Minia; ii) Abu Rimth Formation in the Southern Galala; and iii) Egma Formation on Sinai.
of harder and softer marls. In
Here, the focus is only on the Serai, Egma and Abu
the lower part of section D2, the marls are partly rich
Rimth Formations since they have been described in the
in quartz grains and Nummulitids. section
D2, slumping
In the upper part of
and first Alveolina-rich
study area of the northern part of the Gulf of Suez. In
sand-
this contribution, the authors refer to the Thebes Group
stones occur that could belong to the Southern Galala
when ‘speaking’ of Lower Eocene strata that overly the Esna or Dakhla/Tarawan/Esna Formations (except the
Formation as well, but this transition was not investigated in detail. Bandel et al. (1987)
described the Serai Formation
overlying the Esna Shale from the western escarpment of Wadi Tarfa. Within the upper third of the 1 IO m
Galala Mountains, where the Thebes Group overlies the Southern Galala Formation) and underlie the Minia Formation. In the contribution, different formations is done.
no subdivision of the
thick succession of bedded marly to platy chalks with flint intercalations, a 17 m thick unit of alveolinidnummulitid-bearing limestones aged SBZl 1 - 14 occurs
Authors and type section: Barron and Hume (1902);
that indicate an Early Eocene age. The Thebes Group
redefined
of northern Northern Galala (area 6) is composed
Lindenberg,
well-bedded
dolomitic
mulitids, deformed
limestones
of
partly with num-
alveolinids, few debris flows and
Serai Formation by Lindenberg 1989)
et al.
(in Hermina
and
as facies variation of the Thebes
Group; Gebel Serai, south Wadi Qena, Eastern Desert Stratigraphical
range: Early Eocene
Journal of African Earth Sciences 243
C. SCHEIBNER et al. Synonymy: Synonymous members of the Thebes and the lower
member
of the Thebes
Formation
of
thinly-bedded
micritic
lime-
chalky and cherty with rare shales, grading into massive bioturbated beds with few
allochthonous layers Discussion: The Serai Formation throughout
Formation. Philobbos et al. (in Hermina and Lindenberg, 1989) mentioned that the Abu Rimth Formation overlies
the Esna Formation
However,
Snavely et al. (I 979). Lithology: Fine-grained stones, upward
with the lower and middle Formation by Said (1960)
the Stable
Shelf,
is widely
developed
at the plateau
surface
the Esna Formation shales
in the southern
in St Paul no Upper
of the
Paleocene
occur, only the Lower
Dakhla
Formation.
before, the term Esna Formation sometimes covers the Lower Formation
as well. Therefore,
the Dakhla Formation
parts.
shales
of
Paleocene
As documented is loosely used and Paleocene Dakhla
the strata
overlying
in
St Paul could not belong to the
between the Nile and Kharga Oasis, Wadi Qena, and the Quseir-Safaga region. A special slump facies of
Abu Rimth Formation but should be correctly attributed to the Southern Galala Formation. As a consequence,
mixed
the Abu Rimth Formation
autochthonous
is defined
and allochthonous
separately
Southern
Galala (see below).
described
sediments
as Abu Rimth Formation
by Bandel
in the
The Serai Formation
was
et al. (I 987) in the Wadi Tarfa
by the conglomeratic Galala Formation
in the Galalas is represented
sandy lithologies
and, hence,
of the Southern
has to be attributed
as
area.
a synonym of the latter. The Abu Rimth Formation is present only in the Southern Galala (Philobbos et al.,
Egma Formation
to the areal extension
Author and type section: Beadnell (I 927) and Hermina and Lindenberg (1989) mention no type section, only
mation
in Hermina and Lindenberg,
the type area (Egma Plateau Stratigraphical
according
the term Abu Rimth Formation
turbidite
layers with reworked
fossils. is present
and northern Sinai. It overlies whereas the top is uncovered.
LATERAL
in the
the
Esna
Abu Rimth Formation The following description and Schmitz
posed
from Phillobbos,
(in Hermina
and Lindenberg,
only
Lindenberg
Schmitz
1989)
and Lindenberg,
and
Galala, south-southwest
of the monastery
Liihology: It is composed
of “well-bedded open marine
and thick olistostrome
carbonates,
including
sand.”
conspicuous
slump structures.
Synonymy:
It is synonymous
members
layers containing
clasts of shall0 w water
reefal limestones,
and displaced
thin
Alveolina
They
may
have
with
the lower
Formation
and
by Said
(1960) and the Thebes Formation (I 987).
of Bandel and Kuss
Discussion:
range
Rimth
Formation
Lindenberg, range
The stratigraphical
of the
(Philobbos
1989) above
collides
et al., in Hermina with
mentioned
244 Journal of African Earth Sciences
water
change
and
the stratigraphical Southern
Galala
belt
at the
14 km to the south only
with
are not
carbonates
to Early Eocene times.
of the
from the Late and are ex-
Galala. At these times,
and Dakhla
were deposited
sediments Formations
the basinal exposed.
at St of the accu-
Sudr and In St Paul,
of the Southern
Galala
only during Late Paleocene
The authors
in St Anthony
interpret
that this
is due to the proximal
position
of St Anthony
Wadi
Araba
High
(NGWA)
in the north that shed shallow
water
sedi-
to the
ments from a carbonate CampaniarVMaastrichtian In area 9, shallow during
water
platform as early as the (Kuss et al., 2000). sediments
were deposited
the Campanian-Maastrichtian (Youssef and Shinnawi,
(Exogyra
cf.
1954; El-Shinnawi,
1967) and were possibly equivalent to the St Anthony Formation. In contrast to area 4 (St Anthony) where the shallow Formation
of the Abu
Sudr
Formations
oveNvesI)
of the Thebes
arrived
Interfingerings
Formation
and Sudr-/
in an east-west-trending
water
Dakhla
facies
and marls with intercalated
abundant larger foraminifers, limestones
of St Paul.
range: Early Eocene
to shelf limestones
middle
deeper
water)
and siliciclastics
Paul (Figs 1 and 3), where
shallow
The type area is the Wadi Abu Rimth in the Southern Stratigraphical
carbonates
rim of the Southern
mulated.
Author and type section: Phillobbos,
OF FORMATIONS
Formation were deposited to the Late Maastrichtian
no such sediments is taken
1989): (in Hermina
TRANSITIONS
water
St Anthony Campanian northern
turbidite
For-
Therefore,
should be abandoned.
St Anthony Formation (shallow Dakhla Formations (deep water) Shallow
The Egma Formation
Lindenberg
Galala
results.
on Sinai).
platform deposits of mediumlimestones with tabular chert
bands, chalky frequent
southern Formation
to the authors’
range: Early Eocene
Lithology: Shallow bedded to massive
Discussion:
19891, which corresponds
of the Southern
water was
Paleocene-Eocene sediments
Cretaceous the
St Anthony
by
shallow
Southern
Galala Formation
with Exogyra cf. overwegi
by the deeper This contrast
Upper overlain
water
chalks
of depositional
water on Sinai,
were overlain
of the Sudr Formation. facies could be explained
Maastrichtian-Early
Eocene litho-biostratigraph
y andpakogeograph
by differences in the vertical movements. While the Northern Galala/Wadi Araba area represents the centre of the Northern western
GalalaNVadi
Araba High, nor-th-
Sinai (area 9) was less affected
by this local
Araba. On both sides, south and north of the Northern Galala/Wadi Araba, similar lithologies with slides, slumps and debris flows are present. The only biostratigraphic
minifers
Galala Formation
water
is deposited
area in the Galalas Faraoun). However,
and parts of Sinai (Hamam its areal extension is far larger
than that of the St Anthony between
in an east-west-trending
the deeper
water
Formation.
Interfingering
deposits
of the Dakhla
and Esna Formations and the shallow of the Southern Galala Formation variations
within
best exposed
water limestones and the lateral
the Dakhla and Esna Formations
at the two
Bir Dakhl sections
are
D2 and
occur
Faraoun
(south)
and evidence
palasotopographic
high between
The sediments the northern Southern
NP5. While southern
the Southern
D3 section
Galala
Formation
is represented
bioclastic wackestones, chalky-dolomitic and thicker ‘Dakhla Formation’ type northerly
D2 section shales.
contrast
shows
thicker
It is assumed
in the two
sections
of the Northern
of the
by thin-bedded
that
limestones shales, the
limestones this
and
lithological
is a result of the closer
Galala/Wadi
Araba carbonate
platform to section D2 (Kuss et al., 2000) contemporary increase of platform-derived
and the carbon-
ates (Figs 8 and 9). An even more pronounced logical contrast is evident Lower Eocene succession.
in Wadi
Sudr
Eocene shallow These sedimentary
(north) the
and Hamam existence
of a
both areas.
Southern Galala Formation (shallow water) and Thebes Group (deep water)
sections,
starts in mid-
Galala Formation.
textures
Serai
Galala Formation
described similar with debris flows, and larger fora-
of the Late Paleocene-Early
Southern
D3 (area 2) that are 6 km apart (Figs 8 and 9). In both the Southern
of area 6 studied
from marls of the Esna Formation.
On Sinai (area 91, Gietl (1998) carbonate dominated successions slumps, intercalated siliciclastics
Southern Galala Formation (shallow water) and Dakhla/Esna Formations (deep water) Similar to the St Anthony Formation, the Southern
position
data from the sections
here are obtained
high.
thinner
y of the northern Gulf of Suez region
attributed
Formation
Galala
(THG)
between
the present
detailed
also
both,
which
was
of the deeper water-derived
on their
as
of basic facies not studied
(Fig. 6). In that case,
Galala Formation
studies
be classified
because
contribution
again, an interfingering Group with the shallow the Southern
(area 6) to the lower
may
Galala Formation
similarities within
at Bir Dakhl (area 2) and at
Northern
water Thebes sediments of
may be deduced
contacts
with
from
the Thebes
Group. Snavely et al. (I 979) mentioned sediments of the lower Thebes Group
that were
posited
with thin
as basin-wide
shallow
water
pelagic
facies
carbonates
the de-
near the basin margins.
litho-
in the Upper Paleocene to In the southern D3 section,
distal equivalents of the Southern Galala Formation are represented only by thin siliciclastic intercalations
HIATUSES In the
AND SYNSEDIMENTARY
study
area,
distinguished,
four
types
characterised
of hiatuses
by variable
can be
duration
and/
within the Esna Formation, whereas in the northern D2 section massive siliciclastic limestones with
or different
internally
Major hiatus from Late Cretaceous to Late Paleocene
reworked
clasts have been deposited
(units
B and D) (Figs 8 and 9). Area
3 (St Paul) is a fine example
basin transition.
Three phases of ramp progradation
were observed deposits
of a ramp-to-
that are indicated
of glides,
slumps
by mass transport
and debris flows.
Micro-
facies analysis provided evidence of a change in the origin of the debris flow deposits that reflect a transition
from a basinal-to-outer-ramp
middle-to-inner-ramp distribution
setting
including
of biota (Scheibner
The lithologies
setting a change
to a in the
et a/., 2000).
of the succession
of the northern
Southern
Galala.
intercalated
interfingering shallow
water
Allochthonous
shallow
with hemipelagic
of limestones platform
derived
water
car-
marls show the from the nearby
of the Northern
Galala/Wadi
mechanisms.
Together
with the nowadays
southern
Northern
affected
by the Syrian Arc deformation
eroded Wadi Araba, the
Galala (area 5) represents
part of Said ‘s (1961) Galala, compressional
Unstable
an area
and hence is
Shelf. In the Northern
deformation
erosion and non-deposition
resulted
in uplift,
during the Late Cretaceous
to Late Paleocene. In the Shabraweet area - 70 km north of the Northern Galala/Wadi Araba, Mohammed and
Omran
(1991)
Campanian-Early
area of the Northern Galala (area 6) are very similar to those of areas 2 (Bir Dakhl) and 3 (St Paul) of the bonates
trigger
TECTONICS
in the
Northern
described
a hiatus
from
the
Eocene similar to the hiatus observed Galala.
On Sinai,
area
7 shows
similarities to area 5 (middle to south Northern Galala) where a large hiatus is evident across the Cretaceous/ Palzogene section occur
boundary
as well (Fig. 4a, b). Except
Ezz El-Orban, only latest Paleocene above
the K/Pg boundary.
(I 960) and Moustafa
According
and Khalil(1995),
for
sediments to Said
the boundary
Journal of Afrxan Earth Sciences 245
C. SCHEIBIVER et al. between
the stable/unstable
shelf lies at Wadi Araba
and north of area 8 (north of Abu Zenima). Thus, this area shouldn’t be affected by the Syrian Arc deformation. However, if it was also affected, the boundary between the stable/unstable shelf should be shifted on Sinai south of the area 7. Another possibility is the presence of a local high with non-deposition for which there is no other evidence yet. Bosworth eta/. (I 999) demonstrated that the Syrian Arc deformation also affected regions in stable intraplate settings, at least as far south as the southern part of the Gulf of Suez (Esh El-Mellaha Range and Gebel Zeit), due to far-field compressional stress. In contrast
to all other areas described,
geneous
tectonic
and depositional
and inhomo-
history.
Probably,
it could be subdivided into more areas: into areas with larger hiatuses across the K/Pg boundary; and areas with continuous
sedimentation.
Together
with the two
sons, the Late Paleocene sedimentation and finally resulted in the P3 hiatus.
exact
foraminifers tions
Tl
depositional
that
Arc deformation.
could
sample
not be mapped
Araba
in detail
due to larger
High
during the Late
MAASTRICHTIAN PALAOGEOGRAPHIC NORTHERN Figure 1 Oa-k illustrates depositional
Gietl,
In secbetween
spacing.
High (Youssef and Shinnawi, 1996;
hiatuses
as resulting from times of non-deor very reduced depositional rates
Cretaceous-Late Paleocene in the Northern Galala, the northwestern Sinai was less affected by the tectonic processes of the Northern GalalaNVadi Araba Kulbrok,
nannoplankton.
I), short
with
on planktic
In contrast
GalalaNVadi
that lead to erosion and non-deposition
based
P5 and P6 occur where parts of upper P5 and lower P6 are missing. These short hiatuses are interpreted,
areas were
by the Syrian
only in sections
controls
and calcareous
may lie in the fact that these affected
evident
and T2 (area
The reason for these different
to the uplift of the Northern
become
biostratigraphic
in this study, position/erosion
histories
processes
Minor hiatuses Short-ranging hiatuses within single biozones are possibly present in all sections. However, these
southern areas, areas 7 and 8, the depositional history of central western Sinai would be even more complex. differently
(P3) of Sinai
Some sections of Wadi Feiran/Abu Zenima (area 8) show a hiatus around P3. The authors assume similar reasons for this hiatus as described for that of the Maastrichtian/Palaaogene boundary. Furthermore, a submarine topographic high may have influenced, in combination with some of the above mentioned rea-
short hiatuses
north-west-
ern Sinai (area 9) has the most complex
Hiatus within the Late Paleocene
1954; El-Shinnawi,
1967;
1998).
settings
and defined
Hiatus across the Maastrichtian/Paleocene A hiatus across the Maastrichtian/Paleocene
boundary boun-
TO PALROGENE EVOLUTION OF THE GULF OF SUEZ the regional
summarised
for calcareous
evolution
of the
for 11 time slices
nannoplankton
biozones.
These time slices were chosen because they best characterise the changing of the depositional environments through time. The CC biozones represent two Maastrichtian time slices, NPI -NP9 represent
dary is evident or inferred in most sections. An exception is St Paul with the presence of the Upper Maastrichtian nannoplankton Micula prinsiizone
the Paleocene and NPl 0-NPI 2 represent the Lower Eocene (compare Fig. 4 and the Paleocene-Eocene
and the Lower
boundary
zone.
Paleocene
The sections
plankton
foraminifer
in St Paul are considered
Pcx
one of
the most complete across the K/Pg boundary in Egypt, although they are very condensed. Lijning ef al. (I998a) ranging
also documented
a very complete
across the K/Pg boundary
Comparable stratigraphical et al., 2000),
lithologies,
on eastern
probably
of the
section Sinai. same
range as area 3 (St Paul) (Scheibner are found on Sinai in area 9 (Hamam
Faraoun: Kulbrok, the sections Wadi
1996; Gietl, El-Seig/Wadi
1998). Hialla
Moreover, (Abbass et
al., 1994) evidenced a Late Cretaceous-Palseogene succession with a stratigraphical range similar
to
the St Paul section of area 3. Elsewhere, a hiatus is present at the K/Pg boundary in most of Egypt and probably resulted from a combination of low sedimentation rates, reworking, patterns and sea level changes
246 Journalof African Earth Sciences
changing circulation (Lijning et al., 1998a).
herein).
In areas
of non-deposition
palaeogeographic of time-equivalent position
occurred,
the time of erosion
or eroded
areas,
the
maps illustrate only the absence sediments today. Whether deor not, is not indicated cannot
be pinpointed
because accurately.
For comparison of palaaogeographic maps and stratigraphy of areas of major uplift, see Fig. 4. Within this stratigraphic/palaeogeographic framework, the Wadi El-Esseila succession (El-Askary and Shaaban, 1993) remains questionable because the stratigraphic subdivision here is in no concordance with the stratigraphic subdivision of the surrounding sections. CC25 (Fig. 7Oal During the middle Maastrichtian biozone CC25, the areas west and north of the northern parts of the Gulf of Suez are characterised
by non-deposition
Maastrichtian-Early Eocene litho-biostratigraphy and pala?ogeograph y of the northern Gulf of Suez region
Depositional Setting and Environmental Regime I-III:
~
ill m
basinal limestones (THG)
III [
basinal marls and shales (EF)
III 1//A
basinal chalks (TF)
III m
basinal marls and shales (DF)
III 0
basinal chalks (SF)
II m
shallow-water limestones (SGF)
ll m
shallow-water limestones, siliciclastics and marls (SAF)
l
non-deposition or eroded
l
m
sections considered in the palaeogeographic maps
o sections not considered in the palaeogeographic maps Figure 10. Regional pages).
palasogeographic
In the Maastrichtian,
the two
maps
of
calcareous
calcareous nannoplankton biozones of NPI-N The first regime with hiatuses reflects uplift
11 time
slices
nannoplankton
from
the Maastrichtian-Early
biozones
10 fcl; were chosen. Three and erosion or non-depositon
of CC25
and
Eocene CC26
different environmental l/1. The shallow water
following
two
(a and bl; and in the Paleocene,
(continued
on the
the
regimes can be distingushed II-Ill). influenced shelf and slope deposits
of the Late Campanian-Maastrichtian St Anthony Formation and the Paleocene-Eocene Southern Galala Formation are the second environmental regime 111). The third regime is represented by the Maastrichtian Sudr Formation and the Paleocene-Eocene Dakhla, Tarawan and Esna Formations and Thebes Group reflecting basinal lithologies IIIIJ. The topographic base-map and the location of sections (with 0 and 01 refer due to non-exposure.
to Fig.
1. 0:
sections
with
stratigraphical
information;
0:
sections
with
no stratigraphical
information,
Journal of African Earth Sciences 247
C. SCHEIBNER et al.
*. . i
,:. :: :.; .3 :‘. I?.’ .,*..
LY: Figure 10. continued. Regional pala?ogeographic Paleocene, the calcareous nannoplankton biozones
248 Journal of African Earth Sciences
maps of 4 out of 11 time slices from the Maastrichtian-Early Eocene. ln the of NPI-NlO Id-g) were chosen. See p. 247 for legend and symbol explanations.
Maastrichtian-Early
Eocene litho-biostratigraph
y and palazogeograph y of the northern Gulf of Suez region
2s
2
a Figure
10.
continued.
Reglonal
palazogeographz
Paleocene, the calcareous nannoplankton biozones See p. 247 for legend and symbol explanations.
maps
of 4 out
of NPl-NPIO
of
11 time
slices
from
the
Ih and II; and in the Eocene,
Maastrichtian-Early NPIO-NPl2
Eocene.
4 and kl were
in the chosen.
Journal of African Earth Sciences 249
C. SCHEIBNER et al. that
may reflect
subaerial
exposures
NP7 (Fig. 10~)
or submarine
swells. At the western Gulf of Suez, these areas coincide with the Northern GalalaANadi Araba High. The stratigraphical range of the Northern Galala/ Wadi Araba hiatuses may reach Turonian-Early Paleocene
(Kuss and Leppig,
1989;
Abd-Elshafy
and
The early part of NPI is, similar to the late part of CC26, a time of non-deposition or erosion in the area of investigation (Strougo et al., 1992; Faris, 1997). The basin configuration of the Southern Galala Sub-basin is very similar to that of CC26. It encompasses the St
Atta, 1993). The eroded sediments derived from this area were mainly transported southward, where they were deposited as chalky limestones, marls and sandstones of the St Anthony Formation in the northern parts of the Southern Galala (St Anthony and Gebel Thelmet sections in Fig. 4a).
Paul area in the west to the west central Sinai in the east, but the prevailing lithologies changed in time. Instead of chalks of the Maastrichtian Sudr Formation, marls and shales of the Dakhla and DakhlaRarawan/Esna Formations were deposited in the Early Paleocene.
North
NP2 (Fig. IOdl
of the Northern
Galala/Wadi
Araba,
no sedi-
ments of the St Anthony Formation are present, only the deeper water chalks of the Sudr Formation
During
NP2 times,
Galala
Sub-basin)
(Wadi Nooz: this work;
Dakhla and Dakhlaflarawan/Esna
1996).
The Northern
isolated
island
sediments
Gebel Urn Makhasa: Galala/Wadi
surrounded
that interfinger
Formation.
of the Northern El-Askary
an
water
marly chalks
water
Sudr Formation
and
In addition
to the uplifted
area
GalalaNVadi
of non-deposition
formed
shallow
with chalks,
and marls of the deeper Dakhla
Araba by
Kulbrok,
Araba,
two
local areas
occur on Sinai (Wadi El-Esseila
and Shaaban,
1993)
the established with
Paul to the western figuration.
area)
of the from St
in the same con-
marls of the Dakhla Formation
in the Wadi Tarfa area. All other areas
in the northwest El-Orban
Formations
Sinai remains
Additionally,
were deposited
basin (Southern
the marls and shales
(NGWA) are still
and in the southeast exposed
or areas
(Ezz
of non-
deposition.
of
and in the south
of
NP3 (Fig. 1Oe)
the investigated area (Ezz El-Orban, Morgan 8 and HI of Masters, 1984). It is not clear, whether these two areas were truly exposed islands, local highs
In NP3, the two isolated basins, both parts of the Southern Galala Sub-basin with marls of the Dakhla Formation, were connected through the Bir Dakhl area.
with non-deposition erosion.
Similar to NP2, the Northern GalalaNVadi Araba and the Ezz El-Orban areas remain areas of non-deposition.
or only
the
result
of
later
distribution
is least clear within poor biostratigraphic calcareous (I 978a, were
of the depositional
data of Abdelmalik
197813) and Marzouk relied
upon.
do not offer a better A. mayaroensis
settings
this time slice because of the data. On western Sinai, the
nannoplankton
mainly
wer NP5 (Fig. 1Of)
NP4-lo
CC26 (Fig. 1Obl The regional
and Hussein
The planktic
biostratigraphic
Zone
covers
(1994)
GalalaANadi
Araba in the Wadi Nooz area (this work)
marly sediments Esna Formations
part
as the
of CC25,
Upper NPS-lo wer NP7/8 During
this interval,
and the index fossil A. mayaroensis is very rare in southern Egypt (Luger et al., 1998). In most sec-
Southern
tions
progradation,
time
in this area, interval
to the
ranging
Early
deposition
as well
Paeocene
and/or
from
as in most the upper
is probably
exposure.
of Egypt,
the
part of CC26 a time
During the latest
trichtian, chalks, marly chalks deeper water Sudr and Dakhla
and marls Formations
of non-
(FQ. 1Og)
shallow
Galala Formation
water
prograded
deposits
of the
(Scheibner et a/. ,
2000). Slumps and debris flows evidence the south-ward extending
starting
towards
and progressing
from
the
Southern
Galala,
the south to the area of Bir Dakhl
towards
the north to the area of Wadi
Maas-
Nooz. This ramp progradation
of the were
sea level drop at the base of P4 (within NP5), as Scheibner et al. (2000) demonstrated in the area of St Paul (area 3) and Liining et al. (I 998a) on Sinai.
deposited within a basin that extends from the St Paul/Bir Dakhl area in the west to the west central Sinai in the east (e.g. St Paul area: see this work; Wadi El-Seig/Hialla: Abbass et a/., 1994; Matulla and Nuhkl: Marzouk and Hussein, 1994). It is not clear whether the shallow water sediments of the St Anthony Formation were deposited in the Southern Galala or not.
250 Journal of African Earth Soences
of the Dakhla and Dakhla/Tarawan/ prevail.
foraminifers
solution,
also
et a/.
The configuration of the Southern Galala Sub-basin remains the same. Additionally, north of the Northern
was initiated
by a main
Speijer and Schmitz (I 998) reconstructed a palaeodepth curve of that interval based on studies of benthic foraminifers from Gebel Aweina (ca 300 km to the south). These authors also concluded that a sea level drop occurred during lower P4. In the Southern Galala Sub-basin, the marls and shales of the Dakhla or Dakhla/Tarawan/Esna Formations were deposited.
Maastrichtian-Early
Eocene litho-biostratigraphy
Upper NP 7/84ower During
these
andpalieogeography
include chalks of the Sudr Formation
NP9 (Fig. 7Oh)
biozones,
the chalks
of the Tarawan
Formation were deposited in the south and east of the Northern Galala/Wadi Araba, although on Sinai, the Tarawan Formation is very thin or even missing. Here, the many sediments of the Dakhla/Tarawan/ Esna Formation were deposited. The shallow water sediments of the Southern Galala Formation were deposited now on parts of the Northern Galala, and in the south (Ras Gharib) the area of non-deposition becomes smaller. Anan (1992) and Lining et al. (1998a)
concluded
that the Tarawan
Sinai was deposited
of the northern Gulf of Suez region
Formation
on
during a series of low sea levels.
tian, shaley-marly
sediments
Dakhla/Tarawan/Esna informal formation), Tarawan Formation
in the Maastrich-
of the Dakhla,
Formations
Esna and
(a newly introduced
and chalks and limestones of the in the Paleocene to Early Eocene.
The basinal sediments of the Sudr, Dakhla and Esna Formations interfinger near the structural high of the Northern Galala/Wadi Araba High. This high was subaerially exposed during the Late Cretaceous to Early Eocene. The shallow water slope deposits of the St Anthony and Southern Galala Formations were deposited south of this high, whereas north of the high only the sediments of the Southern Galala Formation
Luger (1985) and Speijer and Schmitz (I 998), on the other hand, reported from southern Egypt that the
came to deposition. Other local highs
sediments
during sea level highstands.
erosion are present on northwest Sinai. In particular, the high around
Upper NP 9-/o wer NP 70 (Fig. 7Oil
indicate that the boundary between the stable unstable shelf on the Sinai lies farther south.
of the Tarawan
The basin configuration
Formation
were deposited
of the Southern
Galala Sub-
basin stays the same, but the lithological character changes again. Now, the marls and shales of the Esna and
the
Dakhla/Tarawan/Esna
deposited.
North of the Northern
the sediments
of the Southern
Formations
were
Galala/Wadi
Araba,
Galala Formation
as far east as Gebel Urn Makhasa
(Kulbrok,
that
led to non-deposition
or
and southwest Ras Gharib could and
Four different types of hiatuses could be distinguished, characterised by varying duration and/or different mechanisms (e.g. sea level changes). At least the palaeogeographical change within calcareous nannozone
NP5 resulted
from a main sea level drop.
reach 1996). ACKNOWLEDGEMENTS
Upper NP IO-lower During this interval, Formation
dominate
Wadi Araba.
of the Southern
the areas of the Northern
The only
the northwestern
1996;
1992).
Galala Galala/
area of non-deposition
Sinai (Wadi Sudr: Gietl,
Sudr: Kulbrok, Zalat,
NP7 I (Fig. 1Oj) sediments
Mitla
Pass: Abdel
For the first
time,
is on
1998;
Ain
Gawad
and
sediments
of the
Dakhla and Dakhla/Tarawan/Esna Formations were deposited in the area of Ras Gharib, which could be part of a basin
Said (1990)
described
in the Early
Eocene around Abu Zenima. UpperNP
1 l-NP12
The difference the deposition
of the limestones
in the Southern and shales Formations. suggested during
(Fig. 1Ok)
from this to the previous
time slice is
of the Thebes Group
Galala Sub-basin
instead
of the marls
Shahin that
(1990)
Palaeogeographic
Group
was
deposited
sea level.
changes
with sample preparation. The investigations were funded by the Graduiertenkolleg ‘Stoff-F&se in marinen Geosystemen’ of the University of Bremen and the German Science Foundation (DFG). Editorial handling -P. Bo wden
regimes:
basinal
sediments;
H.L.
El-Dawy,
trichtian-Early Central Sinar
in the Maas-
in the surrounding
Gulf of Suez based on three environ-
and non-deposition.
REFERENCES Abbass,
M.M.,
platform
slope
The basinal sediments
Dakrory,
A.M.,
1994.
Eocene benthonrc foraminifera from and their importance to stratigraphy
paleoecology. Bulletin 23 (2F), 1 l-35.
are evident
to Early Eocene deposits
of the northern mental
for his help with all the problems the authors
and Ltining et a/. (1998a)
the Thebes
CONCLUSIONS
sediments;
is thanked
encountered during their stays in Egypt. R.P. Speijer, University of Bremen, helped with planktic foraminifers. R.P. Speijer and A.M. Morsi are also thanked for comments on a previous version of this paper. The manuscript benefited much from the thorough revision of S. Liining, LASMO, London. A. Scharf, R. Batzel and M. Brinkmann, University of Bremen, helped
of the Esna and Dakhla/Tarawan/Esna
a time of a lowered
trichtian
A.M. Bassiouni, Ain Shams University, is especially thanked for much logistic support and discussion of the stratigraphy. A.M. Morsi, Ain Shams University,
Faculty
Sctence,
Assiut
MaasWest and
Unrversity
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A.M., Sharkawi, of Mersa Thelmet
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Bulletrn
M.A.E., Marzouk, A., 1970. area, southern Galala, Eastern
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Science,
Cairo
Universrty
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Cretaceous,
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related
sedrments
the
Gulf
of
Ain
Shams
Suez,
Egypt.
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Mrddle
University,
Earth
Stratrgraphy
wrth East
regronal
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side
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Ouda,
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Serra-Keel, J., Hottinger, L., Caus, E., Drobne, K., Ferrandez, C., Jauhri, A.K., Less, G., Pavlovec, Ft., Pignatti, J., Samso, J.M., Schaub, H., Srrel, E., Strougo, A., Tambareau, Y., Tosquella, J., Zakrevskaya, E., 1998. Larger foramrnrferal btostratigraphy of the Tethyan Paleocene and Eocene. Bulletin Socrety Geologre France 169, 281-299. Shafik, S., Stradner, H., 1971. Nannofossrls from the Eastern Desert, Egypt with reference to Maastrichtian Nannofossils from the USSR. Jahrbuch Geologrsche Bundesanstalt SB17, 69-99. Shahrn, A., 1990. Late Cretaceous-Early Tertiary agglutinated benthic foramrnifera and their paleoecology in the Gebel Ekma succession, southwestern Smar, Egypt. Neues Jahrbuch Geologre Palaontologre, Abhandlungen 1990, 493-512. Shahin, A., 1992. Contrrbutron to the foraminiferal biostratrgraphy and paleobathymetry of the late Cretaceous and early Tertiary in the western Central Smar, Egypt. Revue Mrcropaleontologie 35, 157-l 75. Snavely, P.D., Garrison, R.E., Meguid, A.A.A., 1979. Stratigraphy and regional depositional history of the Thebes Formatron (Lower Eocene), Egypt. Annals Geological Survey Egypt 9, 344-362. Sperjer, R.P., Schmrtz, B., 1998. A benthic forammrferal record of Paleocene sea level and trophrc/redox conditrons at Gebel Aweina, Egypt. Palzeogeography, Pala?oclimatology, Palaaoecology 137, 79- 101.
Speijer, R.P., Schmitz, 8.. Luger, P., 2000. Stratigraphy of late Palaeocene events m the Middle East: Implications for low-to middle-latitude successions and correlations. Journal Geological Society, London 157, 37-47. Strougo, A., 1986. The Velascoensis Event: A significant episode of tectonic activity in the Egyptian Paleogene. Neues Jahrbuch Geologie Pallontologie, Abhandlungen 173, 253-269. Strougo, A., Haggag, M.A.Y., Luterbacher, H., 1992. The basal Paleocene ‘Globigerina’ eugubrna zone in the Eastern Desert (St. Paul’s Monastery, South Galala), Egypt. Neues Jahrbuch Geologre Pallontologie, Abhandlungen 1992, 97-l 01. Strougo, A., Faris, M., 1993. Paleocene-Eocene stratigraphy of Wad1 El Dakhl, Southern Galala plateou. Middle East Research Center, Ain Shams University, Earth Science Services 7, 49-62. Tantawy, A.A., Ouda, K., von Salis, K., El-Dtn, M.S., 2000. Biostratigraphy of Paleocene section in Egypt. GFF 122, 163-165. Youssef, M.I., Shinnawi, M.A., 1954. Upper Cretaceous rocks of Wadi Sudr, Western Sinai. Bulletin lnstrtute Desert Cairo 4, 94- 11 1. Zittel, K.A., 1883. Beitrlge zur Geologre und Palaeontologie der Lybischen Wuste und der angrenzenden Gebrete von Agypten. Paleontographrca 30, 1 - 147.
Journal of African Earth Sciences 255
of Almacan Earth Soences,
Pergamon Pll:S0889-8382(00)00038-7
Vol
32,
No
2. PP. 223-255. 2001 Elsewer Science Lfd All rights reserved. Prmted I” Great Brlta~n 0899.5362101 S- see front matter
o 2001
Maastrichtian-Early Eocene litho-biostratigraphy and palaeogeography of the northern Gulf of Suez region, Egypt C. SCHEIBNER’,*, A.M. MARZOUK2 and J. KUSS’ ‘UniversitM Bremen, FB5, PO Box 330440, 28334 Bremen 2Geology Department, Faculty of Science, Tanta University, Tanta 31527,
Egypt
ABSTRACT-The Maastrichtian-Lower Eocene sediments on both sides of the northern Gulf of Suez can be subdivided into eight formal formations (including one group) and one informal formation that are described in detail. These lithostratigraphic units reflect three different environmental regimes of deposition or non-deposition. The first regime is characterised by uplift and erosion or non-deposition resulting mostly from the uplift of the Northern Galalal Wadi Araba structure, a branch of the Syrian Arc Foldbelt. The shallow water carbonate platform and slope deposits of the Late Campanian-Maastrichtian St Anthony Formation and the Paleocene-Lower Eocene Southern Galala and Garra Formations represent the second regime and are found north and south of the Northern Galala/Wadi Araba High. The third regime is represented by basinal chalks, marls and shales of the Maastrichtian Sudr Formation and of the Paleocene-Eocene Dakhla, Tarawan and Esna Formations, the Dakhla/Tarawan/ Esna informal formation and the Thebes Group. The distribution and lateral interfingering of the above mentioned environmental regimes reflect different vertical movements, changing basin morphology, sea level changes and progradation of shallow water sediments and is illustrated on 11 palaeogeographic maps. o 2001 Elsevier Science Limited. All rights reserved. RESUME-Les sediments du Maastrichtien et Eocene inferieur, affleurant de part et d’autre au nord du Golfe de Suez, peuvent dtre subdivises en huit unites bien definies (incluant un groupe) et une unite plus informelle qui sont d&rites en detail. Ces unites lithostratigraphiques temoignent de trois environnements sedimentaires differents. Le premier est caracterise par une surrection et une erosion ou une absence de depots qui resulte pour I’essentiel de la surrection de la structure du Northern Galala/Wadi Arabia, une branche de la ceinture plissee de I’arc Syrien. Un environnement de plateforme carbonatee peu profond, avec des depots de pentes, correspondant a la formation de St Anthony du Campanien superieur-Maastrichtien, et aux formations Paleocene-Eocene inferieur du Southern Galala et du Garra, represente le second regime de depot; il est observe au Nord et au Sud du Northern Galala/Wadi Arabia High. Le troisieme regime est constitue par des craies de bassin, des marnes et des shales de la formation maastrichtienne de Sudr, des formations Paleocene-Eocene de Dakla, Tarawan et Esna, la formation informelle de Dakla/Tarawan/Esna et le groupe Thebes. La distribution des milieux de depots precedents et leurs passages lateraux, temoignent de mouvements verticaux, de variations de la morphologie des bassins et du niveau marin, et de la progradation de sediments d’eaux peu profondes. Ils sont illustres par 11 cartes paleogeographiques. o 2001 Elsevier Science Limited. All rights reserved. (Received 27/l /OO: accepted 20/2/01)
*Corresponding author [email protected],
[email protected]
Journal of African Earth Sciences 223
C. SCHEIBNER et al. INTRODUCTION During the last decades, many authors investigated the stratigraphic subdivision of the Upper CretaceousPalaeogene strata in the Galala Mountains and west central Sinai (Fig. I). Most of these studies were focused on the bio- and lithostratigraphical interpretation of isolated sections. Only a few authors, such as Masters (I 984) and Said (I 9901, concentrated on regional comparisons. In this work, the stratigraphic results from the Galala Mountains and neighbouring areas are combined with literature data from numerous isolated sections (especially in west central Sinai). The authors concentrated on questions of lateral facies transitions and their stratigraphical synchroneity or diachroneity. Special emphasis is put on the interfingering of shallow water limestones over swells and tectonically induced uplifts, and basinal marls and shales. The results of the facies investigation, in combination with the different types of hiatuses observed in the area, led to a detailed palaaogeography of the Maastrichtian to Early Eocene that is documented in 11 maps.
GEOLOGICAL SETTING The investigated area represents a segment of the northern passive margin of the Afro-Arabian Plate. This passive margin formed during the Late Triassic/ Jurassic opening of the Neotethys. The extensional tectonic processes resulted in the formation of eastwest-striking northward-deepening half-grabens that were mostly covered by the Late Triassic-Early Cretaceous seas, depending on, among others, sea level fluctuations. Beginning with the initial stages of the collision between the African and European Plates during Turonian times, a dextral transpressive reactivating of the half-grabens took place along the North African-Arabian Plate boundary (e.g. Moustafa and Khalil, 1995). As a consequence, a system of inverted, uplifted and folded grabens was formed along the Syrian Arc System (Fig. I). This area is also known in Egypt as the ‘unstable shelf’ (Krenkel, 1925; Said, 1960). It contrasts with the tectonically unaffected area further south (‘stable shelf’). While the latter is characterised by lithologically uniform marine strata, formed on a gently north-dipping shelf, small-scaled facies variations are obvious within the basin-swellmorphologies of the unstable shelf area (Kuss et al., 2000). The Galala Mountains in the Eastern Desert, together with areas in western Sinai, represent a southern branch of the Syrian Arc called the Northern Galala/Wadi Araba (NGWA) High (Kuss et a/., 2000) (Fig. 2). The Upper Cretaceous-Palaaogene carbonate dominated successions of a south- and north-dipping carbonate ramp prograde from the Northern Galala/
Wadi Araba High. Facies transitions between the Paleocene shallow water ramp carbonates and deeper water intrashelf marls of the Southern Galala Subbasin (Fig. 2) farther south have been studied in sections along the dip direction. Mass transport deposits like slides, slumps and debris flows occur (Scheibner et al., 2000).
METHODS The study area is exposed around the northern parts of the Gulf of Suez. Eight Upper Cretaceous-Palaeogene sections of the Northern and Southern Galala on the western side of the Gulf of Suez were investigated in detail (Fig. 31, including the northern and southern forelands of the Galalas. Additionally, data of west central Sinai, opposite to the working area, was reviewed. Facies interpretations are based on fine-scale logging of stratigraphic sections in and along the Northern Galala/Wadi Araba High. Studies of 169 thin sections of the Maastrichtian-Early Eocene interval are supplemented by 479 marl samples that formed the base for a high-resolution biostratigraphic frame based on planktic and benthic foraminifers and calcareous nannoplankton.
BIOSTRATIGRAPHY For the Maastrichtian, the biostratigraphic scheme given by Perch-Nielsen (1985) and Norris et al. (I 998) (Fig. 4) was followed. The biostratigraphic schemes of Berggren et a/. (I 995) for planktic foraminifers (Pzones), of Martini (I 971) for calcareous nannolankton (NP-zones) and of Serra-Kiel et a/. (I 998) for shallow benthic foraminifers (SB-zones) are used for the Paleocene and Early Eocene. The calibration of planktic foraminifers and calcareous nannoplankton is from Norris et al. (I 998) for the Cretaceous and from Berggren et al. [I 995) for the Palaeogene (Fig. 4). In section T2 (Fig. 4a), NPI 0 could be divided into four sub-zones, named NPI Oa, NPI Ob, NPl Oc and NPI Cd, following Aubry (I 995). In sections Tl, D2 and D3 (Fig. 4a), NPI 0 can only be subdivided into two subzones (NPI Oa-c and NPl Od) because T. digtiabs could not be found. Faris and Strougo (I 998) and Aubry et a/. (I 999) also used this subdivision in their description of the Esna Shales of Egypt. In addition to Berggren et a/. (I 9951, Speijer et al. (2000) was followed in subdividing the planktic foraminiferal biozone P5 into P5a, P5b and P5c. The very short sub-zone P5b is characterised by the total range of M. allisonensis marking the Late Paleocene thermal maximum. All sections presented in Fig. 4 were recalibrated to the above mentioned schemes. If planktic foraminifers,
Maastrichtian-Early
Eocene litho-biostratigraph
AREA 1
I.
AREA 2
AREA 3
7. The two (see inset).
Galala Plateaus at the western Gulf 1: Palmyrid Fold Belt; 2: Negev-Sinai
5: Bahariya Uplift/Western transitions IT-zoneJ were figure),
AREA 4
T-z
. . . .SGS . .>,
Figure Desert
y and pakogeograph
the boundanes
Desert. During formed roughly
of areas
1-6
y of the northern Gulf of Suez region
AREA 5
1 AREA 6
( NGWA 1 of Suez forming part of a Syrian Arc Fold in the Eastern Fold; 3: Northern Galala/Wadi Araba High; 4: Abu Roash;
Late Cretaceous-Palmogene times, the platform (NGWAI parallel with the strike of the Galalas. In transect A-B
to basin ISGSI (bottom of the
are indicated.
Journal of African Earth Sciences 225
C. SCHEIBNER et al.
Figure
2.
Latest
Maastrichtian
pakeogeographic
map
of the circum-tethyan
The area of investigation is around the Northern Galala/Wadi south. The Southern Galala Sub-basin is part of the Eastern
as well
as calcareous
bio-stratigraphy. given used
nannofossils,
The calcareous
were
used for
nannoplankton
priority. The biostratigraphic scheme (planktic foraminifers or calcareous
plankton)
is indicated
which is nanno-
in the figures.
Luger et al. (I 998) foraminiferal biozonation areas in which
was
presented a new for the Maastrichtian
the Late Maastrichtian
planktic for those
index fossil A.
mayaroensis is very rare or absent. Marzouk and Ltining (1998) described a strong variability of planktic foraminifers
and calcareous
nannoplankton
correlations
realm
(modified
after
Araba and reaches to the Southern Desert lntrashelf Basin.
Camoin Galala
et al., 19931.
Sub-basin
in the
(1883) (Fig. 51, the lithostratigraphic subdivision of the Upper Cretaceous-Eocene successions in Egypt has been the subject
of many discussions,
especially
during the 195Os-1960s
(Nakkady,
Naggar, 1966a, 1966b, today, lithostratigraphic
1968; Sabry 1968). Even terminology is used non-
uniformly Formation terminology,
(Issawi
et a/., 1999),
especially
(Herrnina and Lindenberg, the authors used Hermina
as a basis, especially stratigraphic
1950,
with
subdivision.
respect
1957;
El-
the Esna
1989). For era/. (I 989)
to usage of litho-
In accordance
with recom-
on Sinai, especially in the lower Paleocene, whereas in the upper Paleocene the different zonal correlations are
mendations (Salvador,
in good agreement.
units by a geographic term combined with a unit term instead of a geographic term combined with a litho-
El-Dawoody
Boukhary and Abdelmalik
(1992) reviewed
Late Paleocene-Eocene
succession
LITHOSTRATIGRAPHY
(1983) and
the biostratigraphy
of the
in Egypt.
OF MAASTRICHTIAN-
EARLY EOCENE STRATA Ever since the first description of the Maastrichtian to Eocene sediments in the Western Desert by Zittel
226
Journal of African Earth Sciences
of the International Stratigraphic Guide 19941, they describe lithostratigraphic
logical term to allow for lithological variability (e.g. Esna Formation instead of Esna Shale, as has been used frequently in the past). In the following paragraph, commonly used formations
a short summary of the and their regional dis-
tribution of the Upper Cretaceous-Palasogene lithostratigraphic units for northern Egypt and Sinai is given,
Maastrichtian-Early
Figure 3. Section
Eocene litho-biostratigraph
map of the northern
y and pakogeograph
part of the Gulf of Suez.
y of the northern Gulf of Suez region
The nine rectangles
represent
depositional history. The sections in areas 1-6, on the western side of the Gulf of Suez are based on new and literature data; whereas the sections of areas 7-9, on the eastern Suez
including
(Sinai),
some
are based
additional
on literature
suggestions
data
to Lower
(Fig. 5). A
Eocene sediments
Western Desert 51, the following
(Farafra, Dakhla lithostratigraphic
bottom
Overwegi
to top:
layers;
in the
and Kharga) (Fig. units occur from ash-grey
of different
only.
detailed historical overview can be found in El-Naggar (1966a, 1966b) and lssawi (1972). According to the description of Zittel (I 883) of the Upper Cretaceous
areas
(Galala Mountains), side of the Gulf of
shales
(‘aschgraue
Blatterthone’);
snow-white
layered
lime-
stone or chalk with Ananchytes ovata; green shales (‘grtinliche Blatterthone’); and Operculina limestone (Unterlibysche Stufe). Near Esna, Zittel (18831, miscorrelated the green shales underlying the Operculina limestone Western fusion
with
the Danian
‘ash-grey
shales’
Desert. With this miscorrelation, of
lithostratigraphic
terminology
of the
a long constarted.
Journal of African Earth Sciences 227
Section, author and area g
3r
cy
Tim
P
(Ma.
*
50
zone mneta
%95)
P8 P7
7
b P6
-
-
a
P5 -
:k a C
-_EF
s
11
zi -_ ---DF ----
P4 a iT P3
'HG-
+I - -iF -- -
55 .
SO -
THG
a
0 2 --DF---
r
i
C
?
-
Pl
n.e.
b 3
B&P 6
-
Northern Galala
a
PZOM
Td Ibathom.
mayaro. Uacami. ~cticosa Gans. yanaseri
+ -
Planktonic foraminifera data Nannoplanktondata
+ .
+ +
+ +
+ + + + l&L + -
Formations: THG EF SGF TF GF DF DTE SAF SF
sectrons Eocene
The biostratigraphy taken from kterature.
boundary.
+ .
+ -
+ _
+ +
Lithologies:
Thebes Group Esna Formation Southern Galala Formation Tarawan Formation Garra Formation Dakhla Formation DakhWTarawaMEsna Formation St. Anthony Formation Sudr Formation
Figure 4.
;_
0
cherl I--_-I
hiatus
shale
, I ,
I[
sandstone
LCI
debris flow
[fl
chalk
slides
1 ,‘/I
dolomite
I22
limestone
and lithology of newly measured Maastrichtian-Palseogene secttons, including The broad grey band reflects the current opinion on the position of the Paleocene-
The biozonations
of planktonic
forammifers
fP zones),
calcareous
nannoplankton
INP zones
for
Palsaogene and CC zones for Maastrtchttanl and shallow benthic forammifers LS6.Z~ are listed. In the Maastrichtian, the first and last occurences of calcareous nannoplankton index forms are Indicated. The drfferent biozonal schemes used are indicated with + lusedl and (not used). Other biozonal schemes such as shallow benthic forammifers, macrofossils and ammonites are rarely used here and are not listed. The black areas indicate hiatuses, due to erosion or non-deposmon. Question marks indicate uncertain stratigraphical ranges. (a) Sections of areas together
7-6, wtth
on the western side of the Gulf of Suez sections from literature.
(Galala
Mountamsl,
are mostly
newly
measured
sections
Figure 4. continued. including secttons Paleocene-Eocene
The btostratigraphy
and lithology
of newly
taken from kterature. The broad grey band boundary. The biozonanons of planktomc
measured
Maastrichtian-Palaaogene
INP zones for Palaaogene and CC zones for Maastnchttanl and shallow benthtc the Maastnchtian, the hrst and last occurences of calcareous nannoplankton different shallow areas
secttons,
reflects the current opinion on the position of the forammifers (P zones), calcareous nannoplankton foraminifers index forms
fSBZ) are listed. In are indtcated. The
biozonal schemes used are indicated with + fused) and (not used). Other biozonal schemes such as benthic foramtntfers, macrofosstls and ammonites are rarely used here and are not Itsted. The black
mdtcate
hiatuses,
ranges. lbl Sections of Unfortunately, It IS not section. Because of the 119921 belongs to area
due
to erosion
or non-deposnion.
Question
marks
indicate
uncertain
strattgraphical
areas 7-9, on the eastern side of the Gulf of Suez (Sinail, are entirely from ltterature. clear from which part of Gebel Qabeliat Marzouk and Abou-El-Enein (19971 took their htatus, thts section was attributed to area 8, whereas section Gebel Qabeliat of lsmail 7.
C. SCHEIBNER et al.
I-
Formstions in the Western Desert l--
Zlltd,
IBeadnell,
1905
1888 western
-
ium
*M
1961 1911 vestefl routhem Egypt
southern Egypt
Awadand Gob&l, 1866 southern
Harmin * 81., 1989
El Wv, l@S%a western
southern
Egypt
Egypt
l-
a
!!
Thebes
Y presian
Thebes
:hebes
w
grijnlichs Blatterthone
-
isna Shales Passage B&S
Chalk
, ____( Danian
aschgraue ) BWterthone
k! 6 j
-i!
Upper Esna Chalk
Danian Shales
Lower Esna
i
Formations in the Eastern DesertBinai
Sinai
S. Galala zaafarana
AbdHermina et al., ildmfy, 19( 1 1088 r4. Eastern Sinai r( ; Galalc!_ Desert
S. Galala -S-N-
thimwork N. Eastem _N_
.S_
Serai
Sinai
Desert
Thebes
Thebes
I
Naot Esna
Esna
> Brawan-_ -?/--Esna
1
I
Dahklal Tarawanl Esna
Dakhla
Sudr
Esna
II Maastrichtian Shareb
Gebel Thelmet
Figure
5. Lithostratrgraphtcal
schemes
Sudr Gebel Thelme in the
Western
St. Paul
Desert
and in the Eastern
Desert/Sinai.
Today,
Sudr
in southern
Egypt,
the
lithological subdivison of Said 11961) is accepted. in northern Egypt, this subdivision is not applicable due to the thin or even absent Tarawan Formation (TF). Most authors ignore that fact and just expand the Esna Formation down to the Maastrichtian, but this leads to misinterpretations. SAF: St Anthony Formation; SGF:
230 Journal
of African
Earth Sciences
Therefore, rn this study, Southern Galala Formation.
the informal
Dahkla/Tarawan/Esna
Formation
was
Introduced.
Maastrichtian-Early Beadnell
(1905)
Eocene litho-biostratigraph
described,
y and palzeogeograph y of the northern Gulf of Suez region
for the first time, an ‘Esna
Shale’ unit above the chalk (Tarawan)
and the Danian
shales as passage beds between the Cretaceous the Eocene. Hume (1912) mentioned the Lower
and and
the Upper Esna Shales below and above the chalk (Tarawan), respectively. Later, Said (1961) introduced the Dakhla Shale as a new formation, replacing the Danian shales of Beadnell (1905) and the Lower Esna of Hume (1912). The chalk between the Dakhla and Esna Formations was named the Tarawan Chalk by Awad and Ghobrial (1965). Since then, the terms Dakhla Formation (DF), Tarawan Formation (TF) and Esna Formation (EF) have been generally accepted for the lithostratigraphic (Hermina 1966b)
subdivision
introduced
Middle
in southern
and Lindenberg, Oweina
the Tertiary Formations,
the terms
Chalk
and western
1989).
El-Naggar
Lower
and Upper
Oweina
Oweina
Egypt
(1966a, Shale,
Shale for
part of the Dakhla, Tarawan and Esna but this lithostratigraphic scheme found
little acceptance The subdivision
in the scientific community. of Awad and Ghobrial (1965)
not be applied to the Late Cretaceous-Palaaogene of northern Tarawan Although
Egypt
and Sinai, however,
can-
to Early Eocene
from
referred
to as Esna Formation
Formation
Paleocene
(e.g. Bartov
together
because
and Steinitz,
of their
logical similarities. from Maastrichtian located
Desert
9) (Fig. 4b). The transition Thebes
Sudr Formation,
and underlies the Lower
Eocene limestone (Thebes).” a stratigraphic miscorrelation
This usage has lead to of the Esna Formation
certain.
All sections
studied
stratigraphical the various
correlations lithologies
Therefore,
the authors
Esna Formation unit for Upper
as the latest
Ltining et al., 1998a).
propose
the Dakhla/Tarawan/
(DTE) as an informal Maastrichtian-Lower
lithostratigraphic Eocene
shales
Sudr Formation
(Lower
range:
The contact
Formation
usually
coincides
latest Maastrichtian 4a, b).
however,
the Maastrichtian-Eocene
sions were also subdivided
according
succes-
to the schemes
for southern Israel. There, the synonyms for the Sudr, Tarawan and Esna Formations and Thebes Group are Ghareb Formation, Hafir Member, Taqiye Formation and Mor Formation (Bartov and Steinitz, 1977; Romein, 1979; Benjamini, 1992), the chalky Tarawan Formation
respectively. Where (Hafir Member) is
missing on Sinai, the entire shaley to marly formation,
time,
are given
distribution
of
pala.?ogeographic
Ghorab
(1961);
for 11
Wadi Sudr
Campanian-Maastrichtian
of the Sudr Formation
Dakhla
tiated
Sinai,
the changing
Paleocene?)
boundary,
The Dakhla, Tarawan and Esna Formations and their earlier denotations are widely used in Egypt. On
and litho-
of most sections
(SF) (Figs 4a. b and 7c. e)
and marls in those parts of northern Egypt and Sinai where the Tarawan Formation cannot be differen(Fig. 5).
literature)
maps of the investigated area are presented Maastrichtian to Early Eocene time slices.
Stratigraphical
as early
(and additional
with
ern Egypt
(e.g. Said, 1990;
area is not
1, the biostratigraphical
Author and type section: (west central Sinai)
and Sinai it starts
(SGF) to the deeper
a subject of the study. Therefore, the attribution of these sediments to one or the other formation is less
that ranges in southern and western Egypt only from Upper Paleocene to Lower Eocene, whereas in northMaastrichtian
(area 6)
side of the Gulf
Group (THG) in the working
in Fig. 4a, b. To illustrate
the Esna Formation which overlies the Maastrichtian-
of the Gulf of
of the Early Eocene shallow
Galala Formation
Paleocene
Paleocene
west
of Suez (west central Sinai), the areas 7-9 are also orientated from the south (area 7) to the north (area
water
Wadi Qena and on Sinai b y
and litho-
(area I) to north
(Figs 1, 3, 4a and 6). On the eastern
are listed in Table
in northern
1977).
stratigraphical
from south
mation, they mentioned that “the upperpart of the Dakhla, the Tarawan and the Esna which range from represented
is
The stratigraphic intervals range to Lower Eocene. Areas 1-6 are
in the Eastern
Suez, oriented
the
to Early Eocene age in southern Egypt are
times
1-6) and east (areas 7-9) of the Gulf of Suez (Fig. 3). The sections within the single areas are grouped
Southern
age to the Esna For-
Eocene
(Said, 1990) or Taqiye
Discussed below are the eight formal formations (including one group) and one informal formation and their distributions within the nine areas west (areas
water
because
to Early
FORMATIONS AND THEIR DISTRIBUTION WITHIN THE STUDY AREA
strata
Formation is partly absent or very thin. Hermina and Lindenberg (1989) attributed a
Late Paleocene
ranging
is either with
sharp,
to the overlying in which
or is more gradual,
7, 8) the Sudr Formation
in which
terminates
biozone
or CC26
Massive
limestone
beds with thin intercalations shales
white
case (areas 2, within
CC25
Liihology: calcareous
case it
the Cretaceous/Palasogene late or (Fig.
and cream chalk and chalky
and argillaceous
of light grey
crystalline
lime-
stones. The Sudr Formation was studied in areas 1, 2 and 3 (sections Tl , D2,D3 and Sl-9) where it is composed of alternating beds of white chalk (up to 1.20 m) and thin grey marls (up to 0.10 m). In St Paul (area 3), a 1.3 m thick shaley unit is intercalated in the upper part of biozone CC25c, for transitional beds on Sinai.
which is also typical
Journal of African Earth Sciences 23 1
1 Nadi Tarfa
Area
2 Bir Dahkl
THG THG
1-S-
-N-
Eastern Desert
4 6 5 8 St. Anthony1 i. Not-then J. Northern Bas ihari Abu Zanimal jebel Thelme Galala Galaia b Wadi Feiran
3 St.Paul
THG
THG
-N-
Western Sinai
T
T
I
9 NW. Sinai
THG THG
THG
THG
THG
;GF
b
EF
I
EF
EF
SGF
SGF
TF
EF
I
SGF SGF
SGF
DF DF DF
3 t
SF
3
SF
DF
SF
r” :ormations: THG !F SGF
Thebes Group Esna Formation Southern Galala Formation
Figure 6. Distribution deposition.
In area
of the rock
units
TF GF DF
and age of formations 9, on northwestern
within
Tarawan Formation Gana Formation Dakhla Formation
in the nine investigated
Sinai,
the stratigraphical
The black
is uncertain
units are hiatuses because
Profile/Location
Coordinates exact locatron
Kassab and Keheila,
1994
WTSlWadr
Tarfa
wrthout exact locatron
Kassab and Keheila,
1994
140 km east of El Sherkh fad1
El-Dawy,
1999 1999
SlWadr Hawashiya
151 km east of El Sherkh fad1
El-Dawy,
Tl /Wad1 Hawashiya
N28’13.52’;
E32O13,64’
Thus work
T2lWadi
N28”27,31
‘, E32”13,73’
This work
Tarfa
Nrshi et al ., 1994
Sectron 11 /Wad1 Tarfa
wrthout exact locatron
Sectron U/Wadi
wrthout exact location
Bandel et al ., 1987
Wadi Tarfa
without
Tantawy
DB/Brr Dakhl
N28’36.43
‘; E32=‘23,77
D2/8rr
N28’39.61
‘; E32O23.59’
Dakhl
ranges
Author
wrthout
Dakhl
or non-
stratigraphical
or taken from literature
Hawashiya
WDiWadr
due to erosion
of varying
WHSlWadi
O/Wad1 Hawashrya
2
areas. range
DakhlalTarawanlEsna Formation St. Anthony Formation Sudr Formation
this area.
Table 1. Sections that were newly measured Area 1
DTE SAF SF
Tarfa
exact locatron
wrthout exact
locatron
Abu Rimth l-3
N28O43 ‘; E32O.30
Brr Dakhl
without
If coordmates are grven m the Irterature, geographical pomts, but rather geographical
’
exact location
’
et al ., 2000
This work This work Strougo and Faris, 1993 Gretl, 1998 Metwally
then they are mentroned here. ranges given by the authors.
and Abd El Azeam, Coordmates
wrth
1997 a star
do not
indicate
1
Table 1. continued.
3
SSISt.
N28°50.37’;
Paul
Sl -S8/St.
Author
Coordinates
Profile/Location
Area
E32”31,53’
N28O50.72’;
Paul
St. Paul
N28O50.63
St. Paul
N28O50.63’;
St. Paul
wrthout
Scherbner
E32O31,29’ ‘; E32O32.62
’
E32’32.62’
2000
et a I., 2000
Strougo
et al ., 1992
Haggag
(1991)
lsmail and Abdallah,
exact locatton
Mazhar
4
,
Kuss et al
’
et a/.,
Kuss. 1987,
Grrgrs, 1987;
Faris, 1997:
Kulbrok,
N28O56.72’;
E32O25.14’
without
exact location
Selrma and Askalany,
St. Anthony
wrthout
exact
Zrttel,
1883;
1986;
Bandel and Kuss, 1987:
1989;
Malchus,
Thelmet
location
20/2/S
North Galala
ADlAbu
Darag
Camp/S
North Galala
Several/S
North Galala
wrthout
exact locatron
Abdel-Krreem
without
exact location
Hottrnger,
Awad
1998
this work
1996
1990;
Kuss et al.
and Abdou.
1960;
1979;
wrthout
exact location
Abd-Elazeam
without
exact locatron
Gretl, 1998
wrthout
exact locatron
Abd-ElshafY
2000
1971;
Abdallah Mazhar
1996
Kuss and Lepprg, 1989:
Thus work
,
et a/ ., 1970;
Abdel-Krreem,
Kulbrok,
Kuss,
1979
Abdallah
exact locatron
E32’11.24’
1966;
Kuss and Malchus.
Malchus,
and Metwally,
and Atta,
1993
and Atta,
1993
1990
1998
without
exact
locatron
Gretl, 1998
without
exact
location
Abd-Elshafy
EEOlEzz El-Orban
wrthout exact
location
Ansary and Fahmy.
Qabelrat
wrthout exact
locatron
Marzouk
and Abou-El-Enern,
without
exact locatron
Masters,
1984
(Kerdany
and Abdel Salam,
1970)
of Suez
without
exact locatron
Masters,
1984
(Kerdany
and Abdel Salam,
1970)
E/Gulf of Suez
wrthout
exact locatron
Masters,
1984
(Kerdany
and Abdel Salam,
1970)
of Suez
without
exact locatron
Masters,
1984
(Kerdany
and Abdel Salam,
1970)
Araba
without
exact location
Masters,
1984
without
exact locatron
Anan,
wrthout
exact locatron
Shahin,
Wadr Nooz Wadr NoatlWadr
Nooz
Barakat
JliGulf
of Suez
Alef Well/Gulf Morgan H-l
Well/Gulf
G. ArabalGebel AZlAbu
Zenima
Matulla
locatron
1969
and Fahmy,
1969
Shahin,
1992;
Ismarl, 1992,
and Hussern,
Nezzazat
wrthout exact
Nuhkl
wrthout
exact location
Marzouk
BEM/Brr El-Markha
wrthout
exact locatron
Abdelmalik,
and Hussern, 1978a.
1994
location
Ismarl, 1992
wrthout exact
locabon
Shahrn,
Wadi Ferran
without
exact locabon
Marzouk
and Abou-ECEnern,
Wadi Feiran
without
exact locatron
Masters,
1984
without
exact location
Shahin,
wrthout
exact locatron
Masters,
1984
Masters,
1984
E-Ferran
wrthout exact
Wadi Ferran
locatron
1992
(Kerdany
and Abdel Salam.
1970)
(Kerdany
and Abdel Salam,
1970)
wrthout exact
locatron
Masters,
1984
exact
location
Masters,
1984
without
exact
location
Faris et al.,
without
exact
location
Cherif et a/ ., 1989
wrthout
exact
location
Arafa
without
exact
location
El Sheikh and El Beshtawy,
without
exact
location
El-Deeb and El-Gammal.
Wadr Nukhl
without
exact
locatron
Monechi
Wadi Feiran
‘N28”40’-50’;
of Suez
Gebel Qabelrat 4 SectronslAbu
Ruders
Gebel Nezzazat SE Nezzazat/Wadr some secttonsiwadi
GindrlGebel
Gindi
Ferran Feiran
E33°20’-30’
1986;
Ismail, 1992;
Gebel Urn Makhasa
without
exact location
Kulbrok,
1996
Gebel Gindi
without
exact location
Kulbrok,
1996
Wadi Sudr
N29’50.34’;
Wadi Sudr
without
exact
locatron
1992
1997
et a/ ., 1999
Eweda and El-Sorogy,
exact location
If coordmates are given m the literature, geographrcal points, but rather geographrcal
Allam and Khalrl, 1989
1991
without
E33°05,08’
1997
1990
wrthout
E. GhariblGulf
1999
1978b
wrthout exact
1 /Gulf of Suez
IObaidalla,
1992
Qabeliat
E-Bakr Manne
1996;
1994;
Wadi Fetran
Gebel Ekma
1997
1992
Marzouk
9
1996;
and Abdallah,
wrthout
N29O31.86’;
Nl /Wad1 Nooz
1989;
et a/.,
this work
ef a/.,
8
Kulbrok,
Wadi Askhar
Anthony
Bandel and
Boukhary
A3/E of St. Anthony
Al/St.
and Erssa, 1970;
7
1996;
Kuss and Lepprg. 1989;
1986;
Kuss and Leppig,
E32O21,21
Gebel Thelmet
6
Abdou et a/ ., 1969;
Strougo,
N28’54.95’;
GTlGebel
5
1966:
1979;
1999
Ismarl, 1996
Gretl. 1998 Youssef
then they are mentioned here. ranges given by the authors.
and Shrnnawr, Coordinates
1954; wrth
El-Shrnnawr,
a star
do not
1967 rndrcate
C. SCHEIBNER et al.
234 Journal of African Earth Soences
Maastrichtian-Early
Eocene litho-biostratigraphy
andpalazogeography
of the Sudr Formation,
Synonymy: Synonymous with the St Paul Formation of Kuss (1986), Bandel et a/. (1987) and Bandel and Kuss (1987) (Fig. 5). Regional distribution: The Sudr Formation
of the northern Gulf of Suez region
and El-Shinnawi which correlate Late Maastrichtian
is only found
Youssef
and Shinnawi
(I 954)
(1967) found Exogyra cf. overwegi, in area 4 (St Anthony) to the Middle/ St Anthony
Formation.
in northern Egypt and Sinai. At St Anthony (area 41, the chalks of the Sudr Formation have a Late Campanian age. They are dis-
Depositional setting: The Sudr Formation was deposited as basinal chalks with no shallow water
conformably overlain with an erosional surface by the units of the St Anthony Formation (SAF) (Fig. 7d). The stratigraphical range of the Sudr Formation
depositional environment of the chalks of the Sudr Formation on eastern Sinai in greater detail.
at Abu Zenima/Wadi Feiran (area 8) is not clear. Most authors agree that it terminates in the Upper
(19701, Abdallah et al. (I 970) and Abu Khadrah et al. (19871, erroneously included dolomitic limestones of
Maastrichtian;
the
however,
the Sudr Formation
some authors
continues
indicate
influences.
Paleocene,
that
seems
Leppig
(sediments
of the
and Eissa
Southern
above the cave of St Anthony.
(I 989)
indicated
a Late
Galala Kuss and
Paleocene
age by
Formation. St Anthony Formation (SAF) (section Al in Fig. 4a and Fig. 7d) Authors and type section: Bandel and Kuss (1987);
Hamam Faraoun are of Maastrichtian age (Gansserina gansseri Zone). Both sections in Wadi Nooz (area 6) start with 25 m dolomites,
such as Abdallah
the
at Ain Sudr
(area 9) are of Upper Campanian age (Globotruncana aegyptiaca Zone) and those of Gebel Gindi and
thick bedded
cliff
discussed
means of planktic and benthic foraminifers for these strata and attributed them to the Southern Galala
to depend
on how transitional beds are classified. The chalks Kulbrok (1996) described
massive
white
Formation)
up to the Cretaceous/
which
et a/. (1998b)
Discussion: Other authors,
Palasogene boundary (Fig. 4b). Only lsmail (I 992) extended its stratigraphical range at Gebel Qabeliat to the Lower
Lining
which
Monastery of St Anthony (Eastern Desert) Stratigraphical range: Upper Campanian-Upper Maastrichtian
may be attri-
buted to the Sudr Formation. However, dolomitisation has prohibited a conclusive stratigraphical assignment.
The mainly carbonate lithologies of the St Anthony Formation in the Southern Galala disconformably
Similar
overlie
lithologies
were
described
Formation
of Sinai (Youssef
Shinnawi,
1967).
be attributed
from
the
and Shinnawi,
Alternatively,
Sudr
1954;
these dolomites
to the underlying
Turonian
Strata
chalks of the Sudr Formation
may
overwegiis
(Abd-
present.
Age-equivalent
Elshafy and Atta, 1993). In northwestern Sinai (area 91, Youssef and Shinnawi
Exogyra overwegiwere Desert
in the ‘Overwegi
(1954)
known
as the Beris Oyster
and El-Shinnawi
pinkish-white
bedded
(I 967) described chalks
and chalky
175 m of
Late Campanian
were thought to contain rare Maastrichtian foraminifers and Subbotina triloculinoides of Paleocene age
Selima and Askalany, biostratigraphic data
(El-Shinnawi,
sandy-dolomitic
1967).
The scarcity
of the foraminifers
assignment
into doubt,
possible explanation.
and the poor pre-
strongly
although
Forty-five
indicated
puts the latter
reworking
the
sediments
first described Layers’
(Zittel,
Mudstone
with
in the Western 1883),
Member
now of the
Dakhla Formation (Awad and Ghobrial, 1965; Luger, 1985). The base of the St Anthony Formation is of
limestones
that change to yellowish-white hard dolomitic limestone in its upper part. Samples of the upper part
servation
and underlie
carbonates of the Southern Galala Formation. In the upper part of the St Anthony Formation, Exogyra
El-
age (Kuss,
upper units,
by thin sections.
(I 979) described
may be a
minifers
metres below the base
1986;
Kulbrok,
1996). Although is available from
1996;
only poor the mainly
a Maastrichtian
Abdel-Kireem
Upper Maastrichtian
of the Abathomphalus
age is
and Abdou planktic
mayaroensis
fora-
Zone at
Figure 7. The Late Cretaceous-Palaeogene sediments of the western la-d) and eastern lel side of the Gulf of Suez. la1 Section Tl, the southernmost section tn area 1: the chalks of the Tarawan Formation ITFI are intercalated between the marls and shales
of the
limestones Formation
Dakhla
Formation
of the Serai
are overlatn
Formatton
IDFl
below
of the
by the ltmestones
and
Thebes
the
Esna
Group
Formation
ITHG).
of the Southern
Galala
(EFI
161 Section Formatton
02
above. in area
(SGFI
The cliff
at the
2: the marls
with a gradual
top
is built
and shales
contact.
of chalky
of the Dakhla
The fault at the top
is of younger age and was the result of Red Sea graben tectonics. The section continues left of the picture with the rest of the sediments of the Southern Galala and the Esna Formations and the Thebes Group. (cl Section S9 (Kuss et al., 2000) in area 3: the marls and shales of the Dakhla Formation are sandwiched between chalks of the Sudr Formation (SF) below and shallow
water
influenced
sedtments
of the Southern
Galala
Formation
above.
Idl Section
A 1 in area
4: the marls
and sandy
marls of the St Anthony Formation ISAFI are overlain by the shallow water limestones of the Southern Galala Formation. The Southern Galala Formation forms a steep white cliff along the northern rim of the Southern Galala. fel Wadi Nukhl on Sinai: similar courtesy
to section of R.P.
Tl
(al,
Spetjerl.
the thin
Tarawan
The scales
are
Formation
IS sandwiched
only approximattons
due
between
the Dakhla
to a distorted
and the Esna Formations
(picture
perspective.
Journal of African Earth Sciences 235
C. SCHEBNER Gebel Thelmet
(GT; Fig. 4a). A possible hiatus between
et al.
occurs
within
NP7/8,
where
the Dakhla
Formation
the Late Cretaceous and the Early Tertiary sediments in section Al is assumed but could not be substan-
underlies the Tarawan Formation. The latter or even absent in northern Egypt and Sinai.
tiated in the studied sections by means of planktic foraminifers or calcareous nannoplankton. Lithology: Chalky limestones, marls and sandstones Synonymy: The St Anthony Formation corresponds to the Gebel Thelmet Formation of Abdallah and
Lithology: In the studied area, the Dakhla Formation consists of chalky marls in the uppermost Maastrichtian and of softer shaley grey-green marls in the Paleocene (Fig. 8). The thickness of the Dakhla
Eissa (1970) (Fig. 5). Although their term is older, the authors followed Bandel and Kuss (I 987) because Abdallah and Eissa (I 970) and Abdallah et a/. (1970) were apparently confused by the Cretaceous-Eocene lithologies (see the discussion the Sudr Formation). Other reasons for using
of the
term
and
the
St Anthony thickness
Whereas
Formation
are the accessibility
differences
the section
of the
type
in Gebel Thelmet
sections.
is dangerous
is thin
Formation varies from 6.5 m (D3) to 23.5 m (Tl). Synonymy: The Dakhla Formation is synonymous with the ‘aschgraue Blgtterthone of Zittel (18831, the Lower Esna of Hume (I 912) and the Lower Oweina Shale of El-Naggar (I 966a) (Fig. 5). Regional distribution: The Dakhla Formation in all areas except tigraphical results
is present
areas 4, 5 and 7, where
gap occurs
of this study
and Faris (I 993)
a stra-
(Fig. 6). In contrast
in Bir Dakhl
attributed
to the
(area 21, Strougo
the whole
succession,
to access (due to possible mine occurrences) and has a reduced section thickness, the section at monastery of St Anthony is easily accessible and has a much
which is sandwiched between the top of the Sudr Formation and the base of the Thebes Group, to the Southern Galala Formation. However, they subdivided
larger thickness. Regional distribution:
the Southern Galala Formation a lower light green argillaceous
deposits
The shallow
of St Anthony
along the northern equivalent
Formation
formation
in northern
only
Galala. A time
Egypt
and Sinai is
of the St Anthony
are slope sediments of a shallow water platform. In the lower part of the St Anthony
Formation, exposed.
influenced
are mapped
rim of the Southern
the Sudr Formation (Fig. 6). Depositional setting: The sediments Formation carbonate
water
large slumping structures
occur and are well
In the middle part, limestones
and reworked
shallow
water
with slumping
biota, such as Orbitoides
and Omphalocyclus, occur. In the upper part of section A3 (7 km east of St Anthony; Fig. I), the shallow water
prominent
harder
foraminifers
bioclastic
and thick
green-grey
calcareous
into three main units: limestone; a middle limestone
with
chert
bands;
shale.
In the present
large
and an upper study,
the authors correlated this tripartition, which is evident also in neighbouring sections, to the Dakhla, Southern
Galala and Esna Formations
(from base to
top) (Fig. 8). In the Northern Galala (area 61, the Dakhla Formation has a thickness of 10 m and is composed of papershales and marly limestones, planktic
foraminifers
the latter with abundant
(morozovellids)
in thin sections,
bivalve Pinna and teeth of bony fishes were found that
indicating an age of P3 or younger (section Nl ; Fig. 4a). In the present study, the authors attributed these
thrived
zones of reefs (C. Werner, pers.
sediments
to the Dakhla
comm.). Kulbrok (I 996) assigned the deposits of the St Anthony Formation to a distally steepened ramp, and
lithological
and stratigraphical setting:
The
Selima and Kerdany
deposited
as basinal
marls
influences.
Speijer and Schmitz
in calm water
(1996)
assigned them to shallow
marine environments. Dakhla Formation (DF) (Figs 4a, b and 7a-c, e) Author and type section: Said (1961); Dakhla, north of Mut (Western Desert) Stratigraphical range: Maastrichtian to Upper Paleocene The lowermost occurrence of the Dakhla Formation
Depositional
Formation
because
of their
similarities. Dakhla with
Formation no shallow
(I 998) reported
was water from
Gebel Aweina (300 km to the south), for most of the Dakhla Formation, a pala?owater depth of 200 m. The pala?owater only within (1990)
depth decreases to lower than 100 m the planktic foraminifer zone P3. Shahin
described
bathyal
environments
for the shales
in the Paleocene is at St Paul (area 3), within the middle to upper foraminiferal Parvularugoglobigerina
of the Dakhla Formation. Discussion: In the Western Desert, the Dakhla Formation was subdivided by Awad and Ghobrial (1965)
eugubina Zone (Pcx) (Strougo et a/., 1992) and, respectively, the middle NP 1 calcareous nannofossil zone (Girgis, 1987; Faris, 1997). The top of the Dakhla
into three members: the Mawhoob Shale Member; the Beris Oyster Mudstone Member; and the Kharga Shale Member. The Cretaceous/Palaogene boundary
Formation lies in Bir Dakhl (area 21, St Paul (area 3) and northern Northern Galala (area 6) within NP5, where it underlies the Southern Galala Formation. At Wadi
lies within
Tarfa
(area
I) and in western
236 Journal of African Earth Sciences
Sinai
(areas
8, 91, it
the upper part of the Kharga Shale Member
(Awad and Ghobrial, 1965). In contrast to southern and western Egypt where the base of the Dakhla Formation lies in the Lower Maastrichtian and exhibits
8. Bio- and lithostratigraphic
correlation
of six sections
from areas
1-4
on the western
the shallow water sediments of the St Anthony Formation m the Maastricht/an-Paleocene rectangle in sections 03 and 02 indicates the range of the detailed correlation of F/g. 9.
Figure
of the
Southern
Paleocene-Eocene.
of The black
Best visible is the progradation in the
Desertl. FormatIon
(Eastern Galala
side of the Gulf of Suez and
C. SCHEIBNER et al. the complete succession of all three members, in northern Egypt and Sinai only the equivalent of the younger Kharga Shale Member is present (Fig. 5). Here, the Sudr Formation and St Anthony Formation correlate with the Mawhoob Shale Member and the Beris Oyster Mudstone Member, respectively. In
P4. The Tarawan
Formation
in Ezz El-Orban
thickness
of more
than
20 m in the nearby
northern Egypt and Sinai, the base of the Dakhla Formation lies usually at the Cretaceous/Palaeogene
western
boundary
study area was deposited as basinal stones with no shallow water influences.
and the top within
P4/NP6
(Fig. 4a, b).
is very
thick in comparison to the sections of the Tarawan Formation on Sinai and in the Wadi Tarfa area. These sediments may, more appropriately, be assigned to the Southern Galala Formation, which reaches a north-
Bir Dakhl area.
Depositional
setting: The Tarawan
Formation
in the
chalks/limeAnan (1992)
and Lijning et a/. (I 998a) concluded that the Tarawan Formation on Sinai was deposited during a period of
Tarawan Formation (TF) (Figs 4a, b and 7a. e) Authors and type section: Awad and Ghobrial (1965); Gebel Tarawan, Kharga Oasis (Western Desert).
low sea levels. Luger (1985)
and Speijer and Schmitz
Stratigraphical
(19981,
reported
range: Upper Paleocene
The base lies within within lower the Tarawan
NP7/8/(P4)
NP9/(P5). Formation
and the top lies
The stratigraphical range of comprises biozones P4/NP6
on the other
hand,
Egypt that the sediments
from southern
of the Tarawan
Formation
were deposited during sea level highstands. Discussion: In northern Egypt and Sinai, the Tarawan
to P5/NP9. Kassab and Keheila (19941, however, gave a range from zones P3/mid-NP4 to P4c/lower
Formation has a reduced thickness or is absent (Fig. 5). However, even where the Tarawan Formation is
NP9. It overlies
present
the Dakhla
Formation
and underlies
the Esna Formation. Lithology: In the study is characterised 2.10 m (section
area, the Tarawan
Formation
by a 1.80 m (area 1, section Tl) to T2) thick chalk bed with flint, similar
to the underlying
Sudr Formation.
In the Kharga area,
(thin chalks
interval),
it was
authors,
although
profiles
(northeastern
Matulla:
Obaidalla, of the
siliceous
authors.
The Tarawan
Formation
was described
by earlier authors as Chalk (Zittel, 1883), (Beadnell, 1905) or Middle Oweina Naggar, 1966a, 1966b3 (Fig. 5).
Danian Chalk
Chalk Member
(El-
(WTS)
of Kassab
and Keheila
(1994)
crepancies
with respect to lithology
In section
WHS
these
authors
extending Formation, this
(near to section described
the
exhibit
dis-
and stratigraphy. Tl
the
Tarawan
Dakhla
Formation
Consequently,
Maastrichtian Shafik (1996)
1999;
Tarawan
7e).
misled
The some
attributed
even
Formation
(e.g.
and Stradner, 1971). Selima and Askalany attributed chalky limestones in Wadi Askhar
km east abundant
Formation.
In section
Al
(7
of Wadi Askhar), these chalks contain shallow water biota (corals, coralline algae)
and are attributed
in the present study to the Southern
Galala Formation
(Figs 5 and 6).
Garra Formation
Formation
rests
uncon-
(GF) (Fig. 4b)
Author and type locality: Issawi, 1969; South of Gebel Garra, south Western Desert Stratigraphical range: Upper
overlies
the Sudr Formation
overlain
by the Egma Formation
range with the base lying within
P3 (NP4-
from the observations
in the neighbouring
and
they wrongly
graphical this study)
Matulla:
chalks to the Tarawan
Eocene In northwestern
markedly
1987;
Figs 4b Formation
formably over Late Campanian sediments (Fig. 4a). Moreover, its thickness of 30-50 m and stratiNP 5) differs
by various
the respective
in this study),
down to the Maastrichtian and no Sudr whereas in WTS (near to section T2 in
study)
within
Sinai: Hewaidy,
(area 4) to the Tarawan
Regional distribution: In area 1, sections Wadi Hawashiya section (WHS) and Wadi Tarfa section
at the NP6-NP9
discussed
Ismail, 1992; Wadi Nukhl: Marzouk and Hussein, 1994; Wadi Feiran: Marzouk and Abou-El-Enein, 1997; absence
limestone.
not
it is visible
it is represented by a 3-45 m thick chalk unit, which in places changes into chalky limestone, limestone or Synonymy:
or limestones
often
sections.
(from
Similar
to
within
Sinai,
Paleocene
its base
to Lower
disconformably
and lies within
P3a. It is
of the Thebes Group
P6a.
the hiatuses, these discrepancies may be the result of very local highs and lows controlling deposition of these different lithologies.
Liihology: In area 9, the Garra Formation is composed of a basal white argillaceous limestone with chert near its top, overlain by massive limestones and thus
In section Ezz El-Orban Fahmy (1969), the Tarawan
(area 7) of Ansary and Formation is represented
shows similarities with the Southern Galala Formation at Bir Dakhl (area 2). In Kala ‘t al-Gindi, the Garra For-
m layer of mainly argillaceous limestone, which chalky in its lower part (Fig. 4b). The authors it Middle Oweina Chalk after El-Naggar (1966a, and assigned its stratigraphical range to within
mation has a maximum thickness of 49 m (Fig. 4b). At the type locality, the Garra Formation is composed of well-bedded white limestone and chalk with minor shale and marl intercalations.
by a 43 is partly named 1966b)
238 Journal of Afncan Earth Snences
Maastrichtian-Early Regional distribution:
Eocene litho-biostratigraphy The Garra Formation
cribed only by Hamza et a/. (1997)
andpalazogeograph
was des-
from northwestern
and north central Sinai. Depositional setting: In southern Egypt, the Garra Formation was deposited in the middle to inner shelf (Luger, 19851,
whereas
on Sinai deeper marine set-
tings are assumed (see the discussion of the Southern Galala Formation below). Discussion: In northwestern Sinai (area 91, Hamza et a/., (1997) described limestones of the Garra Formation (mid-P3b-mid-PGa), sandwiched between the chalks of the Sudr Formation and the limestones of the Thebes Group (Fig. 4b). Said and Kenawy (I 956) identified a bathyal fauna in the chalky sediments. Whether these deposits are synonym with the Southern Galala Formation remains uncertain. However, at least the introduction
of the Garra Formation
in this part of Egypt may explain earlier discrepancies in lithological
description
and dating
of the Sudr
Formation and Thebes Group. Hermina and Lindenberg (I 989) described the Garra Formation from the southern Western Desert. It disconformably overlies the Kurkur Formation and underlies the Dungul Formation. The Garra Formation,
y of the northern Gulf of Suez region
Abu Darag (Abd-Elazeam and Metwally, 1998). Malchus (1990) described a hiatus ranging from Late Cenomanian
to Maastrichtian
Formation
limestones with flint. Synonymy: Abu Khadrah et a/. (1987) Galala Formation. NP9/10)
The whole Palaeogene part (P5/6;
of section Wadi Naot (limestones and clayey
siltstones)
in the Northern
Abd-Elshafy
Galala was attributed
and Atta (1993)
which was introduced by Abd-Elshafy (1988)
Galala Formation (Fig. 5). distribution:
In sections
D2 and D3 (area
Galala Formation
starts with the
bed and is characterised
limestones
dant chert layers or nodules
c. d) Authors and locality: Abdallah et a/. (1970);
to 0.7 m thick). The hard limestones
of St Anthony Eocene
Data from this study indicate that the base of the Southern
Galala Formation
lies within the Glomal-
veolina levis Zone (Upper Thanetian,
P4c/NP8)
and
the top lies within the Alveolina dainelliZone (Cuisian, PS/NP13). In Bir Dakhl and St Paul, the Southern Galala Formation
is overlying the Paleocene
Formation (Fig. 4a) with a stratigraphical
Dakhla
range from
and shaley marls (up are partly com-
posed of bioclastic wackestones, and chalky and dolomitic limestones. Figure 9 shows the interfingering of the Southern partly overlying D2 and 03).
Stratigraphical range: Upper Paleocene-Lower
by
(up to 1 m thick) with abun-
Southern Galala Formation (SGF) (Figs 4a. b and 7b,
of monastery
in Wadi
Naot Formation in this study because it is possible to differentiate the Dakhla Formation and Southern
alternating
The reference section 18/2 (Kuss and Leppig, 1989) is situated in a north-south-trending wadi, 6 km west
by
to the Naot Formation,
Naot (Wadi Naot is a synonym of Wadi Nooz used by the authors). The authors did not employ the term
first hard limestone
by Kuss and Leppig (I 989)
introduced the
Useit Formation as a junior synonym of the Southern
2), the Southern
redefined
(alveolina,
thickness of about 250 m. In the southern parts, it is
Regional
(Fig. 5).
sandy fossiliferous
numulitids, coralline algae) limestones and limestone/ sandstone intercalations often conglomeratic with a
parts of the Dakhla,
and Esna Formations
In the
(section Nl of Fig. 4a) and underlies the
Thebes Group. Lithology: Massive
in southern Egypt, is a lateral equivalent of the upper Tarawan
in section 20/2.
northern areas of the Northern Galala, the Southern Galala Formation overlies the Paleocene Dakhla
show
Galala Formation
Esna Formation
In section
abundant
and the
in detail (sections
D2, three limestone
bioturbation
beds and
Thalassinoides.
The
Galala Formation
unit A in sections D2 and D3 (Fig.
9) has a thickness Although
main
of Zoophycos
part of the Southern
of 17 m and 20 m, respectively.
the Southern
Galala Formation
has more
or less the same thickness in these sections, the thickness of the different biozones varies (e.g. NP6 and NP7/8;
Fig. 9).
mid-NP5/(P3/4) to mid-NP9/(P4/5). In section D2, the Southern Galala Formation interfingers with the
is composed
with
locally abundant
Esna Formation,
quartz grains that were deposited
as gravity flows,
and the top lies within
NPI O/P6
At St Paul (area 31, the Southern Galala Formation of limestones
(Figs 6,8 and 9). At St Paul, the top of the Southern Galala Formation lies within SBZlO (NPI 2/P7)
such as glides, slumps and debris flows. A few thin
(Gietl, 1998). In St Anthony, the Southern Galala Formation overlies the Late Campanian-Maastrichtian St Anthony Formation, while farther north it is
lower part (Scheibner et a/. , 2000). The steep white cliff at St Anthony and Gebel Thelmet (area 4) is composed of dolomitic limestones
unconformably
of the Southern Galala Formation (Fig. 7d). Because
underlain by Turonian strata in section
20/2 (Kuss and Leppig, 1989) and other parts of the Northern Galala (Abd-Elshafy and Atta, 1993), and by Campanian limestones of the Matulla Formation in
(maximum
20 cm) marl beds are intercalated
in the
of its white colour and its chalky appearance, which is due to diagenetic alternations, several authors (Abdallah and Eissa. 1970; Abdallah et a/. , 1970; Abu
Journal of African Earth Snences 239
C. SCHEIBNER et a I.
Figure 9. Detailed bio- and lithostratlgraphic units described in the text.
240
Journal
of African
Earth Snences
correlation
of sections
03
and 02
m area
2.
The letters
A-F
indicate
different
Maastrichtian-Early Khadrah strata
Eocene litho-biostratigraph
et a/. , 1987) previously
as chalks
misinterpreted
of the Sudr Formation
y and pal;eogeograph
these
(Fig. 5) or of
the Tarawan Formation (Selima and Askalany, 1996). However, the basal conglomeratic debris flow type deposits of O-2 m thickness are overlain by white diagenetically overprinted limestones with abundant corals in the lower 15 m. In the middle part of the nearly 70 m high cliff, Hottingerina lukasi(SBZ4/P4c) was found, indicating a latest Paleocene age. In section 20/2 (area 5) (Kuss and Leppig, 19891, the Late Paleocene-Early Eocene Southern Galala Formation is build of massive sandy limestones, limestone-sandstone
intercalations
and debris flows.
In Wadi Nooz (area 61, it is formed and
chaotically
lithologic mation the
bedded
similarities
of debris
limestones.
flows
Because
to the Southern
Galala
For-
of area 3 (St Paul), this unit is attributed
Southern
Galala
Formation.
lying Dakhla Formation, found, indicating again Hamam (1998)
Faraoun
to
As in the under-
only morozovellids were an age of P3 or younger. In
in the very
described
of
south
debris flows
of area 9, Gietl
up to 6 m thick
with
Galala
y of the northern Gulf of Suez region
Formation,
overlying
Thebes
or whether
it forms
part of the
Group (Fig. 5).
Esna Formation (EF) (Figs ba, b and 7a, e) Author and type section: Beadnell (1905); Aweina near Esna Stratigraphical range: Late Paleocene
Gebel
to Early Eocene
Its stratigraphical range has been discussed intensively (El-Naggar, 1966a, 1966b, 1968; Sabry, 1968; Issawi, 1972). Today, it is accepted in Egypt, except Sinai, that the Esna Formation is intercalated between two, more or less, chalky limestone units. These units are, the Tarawan Formation below and the Thebes Group above,
and thus represent
Early Ypresian
(P4c/lower
6). On Sinai, quite
often
however,
the term
used to describe
shales sandwiched
Late Thanetian
to
NP9 to mid-P7/NP12;
between
Fig.
Esna Formation
the whole
is
Paleocene
the Sudr Formation
below
and the Thebes Group above (Liining et al., 1998a; Marzouk and Lining, 1998; see discussion below). Liihology: The Esna Formation
is composed
grey shales and marls with planktic
of green-
foraminifers
and
siliciclastic sand and larger foraminifers and shallow water limestones with larger foraminifers of Early
calcareous
Eocene age (SBZ7-9, 9 (Wadi Sudr), Gietl
the ‘grtinliche Blatterthone’ of Zittel (18831, the upper Esna of Hume (1912) and the Upper Oweina Shale of
beds with slumps, minifers. In Gebel described with
chalky
larger
NPI O-l 2). In the north of area (1998) found limestone/marl debris flows Urn Makhasa,
limestones
foraminifers
and larger foraKulbrok (1996)
of SBZ4-6
and corals,
which
(NP8/9) may be
nannoplankton.
Synonymy:
El-Naggar
The Esna Formation
(1966a,
1966b)
is synonymous
with
(Fig. 5).
Regional distribution: In Wadi Tarfa (area l), the Esna Formation
is 10.50
is composed
m (Tl ) to 17.10
of the same
m (T2) thick and
lithology
as the
Dakhla
attributed to the Southern Galala Formation. Depositional setting: The sediments of the Southern
Formation. Nishi et al. (1994) described a section south of the Ras Gharib to El-Sheikh Fadl Road with
Galala Formation
only 5 m of the Esna Formation
are sediments
of a carbonate
plat-
form and slope, which were deposited on and around the Northern Galala/Wadi Araba High. They interfinger with
basinal
sediments
of the Southern
Galala Sub-
basin in area 2 (Bir Dakhl). Kulbrok (I 9961, Gietl (1998) and Scheibner
et al. (2000)
described
platform and slope deposits Formation in more detail. Discussion:
In this study,
the carbonate
of the Southern the classification
Galala of Abu
Khadrah eta/ (1987) and Selima and Askalany (1996) are not followed. The Useit Formation described by
the Thebes Group, whereas
overlain
El-Dawy
21 m of Esna Formation in a section Gharib to El-Sheikh Fadl Road. Strougo section
and Faris (19931, (area
21, described
in their Wadi El-Dakhl
is characterised abundant These
by green-grey
shaley
sandstones
are partly
as Dakhla
Formation
(see the discussion
with layers.
cross-laminated
parts
interpreted
marls
thin (up to 0.22 m thick) sandstone
ever, is of Early Paleocene be regarded
calcareous
shales and cream to light grey laminated argillaceous limestones. In section D3 (area 21, the Esna Formation
have rip-up clasts. The sicliciclastic
should
reported
south of the Ras
green-grey
Abu Khadrah et al. (I 987) was thought to overlie a unit termed Esna Formation In St Paul; which, howage and, therefore,
by chalks of
(1999)
intercalations
and were
as distal fan lobes, of which more proximal
at St Paul were
discussed
in Scheibner
et al.
(2000). In Bir Dakhl (area 21, the Southern Galala Formation grades laterally into shales of the Esna
of the Abu Rimth Formation below). Moreover, the same authors correlated the Zaafarana Formation
Formation,
with the originally Formation
Useit Formation, although the first was described to overlie the Southern Galala and is of middle Eocene age (Abdallah et
section D3 (Fig. 9). In section D2, the intimate interfingering of the Esna Formation with the Southern Galala Formation is evident (Figs 8 and 9). As a con-
al., 1970). It is not clear by the above whether the Zaafarana Formation should be attributed to the Useit
sequence, this part of the section can be subdivided into five units. From the bottom to the top, the following
Formation
five units can be distinguished
and, hence, represent
part of the Southern
best visible in section
Journal
D2 and less clear in
(Fig. 9) as follows:
of African
Earth Sciences
24 1
C. SCHEIBNER et al. i) A: alternating
limestones
layers (see Southern
with
abundant
Galala Formation
chert
above);
iii B: 2.5 m grey-green marl; iii) C: 1.9 m alternation of silty marls and dolomitic limestone with laminations and channel structures; iv) D: 4.4 m grey-green marl at the base silty; v) E: 6 m alternation of shaley, partly silty, marls and dolomitic limestones with laminations, channel structures
and rip-up layers;
Paleocene shales or only Lower Paleocene shales were exposed or where they were separated by the Tarawan Formation. If the shales range from the Lower to the Upper Paleocene, the authors suggest the usage of the Dakhla/Tarawan/Esna Formation (Figs 5 and 6). Snavely et al. (1979) stated that most authors agree with the upper portion of the Esna Formation being assigned to the Ypresian Morozovella subbotinae Zone
and
(PG/NPl O/l 1 of Berggren
the transitional
vi) F: 5.2 m of silty marls.
marly beds typical
et a/. , 19951,
of the conformable
Within this profile, units (A), (C) and (E) exhibit characteristics of the Southern Galala Formation,
Esna-Thebes contact were assigned to the Morozovet/a aragonensis Subzone (P7/NP12 of Berggren et
whereas units (B), (D) and (F) could be attributed to the Esna Formation (Fig. 9). In northern Northern Galala (area 61, the 15 m of the
a/., 1995). However, in this study, it was found that the Esna-Thebes contact in the Eastern Desert was
Esna Formation are of Lower Eocene age (NPI 1 /12/P6), indicated by presence of calcareous nannofossils and planktic
foraminifers.
In contrast,
Gietl (1998)
des-
cribed alveolinids of SBZ5 (NP9/P5) from limestones overlying the Esna Formation; which, however, may have been reworked
from older carbonates.
Depositional setting: The Esna Formation deposited as basinal marls with no shallow influences. in areas
Shallow that
Formation. depth
water
interfinger
deposits with
curve
from
were found
the Southern
Speijer and Schmitz
was water only
Galala
(I 998) gave a palseo-
Gebel Aweina
(ca 300 km to the
usually within NPI 1. In the upper Formation as well as in the Thebes
part of the Esna Group, Nummu-
lites deserti was found (LeRoy, 1953; Hermina and Lindenberg, 19891, indicating an Ypresian age (NPl lNPI 21, which contrasts of that species
with the stratigraphical
mentioned
by Serra-Kiel
as SBZ4 and SBZ5 and which corresponds This discrepancy led to some confusion stratigra-phical example,
range
Gietl (1998)
of the
Thebes
correlated
Group.
(SBZ5 or NP9), which the strati-graphical
would
be in disagreement
Dakhla/Tarawan/Esna
the shales of the Esna Formation
Eocene.
Formation
was given
to Beadnell
of the Esna
(I 905),
although
shales in the vicinity of Esna were mentioned earlier by Zittel (1883) and others (see El-Naggar, 1966a, 1966b). In northern shales
Egypt and on Sinai, the whole Paleocene
and marls
Formation
are often
in areas
where
attributed no Tarawan
to the Esna Formation
exists (Said, 1990) and thus have a stratigraphical range from Upper Maastrichtian to Lower Ypresian (see the discussion of the Dakhla/Tarawan/Esna Formation below). Even if only the lower part of the Paleocene
shales are exposed
(e.g. Abu Khadrah
al., 19871, they were quite often referred Formation, which makes lithostratigraphic
et
to as Esna correlation
very confusing (Abu Khadrah et al., 1987; Hewaidy, 1987; Said, 1990; Cherif and Ismail, 1991; Marzouk and Hussein,
1994)
suggest attributing the Esna Formation, would belong to the is only possible in
(Fig. 5). The authors,
therefore,
only Upper Paleocene shales to whereas Lower Paleocene shales Dakhla Formation. This bipartition areas where either only Upper
242 Journal of African Earth Sciences
Because
Maastrichtian
with
range of our samples.
Stratigraphy: The stratigraphical range formal formation is Upper Maastrichtian
on
For
part of
the Thebes Group to the Alveolina cucumifom?is Zone
depth decreases to 100 m only in the uppermost part of the Esna Formation. According to Shahin (19901, were deposited
to NP9. of the
the lower
south) and reported palaaowater depths of about 200 m for most of the Esna Formation. The palseowater
Sinai in bathyal environments. Discussion: The credit for the introduction
range
et a/. (1998)
Formation (DTE) (Fig. 441)
of the gradual
transition
chalk to the Paleocene
of this into Lower from the
shales, the onset
of the DakhlaTTarawan/Esna Formation in Abu Zenimal Wadi Feiran (area 8) is not clearly fixed lithologically. It varies from a level within
the Upper Maastrichtian
to one at the Cretaceous/Palaeogene A small (Shahin,
hiatus 1992).
(K/Pg) boundary.
at the K/Pg boundary is probable As with the lower stratigraphic boun-
dary, the upper boundary is not well constrained. The transition from the Dakhla/Tarawan/Esna Formation to the Thebes overlies Group.
Group
lies around
the Sudr Formation
Liihology: Green-grey Esna Formation Regional Formation
P6/7,
and underlies
NPl l/l 2. It the Thebes
shales and marls, similar to the
distribution: The Dakhla/Tarawan/Esna is only present on Sinai.
Depositional
setting:
The
Dakhla/Tarawan/Esna
Formation was deposited as basinal the Esna Formation (Shahin, 1990). Discussion: an informal
marls similar to
The Dakhla/Tarawan/Esna formation for the latest
Formation is Cretaceous-
Palseogene grey-green shales in northern Egypt and Sinai, where the Tarawan Formation cannot be
Maastrichtian-Early identified.
Eocene litho-biostratigraph
In most
Tarawan/Esna
sections
within
the
y and pakeogeograph y of the northern Gulf of Suez region
Dakhla/
Formation at around upper P4/5, one
quartz grains. The base lies in lower NP12. sediments
may belong to the Southern
These
Galala For-
mation as well but, again, were not subject of this
or more limestones might be attributed to the Tarawan Formation. Masters (1984) indicated two limestone
study. The Thebes Group in area 8 is composed
beds in Wadi Feiran East, which could be attributed
sequence
to the Tarawan
intercalated
tectonic
Formation
duplication
Because probably
and probably represent a
(R.P.
Speijer,
pers.
comm.).
of the reduced thickness of the beds, not all authors indicated these layers as
1992)
of well-bedded
of a
limestones
with
chert bands (El Sheikh and El Beshtawy,
or of yellowish
limestones
chalky
sandy limestones
with chert bands (Shahin,
followed 1990,
by
1992).
In Wadi Feiran (area 81, Eweda and El-Sorogy (I 999)
Tarawan Formation. The varying ages of the top of the Dakhla/Tarawan/Esna Formation are due not to transitional lithologies but to the different biozonations
divided the Thebes Formation into a lower 180-I 90 m thick cherty chalky limestone member and an upper
used. Authors who have worked with the calcareous
Depositional setting: Only the lower part of the Thebes
nannoplankton bio-zonation gave older (NPI 1 = P6) ages than authors who used the planktic foraminifer
sediments were deposited in a basinal setting without
zonation from
(P6/7).
This discrepancy
the variability
calcareous
in the
nannoplankton
probably
planktic
correlation
results
foraminifers(Marzouk and
50-60
m thick calcareous
claystone
member.
Group in area 1 (Wadi Tarfa) was studied. Here, the any shallow water influences. In areas 2-6, the transition from the Southern Galala Formation to the above
lying Thebes
Shahin (1990)
Group
was not investigated.
and Lining et al. (I 998a)
suggested
Lining, 1998). Another explanation may be the usage of different planktic foraminifer biozonations, which
that the Thebes Group on Sinai was deposited during
were revised in time or different taxonomic
a time of a lowered
concepts
of the authors.
sea level. Snavely et a/. (1979)
proposed the following three-stage
depositional
his-
tory for the Thebes Group: Thebes Group (THG) (Figs 4a, b and 7a. e) Authors: Hermina and Lindenberg (1989) Stratigraphical formations
range: Lower Eocene (see different
below) below)
(see different formations
Regional distribution:
Discussion:
below)
Hermina
At Wadi Tarfa, the base of the
Thebes Group lies within NPI 1 /P6. It is composed of chalky limestones alternating with chalky marls. Some of the chalks have layers or nodules of flint incorporated.
and
The Thebes
by chalky limestones
with abundant
chert layers or
nodules, marly intercalations and sandstones with cross-bedding, lamination and rip-ups. They may alternations
Group was introduced
and Lindenberg
(1989).
It replaces
by the
Thebes Formation of Said (1960) and is equivalent to the ‘Libysche Stufe’ of Zittel(18831, excluding the Esna Shales (Fig. 5). The Thebes Group includes the following formations (Fig. 5): i) Farafra
In Bir Dakhl (area 21, the Thebes Group is formed
contain
iii gradual shallowing;
fi) abrupt lowering of sea level.
Liihology: (see different formations Synonymy:
i) basin-wide pelagic carbonate deposition with thin shallow water facies near the basin margins;
Formation,
Formation,
El-Rufuf
Formation,
Serai
Drunka Formation and Dungul Formation
in the scarps and plateau areas south of Minia; ii) Abu Rimth Formation in the Southern Galala; and iii) Egma Formation on Sinai.
of harder and softer marls. In
Here, the focus is only on the Serai, Egma and Abu
the lower part of section D2, the marls are partly rich
Rimth Formations since they have been described in the
in quartz grains and Nummulitids. section
D2, slumping
In the upper part of
and first Alveolina-rich
study area of the northern part of the Gulf of Suez. In
sand-
this contribution, the authors refer to the Thebes Group
stones occur that could belong to the Southern Galala
when ‘speaking’ of Lower Eocene strata that overly the Esna or Dakhla/Tarawan/Esna Formations (except the
Formation as well, but this transition was not investigated in detail. Bandel et al. (1987)
described the Serai Formation
overlying the Esna Shale from the western escarpment of Wadi Tarfa. Within the upper third of the 1 IO m
Galala Mountains, where the Thebes Group overlies the Southern Galala Formation) and underlie the Minia Formation. In the contribution, different formations is done.
no subdivision of the
thick succession of bedded marly to platy chalks with flint intercalations, a 17 m thick unit of alveolinidnummulitid-bearing limestones aged SBZl 1 - 14 occurs
Authors and type section: Barron and Hume (1902);
that indicate an Early Eocene age. The Thebes Group
redefined
of northern Northern Galala (area 6) is composed
Lindenberg,
well-bedded
dolomitic
mulitids, deformed
limestones
of
partly with num-
alveolinids, few debris flows and
Serai Formation by Lindenberg 1989)
et al.
(in Hermina
and
as facies variation of the Thebes
Group; Gebel Serai, south Wadi Qena, Eastern Desert Stratigraphical
range: Early Eocene
Journal of African Earth Sciences 243
C. SCHEIBNER et al. Synonymy: Synonymous members of the Thebes and the lower
member
of the Thebes
Formation
of
thinly-bedded
micritic
lime-
chalky and cherty with rare shales, grading into massive bioturbated beds with few
allochthonous layers Discussion: The Serai Formation throughout
Formation. Philobbos et al. (in Hermina and Lindenberg, 1989) mentioned that the Abu Rimth Formation overlies
the Esna Formation
However,
Snavely et al. (I 979). Lithology: Fine-grained stones, upward
with the lower and middle Formation by Said (1960)
the Stable
Shelf,
is widely
developed
at the plateau
surface
the Esna Formation shales
in the southern
in St Paul no Upper
of the
Paleocene
occur, only the Lower
Dakhla
Formation.
before, the term Esna Formation sometimes covers the Lower Formation
as well. Therefore,
the Dakhla Formation
parts.
shales
of
Paleocene
As documented is loosely used and Paleocene Dakhla
the strata
overlying
in
St Paul could not belong to the
between the Nile and Kharga Oasis, Wadi Qena, and the Quseir-Safaga region. A special slump facies of
Abu Rimth Formation but should be correctly attributed to the Southern Galala Formation. As a consequence,
mixed
the Abu Rimth Formation
autochthonous
is defined
and allochthonous
separately
Southern
Galala (see below).
described
sediments
as Abu Rimth Formation
by Bandel
in the
The Serai Formation
was
et al. (I 987) in the Wadi Tarfa
by the conglomeratic Galala Formation
in the Galalas is represented
sandy lithologies
and, hence,
of the Southern
has to be attributed
as
area.
a synonym of the latter. The Abu Rimth Formation is present only in the Southern Galala (Philobbos et al.,
Egma Formation
to the areal extension
Author and type section: Beadnell (I 927) and Hermina and Lindenberg (1989) mention no type section, only
mation
in Hermina and Lindenberg,
the type area (Egma Plateau Stratigraphical
according
the term Abu Rimth Formation
turbidite
layers with reworked
fossils. is present
and northern Sinai. It overlies whereas the top is uncovered.
LATERAL
in the
the
Esna
Abu Rimth Formation The following description and Schmitz
posed
from Phillobbos,
(in Hermina
and Lindenberg,
only
Lindenberg
Schmitz
1989)
and Lindenberg,
and
Galala, south-southwest
of the monastery
Liihology: It is composed
of “well-bedded open marine
and thick olistostrome
carbonates,
including
sand.”
conspicuous
slump structures.
Synonymy:
It is synonymous
members
layers containing
clasts of shall0 w water
reefal limestones,
and displaced
thin
Alveolina
They
may
have
with
the lower
Formation
and
by Said
(1960) and the Thebes Formation (I 987).
of Bandel and Kuss
Discussion:
range
Rimth
Formation
Lindenberg, range
The stratigraphical
of the
(Philobbos
1989) above
collides
et al., in Hermina with
mentioned
244 Journal of African Earth Sciences
water
change
and
the stratigraphical Southern
Galala
belt
at the
14 km to the south only
with
are not
carbonates
to Early Eocene times.
of the
from the Late and are ex-
Galala. At these times,
and Dakhla
were deposited
sediments Formations
the basinal exposed.
at St of the accu-
Sudr and In St Paul,
of the Southern
Galala
only during Late Paleocene
The authors
in St Anthony
interpret
that this
is due to the proximal
position
of St Anthony
Wadi
Araba
High
(NGWA)
in the north that shed shallow
water
sedi-
to the
ments from a carbonate CampaniarVMaastrichtian In area 9, shallow during
water
platform as early as the (Kuss et al., 2000). sediments
were deposited
the Campanian-Maastrichtian (Youssef and Shinnawi,
(Exogyra
cf.
1954; El-Shinnawi,
1967) and were possibly equivalent to the St Anthony Formation. In contrast to area 4 (St Anthony) where the shallow Formation
of the Abu
Sudr
Formations
oveNvesI)
of the Thebes
arrived
Interfingerings
Formation
and Sudr-/
in an east-west-trending
water
Dakhla
facies
and marls with intercalated
abundant larger foraminifers, limestones
of St Paul.
range: Early Eocene
to shelf limestones
middle
deeper
water)
and siliciclastics
Paul (Figs 1 and 3), where
shallow
The type area is the Wadi Abu Rimth in the Southern Stratigraphical
carbonates
rim of the Southern
mulated.
Author and type section: Phillobbos,
OF FORMATIONS
Formation were deposited to the Late Maastrichtian
no such sediments is taken
1989): (in Hermina
TRANSITIONS
water
St Anthony Campanian northern
turbidite
For-
Therefore,
should be abandoned.
St Anthony Formation (shallow Dakhla Formations (deep water) Shallow
The Egma Formation
Lindenberg
Galala
results.
on Sinai).
platform deposits of mediumlimestones with tabular chert
bands, chalky frequent
southern Formation
to the authors’
range: Early Eocene
Lithology: Shallow bedded to massive
Discussion:
19891, which corresponds
of the Southern
water was
Paleocene-Eocene sediments
Cretaceous the
St Anthony
by
shallow
Southern
Galala Formation
with Exogyra cf. overwegi
by the deeper This contrast
Upper overlain
water
chalks
of depositional
water on Sinai,
were overlain
of the Sudr Formation. facies could be explained
Maastrichtian-Early
Eocene litho-biostratigraph
y andpakogeograph
by differences in the vertical movements. While the Northern Galala/Wadi Araba area represents the centre of the Northern western
GalalaNVadi
Araba High, nor-th-
Sinai (area 9) was less affected
by this local
Araba. On both sides, south and north of the Northern Galala/Wadi Araba, similar lithologies with slides, slumps and debris flows are present. The only biostratigraphic
minifers
Galala Formation
water
is deposited
area in the Galalas Faraoun). However,
and parts of Sinai (Hamam its areal extension is far larger
than that of the St Anthony between
in an east-west-trending
the deeper
water
Formation.
Interfingering
deposits
of the Dakhla
and Esna Formations and the shallow of the Southern Galala Formation variations
within
best exposed
water limestones and the lateral
the Dakhla and Esna Formations
at the two
Bir Dakhl sections
are
D2 and
occur
Faraoun
(south)
and evidence
palasotopographic
high between
The sediments the northern Southern
NP5. While southern
the Southern
D3 section
Galala
Formation
is represented
bioclastic wackestones, chalky-dolomitic and thicker ‘Dakhla Formation’ type northerly
D2 section shales.
contrast
shows
thicker
It is assumed
in the two
sections
of the Northern
of the
by thin-bedded
that
limestones shales, the
limestones this
and
lithological
is a result of the closer
Galala/Wadi
Araba carbonate
platform to section D2 (Kuss et al., 2000) contemporary increase of platform-derived
and the carbon-
ates (Figs 8 and 9). An even more pronounced logical contrast is evident Lower Eocene succession.
in Wadi
Sudr
Eocene shallow These sedimentary
(north) the
and Hamam existence
of a
both areas.
Southern Galala Formation (shallow water) and Thebes Group (deep water)
sections,
starts in mid-
Galala Formation.
textures
Serai
Galala Formation
described similar with debris flows, and larger fora-
of the Late Paleocene-Early
Southern
D3 (area 2) that are 6 km apart (Figs 8 and 9). In both the Southern
of area 6 studied
from marls of the Esna Formation.
On Sinai (area 91, Gietl (1998) carbonate dominated successions slumps, intercalated siliciclastics
Southern Galala Formation (shallow water) and Dakhla/Esna Formations (deep water) Similar to the St Anthony Formation, the Southern
position
data from the sections
here are obtained
high.
thinner
y of the northern Gulf of Suez region
attributed
Formation
Galala
(THG)
between
the present
detailed
also
both,
which
was
of the deeper water-derived
on their
as
of basic facies not studied
(Fig. 6). In that case,
Galala Formation
studies
be classified
because
contribution
again, an interfingering Group with the shallow the Southern
(area 6) to the lower
may
Galala Formation
similarities within
at Bir Dakhl (area 2) and at
Northern
water Thebes sediments of
may be deduced
contacts
with
from
the Thebes
Group. Snavely et al. (I 979) mentioned sediments of the lower Thebes Group
that were
posited
with thin
as basin-wide
shallow
water
pelagic
facies
carbonates
the de-
near the basin margins.
litho-
in the Upper Paleocene to In the southern D3 section,
distal equivalents of the Southern Galala Formation are represented only by thin siliciclastic intercalations
HIATUSES In the
AND SYNSEDIMENTARY
study
area,
distinguished,
four
types
characterised
of hiatuses
by variable
can be
duration
and/
within the Esna Formation, whereas in the northern D2 section massive siliciclastic limestones with
or different
internally
Major hiatus from Late Cretaceous to Late Paleocene
reworked
clasts have been deposited
(units
B and D) (Figs 8 and 9). Area
3 (St Paul) is a fine example
basin transition.
Three phases of ramp progradation
were observed deposits
of a ramp-to-
that are indicated
of glides,
slumps
by mass transport
and debris flows.
Micro-
facies analysis provided evidence of a change in the origin of the debris flow deposits that reflect a transition
from a basinal-to-outer-ramp
middle-to-inner-ramp distribution
setting
including
of biota (Scheibner
The lithologies
setting a change
to a in the
et a/., 2000).
of the succession
of the northern
Southern
Galala.
intercalated
interfingering shallow
water
Allochthonous
shallow
with hemipelagic
of limestones platform
derived
water
car-
marls show the from the nearby
of the Northern
Galala/Wadi
mechanisms.
Together
with the nowadays
southern
Northern
affected
by the Syrian Arc deformation
eroded Wadi Araba, the
Galala (area 5) represents
part of Said ‘s (1961) Galala, compressional
Unstable
an area
and hence is
Shelf. In the Northern
deformation
erosion and non-deposition
resulted
in uplift,
during the Late Cretaceous
to Late Paleocene. In the Shabraweet area - 70 km north of the Northern Galala/Wadi Araba, Mohammed and
Omran
(1991)
Campanian-Early
area of the Northern Galala (area 6) are very similar to those of areas 2 (Bir Dakhl) and 3 (St Paul) of the bonates
trigger
TECTONICS
in the
Northern
described
a hiatus
from
the
Eocene similar to the hiatus observed Galala.
On Sinai,
area
7 shows
similarities to area 5 (middle to south Northern Galala) where a large hiatus is evident across the Cretaceous/ Palzogene section occur
boundary
as well (Fig. 4a, b). Except
Ezz El-Orban, only latest Paleocene above
the K/Pg boundary.
(I 960) and Moustafa
According
and Khalil(1995),
for
sediments to Said
the boundary
Journal of Afrxan Earth Sciences 245
C. SCHEIBIVER et al. between
the stable/unstable
shelf lies at Wadi Araba
and north of area 8 (north of Abu Zenima). Thus, this area shouldn’t be affected by the Syrian Arc deformation. However, if it was also affected, the boundary between the stable/unstable shelf should be shifted on Sinai south of the area 7. Another possibility is the presence of a local high with non-deposition for which there is no other evidence yet. Bosworth eta/. (I 999) demonstrated that the Syrian Arc deformation also affected regions in stable intraplate settings, at least as far south as the southern part of the Gulf of Suez (Esh El-Mellaha Range and Gebel Zeit), due to far-field compressional stress. In contrast
to all other areas described,
geneous
tectonic
and depositional
and inhomo-
history.
Probably,
it could be subdivided into more areas: into areas with larger hiatuses across the K/Pg boundary; and areas with continuous
sedimentation.
Together
with the two
sons, the Late Paleocene sedimentation and finally resulted in the P3 hiatus.
exact
foraminifers tions
Tl
depositional
that
Arc deformation.
could
sample
not be mapped
Araba
in detail
due to larger
High
during the Late
MAASTRICHTIAN PALAOGEOGRAPHIC NORTHERN Figure 1 Oa-k illustrates depositional
Gietl,
In secbetween
spacing.
High (Youssef and Shinnawi, 1996;
hiatuses
as resulting from times of non-deor very reduced depositional rates
Cretaceous-Late Paleocene in the Northern Galala, the northwestern Sinai was less affected by the tectonic processes of the Northern GalalaNVadi Araba Kulbrok,
nannoplankton.
I), short
with
on planktic
In contrast
GalalaNVadi
that lead to erosion and non-deposition
based
P5 and P6 occur where parts of upper P5 and lower P6 are missing. These short hiatuses are interpreted,
areas were
by the Syrian
only in sections
controls
and calcareous
may lie in the fact that these affected
evident
and T2 (area
The reason for these different
to the uplift of the Northern
become
biostratigraphic
in this study, position/erosion
histories
processes
Minor hiatuses Short-ranging hiatuses within single biozones are possibly present in all sections. However, these
southern areas, areas 7 and 8, the depositional history of central western Sinai would be even more complex. differently
(P3) of Sinai
Some sections of Wadi Feiran/Abu Zenima (area 8) show a hiatus around P3. The authors assume similar reasons for this hiatus as described for that of the Maastrichtian/Palaaogene boundary. Furthermore, a submarine topographic high may have influenced, in combination with some of the above mentioned rea-
short hiatuses
north-west-
ern Sinai (area 9) has the most complex
Hiatus within the Late Paleocene
1954; El-Shinnawi,
1967;
1998).
settings
and defined
Hiatus across the Maastrichtian/Paleocene A hiatus across the Maastrichtian/Paleocene
boundary boun-
TO PALROGENE EVOLUTION OF THE GULF OF SUEZ the regional
summarised
for calcareous
evolution
of the
for 11 time slices
nannoplankton
biozones.
These time slices were chosen because they best characterise the changing of the depositional environments through time. The CC biozones represent two Maastrichtian time slices, NPI -NP9 represent
dary is evident or inferred in most sections. An exception is St Paul with the presence of the Upper Maastrichtian nannoplankton Micula prinsiizone
the Paleocene and NPl 0-NPI 2 represent the Lower Eocene (compare Fig. 4 and the Paleocene-Eocene
and the Lower
boundary
zone.
Paleocene
The sections
plankton
foraminifer
in St Paul are considered
Pcx
one of
the most complete across the K/Pg boundary in Egypt, although they are very condensed. Lijning ef al. (I998a) ranging
also documented
a very complete
across the K/Pg boundary
Comparable stratigraphical et al., 2000),
lithologies,
on eastern
probably
of the
section Sinai. same
range as area 3 (St Paul) (Scheibner are found on Sinai in area 9 (Hamam
Faraoun: Kulbrok, the sections Wadi
1996; Gietl, El-Seig/Wadi
1998). Hialla
Moreover, (Abbass et
al., 1994) evidenced a Late Cretaceous-Palseogene succession with a stratigraphical range similar
to
the St Paul section of area 3. Elsewhere, a hiatus is present at the K/Pg boundary in most of Egypt and probably resulted from a combination of low sedimentation rates, reworking, patterns and sea level changes
246 Journalof African Earth Sciences
changing circulation (Lijning et al., 1998a).
herein).
In areas
of non-deposition
palaeogeographic of time-equivalent position
occurred,
the time of erosion
or eroded
areas,
the
maps illustrate only the absence sediments today. Whether deor not, is not indicated cannot
be pinpointed
because accurately.
For comparison of palaaogeographic maps and stratigraphy of areas of major uplift, see Fig. 4. Within this stratigraphic/palaeogeographic framework, the Wadi El-Esseila succession (El-Askary and Shaaban, 1993) remains questionable because the stratigraphic subdivision here is in no concordance with the stratigraphic subdivision of the surrounding sections. CC25 (Fig. 7Oal During the middle Maastrichtian biozone CC25, the areas west and north of the northern parts of the Gulf of Suez are characterised
by non-deposition
Maastrichtian-Early Eocene litho-biostratigraphy and pala?ogeograph y of the northern Gulf of Suez region
Depositional Setting and Environmental Regime I-III:
~
ill m
basinal limestones (THG)
III [
basinal marls and shales (EF)
III 1//A
basinal chalks (TF)
III m
basinal marls and shales (DF)
III 0
basinal chalks (SF)
II m
shallow-water limestones (SGF)
ll m
shallow-water limestones, siliciclastics and marls (SAF)
l
non-deposition or eroded
l
m
sections considered in the palaeogeographic maps
o sections not considered in the palaeogeographic maps Figure 10. Regional pages).
palasogeographic
In the Maastrichtian,
the two
maps
of
calcareous
calcareous nannoplankton biozones of NPI-N The first regime with hiatuses reflects uplift
11 time
slices
nannoplankton
from
the Maastrichtian-Early
biozones
10 fcl; were chosen. Three and erosion or non-depositon
of CC25
and
Eocene CC26
different environmental l/1. The shallow water
following
two
(a and bl; and in the Paleocene,
(continued
on the
the
regimes can be distingushed II-Ill). influenced shelf and slope deposits
of the Late Campanian-Maastrichtian St Anthony Formation and the Paleocene-Eocene Southern Galala Formation are the second environmental regime 111). The third regime is represented by the Maastrichtian Sudr Formation and the Paleocene-Eocene Dakhla, Tarawan and Esna Formations and Thebes Group reflecting basinal lithologies IIIIJ. The topographic base-map and the location of sections (with 0 and 01 refer due to non-exposure.
to Fig.
1. 0:
sections
with
stratigraphical
information;
0:
sections
with
no stratigraphical
information,
Journal of African Earth Sciences 247
C. SCHEIBNER et al.
*. . i
,:. :: :.; .3 :‘. I?.’ .,*..
LY: Figure 10. continued. Regional pala?ogeographic Paleocene, the calcareous nannoplankton biozones
248 Journal of African Earth Sciences
maps of 4 out of 11 time slices from the Maastrichtian-Early Eocene. ln the of NPI-NlO Id-g) were chosen. See p. 247 for legend and symbol explanations.
Maastrichtian-Early
Eocene litho-biostratigraph
y and palazogeograph y of the northern Gulf of Suez region
2s
2
a Figure
10.
continued.
Reglonal
palazogeographz
Paleocene, the calcareous nannoplankton biozones See p. 247 for legend and symbol explanations.
maps
of 4 out
of NPl-NPIO
of
11 time
slices
from
the
Ih and II; and in the Eocene,
Maastrichtian-Early NPIO-NPl2
Eocene.
4 and kl were
in the chosen.
Journal of African Earth Sciences 249
C. SCHEIBNER et al. that
may reflect
subaerial
exposures
NP7 (Fig. 10~)
or submarine
swells. At the western Gulf of Suez, these areas coincide with the Northern GalalaANadi Araba High. The stratigraphical range of the Northern Galala/ Wadi Araba hiatuses may reach Turonian-Early Paleocene
(Kuss and Leppig,
1989;
Abd-Elshafy
and
The early part of NPI is, similar to the late part of CC26, a time of non-deposition or erosion in the area of investigation (Strougo et al., 1992; Faris, 1997). The basin configuration of the Southern Galala Sub-basin is very similar to that of CC26. It encompasses the St
Atta, 1993). The eroded sediments derived from this area were mainly transported southward, where they were deposited as chalky limestones, marls and sandstones of the St Anthony Formation in the northern parts of the Southern Galala (St Anthony and Gebel Thelmet sections in Fig. 4a).
Paul area in the west to the west central Sinai in the east, but the prevailing lithologies changed in time. Instead of chalks of the Maastrichtian Sudr Formation, marls and shales of the Dakhla and DakhlaRarawan/Esna Formations were deposited in the Early Paleocene.
North
NP2 (Fig. IOdl
of the Northern
Galala/Wadi
Araba,
no sedi-
ments of the St Anthony Formation are present, only the deeper water chalks of the Sudr Formation
During
NP2 times,
Galala
Sub-basin)
(Wadi Nooz: this work;
Dakhla and Dakhlaflarawan/Esna
1996).
The Northern
isolated
island
sediments
Gebel Urn Makhasa: Galala/Wadi
surrounded
that interfinger
Formation.
of the Northern El-Askary
an
water
marly chalks
water
Sudr Formation
and
In addition
to the uplifted
area
GalalaNVadi
of non-deposition
formed
shallow
with chalks,
and marls of the deeper Dakhla
Araba by
Kulbrok,
Araba,
two
local areas
occur on Sinai (Wadi El-Esseila
and Shaaban,
1993)
the established with
Paul to the western figuration.
area)
of the from St
in the same con-
marls of the Dakhla Formation
in the Wadi Tarfa area. All other areas
in the northwest El-Orban
Formations
Sinai remains
Additionally,
were deposited
basin (Southern
the marls and shales
(NGWA) are still
and in the southeast exposed
or areas
(Ezz
of non-
deposition.
of
and in the south
of
NP3 (Fig. 1Oe)
the investigated area (Ezz El-Orban, Morgan 8 and HI of Masters, 1984). It is not clear, whether these two areas were truly exposed islands, local highs
In NP3, the two isolated basins, both parts of the Southern Galala Sub-basin with marls of the Dakhla Formation, were connected through the Bir Dakhl area.
with non-deposition erosion.
Similar to NP2, the Northern GalalaNVadi Araba and the Ezz El-Orban areas remain areas of non-deposition.
or only
the
result
of
later
distribution
is least clear within poor biostratigraphic calcareous (I 978a, were
of the depositional
data of Abdelmalik
197813) and Marzouk relied
upon.
do not offer a better A. mayaroensis
settings
this time slice because of the data. On western Sinai, the
nannoplankton
mainly
wer NP5 (Fig. 1Of)
NP4-lo
CC26 (Fig. 1Obl The regional
and Hussein
The planktic
biostratigraphic
Zone
covers
(1994)
GalalaANadi
Araba in the Wadi Nooz area (this work)
marly sediments Esna Formations
part
as the
of CC25,
Upper NPS-lo wer NP7/8 During
this interval,
and the index fossil A. mayaroensis is very rare in southern Egypt (Luger et al., 1998). In most sec-
Southern
tions
progradation,
time
in this area, interval
to the
ranging
Early
deposition
as well
Paeocene
and/or
from
as in most the upper
is probably
exposure.
of Egypt,
the
part of CC26 a time
During the latest
trichtian, chalks, marly chalks deeper water Sudr and Dakhla
and marls Formations
of non-
(FQ. 1Og)
shallow
Galala Formation
water
prograded
deposits
of the
(Scheibner et a/. ,
2000). Slumps and debris flows evidence the south-ward extending
starting
towards
and progressing
from
the
Southern
Galala,
the south to the area of Bir Dakhl
towards
the north to the area of Wadi
Maas-
Nooz. This ramp progradation
of the were
sea level drop at the base of P4 (within NP5), as Scheibner et al. (2000) demonstrated in the area of St Paul (area 3) and Liining et al. (I 998a) on Sinai.
deposited within a basin that extends from the St Paul/Bir Dakhl area in the west to the west central Sinai in the east (e.g. St Paul area: see this work; Wadi El-Seig/Hialla: Abbass et a/., 1994; Matulla and Nuhkl: Marzouk and Hussein, 1994). It is not clear whether the shallow water sediments of the St Anthony Formation were deposited in the Southern Galala or not.
250 Journal of African Earth Soences
of the Dakhla and Dakhla/Tarawan/ prevail.
foraminifers
solution,
also
et a/.
The configuration of the Southern Galala Sub-basin remains the same. Additionally, north of the Northern
was initiated
by a main
Speijer and Schmitz (I 998) reconstructed a palaeodepth curve of that interval based on studies of benthic foraminifers from Gebel Aweina (ca 300 km to the south). These authors also concluded that a sea level drop occurred during lower P4. In the Southern Galala Sub-basin, the marls and shales of the Dakhla or Dakhla/Tarawan/Esna Formations were deposited.
Maastrichtian-Early
Eocene litho-biostratigraphy
Upper NP 7/84ower During
these
andpalieogeography
include chalks of the Sudr Formation
NP9 (Fig. 7Oh)
biozones,
the chalks
of the Tarawan
Formation were deposited in the south and east of the Northern Galala/Wadi Araba, although on Sinai, the Tarawan Formation is very thin or even missing. Here, the many sediments of the Dakhla/Tarawan/ Esna Formation were deposited. The shallow water sediments of the Southern Galala Formation were deposited now on parts of the Northern Galala, and in the south (Ras Gharib) the area of non-deposition becomes smaller. Anan (1992) and Lining et al. (1998a)
concluded
that the Tarawan
Sinai was deposited
of the northern Gulf of Suez region
Formation
on
during a series of low sea levels.
tian, shaley-marly
sediments
Dakhla/Tarawan/Esna informal formation), Tarawan Formation
in the Maastrich-
of the Dakhla,
Formations
Esna and
(a newly introduced
and chalks and limestones of the in the Paleocene to Early Eocene.
The basinal sediments of the Sudr, Dakhla and Esna Formations interfinger near the structural high of the Northern Galala/Wadi Araba High. This high was subaerially exposed during the Late Cretaceous to Early Eocene. The shallow water slope deposits of the St Anthony and Southern Galala Formations were deposited south of this high, whereas north of the high only the sediments of the Southern Galala Formation
Luger (1985) and Speijer and Schmitz (I 998), on the other hand, reported from southern Egypt that the
came to deposition. Other local highs
sediments
during sea level highstands.
erosion are present on northwest Sinai. In particular, the high around
Upper NP 9-/o wer NP 70 (Fig. 7Oil
indicate that the boundary between the stable unstable shelf on the Sinai lies farther south.
of the Tarawan
The basin configuration
Formation
were deposited
of the Southern
Galala Sub-
basin stays the same, but the lithological character changes again. Now, the marls and shales of the Esna and
the
Dakhla/Tarawan/Esna
deposited.
North of the Northern
the sediments
of the Southern
Formations
were
Galala/Wadi
Araba,
Galala Formation
as far east as Gebel Urn Makhasa
(Kulbrok,
that
led to non-deposition
or
and southwest Ras Gharib could and
Four different types of hiatuses could be distinguished, characterised by varying duration and/or different mechanisms (e.g. sea level changes). At least the palaeogeographical change within calcareous nannozone
NP5 resulted
from a main sea level drop.
reach 1996). ACKNOWLEDGEMENTS
Upper NP IO-lower During this interval, Formation
dominate
Wadi Araba.
of the Southern
the areas of the Northern
The only
the northwestern
1996;
1992).
Galala Galala/
area of non-deposition
Sinai (Wadi Sudr: Gietl,
Sudr: Kulbrok, Zalat,
NP7 I (Fig. 1Oj) sediments
Mitla
Pass: Abdel
For the first
time,
is on
1998;
Ain
Gawad
and
sediments
of the
Dakhla and Dakhla/Tarawan/Esna Formations were deposited in the area of Ras Gharib, which could be part of a basin
Said (1990)
described
in the Early
Eocene around Abu Zenima. UpperNP
1 l-NP12
The difference the deposition
of the limestones
in the Southern and shales Formations. suggested during
(Fig. 1Ok)
from this to the previous
time slice is
of the Thebes Group
Galala Sub-basin
instead
of the marls
Shahin that
(1990)
Palaeogeographic
Group
was
deposited
sea level.
changes
with sample preparation. The investigations were funded by the Graduiertenkolleg ‘Stoff-F&se in marinen Geosystemen’ of the University of Bremen and the German Science Foundation (DFG). Editorial handling -P. Bo wden
regimes:
basinal
sediments;
H.L.
El-Dawy,
trichtian-Early Central Sinar
in the Maas-
in the surrounding
Gulf of Suez based on three environ-
and non-deposition.
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