http://france.elsevier.com/direct/GEOBIO
Geobios 40 (2007) 445–454
Original article
New biostratigraphic data from Cretaceous planktic foraminifera in
Sahlabad province, eastern Iran
´ `
Nouvelles donnees biostratigraphiques des foraminiferes planctoniquesdu Cretace dans la province de Sahlabad, Iran oriental
Seyed Ahmad Babazadeh a,*, Francis Robaszynski b, Marie Denis Courme c
a Birjand Payame-noor University, Birjand, Iranb Faculte polytechnique de Mons, 9, rue de Houdain, 7000 Mons, Belgium
c 6, rue Porte-Vendomoise, 45190 Beaugency, France
Received 14 March 2006; accepted 1 August 2006
Abstract
The foraminiferal content of two stratigraphic sections, located in eastern Iran within the Sahlabad province, between the Lut and Afghan
blocks and ranging in age from Turonian to Campanian is investigated. Previous studies were general and only indicated the presence of planktonic
foraminifera in this province. This paper presents a detailed study of planktonic foraminifera of the Shirshotor unit and establishes for the first time
a local biostratigraphy consisting of five biozones. Biozones from the upper Turonian to lower Campanian are recognized, but the upper lower
Campanian to lower upper Campanian strata are missing, as demonstrated by the lack of the Globotruncana ventricosa biozone. Tectonic activity
in this region during the late early Campanian and mid-Campanian resulted in the presence of an unconformity together with debrites (debris flow
deposits) in the lower upper Campanian. About twenty-five planktonic foraminiferal species are reported and illustrated. The largest faunal
diversity is encountered in the upper Santonian. The planktonic foraminiferal biozones are precisely defined in selected stratigraphic sections and
allow age determinations for the deepest marine sediments (pelagic limestones and bedded cherts) before the collision of the Lut and Afghan
blocks.
# 2007 Published by Elsevier Masson SAS.
Resume
Des series stratigraphiques situees en Iran oriental, dans la province de Sahlabad entre le bloc de Lut et le bloc afghan, ont livre des
foraminiferes. Leur etude, dans deux coupes, a permis de les dater du Turonien au Campanien. Les travaux anterieurs signalaient seulement la
presence de foraminiferes planctoniques dans cette zone de suture. Cet article presente une etude detaillee des foraminiferes planctoniques de
l’unite de Shirshotor et definit, pour la premiere fois, une biostratigraphie locale comportant cinq biozones. Les biozones du Turonien superieur au
Campanien inferieur sont en continuite, mais l’absence de la biozone a Globotruncana ventricosa atteste d’une lacune depuis les niveaux
superieurs du Campanien inferieur jusqu’aux niveaux de base du Campanien superieur. L’activite tectonique de cette region, durant le Campanien
inferieur terminal et le Campanien moyen, se manifeste par la presence d’une discordance associee a des debrites (coulees boueuses ou debris-
flows) au cours du Campanien superieur basal. Environ 25 especes de foraminiferes planctoniques sont signalees et illustrees. La plus grande
diversite s’observe dans le Santonien superieur. Les biozones de foraminiferes planctoniques sont definies de facon precise dans des coupes
stratigraphiques choisies et permettent de dater les sediments les plus profonds (calcaires pelagiques et cherts lites), avant la collision des blocs de
Lut et Afghan.
# 2007 Published by Elsevier Masson SAS.
Keywords: Planktic foraminifera; Cretaceous; Sahlabad province; Eastern Iran
Mots cles : Foraminiferes planctoniques ; Cretace ; Province de Sahlabad ; Iran oriental
* Corresponding author.
E-mail address: [email protected] (S.A. Babazadeh).
0016-6995/$ – see front matter # 2007 Published by Elsevier Masson SAS.
doi:10.1016/j.geobios.2006.08.002
S.A. Babazadeh et al. / Geobios 40 (2007) 445–454446
1. Introduction
The studied area (Shirshotor region) is situated in eastern
Iran within the Sistan Ocean that is between two blocks: the Lut
in the west and Afghan in the east. The Sistan Suture Zone
(Tirrul et al., 1983), is part of Cenozoic Alpide suture of Sengor
et al. (1988), and is subdivided into two provinces: Gazik and
Sahlabad provinces in north-central part of Sistan Ocean
(Babazadeh, 2003). The Shirshotor region is situated in the
northern part of this suture at the Sahlabad Province. The study
area is located between 598560 to 598580E longitude and 328140
to 328170N latitude (Fig. 1).
The planktic foraminifera in the Upper Cretaceous
sections of eastern Iran were rarely studied in previous
works (Stocklin et al., 1972; Tirrul et al., 1983; Fauvelet and
Eftekhar-nezhad, 1990). In this paper the stratigraphy and
micropalaeontological investigation of outcrop samples,
collected in measured sections from the Tethyan Sistan Ocean,
in the Shirshotor region, are presented and discussed. The
material is composed of 55 samples which all have been
examined in thin section.
The aim of this paper is to present Upper Cretaceous
biostratigraphic data that allows reconstruction of the
palaeogeography of this region during the Late Cretaceous.
Fig. 1. Geologic map of Shirshotor region and the location of studied sections (Eft
2. Regional setting
Iran is a part of short sections of the Alpine orogenic belts
that is located between the Arabian–African Block (Gondwana
margin) and the Asian Plate (Eurasia margin). It is interpreted
as an assemblage of marginal Gondwana fragments detached
from the Gondwanian–Arabian plate during the late Paleozoic
(Permian) or early Triassic (Stocklin, 1977). It has been
attached to the Turanian (Eurasia) Plate at the end of middle or
late Triassic (Stocklin, 1974, 1977; Sengor and Kidd, 1979;
Wensink and Varekamp, 1980; Soffel and Forster, 1980;
Davoudzadeh and Schmidt, 1982). In the late Cretaceous, Iran
again rejoined with the Gondwanian Afro–Arabia plate, but the
ocean area was not completely closed as evidenced by the
presence of Cretaceous-Tertiary flysch deposits in eastern Iran
(Babazadeh, 2003).
Three major tectonic units (Turanian, Iranian and Arabian
plates) recognized by Lensch et al. (1984) in Iran, are separated
from each other by ophiolitic complexes (Stocklin, 1977)
(Fig. 2). These are subdivided into smaller elements, such as
Kopet Dagh, Southern Caspian Sea, Zagros Thrust, Zagros
folded Belt, Alborz mountain and Central Iran. The Central Iran
comprises Sanandaj–Sirjan Belt, Orumiyeh–Dokhtar Belt,
Central-East-Iran microplate (Davoudzadeh and Schmidt,
ekhar-nezhad and Stocklin, 1974), Ksh: Shirshotor section; Ch: Chatot section.
Fig. 2. Modified sketch map of Iran showing the major tectonic units, the inner nucleus and the positions of the main ophiolites (Lensch et al., 1984; Sengor et al.,
1988; Stocklin, 1977; Dilek and Delaloye, 1992; Babazadeh, 2003).
S.A. Babazadeh et al. / Geobios 40 (2007) 445–454 447
1981), the latter is subdivided into Yazd, Tabas and Lut blocks
(Fig. 2).
There are the remnants of oceanic basin that separated
segments of the Alpine belt. The three components of the inner
microcontinental nucleus (formerly termed the Lut block by
Stocklin, 1968), including the Yazd, Tabas, and Lut blocks, are
separated by fracture zones and have been rearranged from their
original position (Sengor et al., 1988).
In Central Iran, there are two ophiolite belts that include
melanges and deep marine sedimentary rocks: (I) one of these
ophiolite complexes extends from Esfandagheh to the Nain area
and along the Great Kavir Fault to the extensive ophiolitic
melange exposures around Sabzevar and (II) the second major
belt, the Sistan Suture Zone (Sistan Ocean), branches from the
central Makran Ranges northward to the Birjand area, but does
not join the melange of the Sabzevar Zone (Stocklin, 1977)
(Fig. 2). The ophiolite-flysch range in the Sistan suture zone
belonging to the second belt is subdivided into two provinces:
the Gazik and Sahlabad provinces in the north-central part of
the Sistan Ocean. The studied area is situated within this ocean,
at the Sahlabad Province (Babazadeh, 2003).
3. Lithology
Most sedimentary outcrops across the Upper Cretaceous in
eastern Iran consist of three facies: a mixture of deep and
shallow sedimentary rocks, turbidites (flysch) and reefs. This
paper discusses the deep oceanic sedimentary rocks as basin
facies and sedimentation depends on the amount of influx of
fine argillaceous, calcareous and siliceous material together
with the plankton rain. In the Shirshotor unit (informal
lithostratigraphic subdivision), these rocks were deposited
Fig. 3. Correlation chart for the two studied sections in the Shirshotor region.
S.A. Babazadeh et al. / Geobios 40 (2007) 445–454448
S.A. Babazadeh et al. / Geobios 40 (2007) 445–454 449
during the opening of an oceanic area between the Lut and
Afghan blocks. In order to develop a comprehensive biostrati-
graphic record of the planktonic foraminifera, the Shirshotor
and Chatot sections located in this area, were examined (Ksh
and Ch, respectively in Fig. 1).
In general, the Shirshotor unit is divided in two members:
Member I consists of sedimentary and volcano-sedimentary
lithologies and Member II is made of re-sedimented deposits.
3.1. Shirshotor section
In this section, the Shirshotor unit includes only Member I,
which is mainly composed of sedimentary and volcano-
sedimentary lithologies (Fig. 3).
Above tuffs and diabases, the sequence begins with a
succession of gray to cream bedded micritic limestones and
argillaceous limestones contains radiolaria and planktonic
foraminifera. It passes upward to the limestones and red
radiolarian cherts with the intercalated layers of volcano-
sedimentary rocks. The volcano-sedimentary rocks consist of
green vitric tuffs, radiolarian tuffs and tuffaceous sandstones.
The upper part consists of gray to cream fine-grained
limestones without volcano-sedimentary rocks. The thickness
of the Shirshotor section reaches about 64 m. This unit
conformably overlies the tuffs and diabases of Late Cretaceous
age (Cenomanian?) and is covered by a conglomerate layer.
3.2. Chatot section (Fig. 3)
In contrast with the preceding one, the Chatot section is
composed of both Members I and II. At the base of Member I,
there are bedded volcano-sedimentary rocks (green tuffs) with
underlying breccia and intercalations of red radiolarian cherts.
This sequence continues with gray limestones containing
radiolaria and planktonic foraminifera. The upper part of
Member I is dominated by the bedded limestone, such as in the
Shirshotor section. The thickness of Member I is 85 m. The top
of the sequence is unconformably overlain by a conglomeratic
horizon passing upward to a debris flow deposit (debrite)
assigned to Member II. The latter consists of mixed lithologies
ranging from sandy mudstones to boulder-sized clasts to a
bouldery mass containing mud. This deposit is an ‘‘olistos-
trome’’. The planktonic foraminifera are found in the
mudstone. The thickness of Member II attains 115 m; it is
composed of three parts. Each part begins with a muddy gravel
body resulting from proximal currents with high density (Lowe,
1979), changes to medium grained carbonate turbidites
(Meischner, 1964), and is terminated by argillaceous lime-
stones and biomicrites. This cycle is repeated three times in this
resedimented unit. The lower and upper contacts of the section
are faulted. The total thickness of the Shirshotor unit is 200 m in
the Chatot section.
4. Biostratigraphy
The Shirshotor unit was deposited in a deep marine
environment and it is more accurately dated with the succession
of index planktonic foraminiferal species. Also, the presence of
a well-preserved globotruncanid assemblage makes this region
important for biostratigraphic studies.
4.1. Zonal subdivisions
Five biozones have been identified on the occurrence of
index planktonic foraminifera in the Shirshotor unit (Figs. 4 and
5). Four biozones are recognized from the upper Turonian to the
Lower Campanian in the Shirshotor section and five biozones
are distinguished in the Chatot section. Identification of
specimens is based on microscopic observations of thin
sections (Fig. 6). The definitions of the biozones are given
following the works of Caron (1985), Sliter (1989), Premoli
Silva and Sliter (1994) and Robaszynski and Caron (1995).
� B
iozone A: Marginotruncana sigali ZoneAge: Late Turonian.
Definition: Interval zone between the last occurrence
(LO) of Helvetoglobotruncana helvetica (supposed) and the
first occurrence (FO) of Dicarinella concavata.
Remarks: The diversification of Marginotruncana and the
presence of the large, compressed marginotruncanids
(Marginotruncana undulata) (Sliter, 1989) fall within this
zone. This interval is also known as Marginotruncana
schneegansi zone (Sliter, 1989; Robaszynski and Caron,
1995). This zone includes: Hedbergella delrioensis, Margin-
otruncana sigali, Marginotruncana schneegansi and Margin-
otruncana renzi.
In the Shirshotor section, from bed of nos. k-sh-1 to k-sh-8,
this interval contains Marginotruncana cf. renzi, M. cf.
schneegansi, M. sigali, Dicarinella cf. primitiva and
Hedbergella cf. simplex.
In the Chatot section, from bed of nos. Ch1 to Ch2, this
interval contains Marginotruncana sigali, Dicarinella cf.
primitiva, Gavellinella sp.
� B
iozone B: Dicarinella concavata ZoneAge: Latest Turonian to Early Santonian.
Definition: Interval zone between the FO of Dicarinella
concavata and the FO of Dicarinella asymetrica.
Remarks: This zone contains the LO of Marginotruncana
sigali and the FO of Contusotruncana near the upper
boundary. In this zone, the dominant taxa belong to the genus
Marginotruncana (e.g., M. marginata, M. renzi, M. sinuosa,
M. pseudolinneiana) and Dicarinella concavata. The species
Contusotruncana fornicata and Hedbergella sp. are rare.
In the Shirshotor section, from bed of nos. k-sh-9 to k-sh-
11. The age of this succession is given on the basis of the
assemblage Dicarinella concavata, Marginotruncana sigali,
M. sinuosa, M. cf. pseudolinneiana and Contusotruncana
fornicata.
In the Chatot section, from bed of nos. Ch3 to Ch5. This
interval yields Dicarinella concavata, Marginotruncana
sinuosa, M. sigali, M. marginata, M. cf. pseudolinneiana
and M. coronata.
� B
iozone C: Dicarinella asymetrica ZoneAge: Santonian.
Fig. 4. Planktonic foraminiferal distribution from the Shirshotor section.
S.A. Babazadeh et al. / Geobios 40 (2007) 445–454450
Fig. 5. Planktonic foraminiferal distribution from the Chatot section.
S.A. Babazadeh et al. / Geobios 40 (2007) 445–454 451
Fig. 6. Cretaceous planktonic foraminifera from Shirshotor unit. All materials are from the two sections. 1. Globotruncana arca (Cushman), K-sh-16, early
Campanian, �55. 2. Globotruncana bulloides Vogler, Ch8, early Campanian, �55. 3. Globotruncana linneiana (D’Orbigny), Ch9, early Campanian, �55. 4.
Globotruncanita cf. calcarata (Cushman), Ch20, middle-late Campanian, �55. 5. Globotruncanita stuartiformis (Dalbiez), Ch20, middle Campanian, �45. 6.
Globotruncanita stuarti (De Lapparent), Ch19, middle Campanian, �45. 7. Globotruncanita cf. elevata (Brotzen), Ch20, middle Campanian, �45. 8. Margin-
otruncana coronata (Bolli), Ch3, Coniacian, �45. 9. Marginotruncana sigali (Reichel), K-sh-5, late Turonian, �55. 10. Dicarinella asymetrica (Sigal), Ch6,
Santonian, �55. 11. Marginotruncana cf. pseudolinneiana Pessagno, Ch3, Coniacian, �45. 12. Dicarinella concavata (Brotzen), Ch7, Santonian, �55. 13.
Hedbergella holmdelensis Olsson, Ch7, early Campanian, �55. 14. Marginotruncana cf. schneegansi (Sigal), Ch3, Coniacian, �80, 15. Dicarinella cf. primitiva
(Dalbiez), K-sh-8, late Turonian, �80.
S.A. Babazadeh et al. / Geobios 40 (2007) 445–454452
Definition: The total range of the nominal species (Sigal,
1977; Sliter, 1992; Robaszynski and Caron, 1995).
Remarks: The upper boundary of this zone coincides
with the extinction of Dicarinella. The marginotruncanids
tend to become rare except for M. pseudolinneiana and
M. coronata, whereas M. renzi and M. sigali become extinct
before this zone. In this zone: Dicarinella asymetrica,
D. concavata, Contusotruncana fornicata, Marginotruncana
S.A. Babazadeh et al. / Geobios 40 (2007) 445–454 453
coronata, M. marginata and M. pseudolinneiana can be
found.
In the Shirshotor section, from bed of nos. k-sh-12 to
k-sh-15. The faunal assemblage observed in the entire interval
is as follows: Dicarinella asymetrica, Contusotruncana
fornicata, Marginotruncana coronata, M. undulata and
M. marginata.
In the Chatot section, from bed of nos. Ch6 to Ch7-2. The
faunal assemblages is represented by Dicarinella asymetrica,
D. concavata, Marginotruncana marginata, M. cf. pseudo-
linneiana, Contusotruncana fornicata, Hedbergella flandrini
and H. holmdelensis.
� B
iozone D: Globotruncanita elevata ZoneAge: Early Campanian.
Definition: Zone defined by the FO of Globotruncanita
elevata.
Remarks: This zone is characterized by the presence of
Globotruncanita elevata, Globotruncanita stuartiformis
associated with Globotruncana arca, Globotruncana linnei-
ana, Globotruncana bulloides and Contusotruncana for-
nicata.
In the Shirshotor section, from bed of nos. k-sh-16 to
k-sh-22. This interval yields Globotruncanita elevata,
Globotruncanita stuartiformis, Globotruncana arca, Globo-
truncana lapparenti, Globotruncana bulloides, Globotrun-
cana linneiana and Contusotruncana fornicata.
In the Chatot section, from bed of nos. Ch7-3 to Ch9. This
interval contains Globotruncanita elevata, Globotruncanita
stuartiformis, Globotruncana arca, Globotruncana bul-
loides, Globotruncana linneiana and Contusotruncana
fornicata.
� B
iozone E: Globotruncana ventricosa ZoneAs the succession is truncated by an olistostrome this
biozone is lacking.
� B
iozone F: Globotruncanita calcarata ZoneAge: Early Late Campanian.
Definition: It is defined as total range zone of
Globotruncanita calcarata.
Remarks: The planktonic foraminifera assemblage of this
zone includes Globotruncanita stuarti, Globotruncanita
calcarata, Globotruncana arca and Contusotruncana for-
nicata.
In the Chatot section, from bed of nos. Ch10 to Ch25. It is
dated by the presence of Globotruncanita calcarata and
Globotruncanita stuarti.
5. Conclusions
The planktonic foraminifera assemblages from the upper
Cretaceous of eastern Iran belong to the Tethyan warm water
bioprovince, which is characterized by diverse keeled associa-
tions rich in thick-walled species. This assemblage is composed
of representatives of the genera Marginotruncana, Globotrun-
cana and Globotruncanita.
Five planktic foraminiferal biozones have been identified in
the Shirshotor area. In ascending order they are Biozone A
(Marginotruncana sigali Zone), Biozone B (Dicarinella
concavata Zone), Biozone C (Dicarinella asymetrica Zone),
Biozone D (Globotruncanita elevata Zone) and Biozone F
(Globotruncanita calcarata Zone). A distinct unconformity has
been identified in the Shirshotor unit (section B). This
unconformity is here correlated with a major tectonic activity
of the Laramide Orogeny.
The succession of planktic foraminiferal assemblages in
the Shirshotor unit shows a continuity of the sedimentation
during the Late Cretaceous from the late Turonian to early
Campanian, but during the late-early Campanian and middle
Campanian, there is sedimentary gap evidenced by the lack of
the Globotruncana ventricosa Zone. There is no record of
Maastrichtian biozones such as: the Gansserina gansseri and
Abathomphalus mayaroensis Zones in any of the two studied
sections.
The age of the resedimented deposits or Member II in the
section B formerly attributed to the Eocene (Eftekhar-nezhad
and Stocklin, 1974), on the basis of the new data is changed to
early late Campanian.
Acknowledgements
The first author thanks M.F. Hassani, chairman of Birjand
Payame-noor University for fieldwork facilities. We are
grateful to Dr. J.P. Bellier for helpful suggestions and his
critically reading of the manuscript.
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