Biostratigraphy Study of Tarbur Formation
Transcription
Biostratigraphy Study of Tarbur Formation
Journal of Earth Science, Vol. 25, No. 2, p. 263–274, April 2014 Printed in China DOI: 10.1007/s12583-014-0431-9 ISSN 1674-487X Biostratigraphy Study of Tarbur Formation (Upper Cretaceous) in Tang-E Kushk and East of Sarvestan (SW of Iran) Massih Afghah*, Shohreh Yaghmour Geology Department of Islamic Azad University, Shiraz Branch, Shiraz, Iran ABSTRACT: In this study, 465 m of Tarbur Formation in Tang-e Kushk and east of Sarvestan area stratigraphic sections are studied and 185 thin sections are provided and analyzed. Based on lithostratigraphic studies, Tarbur Formation in these two stratigraphic sections is divided into upper and lower parts. Lower part includes medium-bedded rudist limestones which is consist of iron nodules with Gastropoda. Upper part is made of light grey massive organodetrital limestone. Identified foraminifers of both studied sections are comprised of: Orbitoides media, Orbitoides triangularis, Orbitoides tissoti, Orbitoides orientalis, Orbitoides apiculata, Antalyna korayi, Rotalia skourensis, Dicyclina schlumbergeri, Nezzazatinella sp., Omphalocyclus macroporus, Trochospira sp., Siderolites calcitrapoides, Broeckinella sp., Lepidorbitoides socialis, Gavelinella pertusa, are detected, and also it has Dasycladacea of Salpingoporella dinarica, Salpingoporella turgida, Salpingoporella sp.. According to diagnosed foraminifera, the age determination of Tarbur Formation is assigned to Upper Maastrichtian. KEY WORDS: Maastrichtian, Tarbur Formation, biostratigraphy, foraminifera, Zagros, Iran. 1 INTRODUCTION Upper Cretaceous succession of the Zagros Basin is so significant because of variation of litho and biofacies. Discrepancy between lithostratigraphic data and biostratigraphic limit in various stratigraphic sections have been recorded in Fars Platform before (Afghah and Farhoudi, 2012). Upper Cretaceous succession was described in Zagros Basin, Fars area as Tarbur Formation by James and Wynd (1965) which is composed rudist limestone. The age determination of Tarbur Formation is assigned to Campanian-Maastrichtian by their work. It should emphasize that the age determination of the Tarbur Formation has been provided by rudists. Actually rudist fragments are well distributed in Tarbur limestone which are associated with foraminifers. Askari et al. (2012) identified rudist taxa in Central Zagros region. According to Askari et al. (2012), Praeradiolites plicatus, Sauvagesia cf. somalica, Bornonia anatolica, Hippurites cornucopiae have recorded from Tarbur Formation. Based on their study, the Tarbur Formation is assigned to Maastrichtian. Other studies support that the Tarbur limestone is related to different ages in various stratigraphic sections (Afghah and Farhoudi, 2012; Afghah, 2005; Khosrow and Afghah, 2004). Then various biostratigraphic limits of the Tarbur outcrops have great support for reconstruction of paleogeographic interpretation of studied area during Upper Cretaceous. However foraminifer biostratigraphy is common method to determine biostratigraphic limits of Zagros rock units *Corresponding author: [email protected] © China University of Geosciences and Springer-Verlag Berlin Heidelberg 2014 Manuscript received April 23, 2013. Manuscript accepted November 12, 2013. particularly in Tarbur Formation. Since Tarbur Formation is well distributed in narrow line which is parallel to Zagros main thrust fault (Afghah, 2010), therefore establishment of biozones so significant for completely biostratigraphic data of Tarbur rudist limestone. Tarbur rudist is distinguished between Gurpi (at the base) and Marl of Sachun (on the top) formations. Many workers have documented an iron nodule zone between Tarbur and Sachun formations as erosional period (Khosrow and Afghah, 2004; James and Wynd, 1965). The upper limit of this formation is usually selected from the anhydrite horizon base or marly limestone sequence of Sachun Formation basal part (Arzaghi et al., 2012). Evaporites of Sachun is not common in all exposures along Fars Platform, generally marls and limy marls are observed in eastern of Shiraz area. Importance of biostratigraphic study of the Tarbur Formation in Tang-e Kushk and east of Sarvestan stratigraphic sections supports regional aspect of geologic setting and paleogeographic reconstruction of Upper Cretaceous strata along study area. Furthermore comparison of biostratigraphic data of mentioned area with other stratigraphic section which are located in other part of Zagros led us to interpret paleoenvironmental condition of the Tarbur Formation. 2 GEOGRAPHICAL AND GEOLOGIC SETTING The studied stratigraphic sections are located between geographical coordination such as: 53°N to 54°N and 22°30'E to 29°00'E which are located in eastern Shiraz City (Fig. 1). Geographic coordination of Tang-e Kushk stratigraphic section is related to 29°23'8''N and 53°21'34''E and Sarvestan stratigraphic section locality is situated at geographic coordination (29°17'45''N and 53°15'15''E). Based on Iran structural division (Stoecklin, 1968), the studied stratigraphic sections are located within Zagros folded zone. Alavi (2004) have confirm tectonic Afghah, M., Yaghmour, S., 2014. Biostratigraphy Study of Tarbur Formation (Upper Cretaceous) in Tang-E Kushk and East of Sarvestan (SW of Iran). Journal of Earth Science, 25(2): 263–274, doi:10.1007/s12583-014-0431-9 264 Massih Afghah and Shohreh Yaghmour 29o28'N Caspian Sea N Shiraz 52o54'E 29o38' Dariyan Iran Kherameh Shiraz Tang-e Kushk rs ia n G ul f Sarvestan 0 8.6 km 53o12'E Pe Figure 1. Location map of the studied stratigraphic sections, each stratigraphic section is represented by star. zonal classification similar Stoecklin (1968). Based on James and Wynd (1965) both stratigraphic sections are located in interior Fars area. 2.1 History of Tarbur Formation Studies Tarbur Formation was firstly studied by James and Wynd (1965) have selected type section of the Tarbur Formation. A collection of rich-rudist deposits have been expanded in the south east of Tethys during Campanian–Maastrichtian time, which is called Tarbur Formation in Zagros zone (Motiei, 1992). Based on Kalantari (1976) the Tarbur Formation has comprised of a row of dark gray or brown crystalline limestone along with argilltic and organodetrital limestone with intercalation gray calcareous silty shales, and finally, grey organodetrital dolomites. His biostratigraphic study has been reflected Maastrichtian age of Tarbur Formation. Moosavi and Askari (2008) had studied biostratigraphgy of Tarbur Formation in Dorahan (Charmahal & Bakhtiyari Province). Afghah and Khosrow (2004) had studied and analyzed lithostratigraphic units and depositing environment of Tarbur Formation in the northeast and southeast of Shiraz. Based on their study, Tarbur limestone is divided into two distinct lithostratigraphic units. They believe that the reefs of Tarbur Formation in the interior Fars with regard to their bedding in sedimentary basin are tidal continental margin reef. Also, microbiostratigraphy, microfacies, and sedimentary environment of Tarbur Formation in the south east of Shiraz have been analyzed by Afghah and Yousefzadeh (2006). Lithostratigraphic subdivisions of the Tarbur Formation was finalized in Fars area by Afghah (2009). 3 METHODS AND MATERIALS In order to biostratigraphy study in eastern Shiraz two stratigraphic columns were selected. Lithostratigraphic limits of both sections were determined by field work. Over 250 samples were collected. Stratigraphic distribution of lithofacies are marked. By 1 : 250 000 map of National Iranian Oil Co. tectonic setting and other lithostratigraphic units are studied particularly trend of major faults. Thin sections are provided from collected samples. In order to identification of foraminifers, we used Afghah and Farhoudi (2012), Dieni (2010), Çaglar (Kaya) and Önal (2009), Georgescu and Almogi-Labin (2008), Khosrow and Afghah (2004), Permoli and Verga (2004), Abdelghany (2003), Permoli et al. (1995), Kalantari (1994, 1976) and Rahaghi (1976). 4 LITHOSTRATIGRAPHY As mentioned before, Tarbur Formation is marked as rudist limestone between shaly Gurpi and marly Sachun formations. Field investigations are great support of lower and upper lithostratigraphic boundary of Tarbur limestone in Tang-e Kushk stratigraphic section whereas lower contact of Sarvestan Tarbur stratigraphic column is not exposed. The Tarbur Formation of both stratigraphic sections are divided into two separated lithostratigraphic parts which are composed lower wellbedded rudist limestone and upper massive organodetrital limestone. Field measurement of Tarbur lower part is reflected 130 m thickness of brown to green well-bedded limestone with iron nodules. Organic constituents of this part are consisted of Gastropoda, rudist, and foraminifers. Lower contact of Tarbur Formation has developed discontinuously Gurpi Formation in Tang-e Kushk Section. Upper portion of the Tarbur limestone is mainly consisted of grey to milky rudist massive limestone which is covered by marly limestone of Sachun Formation. Whole thickness of Tarbur Formation is measured 365 m in this stratigraphic column (Fig. 2). The lower contact of Tarbur Formation of Sarvestan stratigraphic section is not exposed, but similar Tang-e Kushk Section, two separated lithostratigraphic portions are distinguishable which are described as lower and upper parts. The lower part is generally composed cream, brown to grey medium-bedded rudist limestone. Recognized iron nodules are rarely detected in this portion. Additionally the lower part is extended 32 m. The upper part is mainly consisted of light grey, cream to grey massive rudist limestone which is underlain by evaporites of Sachun Formation (Fig. 3). It should be notice the rudists are observable as crushed fragments in both stratigraphic sections, but rarely uncrushed rudists are investigated. 4.1 Biozonation of Tarbur Formation in Tang-e Kushk Stratigraphic Section Stratigraphic distribution of well known foraminifers have supported one biozone in each stratigraphic column of Tarbur Formation. The established biozone of Tang-e Kushk stratigraphic section is nominated as Orbitoides media and Omphalocyclus macroporus assemblage zone and described biozone of Sarvestan stratigraphic column is named Orbitoides media Biostratigraphy Study of Tarbur Formation (Upper Cretaceous) 265 zone. Lower biostratigraphic limit of the Tang-e Kushk Tarbur Formation is marked by disappearance of Early Maastrichtian planktonic foraminifers of Gurpi Formation which is synchronous with appearance of benthic foraminifers of Tarbur Formation. Diagnosed planktonic Foraminifers of uppermost Gurpi Formation are including Globotruncana ventricosa and Globotruncana arca. assemblage zone. Actually this biozone is marked by the first occurrence of Orbitoides media and Omphalocyclus macroporus. The common foraminifer taxa which are associated with both of mentioned Foraminifera are comprised by Dicyclina schlumbergeri, Antalyna korayi, Rotalia skourensis, Orbitoides tissoti, Orbitoides sp., Dicyclina sp., Minouxia sp., Nezzazatinella sp., Rotalia sp., Lepidorbitoides socialis, Trochospira sp. Rotalia skourensis, Orbitoides triangularis, Orbitoides orientalis, Dictyoconella sp., Broeckinella sp., Trochospira sp., Loftusia minor, Siderolites sp., Siderolites calcitrapoides, and dasycladacea are including Salpingoporella dinarica, Salpingoporella turgida, Salpingoporella sp.. Rahaghi (1976) 4.2 Tang-e Kushk Biozone As mentioned before, established biozone of this section is named as Orbitoides media and Omphalocyclus macroporus Figure 2. Lithostratigraphic diagram of Tang-e Kushk stratigraphic section. Thickness (m) Stratigraphical column Member Stage Danian Formation Series Lower Massive limestone, cream and grey weathered color, with rudist fragment Massive limestone, cream and grey weathered color 60 Tarbur Formation Maastrichtian Upper Upper 90 Cretaceous Field description Sachun Formation System Massih Afghah and Shohreh Yaghmour Paleocene 266 Massive limestone, milky and grey weathered color with rudist fragment Massive limestone, milky and grey weathered color 30 Lower Medium-bedded limestone, grey and brown weathered color Medium-bedded limestone, cream and brown weathered color with iron nodules Medium-bedded limestone, cream and brown weathered color 0 Massive limestone Medium-bedded limestone Hormoz salt Marly limestone 5.5 m 0 ? Figure 3. Lithologic column of Tarbur Formation at east Sarvestan section. has been recorded Orbitoides orientalis from Maastrichtian strata of western Iran. Zambetakis and Kemeridou (2004) have recognized Omphalocyclus macroporus, Loftusia minor, Orbitoides media, Orbitoides apiculata, and Siderolites calcitrapoides from Maastrichtian succession of eastern Greece platform. The stratigraphic section of Tang-e Kushk has diversity and abundance of different species. Lepidorbitoides socialis, Trochospira sp. and also rarely Salpingoporella turgida are recognized in the lower portion of the stratigraphic section of Tang-e Kushk. Rotalia skourensis, Rotalia sp., Orbitoides media, Orbitoides triangularis, Orbitoides tissoti, Orbitoides orientalis, Orbitoides sp., Antalina korayi, Dicyclina schlumbergeri, Dicyclina sp., Minouxia sp., Nezzazatinella sp., Dictyoconella sp. are common in packstone and grainstone lithofacies of upper part of this stratigraphic section of Tarbur Formation. Miliolids and other imperforate foraminifers are associated with orbitoids as faunal assemblage particularly in upper portion of Tang-e Kushk stratigraphic section of Tarbur limestone. Antalyna korayi have been recorded from Late Maastrichtian strata of Iran and Turkey by many authors (Afghah, 2010; Khosorow and Afghah, 2004). The first appearance of Biozone Species Salpingoporella dinarica Salpingoporella sp. Nezazzatinella sp. Lepidorbitoides sp. Dicyclina sp. Loftusia minor Orbitoides sp. Orbitoides media Thickness (m) Stratigraphical column Member Formation Stage Danian Sachun Formation Series Maastrichtian age (Permoli and Verga, 2004). Biostratigraphic data of uppermost of Gurpi and lowermost of Tarbur formations have supported disconformity between these rock units during Middle Maastrichtian age which is different from the other biostratigraphy study of Tarbur in this area (Afghah and Yousefzadeh, 2006). Lower Antalyna korayi is synchronous with lower contact of the Tange Kushk Tarbur Formation, therefore it is approval Late Maastrichtian age of Tarbur limestone in this stratigraphic section. Gurpi Formation collected samples have comprised of Globotroncana ventricosa, Globotroncana arca, Globotroncana orientalis, and Heterohelix sp., which are indicative of Early System 267 Paleocene Biostratigraphy Study of Tarbur Formation (Upper Cretaceous) 60 Orbitoides media zone Tarbur Formation 30 Lower Maastrichtian Upper Cretaceous Upper 90 0 Massivelimestone Medium-bedded limestone Hormoz salt Marly limestone ? Figure 4. Vertical distribution of Tang-e Kushk stratigraphic section index foraminifers and established biozone. 4.3 Biozonation of Tarbur Formation in East Sarvestan Stratigraphic Section The East Sarvestan stratigraphic section as compared with Tang-e Kushk stratigraphic section, is of few and rare variation from the point of view of frequency and variability of well known foraminifers. Microscopic investigations have reflected distributed dolomitization of basal part of this section. Also lower contact 268 Massih Afghah and Shohreh Yaghmour of the Sarvestan stratigraphic section is not exposed. The first taxon which have been identified in this stratigraphic section was Orbitoides media. Generally one biozone is established in this stratigraphic column which is named Orbitiodes media biozone. 4.4 Orbitoides media Biozone This biozone is described by the first occurrence of Orbitoides media. It is comprised of medium to massive grey rudist limestone which is measured 95 m in thickness. As mentioned before, the basal part of Tarbur Formation is dolomitized. Hence, there is no evidence of foraminiferal biofacies. Orbitoides media taxon range zone is associated with Nezzazatinella sp., Orbitoides sp., Lepidorbitoides sp., Loftusia minor, Dicyclina sp., Caskinolina sp., and dasycladacea Salpingoporella dinarica and Salpingoporella sp. (Fig. 5). There are many documents that confirm Maastrichtian age of each identified foraminifer of this biozone. Afghah and Farhoudi (2012) Figure 5. Biostratigraphic diagram as of East Sarvestan stratigraphic section. 5 CONCLUSION Biostratigraphic data of this article confirm different age determination of Tarbur Formation studied outcrops. Vertical distribution of the diagnosed foraminifers reflects the diversity of foraminiferal genus and species studied in these two sections particularly in Tang-e Kushk stratigraphic section. Faunal assemblage of both studied sections are the same as previous biostratigraphic data (Afghah and Farhoudi, 2012; Khosrow and Afghah, 2004). Upper biostratigraphic limit of both stratigraphic columns are similar, therefore it acceptable boundary between Upper Cretaceous and Lower Paleocene as synchronous in both stratigraphic sections. Stratigraphic distribution of index foraminifers confirms Upper Maastrichtian age of the Tarbur Formation in Tang-e Kushk stratigraphic column whereas there is no biostratigraphic data of separable of Maastrichtian strata in east of Sarvestan stratigraphic section. There are many documents which confirm continuous sedimentation between Gurpi and Tarbur Formations (Afghah and Farhoudi, 2012; Khosrow and Afghah, 2004; James and Wynd, 1965). Occurrence of Early Campanian pelagic foraminifers of upper parts of Gurpi Formation approved obvious disconformity between Gurpi and Tarbur formations in studied area. It is necessary to note that Kalantari’s study (1976) did not distinguish this disconformity. Since Sarvestan fault affected this area, it is logic to conclude Tang-e Kushk section biozone was controlled by this fault during Maasrtichtian. Biostratigraphic data of upper lithostratigraphic limit of Gurpi and lower Tarbur formations are a proof of a stratigraphic gap in Middle Maastrichtian period. The lower limit of Tang-e Kushk stratigraphic section is discontinuous with Gurpi Formation. Also, the lower limit of the East Sarvestan stratigraphic section has been limited with salt dome, while upper limit of Tarbur Formation in both sections comprises of evaporites of Sachun Formation. Although there is a difference between the lower limit of Tarbur Formation in both sections under study, the upper limit of which is upper Maastrichtian and the datum line could be considered as the end of Maastrichtian (Fig. 6). Maastrichtian Tarbur Formation Cretaceous Upper have recorded Loftusia minor from Maastrichtian succession of eastern Shiraz (SW of Iran). Zambetakis and Kemeridou (2004) documented Loftusia minor from Maastrichtian sediment of Greece. Based on Wynd’s (1965) biozonation which confirm Orbitoides media as Campanian taxon in interior Fars area whereas it is recognizable with Masstrichtian foraminifer taxa. Khosrow and Afghah (2004), Afghah and Yousefzadeh (2006) and Afghah and Farhoudi (2012) documented association of Orbitoides media with index Maastrichtian foraminifer taxa such as: Lepidorbitoides sp. Loftusia minor. Therefore the age of this biozone is assigned to Maastrichtian age. Globotruncana ventricosa, Globotruncana arca, Heterohelix sp., Globotruncana stauriformis, Globotruncana orientalis species have all been distinguished according to the studies carried out on Gurpi Formation which is, actually, the lower stratigraphic section to have been studied, based on which all Gurpi formation age in this zone is Early Maastrichtian (Fig. 5) 269 Paleocene Lower Danian Sachun Formation Biostratigraphy Study of Tarbur Formation (Upper Cretaceous) 20 m 0 Datum line Limestone Shale Well-bedded limestone Marly limestone Covered Hormoz salt Figure 6. Correlation of both studied sections of the Tarbur Formaion. REFERENCES CITED Abdelghany, O., 2003. Late Campanian-Maastrichtian Foraminifera from the Simsima Formation, on the Western Side of the Northern Oman Mountains. Cretaceous Research, 24(4): 391–405 Afghah, M., 2005. Microbiostratigraphic Study of Tarbur Formation in Khan-E Kat & Chehelcheshmeh. 9th Iranian Geology Society, Tehran. 354–367 Afghah, M., 2009. New Investigations of the Tarbur Formation Lithostratigraphy in the Review of Type Section and Its Correlation with Kuk-E Tir Section. Journal of Science Islamic Azad University, 19(73): 183–196 Afghah, M., 2010. Biozonation and Biostratigraphic Limits of the Tarbur Formation around Shiraz (SW of Iran): [Dissertation]. Westefaelische Wilhelms Universitaet, Muenster. 171 Afghah, M., Farhoudi, G., 2012. Boundary between Upper Cretaceous and Lower Paleocene in the Zagros Mountain Ranges of Southwestern Iran. Acta Geologica Sinica, 86(2): 325–338 Afghah, M., Khosrow, T. K., 2004, Lithostratigraphic Units of Tarbur Formation in North East and South East of Shiraz. Journal of Science Islamic Azad University, 14(53): 1–30 Afghah, M., Yousefzadeh, E., 2006. Microfacies and Sedimentary Environment of Carbonate Deposits of Tarbur Formation in Kherameh Section, the South East of Shiraz. Applied Geology Publication, 3(2): 1–6 Alavi, M., 2004. Regional Stratigraphy of the Zagros FoldThrust Belt of Iran and Its Proforeland Evolution. American Journal of Science, 304: 1–20 Arzaghi, S., Khosrow Tehrani, K., Afghah, M., 2012. Sedimentology and Petrography of Paleocene–Eocene Evaporites: the Sachun Formation, Zagros Basin, Iran. Carbonates 270 and Evaporites, 27(1): 43–53 Askari, B., Khazaei, A. R., Jafarian, K. T, K., et al., 2012. Biostratigraphy of Sabz Kuh (West of Broojen). Journal of Researches of Stratigraphy and Sedimentology, 27(4): 49–64 Çaglar (Kaya), M., Önal, M., 2009. Systematic Paleontology, Biostratigraphy, Paleobiogeography of Loftusia (Foraminifera) and Rudist Assemblage in a Regressive Sequence in the Hekimhan-Malatya Area (Eastern Anatolia) Turkey. Journal Geological Society of India, 74: 329–342 Checchia-Rispoli, G., 1911. La Serte Nummulitica di Dontorni di Bagher in Provinc Palermo. Giorn. Sci. Nat. bocon, 28: 168 Cushman, J. A., 1926. Some foraminifera from the Mendez Shale of Eastern Mexico. Contributions from the Cushman Foundation for Foraminiferal Research. 2: 16–28 d’Archiac, A. D., 1837. Mémoire Sur la Formation Crétacé du Sud-Ouest de la France, Mémoires de la Société Géologique de France, 2(7):157–192 Dieni, I., 2010. Maastrichtian and Selandian Decapod Crustaceans from Sardinia. Bullettino della Societá Paleontologica Italiana, 49(2): 135–144 Ehrenberg, G. C., 1840. Über Die Bildung der Kreidefelsen und des Kreidemergels Durch Unsichtbare Organismen. Abhandlungen der Königliche Akademie der Wissenschaften Zu Berlin, 1838: 59–147 Farinacci, A., Köylüoglu, M., 1985. Antalyna korayi n.sp., in the Phyletic Lineage of the Nezzazatidae (Foraminifera), Revue de Micropaléontologie, 6: 19–22 Geogescu, M. D., Almogi-Labin, A., 2008, New Data to Support the Phylogenetic Relationship between the Serial Planktonic Foraminifera (Family Heterohelicidae Cushman, 1972) and Some Large-Sized Benthic Foraminifera (Family Orbitoididae Schwager, 1876) of the Late Cretaceous. Revue de Paléobiologie, 27(1): 15–24 Henson, F.R.S., 1948. Larger Imperforate Foraminifera of South-Western Asia. Brit. Mus. (Nat. Hist.), London. 127 James, G. A., Wynd, J. G., 1965. Stratigraphic Nomenclature of Iranian Oil Consortium Agreement Area. American Association Petroleum Geologists Bull., 49(12): 2182–2245 Kalantari, A., 1976. Microbiostratigraphy of Sarvestan Area. National Iranian Oil Co., Iran. 5: 129 Kalantari, A., 1994. Zagros Lithostratigraphy & Microfacies. National Iranian Oil Company, Geological Lab, Zagros. 421 Khosrow, T. K., Afghah, M., 2004. Microbiostratigraphic Study of Tarbur Formation in the North, North East and South East of Shiraz. Geology Survey of Iran, Geosciences, 53(12): 76–85 Lamark, J. B., 1816. Historie Naturelle des Animaux sans Vertebres, vol.2, Paris, verdiere. 1–568 Marsson, T., 1878. Die Foraminiferen der Weissen Schreibkreide der Inseln Ruegen, Mitteilungen des Massih Afghah and Shohreh Yaghmour Naturwissenschaftlichen Vereins fuer Neu-Vorpommern und Rugen in Greiswald, 10: 115–196 Moosavi, M. H., Askari, P. B., 2008. Microfacies and Sedimentary Environment of Tarbur Formation in Dorahan Area. (East Lordegan). Journal of Applied Geology, 4(3): 195–206 Motiei, H., 1992. Iran’s Geology, Zagros Stratigraphy. Geological Survey of Iran, Iran. 525 Munier-Chalmas, E., 1887. Sur la Cyclolina et Trios Nouveaux Geners de de Couches á Rudistes: Cyclopsina , Dicyclina et Spirocyclina, Compte Rendu des Séances, Société Géologique de France, xxx-xxxi Permoli, S. I., Nicora, A., Vanneau, A. A., 1995. Upper Cretaceous Larger Foraminifer Biostratigraphy from Wodejebato Guyot, Sites 873 through 877. Proceeding of Ocean Drilling Program, 144: 1–27 Permoli, S. I., Verga, D., 2004. Practical Manual of Cretaceous Planktonic Foraminifera, Course 3. In: Verga, D., Rettori, R., eds., International School on Planktonic Foraminifera: Universities of Perugia and Milano, Tipografiadi di Pontefekcino, Perugia. 283 Pessagno, E. A., 1967. Upper Cretaceous Planktonic Foraminifera from Western Gulf Coastal Plain. Paleontographica Americana, 5: 245–445 Radoičić, R., 1959. Salpingoporella Dinarica n. sp. dans les Sédiments Crétacés Inférieurs des Dinarides. Geolles Glasnik, 3: 33–43 Radoičić, R., 1965. Pianella turgida n. sp. from the Cenomanian of the Outer Dinarids. Geol. Vjesnik, 18(1): 195– 1999 Rahaghi, A., 1976. Contribution à l’Étude de Quelques Grands Foraminifères de L’Iran. Parts 1–3. National Iranian Oil Co. Publication, Tehran. 6: 79 Schlumberger, C. H., 1901. Premiiere Note sur les Orbitoïdes I-IV, Extracts Bull. Soc. Géol. France, (4): 459–467 Schlumberger, C. H., 1902. Premiiere Note sur les Orbitoïdes, Bulletin de la Sociéte Géologique de France, Sér. 42: 255–261 Stoecklin, J., 1968. Structural History and Tectonics of Iran: A Review. American Association Petroleum Geologists Bull., 52(7): 1229–1258 Wynd, J. G., 1965. Biofacies of Iranian Oil Consortium Agreement Area. IOOC Report No. 1082, Tehran (unpublished) White, M. P., 1928. Some Index Foraminifera of the Tampico Embayment of Mexico, Part 2, Journal of Paleontology 2(4): 280–313 Zambetakis, L. A., Kemeridou, A., 2004. Loftusia cf. anatolica in Upper Maastrichtian of the Eastern Greece Platform (Mount Ptoon, Boeotia, Greece): Paleogeo-Graphical Remarks, Proceedings of the 10th International Congress. Thessaloniki, Bull. Geol. Soc. Greece, 36(2): 792–794 Biostratigraphy Study of Tarbur Formation (Upper Cretaceous) Plate I 1. Orbitoides triangularis Checchia-Rispoli, 1911, longitudinal section, Tang-e Kushk Section. 2. Orbitoides orientalis Rahaghi, 1976, longitudinal section,Tang-e Kushk Section. 3. Orbitoides media (d’Archic, 1873), longitudinal section, Tang-e Kushk Section. 4. Lepidorbitoides socialis Schlumberger, 1901, sub longitudinal section, Sarvestan Section. 5. Orbitoides apiculata Schlumberger, 1902, longitudinal section, Tang-e Kushk Section. 6. Gavelinella pertusa (Marsson, 1878), axial section, Tang-e Kushk Section. 271 272 Plate II 1. Salpingoporella dinarica Radoicic, 1959, Tang-e Kushk Section. 2. Coskinollina sp. sub axial section, Sarvestan Section. 3. Dicyclina shlumbergeri (Munier-Chalmas 1887), longitudinal Section, Sarvestan Section. 4. Acordiella sp., sub axial section, Tang-e Kushk Section. 5. Nezzazatinella sp. sub axial section, Sarvestan Section. 6. Antalyna korayi Farinacci and Köylüoglu, 1985, axial section, Tang-e Kushk Section. Massih Afghah and Shohreh Yaghmour Biostratigraphy Study of Tarbur Formation (Upper Cretaceous) Plate III 1. Salpingoporella turgida (Radoičić, 1965), Sarvestan Section. 2. Dicyclina shlumbergeri (Munier-Chalmas 1887), longitudinal section, Tang-e Kushk Section. 3. Omphalocyclus macroporus (Lamark, 1816), sub longitudinal section, Tang-e Kushk Section. 4. Loftusia sp., axial section, Tang-e Kushk Section. 5. Minouxia sp., sub longitudinal section, Sarvestan Section. 6. Rotalia skourensis Henson, 1948, sub axial section, Tang-e Kushk Section. 273 274 Plate IV 1. Globotruncana arca (Cushman, 1926), Gurpi Formation, Tang-e Kushk Section. 2. Globotruncana ventricosa White, 1928, Gurpi Formation, Tang-e Kushk Section. 3. Heterohelix globulosa (Ehrenberg, 1840), Gurpi Formation, Tang-e Kushk Section. 4. Macroglobigerinelloides bollii (Pessagno, 1967), Gurpi Formation, Tang-e Kushk Section. Massih Afghah and Shohreh Yaghmour