Biostratigraphy, microfacies, depositional environment and sequence stratigraphy of the Sarvak Formation in one of the oilfields, southwest Iran

Document Type : مقالات پژوهشی

Authors

• Behzad Saeedi Razavi ¹
• Fatemeh Asgari ²
• Mohammad Reza Kamali ³
• Ezatallah Kazemzadeh ³

¹ Standard Research Center

² Islamic Azad University, Science and Research Branch

³ Research Institute of Petroleum Industry

10.22067/sed.facies.v12i1.78443

Abstract

Introduction

Sarvak Formation is one of the units in the Bangestan lithostratigraphic group with Albian-Turonian age. The shallow sea at the end of the Albian to Cenomanian time has deposited large amounts of the shallow marine carbonates (Sarvak Formation) over a large area of the Zagros basin (Motiei, 1995). The Sarvak Formation has two different facies. At the type section and coastal Fars, shallow marine facies of this formation mostly formed while in the Lorestan area, the facies are belonging to deeper water (Motiei, 1995). The Sarvak Formation is a reservoir of hydrocarbon in the Zagros sedimentary basin. Therefore, a detailed study of this formation, based on microfacies and sequence stratigraphy, will provide useful and valuable information for further exploration in this basin. The purpose of this study was to evaluate the biostratigraphy, microfacies, depositional environment and sequence stratigraphy of the Sarvak Formation.
 
Methods and Results 
To approach the objectives of this research, two stages have been taken: Preparation of 195 thin sections from drill cores and cuttings (National South Oil Company), then Laboratory studies of thin sections prepared by binocular microscopy and identification of allochems and orthochems and the preparation of photomicrographs. The identified biozones correspond to biozones named after Wynd (1965). In this study, Flugel (2010) method used to describe the microfacies, and also Reading (1996) and Dunham (1962) methods used to determine rock texture and nomenclature Identification, photography and the creation of the Atlas of microfossils, their distribution in stratigraphic column, representation of identified biozones, and sedimentary sequence lithology in the studied area has been made possible through the study of graphs and logs, thin sections, and the use of various research satellites such as Bolli (1945; 1959; 1966), Postuma (1971) and Caron (1983). Sequence stratigraphy of the Sarvak Formation has been studied based on sequence stratigraphic methods and principles (Haq et al., 1987; Van Wagoner et al., 1988; Emery and Myers, 1996; Simmons et al., 2007).
 
Results and Conclusion
Based on this study, 5 genus and 2 species of pelagic microfossils and 25 genus and 28 species of benthic microfossils were identified. Therefore, three biozones including Nezzazata - alveolinids assemblage zone # 25, Rudist debris zone # 24, and Oligosteginid flood zone # 26 were introduced that are corresponding to the biozones introduced by Wynd (1965). Based on the studied faunal assemblage, the age of the Sarvak Formation is from Cenomanian to Turonian in the studied wells. The upper boundary of the Sarvak Formation with the Gurpi Formation is discontinuous due to the presence of glauconitic nodules at the base of the Gurpi. According to the regional geology of this area and information from the studied wells, the Ilam Formation and the 30th Wynd Biological Zone (Wynd, 1965), as well as the biodegradation of Wynd (1965) at the top of the Sarvak Formation, are absent. The drilling has not reached the base of the Sarvak Formation, therefore the lower boundary is not clear. 7 microfacies identified in the Sarvak Formation in the studied wells. These microfacies are formed in 3 main facies belts including 1- open sea, 2- shoal, and 3- lagoon. Investigation of carbonate rocks of the Sarvak Formation in the study area shows that the sedimentary environment of the Sarvak Formation in the studied field was a shallow carbonate platform of the carbonate ram type. The Sarvak Formation in the study area consists of 1 complete sedimentary sequence and 2 incomplete sequences, which are generally HST and TST in the studied sections. The HST facies in this sequence originate from a variety of marine microfacies and finished with the lagoon. The TST facies is mainly related to the open marine. Finally, the HST facies is related to the inner and middle parts of the platform; while the TST facies is related to the outer and middle parts of the platform.
 
Acknowledgment
The authors would like to thank Dr. Mohammad Reza Ghotbi Ravandi for their helpful assistance and Dr. Mojgan Rikhtgarzadeh for their help in drawing figures and logs.
 
Keywords: Biostratigraphy; microfacies; sequence stratigraphy; Sarvak Formation; Cenomanian Turonian.
 
References
Bolli, H.M., 1945. Zur Stratigraphie der Oberen Kreide in den hoheren Helvetischen Dechen. Eclogae Geologicae Helvetiae, 37: 217-328.
Bolli, H.M., 1959. Planktonic Foraminifera from the Cretaceous of Trinidad. Bulletins of American Paleontology, 39: 21-57
Bolli, H.M., 1966. Zonation of cretaceous to Pliocene marine sediments based on planktonic foraminifera Bolethin Informative Asociacion Venezolana De Geologia. Mineria-y-Petroleo, 9: 3-32.
Caron, M., 1983. Taxonomie et phylogenie de la famille des Globotruncanidae. 2nd kreide symposium, Munchen, 1982, Zitteliana, Munchen, 10: 667-681.
Dunham, R.J., 1962. Classification of carbonate rocks according to depositional texture. American Association of Petroleum Geologists, Memoir, 1: 108–121.
Emery, D., & Myers, K.J., 1996. Sequence Stratigraphy, Blackwell Science. Oxford, 297 p.
Flügel, E., 2010. Microfacies of carbonate rocks, analysis, interpretation and application. Springer, Berlin, 976 p.
Haq, B.U., Hardenbol, J., & Vail, P.R., 1987. Chronology of fluctuating sea level since the Triassic. Science, 235: 1156-1167.
Husinec, A., Velic, L., Fucek, L., Vlahovic, I., Maticec, D., Ostric, N., Korbar, T., 2000. Mid Cretaceous Orbitolinid (Foraminiferida) record from the islands of Cres and Los˘inj (Croatia) and its regional stratigraphic correlation. Cretaceous Research, 21: 155-171.
Motiei, H., 1993. Geology of Iran: Stratigraphy of Zagros. Geological Survey of Iran, 536 p. (In Persian).
Postuma, J., 1971. Manual of Planktonic Foraminifera. Elsevier Publishing Company, Amsterdam, 420 p.
Reading, H.G., 1996. Sedimentary Environments. Processes, Facies and Stratigraphy, 3rd edition. Blackwell, 688 p.
Simmons, M.D., Sharland, P.R., Casey, D.M. Davies R.B., & Sutcliffe, O.E., 2007, Arabian Plate sequence stratigraphy, Potential implications for global chronostratigraphy. GeoArabia, 12 (4): 101-130.
Van-Wagoner, J.C., W., Posamentier, Mitchum, H. R.M.Jr., Vail, P.R., Sarg, J.F., Loutit, T.S., & Hardenbol, J., 1988. An Overview of the Fundamentals of Sequence Stratigraphy and Key Definitions. In: Wilgus, C.K., Hastings, B.S., Posamentier, H., Van Wagoner, J., Ross, Ch.A., & Kendall, Ch.G.St.C. (eds.), Sea Level Changes: An Integrated Approach. SEPM Special Publication, 42: 39-45.
Wilson, J.L., 1975. Carbonate Facies in Geologic History. Springer-Verlag, New York, 471 p.
Wynd, J.G., 1965. Biofacies of the Iranian consortium-agreement area. Iranian Offshore Oil Company, Report 1082.

Keywords

• Biostratigraphy
• microfacies
• Sequence stratigraphy
• Sarvak Formation
• Cenomanian - Turonian

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