تاثیر ویژگی های ریزرخساره ای و دیاژنزی در کنترل کیفیت مخزنی سازند آسماری در میدان گازی گورزین، حوضه زاگرس، جنوب ایران
محورهای موضوعی : زمین شناسی مخازن نفتکریم ممبنی 1 , نصراله عباسی 2 * , احمد یحیایی 3
1 - زمین شناسی، ، دانشگاه زنجان
2 - دانشگاه زنجان
3 - شرکت نفت فلات قاره
کلید واژه: سازند آسماری ریزرخساره رمپ کربناته دیاژنز کیفیت مخزن میدان گازی گورزین,
چکیده مقاله :
سازند آسماری در میدان گازی گورزین با مرز ناپیوستگی فرسایشی بر روی نهشته های پلاژیک و مارن سازند پابده قرار دارد و با یک مرز تدریجی توسط نهشته های تبخیری سازند گچساران به عنوان سنگ پوش مخزن آسماری پوشیده می شود. مجموع ضخامت بررسی شده در یکی از چاه های این میدان، 183 متر است. سنگ شناسی آسماری در این برش شامل تناوبی از سنگ آهک، آهک دولومیتی و رسی و شیل، به همراه مارن سبز است. با مطالعات سنگ شناسی و آنالیز رخساره ای توالی این سازندها، 12ریزرخساره شناسایی شدند که یک رمپ کربناته از مناطق ژرف دریایی تا محیط سبخایی است و در یک سکانس پسرونده ایجاد گردیده است. این رمپ شامل محیط های عمیق، دریای باز، ریف کومه ای، سد زیستی- غیر زیستی، لاگون و محیط جزر و مدی است که با توجه به تغییرات سریع رخساره ها و نهشته شدن رسوبات تبخیری گچساران، موید یک محیط در حال بسته شدن می باشد. تاریخچه دیاژنزی که کربنات های آسماری در برش مورد مطالعه طی کرده اند شامل: الف) دیاژنز فریاتیک دریایی: جایی که زیست آشفتگی، میکریتی شدن و سیمانی شدن رخ داده است. ب) دیاژنز آبهای جوی: جایی که باز بلوری شدن، سیمانی شدن و انحلال به ثبت رسیده است. ج) دیاژنز دفنی: جایی که انحلال حاصل از فشار-تراکم و شکستگی رایج هستند رخ داه است. ریزرخساره ها دارای تنوع گسترده ای از خصوصیات مخزنی می باشند به همین دلیل یک مخزن ناهمگن را شکل داده اند. در این بین ریز شکستگی ها عمدتاً یک تاثیر بسیار قوی بر کیفیت مخزن در این رخساره ها اعمال می کنند. حضور همزمان فضاهای انحلال یافته و شکستگی در مخزن مقدار زیادی تراوایی را افزایش داده است. بهترین کیفیت مخزنی در ریزرخساره گرینستون/ پکستون دارای دانه های پوششی با تخلخل از نوع قالبی می باشد که به واسطه انحلال لیتولوژی پکستون اووئیددار در جریان دیاژنز آب های جوی ایجاد شده است.
Asmari Formation from the Gavarzin gas field have erosional unconformity boundary on marl and pelagic limestones of Pabdeh Formation and gradually change to evaporate cap rock of Gachsaran Formation. Cores studies from the one of wells of Gavarzin field is 183 m in thickness, which includes 1.30 m from the top of Pabdeh, 162.4 m from the Asmari Formation and 19.30 m from the base layers of Gachsaran. Asmari Formation includes alternation of limestone, calcite dolomitic, claystone and shale with green marl. Petrology and facies analysis of the sequence of these formations identified 12 microfacies, a carbonate ramp from deep-sea to sabkha environments and formed in a retrograded sequence. This ramp includes deep environments, open sea, patch reef, bio-, clastic-bars, lagoon and tidal environments, which confirms a changing environment due to rapid facies changes and deposition of evaporative sediments in Gachsaran as a restricted environment. Diagenesis processes are considered as the main factors in carbonate reservoir quality of Gavarzin field. The diagenesis history of the Asmari carbonates of the studied cores is summarized as A) marine phreatic diagenesis, bioturbation, micritization and cementation processes occurred. B) vadose zone diagenesis, where the crystallization, cementation, and dissolution occurred. C) burial diagenesis, comprises compression-induced, pressure dissolution and fracturing are common. The microfacies show a wide varieties of reservoir characteristics and therefore a heterogeneous reservoir has been formed. Micro-fractures, however have strongly influence on the reservoir quality in the section. The simultaneous presence of dissolved spaces and fractures in the reservoir the permeability greatly increased. The best reservoir quality in the Grainstone/Packston facies are coated grains with moldic porosity that were created by the leaching of Ooid-bearing Packston lithology during the diagenesis of atmospheric waters.
[1]مطیعی، ه.، 1372. زمین شناسی ایران، چینه شناسی زاگرس، انتشارات سازمان زمین شناسی کشور، ص 536.
[2]ممبنی، ک. 1396، دیرینه شناسی، ریزرخساره و تحلیل محیط رسوبی سازند آسماری در میدان گازی گورزین. پایان نامه کارشناسی ارشد، دانشگاه زنجان.
[3]AGHAEI, A., MAHBOUBI, A., MOUSSAVI-HARAMI, R., HEUBECK, C., NADJAFI, M., 2013, Facies analysis and sequence stratigraphy of an Upper Jurassic carbonate ramp in the Eastern Alborz range and Binalud Mountains, NE Iran. Facies, 59(4), 863-889.
[4]ALSHAHRAN A., KENDALL, C., 2011, Introduction to Quaternary carbonate and evaporite sedimentary facies and their ancient analogues. International Association of Sedimentologists 43:1-10.
[5]AMIRSHAHKARAMI, M., VAZIRI-MOGHADDAMoghaddam, H., and TAHERI, A., 2007, Sedimentary facies and sequence stratigraphy of the Asmari Formation at Chaman - Bolbol, Zagros Basin Iran, Journal of Asian Earth Science, 29 (5-6), 947-959.
[6]ALAVI, M., 2004, Regional stratigraphy of the Zagros fold-thrust belt of Iran and its proforland evolution. Am J Sci 304:1–20.doi:10.2475/ajs.304.1.1.
[7]BASSI, D., HOTTINGER, L. AND NEBELSICK, J. H., 2007, Larger Foraminifera from the Upper Oligocene of the Venetian area, northeast Italy: Palaeontology, Vol. 50, no. 4, 845-868.
[8]BARATTOLO, F., BASSI, D., ROMERO, R., 2007, Upper Eocene larger foraminiferal-coralline algal facies from the Klokova Mountain (south continental Greece). Facies, 53, pp. 361–375.
[9]BEYDOUN, Z. R., HUGHES CLARKE, M.W., STONELET, R., 1992, Petroleum in the Zagros Basin: a Late tertiary foreland basin overprinted onto the outer edge of a vast hydrocarbon-rich Paleozoic–Mesozoic passivemargin shelf. In: Maequeen RW, Lackie DH, editors. Foreland basins and fold belts, 55. USA: AAPG Memoir; p. 309–339.
[10]BRANDANO, M., CORDA, l., 2002, Nutrients, sea level and tectonics: constrains for the facies architecture of a Miocene carbonate ramp in central Italy. Terra Nova, 14, pp. 257–262.
[11]BRASIER, M.D., 1975, An outline history of sea-grass communities. Paleontology 18:681–702.
[12]CHOQUETTE, P. W., and PRAY, L. C., 1970, Geologic nomenclature and classification of porosity in sedimentary carbonates: American Association of Petroleum Geologists Bulletin, v. 54, p. 207-250.
[13]DROSTE, H., 1990, Depositional cycles and source rock development in an epeiric intra-platform basin: the Hanifa Formation of the Arabian Peninsula: Sediment. Geol., 69: 281-296.
[14]DUNHAM, R. J., 1962, Classification of carbonate rocks according to their depositional texture, in W. E., Ham, ed., Classification of carbonate rocks American Association of Petroleum Geologists Memoir, Vol. 1, pp. 108-121.
[15]CORDA, L., and BRANDANO, M., 2003, A photic zone carbonates production on a Miocene ramp, Central Apennines, Italy, Sedimentary Geology, 161, 55-70. DICKSON, J.A.D., 1965, A Modified Staining Technique for Carbonates in Thin Section, Nature, pp 205-587.
[16]EMBERY, A.F., KLOVEN, J.E., 1971, A Late Devonian reef tract on northeastern Banks Island, Northwest territories. Bull Can Petrol Geol 19:730–781. EHRENBERG, S.N., 2006, Porosity destruction in carbonate platforms. Journal of Petroleum Geology., Vol. 29, PP. 41-52.
[17]FLÜGEL, E., 2004, Microfacies of carbonate rocks: analysis, interpretation and application. Springer, Berlin; New York. Pp. 976.
[18]FLÜGEL, E., 2010, Microfacies of carbonate rocks: analysis, interpretation and application. Springer, Heidelberg Dordrecht London New York. pp. 634.
[19]FOLK, R.L., 1959, Parctical Petrographical Classification of limestones, AAPG Bull., 43, pp 1-38.
[20]GEEL, T., 2000, Recognition of Stratigraphic sequence in carbonate platform and slope deposits: empirical models based on microfacies analyses of palaeogene deposits in southeastern Spain. Palaeogeography, Palaeoclimatology, Palaeoecology 155, pp. 211-238.
[21]HEYDARI, E., 2008, Tectonics versus eustatic control on super sequences of the Zagros Mountains of Iran, Tectonophysics,451, 56–70.
[22]HARZAUSER, M., LATAL, C. and PILLER, W.E., 2007, The stable isotope archive of Lake Pannon as a mirror of Late Miocene climate change. Palaeogeogr. Palaeoclimatol. Palaeoecol., 249, pp. 335–350.
[23]LACOMBE, O., GRASEMANN, B. and SIMPSON, G. 2011, Introduction: geodynamic evolution of the Zagros. Geodynamic Magazin, 148 (5-6): 689-691.
[24]LOEBLICH, A.R., and TAPPAN, H., 1988, Foraminiferal Genera & Their Classification. Department of Space Sciences & Center for the study of Evolution, University of California; Los Angeles. Van Nostrand Reinhold; New York.
[25]LANGER, M.R., & HOTTINGER, L., 2000, Biogeography of selected larger foraminifera. Micropaleontology, 46:57-86.
[26]LUCIA, F.J. 2007, Carbonate reservoir characterization. Springer-Verlag Berlin Heidelberg,341p.
[27]LUCIA, F. J. 1995, Rock-fabric/petrophysical classification of carbonate pore space for reservoir characterization. American Association of Petroleum Geologists Bulletin, 79, 1275–1300.
[28]LUCIA, F. J., 1999, Carbonate reservoir characterization: New York, Springer-Verlag, 226 p.
[29]LAND L.S., MACKENZIE, F.T., and GOULD, S. J., 1967, Pleistocene history of Bermuda: Geol.Soc. America Bull., v. 78, p.993.
[30]LEE, Y.L. and FRIEDMAN, G.M., 1987, Deep-Burial dolomitization in the lower Ordovician Ellenburger Group Carbonates in west Texas and southeastern New Mexico: Jou. Sed. Petrology, 57., 544-577.
[31]MOORE, C. H., 2001, Carbonate reservoir porosity evolution and diagenesis in a sequence stratigraphic framework, Amsterdam, Elsevier, p. 444.
[32]MAHBOUBI, A., MOUSSAVI-HARAMI, R., MANSOURI-DANESHVAR, P., NADJAFI, M., BRENNER, L., 2006, Upper Maastrichtian depositional environments and sea-level history of the Kopet-Dagh Intracontinental Basin, Kalat Formation, NE Iran. Facies 52, pp. 237–248.
[33]NEBELSICK, J.H., RASSER, M., BASSI, D., 2005, Facies dynamic in Eocene to Oligocene circumalpine carbonates. Facies 51 (4), pp. 197–216.
[34]SCHOLLE, P.A., and ULMER-SCHOLLE, D.S., 2003, A Colour Guide to the Petrography of Carbonate Rocks: Grains, textures, porosity, diagenesis. American Association of Petroleum Geologists.
[35]SADEGHI, S.H. and SAEIDI, P., 2010, Reliability of Sediment Rating Curves for a Deciduous Forest Watershed in Iran. Hydrol. Sci. J. 55(5): pp. 821–831.
[36]RAJABI, P., 2016, Micro-Bio Stratigraphy of Asmari Formation in Mamoolan Stratigraphy Section, Sout of Khorramabad, Open Journal of Geology, 2016, 6, 459-467.
[37]ROMERO, J. CAUS, E. and J. ROSSEL, 2002, A model for the palaeoenvironmental distribution of larger foraminifera based on Late Middle Eocene deposits on the margin of the south Pyrenean basin (SE Spain): Palaeogeography, Palaeoclimatology, Palaeoecology, v. 179, pp. 43-56.
[38]PIROUZ, M., SIMPSON, G., BAHROUDI, A. and AZHDARI, A. 2011, Neogene sediments and modern depositional environments of the Zagros foreland basin system. Geological Magazine,148: 838-853.
[39]POMAR, L., 2001. Types of carbonate platforms: a genetic approach, Basin Research, 13, pp. 313-334.
[40]TUCKER, M.E.1991, Sedimentology Petrography: An introduction to the origin of sedimentology rocks, Black well, pp. 260.
[41] BUCHMAN, F.S.P., ALLAN, T.L., LAURSEN, G.V., LOTFPOUR, M., MOALLEMI, A., MONIBI, S., MOTIEI, H., PICKARD, N.A.H., TAHMSEBI, A.R., VEDRENNE, V.,, VINCENT, B., 2010. Regional stratigraphic architecture and reservoir typesof the Oligo-Miocene deposits in the Dezful Embayment (Asmari and Pab-deh formations) SW Iran. Geological Society, London, Special Publications. 329, pp. 219–263.
[42]VENNIN, E., VAN BUCHEM, F. S. P., JOSEPH, et al., 2003, A 3D outcrop analogue model for Ypresian nummulitic reservoirs: Jebel Qussalat, northern Tunisia Petroleum Geoscience, 9, 145-161.
[43]VAZIRI-MOGHADDAM, H., SEYRAFIAN, A., TAHERI, A., MOTIEI, H., 2010, Oligocene–Miocene ramp system (Asmari Formation) in the NW of the Zagros basin, Iran: Microfacies, paleoenvironment and deposi-tional sequence. Revista Mexicana de Ciencias Geológicas 27 (1), pp. 56–71.
[44]WILSON, J.L., 1975, Carbonate facies in geologic history. Springer-Verlag, Berlin; New York. Pp. 471.
[45]WARREN, J.K. and KENDALL, C.G.St.C., 1985. Comparison of marine sabkhas (subaerial) and salina (subaqueous) evapor- ites: modern and ancient. Bull. Am. Ass. Petrol. Geol., 69, pp. 1013-1023.