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However, in the Qom Basin a faunal turnover and change in faunistic relationships of pectinids already took place during the Bur 2 cycle (sequence 7 of Qom section) when the central seaway was still open. Whereas pectinid faunas from the a- to e-Members show a clear Indo-Pacific affinity until the early Burdigalian, f-Member pectinid faunas indicate a strong Mediterranean signal towards the mid-Burdigalian (Mandic 2000 ). The same development is shown by corals and gastropod faunas from the central Iranian Basins, in which Indo-Pacific elements diminish during the Early Miocene (Schuster and Wielandt 1999
; Harzhauser et al. 2002 ; Harzhauser et al. 2007 ). This
suggests that faunal exchange between the Qom Basin and the Indo-Pacific ceased, while at the same time the con- nectivity with the Mediterranean was enhanced. Even if Eurasia and Africa were not connected by a fully formed landbridge at this time, it is plausible that hypersaline waters in the shallow remaining Tethyan Seaway possibly formed a biogeographic barrier for Indo-Pacific marine biota shortly before the TTE. Summary and conclusions The Qom Formation was deposited on extended, mixed carbonate-siliciclastic, homoclinal ramps at the north- eastern coast of the Tethyan Seaway in the Qom back-arc and Esfahan-Sirjan fore-arc basins (central Iran). It includes seven stratigraphic sequences that span the late Rupelian to mid-Burdigalian time interval and can be attributed to the Ru 3 to Bur 2 third order sea-level fluc- tuations of Hardenbol et al. ( 1998
). The recognition and dating of these sequences in the Esfahan-Sirjan Basin and in the Qom Basin allows a basin-spanning stratigraphic correlation of the Qom Formation for the first time. The elaborated stratigraphic scheme documents contin- uous restriction of the Tethyan Seaway with advanced collision of the African/Arabian and Eurasian/Iranian plates. For the Oligocene a normal marine milieu is dis- played throughout the sedimentary successions of the fore- and back-arc basins. In the fore-arc basin these conditions endured during the Aquitanian and Early Burdigalian, while in the Qom Basin, as well as in other marginal basins on both coasts of the Tethyan Seaway, intermittent epi- sodes with restricted marine conditions and emersions are documented. However, persisting gateways connecting the Qom Basin with the Mediterranean and Indo-Pacific sides of the Tethyan Seaway until the late Early Burdigalian is documented by Tethyan faunal elements from both sides of the Tethyan Seaway in the central Iranian basins. Yet after the Bur 2 lowstand emersion of the Qom Basin its recol- onization occurred from the Mediterranean region only. Thus, the differentiation into an Atlantic-Mediterranean and an Indo-Pacific bioprovince took place before the final Fig. 12
Schematic block diagrams illustrating the development of the Esfahan-Sirjan Basin and Qom Basin from Late Oligocene to Early Miocene times (paleogeographic maps modified from Harzhau- ser and Piller 2007 ). The black arrows in paleogeographic maps tag the positions of the Zagros Basin (ZB), Qom Basin (QB) and Esfahan- Sirjan Basin (ESB); white arrows in block diagrams show the permeability of gateways. Oligocene: broad Tethyan Seaway and fully marine connections to the western Tethys via seaways to the north and south of Qom Basin. Early Miocene: restriction of the Tethyan Seaway, and closure of the gateways between Qom Basin and the Proto-Indopacific due to ongoing collission of Africa/Arabia with Eurasia, and upthrust of the Zagros mountain ranges. Transpar- ent gray arrows indicate evaporation in the Qom Basin Int J Earth Sci (Geol Rundsch) 123
paleogeographic disjunction of the Tethys (TTE), as shown by the comparison with the Zagros Basin, where marine sedimentation continued until the end of Burdigalian. It is therefore suggested that the continuous shallowing and restriction of the seaway generated an increasingly hostile hypersaline environment and a biogeographic barrier for marine biota. Acknowledgments Our special thanks go to the other members of the research projects on Late Oligocene—Early Miocene circum- Mediterranean palaeobiogeographical relations, the project leaders F. F. Steininger (Eggenburg) and J. H. Nebelsick (Tu¨bingen), as well as the researchers M.W. Rasser (Stuttgart), J. Reisinger (Korneuburg), F. Schuster (Freiburg), and J. Schlaf (Aberdeen). We also appreciate the comments from an anonymous reviewer. This work was supported by the Austrian FWF (P11886-GEO) and the Deutsche Forschungs- gemeinschaft (STE 857/1-1; NE 537/1-1, -2). References Abaie IL, Ansari HJ, Badakhshan A, Jaafaki A (1963) History and development of the Alborz and Seraih fields, central Iran. In: Proc 6th world petrol conf, Frankfurt, pp 1–111 Adams CG (1968) A revision of the foraminiferal genus Austrotrillina Parr. Bull Brit Nat Hist Geol 16:73–97 Adams CG, Gentry AW, Whybrow PJ (1983) Dating the terminal Tethyan event. Utrecht Micropaleontol Bull 30:273–298 Ala MA (1982) Chronology of trap formation and migration of hydrocarbons in Zagros sector of southwest Iran. AAPG Bull 66:1536–1542 Alsharhan AS, Nairn AEM (1995) Tertiary of the Arabian Gulf: sedimentology and hydrocarbon potential. Palaeogeogr Palaeo- climatol Palaeoecol 114:369–384 Amidi SM (1983) Abadeh. Geological quadrangle map of Iran no. G9. Scale 1:250 000. Ministery of Mines and Metals and Geol Surv Iran Amidi SM, Zahedi M (1991) Kashan. Geological quadrangle map of Iran no. F7. Scale 1:250 000. Ministery of Mines and Metals and Geol Surv Iran Beavington-Penny SJ, Wright VP, Racey A (2006) The middle Eocene Seeb formation of Oman: an investigation of acyclicity, stratigraphic completeness, and accumulation rates in shallow marine carbonate settings. J Sed Res 76:1137–1161 Berggren WA, Kent DV, Aubry MP, Hardenbol J (1995) Geochro- nology, time scales and global stratigraphic correlation. SEPM Spec Publ 54:1–386 Bizon G, Bizon JJ (1972) Atlas des pincipaux foraminife´res planctoniques du basin me´diterrane´en. Oligoce´ne a´ quaternaire IX:1–316 Bolli HM, Saunders JB (1985) Oligocene to Holocene low latitude planktic foraminifera. In: Bolli HM, Saunders JB, Perch-Nielsen K (eds) Plankton stratigraphy. Cambridge University Press, London, pp 155–262 BouDhager-Fadel M, Banner FT (1999) Revision of the stratigraphic significance of the Oligo-Miocene ‘‘Letter-Stages’’. Rev Micro- paleontol 42(2):93–97 Bozorgnia F (1966) Qum formation stratigraphy of the Central Basin of Iran and its intercontinental position. Bull Iran Petrol Inst 24:69–76 Cahuzac B, Poignant A (1997) Essai de biozonation de l‘Oligo- Mioce`ne dans les bassins europe`ens a` l’aide des grands foraminife`res ne`ritiques. Bull Soc Ge`ol Fr 168:155–169 Chahida MR, Papp A, Steininger F (1977) Fossilfu¨hrung der Oligo/ Mioza¨nen Qum-formation in Profilen bei Abegarm-Zefreh bei Isfahan (Zentraliran). Beitr Pala¨ont O ¨ sterr 2:79–93 Coleman-Sadd SP (1982) Two stage continental collision and plate driving forces. Tectonophysics 90:263–282 Ctyroky P, Karim SA, van Vessem EJ (1975) Miogypsina and Borelis in the Euphrate limestone formation in the Western Desert of Iraq. N Jb Geol Pala¨ont Abh 148:33–49 Emami MH (1991) Qom. Geological quadrangle map of Iran no. E6. scale 1:250 000. Ministery of Mines and Metals and Geol Surv Iran
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Int J Earth Sci (Geol Rundsch) 123 Document Outline
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