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Geodynamic Evolution of the Sanandaj-Sirjan Zone, Zagros Orogen, Iran

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Geodynamic Evolution of the Sanandaj-Sirjan Zone, Zagros Orogen, Iran Turkish Journal of Earth Sciences Turkish J Earth Sci (2015) 24: 513-528 http://journals.tubitak.gov.tr/earth/ © TÜBİTAK Review Article doi:10.3906/yer-1404-12 Geodynamic evolution of the Sanandaj-Sirjan Zone, Zagros Orogen, Iran Javad MEHDIPOUR GHAZI1,*, Mohssen MOAZZEN2 1Faculty of Earth Science, Shahid Beheshti University, Tehran, Iran 2Department of Earth Sciences, University of Tabriz, Tabriz, Iran Received: 21.04.2014 Accepted/Published Online: 02.06.2015 Printed: 04.09.2015 Abstract: The Sanandaj-Sirjan Zone is a metamorphic–magmatic belt, associated with the Zagros Orogen and part of the Alpine- Himalayan orogenic system in Iran. Stratigraphic, metamorphic, magmatic, and tectonic evidence presented here indicates that the Sanandaj-Sirjan Zone, the Central Iranian Microcontinent, and the North West Iranian Plate were a part of the Arabian plate until the Late Permian, when they separated during the opening of the Neotethys. Later subduction of the Neotethys oceanic crust beneath the Sanandaj-Sirjan Zone resulted in the complete closure of the Paleotethys Ocean in the Early Upper Triassic. The following extensional regime (related to slab roll-back) caused separation of the Sanandaj-Sirjan block, Central Iran Microcontinent, and North West Iranian Plate during the Upper Triassic to Lower Jurassic. The separation of these continental blocks caused sedimentation differences during that time. The North Tabriz and Nain-Baft Faults are probably the boundary between the Sanandaj-Sirjan Zone and Central Iran. The basin between the Sanandaj-Sirjan Zone and the Central Iranian block (the Iranian Microcontinent and North West Iranian Plate) closed in the Late Cretaceous. After that, these terranes experienced similar geological evolution, especially from the Oligocene to the Miocene. Key words: Sanandaj-Sirjan Zone, geodynamics, Iranian plate, Arabian plate, Neotethys 1. Introduction belt. Compared to the high Zagros Mountains, most of the The geology and especially the tectonic style of Iran are Sanandaj-Sirjan Zone has a relatively low relief, typically highly influenced by the history and evolution of the no more than 1400 m. The Zagros Main Thrust bounds Tethyan oceans. The Iranian crust is divided into several the southern margin of the Sanandaj-Sirjan Zone and geotectonic units, namely the Zagros, Makran, Sanandaj- separates it from Zagros. Central Iran is separated from the Sirjan Zone, Urmia-Dokhtar Magmatic Assemblage Sanandaj-Sirjan Zone by a belt of steep and straight faults (UDMA), Central Iran block, and Sistan Suture Zone including the Tabriz and Nain-Baft Faults (Şengör, 1979). (Figure 1). Each unit is characterized by a relatively unique Overall, the scarcity of Tertiary volcanic rocks, the high record of stratigraphy, magmatic activities, metamorphism, volumes of Mesozoic (and somewhat Tertiary) intrusions, orogenic events, tectonics, and overall geological style. The the relatively high abundance of Paleozoic volcanic rocks (Silurian, Devonian, and Permian), and metamorphism Zagros Orogen is part of the Alpine-Himalayan mountain due to Cimmerian movements are the main features of the chain. From the northeast to the southwest, the Zagros Sanandaj-Sirjan Zone (e.g., Aghanabati, 2006; Ghasemi Orogen consists of four parallel tectonic zones: (i) the and Talbot, 2006). These characteristics indicate that the UDMA, (ii) the Sanandaj-Sirjan Zone, (iii) the Zagros Sanandaj-Sirjan Zone cannot be assigned to any other Fold Thrust belt, and (iv) the Mesopotamian-Persian gulf geological and structural subdivision of Iran. foreland basin (Stöcklin, 1968; Berberian and King, 1981; The geodynamic evolution of the Sanandaj-Sirjan Alavi, 1994; Mohajjel and Fergusson, 2000). Zone was controlled by the opening and subsequent The metamorphic and igneous zone of the Zagros closure of the Neotethys Ocean at the northeastern margin Orogen, the Sanandaj-Sirjan Zone, was named by Stöcklin of Gondwana (Alavi, 1994). Two main opinions are (1968). The Sanandaj-Sirjan Zone extends ~1500 km from postulated on whether the Sanandaj-Sirjan Zone was part the northwest (Sanandaj) to southeast (Sirjan) with a of the Iranian or Arabian plate during the formation of the width of 150–200 km, parallel to the Zagros Fold Thrust Neotethys: * Correspondence: [email protected] 513 MEHDIPOUR GHAZI and MOAZZEN / Turkish J Earth Sci 50 55 60 Tabriz Fault Kh Caspian Sea Urmia Lake Paletethys Suture Zone Sa 35 Darouneh Fault Ke Sagand Bi Na Main Zagros rust GavkhooniNain-Ba Fault 30 Ba Nehbandan Fault Ny Jazmorian Persian Gulf M 250 Km 25 Makran Zone UDMA (Urmia-Dokhtar Magmatic Assemblage) NWIP (North West Iranian Plate) Zagros Afghan Block Eurasia CIM (Central Iranian Microcontinent) (covered and low deformed part) Sanandaj - Sirjan Zone Ophiolite (high deformed part) Sistan Suture Zone Figure 1. Main tectonic elements of Iran (modified after Stöcklin, 1968). Na: Nain, Ba: Baft, Kh: Khoy, Ny: Neyriz, Ke: Kermanshah, Sa: Sabzevar, M: Makran, and Bi: Birjand Ophiolites. 1) The Sanandaj-Sirjan Zone has been interpreted as i) The Sanandaj-Sirjan Zone was detached from Central an active continental margin of the Neotethys, separated Iran (Şengör, 1979, 1990; Stampfli and Borel, 2002) ever from the passive Arabian continental margin by the Zagros since they both separated from Gondwana in the Upper suture (e.g., Dewey et al., 1973; Haynes and McQuillan, Permian. 1974; Berberian and King, 1981; Dercourt et al., 1986; ii) Ghasemi and Talbot (2006) suggested that the Şengör, 1984). According to this model, the Neotethys Central Iranian Microcontinent (CIM), the Sanandaj- opened and closed along the southwestern margin of the Sirjan Zone, and the North West Iranian Plate (NWIP) Sanandaj-Sirjan Zone, while the Paleotethys is placed to formed one single block, the Iranian plate. The Sanandaj- the north of the Sanandaj-Sirjan Zone. Based on similar Sirjan Zone was situated to the south of Central Iran and is sedimentary and tectonic history and common magmatic considered as the active continental margin of the Iranian and metamorphic activities, the Sanandaj-Sirjan Zone plate. The Paleotethys was located to the north of the is conventionally considered as a subzone of the Iranian NWIP, which itself borders the northern side of the CIM. plate. There are two interpretations regarding the position These three blocks separated only after the Paleotethys of the Paleo- and Neotethys: closure during the Jurassic. 514 MEHDIPOUR GHAZI and MOAZZEN / Turkish J Earth Sci 2) In this scheme, the Sanandaj-Sirjan represents the (both in Central Iran and the Sanandaj-Sirjan Zone) is northeastern extension of the Arabian passive continental Precambrian in age (Horton et al., 2008). However, the vast margin (Falcon, 1969; Haynes and McQuillan, 1974; exposure of Paleozoic and Mesozoic metamorphic rocks Alavi, 1980, 1994) based on similar structural trends makes this zone different from other Iranian geotectonic and deformation patterns in Zagros and the Sanandaj- units. Sirjan Zone. The Neotethys suture thus runs along the Deformation recorded in the metamorphic rocks of northeastern border of the Sanandaj-Sirjan Zone. the Sanandaj-Sirjan Zone and the I-type nature of plutons Obviously, the Sanandaj-Sirjan Zone is an important are related to the subduction of the southern Neotethys tectonic unit of Iran that remains poorly documented. sea floor northeastwards beneath the continental blocks However, it is crucial to understand this part of the (Mohajjel, 1997). Zagros belt, and especially to model the relationship 2.2. Zagros between Central Iran and Arabia through Precambrian The Zagros Fold Thrust belt forms the less exposed to Cenozoic times. Understanding its geological evolution external part of the orogen. This belt consists of folded and could unravel the regional correlation to adjacent areas faulted mainly Paleozoic and Mesozoic successions of 4–7 such as North West Iraq, South East Turkey, and the km thick overlain by Cenozoic siliciclastic and carbonate eastern continuation of the Alpine-Himalayan orogenic rocks of 3–5 km thick, resting on highly metamorphosed belt. We integrated existing data from sedimentary, Proterozoic Pan-African basement that was affected by igneous, and metamorphic rocks and structural features Late Neoproterozoic–Cambrian Najd strike-slip faults and characteristics of the related ophiolites in this paper (Alavi, 2004). The Zagros Mountains gradually rise to compare the various existing geodynamic models. northeastward from an unfolded shelf, extending through We discuss the situation of the Paleo- and Neotethys a fold belt into a thrust belt and imbricated zone (Berberian with respect to the Sanandaj-Sirjan Zone and propose a and King, 1981). regional scenario that may help understand this part of the Tethyan domain. 2.3. Central Iran Central Iran is located between the convergent Arabian 2. Geological setting and Eurasian plates. Central Iran comprises two major The Sanandaj-Sirjan Zone is a NW-SE trending belt of crustal domains: the NWIP and the CIM. The NWIP mainly metamorphic and igneous rocks, located at the comprises the region north of the Darouneh and Tabriz northeastern extension of the Zagros Orogen (Figure 1). Faults. The CIM (Takin, 1972) comprises terrain limited To the northeast, it is bordered by Central Iran and the by the Sistan, Nain-Baft, Makran, and Sabzevar Ophiolites UDMA, and to the southwest by the Zagros Fold Thrust (Şengör, 1990) and is affected by a complex system of belt (Alavi, 2004). active continental strike-slip
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