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Constraints from the Northern Portion of the Cenozoic Kongur Shan Extensional System, Western China

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Constraints from the Northern Portion of the Cenozoic Kongur Shan Extensional System, Western China Tectonic evolution of the northeastern Pamir: Constraints from the northern portion of the Cenozoic Kongur Shan extensional system, western China Alexander C. Robinson† An Yin‡ Craig E. Manning§ T. Mark Harrison# Department of Earth and Space Sciences and Institute of Geophysics and Planetary Physics, University of California, Los Angeles, California, 90095-1567, USA Shuan-Hong Zhang†† Xiao-Feng Wang‡‡ Institute of Geomechanics, Chinese Academy of Geological Sciences, Beijing 100081, People’s Republic of China ABSTRACT the northern Pamir prior to the Indo-Asian changes dramatically from ~500 km in the collision. A third Late Miocene (ca. 9 Ma) west across the Pamir and western Himalayan The late Cenozoic Kongur Shan exten- amphibolite-facies metamorphic event syntaxis region to >1500 km in the central and sional system lies along the northeastern (~650–700 °C, 8 kbar) is recorded in footwall eastern portions of the Tibetan Plateau (Fig. 1A). margin of the Pamir at the western end of gneisses of the Kongur Shan massif. North of Three end-member models have been proposed the Himalayan-Tibetan orogen, accommo- the Kongur Shan massif, rapid cooling in the to explain the development of this asymmetry: dating east-west extension in the Pamir. At footwall beginning at 7–8 Ma is interpreted (1) different magnitudes of convergence between the northern end of the extensional system, to date the initiation of exhumation along India and Asia between the eastern and western the Kongur Shan normal fault juxtaposes the Kongur Shan normal fault. A minimum Himalayan syntaxes (e.g., Dewey et al., 1988, medium- to high-grade metamorphic rocks of 34 km of east-west extension is inferred 1989; Le Pichon et al., 1992), (2) eastward lateral in both its hanging wall and footwall, which along the Kongur Shan massif based on the extrusion of Tibetan crust (Molnar and Tappon- record several Mesozoic to Cenozoic tectonic magnitude of exhumation since the Late nier, 1975; Tapponnier et al., 1982; Peltzer and events. Schists within the hanging wall pre- Miocene (~29 km) and the present dip of Tapponnier, 1988), and (3) distributed shortening serve a Buchan metamorphic sequence, the Kongur Shan normal fault (~40°). Field across the Indo-Asian collision zone interacting dated as Late Triassic to Early Jurassic observations and interpretation of satellite with lateral heterogeneities in the strength of (230–200 Ma) from monazite inclusions in images along the southernmost segment of the Asian crust (i.e., Tarim basin) (England and garnet. Metamorphic ages overlap with U-Pb the Kongur Shan extensional system indicate Houseman, 1985; Houseman and England, 1996; zircon ages from local granite bodies and are that the magnitude of late Cenozoic east-west Neil and Houseman, 1997). As an alternative to interpreted to be the result of regional arc extension decreases signifi cantly toward the these conceptual models, based on offset of the magmatism created by subduction of the south. This observation is inconsistent with Western and Eastern Kunlun batholiths, Cowgill Paleo-Tethys ocean. The northern portion of models in which east-west extension in the et al. (2003) suggest that the asymmetry of the the footwall of the extensional system exposes Pamir is driven by northward propagation Tibetan Plateau is a result of the development an upper-amphibolite-facies unit (~650 °C, of the right-slip Karakoram fault, suggesting of Tertiary thrust belts with opposite polarities 8 kbar), which structurally overlies a low- instead that extension is driven by vertical linked by the left-slip Altyn Tagh fault. grade metagraywacke unit. The high-grade extrusion due to topographic collapse, radial The observations by Cowgill et al. (2003), as unit records late Early Cretaceous crustal thrusting along the Main Pamir Thrust, or well as documented Tertiary strike-slip faulting thickening at ca. 125–110 Ma, followed by oroclinal bending of the entire Pamir region. and crustal shortening in western Tibet (Ratsch- emplacement over the low-grade metagray- bacher et al., 1994; Matte et al., 1996; Searle et wacke along a north-northeast–directed Keywords: Pamir, tectonics, metamor- al., 1998; Kapp et al., 2003), suggest that both thrust prior to ca. 100 Ma. Together these phism, age determination, extension, crustal lateral extrusion and distributed shortening have results indicate signifi cant middle Creta- shortening. occurred synchronously. However, the relative ceous crustal thickening and shortening in contribution of these mechanisms in the evolu- INTRODUCTION tion of the Indo-Asian collision belt, and the asymmetry of the Himalayan-Tibetan orogen, †E-mail: [email protected]. A prominent feature of the Indo-Asian col- remains poorly understood (e.g., Le Pichon et ‡E-mail: [email protected]. lision zone is the pronounced asymmetry in al., 1992; Johnson, 2002). Key to determining the §E-mail: [email protected]. #E-mail: [email protected]. the region of thickened and elevated crust relative contributions of these different deforma- ††E-mail: [email protected]. immediately north of the Indian craton. In map tion mechanisms is understanding the differences ‡‡E-mail: [email protected]. view, the north-south width of thickened crust in the tectonic evolution between the western GSA Bulletin; July/August 2004; v. 116; no. 7/8; p. 953–973; doi: 10.1130/B25375.1; 21 fi gures; 2 tables; Data Repository item 2004107. For permission to copy, contact [email protected] © 2004 Geological Society of America 953 ROBINSON et al. 70° 80° 90° 100° Tian Shan Thrust Tian Shan Suture Zone A B Karakul rift Main Pamir Tian Shan 40° ult Fig. 1b Pamir Kashgar hern 40° Altyn Tagh fa ort N Figure 2 Tarim Basin l Pamir T entra adjik depre ult C Karakoram fault Kongur Shan ssion TIBETAN PLATEAU extensional system Pulan rift 30° Kudi Suture Darvaz fa Karakoram ush- u K rrane Western Kunlun thrust belt nd te Hi INDIA in Karakoram North Kunl Ayimaqin-Kunlun- Ma thru South Kunlun terrane st Muztagh suture Herat fault yok suture un terrane Sh Karaka Kohistan Arc x fault Karakoram fault Lada Helmand fault lock Songpa kh Arc terrane n Main Mantle Thrust -Ganzi Kabul b Jinsha suture 35° Chaman fault ult nd n Bou ary Thrust Gardez fa ai Islamabad M Bangong-Nu Qiangtang STDS terrane MCT Lhasa jiang suture hrust terrane Main Frontal T 70° 75° 80° Figure 1. (A) Simplifi ed regional tectonic map of the Himalayan-Tibetan orogen. (B) Tectonic map of the Pamir–western Himalayan syn- taxis showing tectonic terranes and major Cenozoic structures, after Tapponnier et al. (1981), Burtman and Molnar (1993), Treloar and Izatt (1993), Brunel et al. (1994), Strecker et al. (1995), Schneider et al. (1999), Rumelhart et al. (1999), Yin et al. (2002), and Cowgill et al. (2003). STDS—South Tibetan Detachment, MCT—Main Central Thrust. segment (the Pamir–western Himalayan syntaxis) crustal-scale faults accommodating northward Tibet (Hodges, 2000), and (3) the role and his- and central and eastern segments (the Tibetan Pla- underthrusting of India beneath Asia. tory of strain transfer between thrust belts and teau) of the Himalayan-Tibetan orogenic belt. Earthquake hypocenter relocations indicate extensional systems of the Pamir and western active intracontinental subduction beneath the Tibet (Ratschbacher et al., 1994; Murphy et Tectonic Setting Pamir–western Himalayan syntaxis (Burtman al., 2000). Studies along the central segment of and Molnar, 1993; Fan et al., 1994; Pegler and the Karakoram fault document 120–150 km of The Pamir–western Himalayan syntaxis lies at Das, 1998). Interpretation of relocated seismic right-slip motion initiating in the Middle Mio- the western end of the Indo-Asian collision zone events along the southern margin of the Pamir– cene (Searle, 1996; Dunlap et al., 1998; Searle and is bounded by the Main Pamir Thrust to the western Himalayan syntaxis region suggest et al., 1998). Additionally, studies along the north, and the Main Boundary Thrust and Main shallow north-directed subduction of the Indian southern portion of the Karakoram fault have Frontal Thrust to the south (Fig. 1B). The Main plate beneath Asia (Fan et al., 1994; Pegler and indicated that Late Miocene southward propa- Pamir Thrust is a crustal-scale fault, interpreted Das, 1998). A steeply south-dipping zone of gation of the fault resulted in 66 ± 5.5 km of to have accommodated northward translation of seismicity under the Pamir reaches depths of right-slip displacement, as well as the develop- the Pamir ~300 km over the Tarim basin, Tadjik ~200 km, and projects to the surface trace of the ment of the north-south–striking Pulan rift and basin, and Alai Valley (Burtman and Molnar, Main Pamir thrust (Burtman and Molnar, 1993). Gurla Mandhata detachment system (Murphy 1993; Brunel et al., 1994; Strecker et al., 1995; Interpretation of this zone is controversial and et al., 2000, 2002). These studies suggest that Matte et al., 1996; Pavlis et al., 1997; Sobel and has been described as either southward-sub- the Karakoram fault has played a minor role Dumitru, 1997; Arrowsmith and Strecker, 1999). ducted Asian lithosphere (Burtman and Molnar, in the eastward extrusion of Tibetan crust (i.e., To the east, the Main Pamir Thrust links with 1993; Fan et al., 1994) or a rotated portion of <150 km, cf. Armijo et al., 1986, 1989). the Western Kunlun thrust belt, which forms subducted Indian lithosphere (Pegler and Das, In the Pamir–western Himalayan syntaxis the southwest termination for the left-slip Altyn 1998; Pavlis and Das, 2000). region, Cenozoic deformation appears to have Tagh fault (Burchfi el et al., 1989; Yin et al., The eastern margin of the Pamir–western been dominated by north-south shortening 2002; Cowgill et al., 2003). The large magnitude Himalayan syntaxis region is bounded by the along east-trending structures (e.g., the Main of northward displacement of the Pamir salient ~1000-km-long right-slip Karakoram fault, Mantle Thrust, Main Karakoram Thrust, Rushan has resulted in the development of right-slip which extends from the eastern Pamir to south- Pshart zone, and Main Pamir Thrust) (Fig.
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