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Tectonic and Erosional History of Southern Tibet Recorded by Detrital Chronological Signatures Along the Yarlung River Drainage

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Tectonic and Erosional History of Southern Tibet Recorded by Detrital Chronological Signatures Along the Yarlung River Drainage Tectonic and erosional history of southern Tibet from rivers Tectonic and erosional history of southern Tibet recorded by detrital chronological signatures along the Yarlung River drainage Barbara Carrapa†, Mohd Faiz bin Hassim, Paul A. Kapp, Peter G. DeCelles, and George Gehrels Department of Geosciences, University of Arizona, 1040 E. 4th Street, Tucson, Arizona 85721, USA ABSTRACT INTRODUCTION zone provides an opportunity to broadly sample source rocks in the region and to study the tim- The Indus-Yarlung suture zone, within the The Indus-Yarlung suture zone in southern ing of regional cooling and inferred erosion larger Indo-Asia collision zone in southern Tibet (Fig. 1A) is part of the larger Indo-Asia related to processes following India-Asia col- Tibet, is characterized by a central depres- collision zone, which represents the modern lision (e.g., Hoang et al., 2009; Zhang et al., sion with two oppositely directed axial rivers: surface expression of the contact between the 2012; Saylor et al., 2013). Whereas previous the eastward-flowing Yarlung River and the Indian and Eurasian continental plates as a result work focused on detrital zircon U-Pb geochro- westward-flowing Indus River. The axial of Paleocene collision (e.g., Garzanti et al., 1987; nology of modern rivers from the main Yarlung valley is flanked by high-elevation ranges Najman et al., 2010; DeCelles et al., 2014; Hu River and the eastern part of its drainage system of the southern Lhasa terrane to the north et al., 2015). The Indus-Yarlung suture zone is (Zhang et al., 2012; Cina et al., 2009), this study and the Tethyan Himalaya to the south. This characterized today by a depression occupied by includes the poorly studied western portion of study analyzes the detrital geochronological the eastward-flowing Yarlung River, with tribu- the Yarlung drainage system and two rivers and thermochronological signatures of rivers taries that drain the Gangdese magmatic arc, draining the Kailas and Xiao Gurla ranges into draining into the Indus-Yarlung suture zone Xigaze forearc, and Cenozoic strata to the north, La’nga and Mapan Yum lakes respectively. as a proxy for the timing of tectonic, mag- and Paleo zoic–Mesozoic Tethyan Himalayan Detrital studies commonly assume that the matic, and erosional processes in southern strata to the south (Fig. 1). The Yarlung drainage sample age distributions from sedimentary ba- Tibet. Zircon U-Pb ages reflect source area includes several large nonmarine Cenozoic sedi- sin strata and modern river sand samples closely crystallization ages, and their distribu- mentary basins, such as the Oligocene–Miocene match the age spectra within the drainage catch- tion is proportional to the relative area of Kailas basin (Aitchison et al., 2002; DeCelles ments of the eroding source region. For ex- source rocks exposed in the catchment areas. et al., 2011), and the Miocene Liuqu basin (Li ample, the degree of mixing of different source Rivers draining the northern side of the colli- et al., 2015a; Leary et al., 2016a). Formation of signals, as recorded by detrital zircon U-Pb sion zone are dominated by ages between the Kailas basin has been associated with ex- detrital ages in modern river sands, has been ca. 40 Ma and ca. 60 Ma, similar to ages of tension possibly related to slab rollback or trans- shown to be proportional to the exposed source rocks in the Gangdese arc, whereas one river tension along the Karakoram fault (DeCelles area within the catchment (Saylor et al., 2013). sample draining the southern side records et al., 2011). Thermochronological studies show This approach is based on the assumption that a Tethyan Himalayan signature character- cooling of the Kailas (Carrapa et al., 2014) fertility of source rocks is the same in all of the ized by age clusters at ca. 500 Ma and ca. and Liuqu basins (Li et al., 2015a; Leary et al., drained lithological units. This assumption may 1050 Ma. U-Pb zircon ages from the modern 2016a) at ca. 17 Ma and ca. 12–10 Ma respec- not be valid if significant volumes of ultramafic drainages are similar to signals preserved in tively, which is consistent with >4 km of basin rocks and limestone are present in the drainage the Oligocene−Miocene Liuqu and Kailas exhumation. Cooling of the Gangdese arc and of area. Our study area does not contain significant basins, suggesting that the geology of the the Tethyan Himalaya near Lhasa between ca. limestone and ultramafic rocks, and therefore Ceno zoic drainages was similar to modern, 20 Ma and 10 Ma has been associated with ac- we consider this assumption to be valid. albeit with significant erosion in the Miocene. celerated upper-crustal exhumation (Fig. 1; e.g., Other studies have documented that zircon New apatite fission-track (AFT) ages from Dai et al., 2013; Li et al., 2015b). An early Mio- U-Pb ages of modern samples not only reflect some of the same rivers show an early Mio- cene pulse of at least local rapid exhumation in- mixing of upstream bedrock sources, but are also cene regional exhumation signature, which is ferred from rock cooling was detected by Cope- influenced by a dilution effect owing to progres- interpreted to record regional uplift-induced land et al. (1987) and Harrison et al. (1992) in sive downstream mixing, topographic relief, and erosion coupled with efficient river incision some of the earliest thermochronological work precipitation (Zhang et al., 2012). Although this by the Indus-Yarlung fluvial system as a re- in southern Tibet. However, the regional extent, is an important issue to consider when sampling sult of renewed underthrusting (following timing, and magnitude of such Cenozoic cooling progressively downstream along a main trunk rollback) of India under Asia. Late Miocene in southern Tibet and underlying mechanisms river, it should not be an issue when sampling (ca. 8 Ma) apatite (U-Th)/He (AHe) ages are remain poorly constrained. Another feature that tributaries with smaller drainage basins. consistent with cooling and exhumation asso- is not well understood is the timing of establish- The goal of this study was to test the follow- ciated with E-W extension followed by a de- ment of the modern Yarlung drainage. ing hypotheses. (1) Detrital minerals from the crease in erosion after ca. 6 Ma. Detritus from modern rivers, mostly includ- Yarlung drainage, including the Indus-Yarlung ing tributaries of the Yarlung River, draining suture zone within the larger Indo-Asia collision †bcarrapa@ email .arizona .edu southern Tibet and the Indus-Yarlung suture zone (Fig. 1), directly reflect cooling due to ero- GSA Bulletin; Month/Month 2016; v. 128; no. X/X; p. 1–12; doi: 10.1130/B31587.1; 6 figures; 1 table; Data Repository item 2016356.; published online XX Month 2016. For permission to copy, contact [email protected] Geological Society of America Bulletin, v. 1XX, no. XX/XX 1 © 2016 Geological Society of America Carrapa et al. 1A 72o E 80o E 88o E 96o E 36o N Indus Rive Ladakh r TIBET Zhang et al. (2012) batholith Li et al. (2016) 1B 32o N Li et al. (2015) Mt. Kailas Dai et al. (2013) Lhasa Yarlung RiLopu Range Namche ver g R Leary et al. (2016) Satlej Ri Ganges Ri rnali ive S Barwa i r Xigaze a Ka n Kailas basin River g R. o ve Mt. Everest 28 N r r 200 km Brahmaputra Rive Indus River Karakoram Faul India-Asia 1B 1C A′ A suture zone o Main Central Thrust Xigaze 32 N Forearc Kailas Fm. Tethyan Thrust Belt Liuqu Fm. Gangdese Arc t Lesser Him. Sequence subduction complex Asian plate Indian plate Mt. Kailas ~25 km Greater Himalayan Lhasa terrane Sequence 0~100 km o River 7 River 6 31 N La'nga Lake subduction complex Xiao Gurla A Mapam Yarlung drainage Yum Lake Lopukangri 30oN Range River 5 River 3 Geydo Jiada Yarlung River River 2 Dogxhun River 4 Xigaze Karnali River 1 29oN River Shab Chu Kaligandaki River A' 28oN 0 200 km 81oE83oE 85oE87oE89oE 91oE 1D River 7 River 6 River 5 River 1 2% 9% 3% 10% 2% 2% 72% 39% 53% 39% 4% 58% 8% 13% 3% 48% 17% 5km River 4 RiverRiv 2 4% 18% 9% 23% 9% River 3 14% 21% 17% 20% 35% 1% 20% 28% 9% 33% 12% 14% 31% Gangdese arc plutonic rocks Gneiss domes Tethyan Himalaya rocks Ophiolites Cenozoic sedimentary rocks Xigaze Fm. Kailas Formation and Melanges Linzizong volcanics Figure 1. (A–B) Digital topographic maps of the southern Tibetan Plateau and the Himalayan orogen based on Global Multi-Resolution Topography (GMRT) data. Main streams of the rivers are marked by blue lines; their tributaries are marked by red lines. Rivers 1–7 mark locations of sand samples collected from tributaries of the Yarlung River in this study. (C) Simplified cross section across southern Tibet and the Himalaya, modified after Murphy (2007). (D) Diagrammatic maps of the bedrock geology (from 1:1,500,000 geological map of Tibet; Pan et al., 2004) in each of the analyzed river catchment areas; pie charts indicate relative proportions of different rock types. 2 Geological Society of America Bulletin, v. 1XX, no. XX/XX Tectonic and erosional history of southern Tibet from rivers sion of the source area and therefore are repre- rocks and Cenozoic sedimentary strata. Most of cons and apatites were separated from river sentative of regional tectono-thermal signatures. the sampled rivers drain into the Yarlung River sand samples using standard techniques. The (2) Miocene exhumation in southern Tibet (except for Rivers 6 and 7), which in turn flows interpreted zircon U-Pb ages and main popu- was widespread and had tectono-climatic sig- eastward to the eastern Himalayan syntaxis, lations are shown on relative age-probability nificance.
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