| Citation: |
Hua-wen Cao, Qiu-ming Pei, Xiao Yu, Ai-bin Cao, Yong Chen, Hang Liu, Kai Zhang, Xin Liu, Xiang-fei Zhang, 2023. The long-lived partial melting of the Greater Himalayas in southern Tibet, constraints from the Miocene Gyirong anatectic pegmatite and its prospecting potential for rare element minerals, China Geology, 6, 303-321. doi: 10.31035/cg2022061
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The long-lived partial melting of the Greater Himalayas in southern Tibet, constraints from the Miocene Gyirong anatectic pegmatite and its prospecting potential for rare element minerals
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Abstract
The Cenozoic Himalayan leucogranite-pegmatite belt has been a hotspot for rare metal exploration in recent years. To determine the genesis of the pegmatite in the Himalayan region and its relationship with the Greater Himalayan Crystalline Complex (GHC), the Gyirong pegmatite in southern Tibet was chosen for geochronological and geochemical studies. The dating analyses indicate that the U-Th-Pb ages of zircon, monazite, and xenotime exhibit large variations (38.6‒16.1 Ma), with the weighted average value of the four youngest points is 16.5 ± 0.3 Ma, which indicates that the final stage of crystallization of the melt occurred in the Miocene. The age of the muscovite Ar-Ar inverse isochron is 15.2 ± 0.4 Ma, which is slightly later than the intrusion age, showing that a cooling process associated with rapid denudation occurred at 16‒15 Ma. The εHf(t) values of the Cenozoic anatectic zircons cluster between −12 and −9 with an average of −11.4. The Gyirong pegmatite shows high contents of Si, Al, and K, a high Al saturation index, and low contents of Na, Ca, Fe, Mn, P, Mg, and Ti. Overall, the Gyirong pegmatite is enriched in Rb, Cs, U, K, Th and Pb and depleted in Nb, Ta, Zr, Ti, Eu, Sr, and Ba. The samples show a high 87Sr/86Sr(16 Ma) ratio of ca. 0.762 and a low εNd(16 Ma) value of −16.0. The calculated average initial values of 208Pb/204Pb(16 Ma), 207Pb/204Pb(16 Ma) and 206Pb/204Pb(16 Ma) of the whole rock are 39.72, 15.79 and 19.56, respectively. The Sr-Nd-Pb-Hf isotopic characteristics of the Gyirong pegmatite are consistent with those of the GHC. This study concludes that the Gyirong pegmatite represents a typical crustal-derived anatectic pegmatite with low metallogenic potential for rare metals. The Gyirong pegmatite records the long-term metamorphism and partial melting process of the GHC, and reflects the crustal thickening caused by thrust compression at 39‒29 Ma and the crustal thinning induced by extensional decompression during 28‒15 Ma.
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Hua-wen Cao, Qiu-ming Pei, Xiao Yu, Ai-bin Cao, Yong Chen, Hang Liu, Kai Zhang, Xin Liu, Xiang-fei Zhang, 2023. The long-lived partial melting of the Greater Himalayas in southern Tibet, constraints from the Miocene Gyirong anatectic pegmatite and its prospecting potential for rare element minerals, China Geology, 6, 303-321. doi: 10.31035/cg2022061
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Figure 1.
Geological framework and distribution of Cenozoic granites in the Himalayas (modified from Cao HW et al. , 2022a). a‒Geographical location of the study area; b‒distribution map of leucogranites and gneiss domes (NHGDs) in the Himalayan region; c‒geological profile of the eastern Himalayas. Gneiss domes and Cenozoic granites in the Tethyan Himalayas: 1. Zanskar (Gianbul‒Gumburanjun), 2. Tso Morari, 3. Leo Pargil, 4. Zhada 5. Grula Mandhata‒Xiao Gurla, 6. Mayum, 7. Mustang‒Dlou‒Mugu, 8. Qukangyi, 9. Niuku, 10. Changguo, 11. Qiazuweng‒Kung Tang, 12. Cuobu‒Malashan‒Paiku, 13. Xiaru, 14. Suozuo‒Dingri‒Zharishizhong, 15. Dinggye‒Ama Drime, 16. Lhagoi Kangri, 17. Mabja‒Sakya‒Kuday, 18. Kangpa, 19. Kangma, 20. Ramba, 21. Langkazi‒Zhegu‒Haweng‒Cuomei, 22. Luozha‒Lalong, 23. Yalaxiangbo‒Dala, 24. Longzi‒Liemai‒Ridang‒Quedang, 25. Cuonadong, 26. Kongbugang; Cenozoic granites in the Greater Himalayas: 27. Sutlej, 28. Garhwal‒Gangotri, 29. Shivling, 30. Malari, 31. Bura Buri, 32. Dhaulagili‒Annapurna‒Thakkhola, 33. Manaslu, 34. Gyirong‒Langtang, 35. Shisha Pangma, 36. Nyalam, 37. Qomolangma‒Lhotse‒Rongbuk‒Pushila‒Qiongjiagang, 38. Makalu, 39. Kanchenjunga‒Sikkim, 40. Yadong‒Dingga‒Gaowu, 41. Lingshi‒Jomolhari, 42. Wagya La‒Chongba, 43. Masang Kang‒Paro, 44. Kula Kangri‒Luozha‒Lalong, 45. Lakang‒Kuju, 46. Cuona‒Yamarong‒Lebugou‒Tawang, 47. western Himalayan syntaxis‒Nanga Parbat, 48. eastern Himalayan syntaxis‒Namcha Barwa.
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Figure 2.
Tectonic setting (a) and geological section (b) of the Gyirong area showing the sampling location (modified from Wang XX et al., 2017).
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Figure 3.
The field outcrop (a), hand specimen photographs (b) and photomicrographs (c and d) show the petrological characteristics of the pegmatite in the Gyirong town. The main minerals are quartz (Qz), alkali feldspar (Afs), plagioclase (Pl), muscovite (Ms), tourmaline (Tur) and garnet (Grt).
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Figure 4.
Cathodoluminescence (CL) images of zircons (a), backscattered electron (BSE) images of monazite (b) and xenotime (c) showing the dating position and ages. Normalized rare earth element compositions of zircon, monazite and xenotime (e). Chondrite meteorite values are quoted from Sun SS and McDonough WF (1989).
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Figure 5.
Zircon, monazite and xenotime U-Th-Pb geochronology of the Gyirong pegmatite. Zircon U‒Pb concordia diagrams (a), kernel density estimates (KDEs) showing age frequency distribution (b), and the weighted mean ages (c). Monazite U‒Pb concordia diagrams (d), KDEs (e), and the weighted mean ages (f). Xenotime U‒Pb concordia diagrams (g), KDEs (h), and the weighted mean ages (i).
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Figure 6.
Histograms of the zircon εHf(t) (a) and two‒stage model age results (b). Scatter plot of the zircon U‒Pb age versus εHf(t) (c).
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Figure 7.
40Ar-39Ar plateau age of muscovite from the Gyirong pegmatite (a). Isochron Ar-Ar age of muscovite (b).
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Figure 8.
Histogram of U‒Pb age of zircon, monazite and xenotime and Ar-Ar age of muscovite from Gyirong pegmatite (a). Metamorphic pressure‒temperature‒time (P‒T‒t) path and stages of the Greater Himalayan sequence, showing the duration of muscovite and biotite dehydration and melt crystallization (b). Modified from Zhang ZM et al. (2022) and Gou ZB et al. (2022).
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Figure 9.
Classification nomenclature diagram of SiO2 versus Na2O+K2O‒CaO (a). Modified from Frost CD and Frost BR (2011). Cationic classification of A=Al‒(K+Na+2Ca) versus B=Fe+Mg+Ti (b). Modified from Debon F and Le Fort P (1983). Diagram of A/CNK versus A/NK (c). Modified from Maniar PD and Piccoli PM (1989).
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Figure 10.
Chondrite- and primitive mantle-normalized rare earth element (a) and trace element (b) spider charts for the Gyirong pegmatite. Chondrite meteorite and primitive mantle values are quoted from Sun SS and McDonough WF (1989) and McDonough WF and Sun SS (1995). The average values for the total continental crust are quoted from Rudnick RL and Gao S (2014).
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Figure 11.
Diagrams of whole-rock 87Rb/86Sr versus 87Sr/86Sr (a), 87Sr/86Sr25 Ma versus εNd(16 Ma) (b), 207Pb/204Pb(16 Ma) versus 206Pb/204Pb(16 Ma) (c) and 208Pb/204Pb(16 Ma) versus 206Pb/204Pb(16 Ma) (d) for the Gyirong pegmatite. The Sr-Nd-Pb isotopes of GHC are from Cao HW et al. (2022a).