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Minerals 2019, 9, 528 10 of 15 abundant Li to the waters [69,81]. This conclusion may shed light on the phenomenon that Li-rich salt lakes mainly distributed around the suture zones. Besides the widespread modern geothermal springs, ancient geothermal activities were also intensive on the QTP, certified by extensive geyserites and travertine deposits with high concentrations of Li, Rb, Cs and B [82,83]. Geyserites or travertine deposits are widespread in several Li-rich salt lakes, such as Dangxiong Co, Zabuye Lake, Duogecuoren Co, etc. In the Zabuye Lake, ancient travertine deposits occur extensively along the faults in the central and western parts. Some travertine mounds are still active and spring waters supply into the Zabuye Lake. These spring waters usually contain high Li concentrations (0.02–4.70 mg/L), which is an important source of Li in the Zabuye Lake. Zheng and Liu [15] reported a Miocene Li-rich (20–111 μg/g) volcanic-sedimentary sequence in the northwestern part of Ngangla Ringco Lake on the QTP, and emphasized that weathering of these rocks provides significant part of Li in the salt lakes in this region. Similarly, in the Zabuye Lake, Li is also enriched in inflowing rivers (0.2–1.1 mg/L) and has an increasing trend from the upper to lower reaches, suggesting that weathering of surrounding rocks and sediments also provides Li to the lake. Besides the above three sources of Li, brine migration also takes part in the formation of Li-rich brines in several salt lakes on the QTP. The low-lying Laguo Co receives a significant part of solutes from the neighboring topographical-high Jibu Chaka, Jiangge Co and Xizha Co. A similar process is also observed from the high-altitude Rejue Chaka to low-lying Kangru Chaka, the Songmuxi Co to Longmu Co, and the Taruo Co to Zhabuye Lake [40,41,84]. In recent years, Li-rich deep brines (a potential Li resources with Li concentrations ranging from 0.22–1890 mg/L), discovered in some anticlines in the western Qaidam Basin, may be another Li source for the salt lakes in this region [85,86]. The deep geothermal waters related to felsic volcanic rocks may provide Li to the deep brines in the western Qaidam Basin [80]. 4.2. The Formation Model of Li Brine Deposits on the QTP Zheng and Liu [15] and Li et al. [11] emphasized the climate and tectonic-geomorphologic conditions for the high Li concentrations in salt lakes on the QTP. These conclusions are of great importance to understanding the formation of Li brine deposits in salt lakes on a large scale. The primary condition for the formation of Li-rich salt lakes on the QTP should be the sufficient sources of Li, including the geothermal waters, weathering of igneous rocks and Li-rich sediments, which were discussed in the Section 4.1. Salt lakes in the Xinjiang and Inner Mongolia provinces, western China, have barely any Li brine deposits due to lack of geothermal activities. Even on the QTP, Li-rich salt lakes are mainly clustered in major suture zones and igneous/volcanic rock areas, which can be supplied by Li-rich geothermal/river waters. Then, endorheic basins related to topographical low, such as the Qaidam Basin, provide suitable residual places for the Li-rich spring or river waters. Finally, under arid climate, suggesting strong evaporation and less precipitation, these waters can evolve to Li-rich brines with sufficient time. Salt lakes on the QTP are mainly distributed in the west part of the QTP with the stronger aridity; meanwhile Li-rich salt lakes are not presented in the southern and eastern part of the QTP where geothermal activities are very strong (Figure 1). This is due to the relatively humid climate and extensive exorheic watershed in the southern and eastern QTP. Even though there are sufficient Li sources, arid climate and endorheic basin in the Yahu Lake in the Qaidam Basin, Li brine deposit is not formed because of the short residual time. Thus, the above four factors jointly constrain the distribution, Li grades of Li-rich salt lakes on the QTP. The schematic formation model of Li-rich salt lakes on the QTP is shown in Figure 4. In addition, when studying the formation of Li brine deposits in salt lakes on the QTP, some basin scale processes, including absorption of Li by clay, evaporites formation, should be considered. For example, Li reserves in the Bielatan and Yiliping playas, Dongtai and Xitai salt lakes are 2.3 million tons; however, according to the recharge time (>10,000 years), the annual runoff (~10.83 × 108 m3), Li content (0.727 mg/L) of the supplying Nalenggele River water, the total Li (~7.9 million tons Li) supplied by river is much larger than the present reserves [33–35]. The Li may be lost during the riverPDF Image | Lithium-Rich Brines in Salt Lakes on the Qinghai-Tibetan
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