《Table 1 Fluid inclusion microthermometric data for the Jiama deposit》

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《"Fluid Evolution and Ore-forming Processes of the Jiama Cu Deposit, Tibet: Evidence from Fluid Inclusions"》

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Note:Th-Homogenization Temperature；Tice-Final ice melting temperature；Ts-Solid dissolution temperature for type ii-1 fluid inclusions；Tv-Vapor disappearance temperature for ii-2 fluid inclusions.

In the early hydrothermal stage，the first boiling took place，inferred from the coexistence of liquid-and vapordominated fluid inclusions in wollastonite of the skarns，type A quartz veins in the porphyry and type a veins in the hornfels（Fig.6a–b，g–h）.Fluid evolution led to development of a vapor phase in the 245–417°C temperature range，a low to moderate salinity（0.9–22.5wt%）liquid phase in the 243–455°C temperature range，and a high-salinity（30.2–43.4 wt%）liquid phase in the240–418°C temperature range（Table 1，Fig.8）.The second boiling event took place in the late hydrothermal stage，inferred from the coexistence of liquid-and vapordominated fluid inclusions in type B quartz veins in the porphyries，type I veins in the skarns and type c veins in the hornfels（Fig.6c–f，i–j）.This boiling event is also inferred from the brecciated skarns and stockwork structures in the hornfels（Fig.3i–j），which are consistent with sudden release of overpressured fluid.Fluid evolution in this late hydrothermal stage led to development of a vapor phase in the 225–386°C temperature range，a low to moderate salinity（2.1–23.2wt%）liquid phase in the 210–453°C temperature range，and a high-salinity（29.9–43.0wt%）liquid phase in the 237–459°C temperature range（Table 1，Fig.8）.Guo Wenbo et al.（2014）made a H-O isotope study of quartz in three types of veins in hornfels and skarns，corresponding to type a，type b/c and type I veins in this paper.TheδD andδ18OH2O data show a trend of groundwater mixing with magmatic fluid in the late hydrothermal stage（Fig.11），suggesting that the second boiling event was accompanied by groundwater mixing.