The Relin Cu–Mo deposit in the Zhongdian region, located in the south portion of the Yidun Arc, is hosted by Late Cretaceous post-magmatic granitoids. The types of mineralization are associated with hornfels, quartz vein and altered granite. The mineral paragenesis can be divided into four stages: (1) pyrite ± chalcopyrite–quartz (I); (2) pyrite–chalcopyrite ± molybdenite–quartz (II); (3) molybdenite ± chalcopyrite–quartz (III); and (4) chalcopyrite–quartz–calcite (IV), with copper–molybdenum minerals being introduced mainly in stages II and III. Four types of fluid inclusions were identified in the vein mineral assemblages: H2O\documentclass[12pt]{minimal}
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\begin{document}$$\hbox {H}_{2}\hbox {O}$$\end{document}–NaCl (VL- and LV-type), NaCl–H2O\documentclass[12pt]{minimal}
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\begin{document}$$\hbox {H}_{2}\hbox {O}$$\end{document} (SL-type), and H2O\documentclass[12pt]{minimal}
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\begin{document}$$\hbox {CO}_{2}$$\end{document}–NaCl (LC-type). The ore-forming fluids experienced a transition from H2O\documentclass[12pt]{minimal}
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\begin{document}$$\hbox {H}_{2}\hbox {O}$$\end{document}–NaCl systems. The main ore-forming fluids are magmatogenic fluids and metal-bearing hot brines. Unmixing of fluids may be the main mechanism for sulfide precipitation, and fluid boiling and degassing of CO2\documentclass[12pt]{minimal}
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\begin{document}$$\hbox {CO}_{2}$$\end{document} are the key processes of ore deposition. Fluid inclusions, REE and trace element data, and S, Re, C, H, O isotopes indicate that the ore-forming fluid is of magmatic origin and contains H2S\documentclass[12pt]{minimal}
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\begin{document}$$\hbox {H}_{2}\hbox {S}$$\end{document} and CO2\documentclass[12pt]{minimal}
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\begin{document}$$\hbox {CO}_{2}$$\end{document}, originating from Late Cretaceous Relin intrusions emplaced in shallow crustal levels. The geochronological data indicate that Cu–Mo mineralization in the Relin district formed at ∼\documentclass[12pt]{minimal}
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\begin{document}$$\sim $$\end{document}82–80 Ma. The results show that the Relin Cu–Mo deposit is a granite-related hypothermal deposit formed in a post-orogenic extensional environment due to significantly lower crustal partial melting and thickening the Yangtze Terrane during the Late Cretaceous (85–75 Ma).
