The Yanbian mining district is located at the eastern end of the Central Asian orogenic belt and northeast of the western Pacific continental margin metallogenic belt. It is a porphyry-epithermal Cu-Au mining district related to Mesozoic continental volcanic eruptions and hypabyssal magmatism. To explore the genesis and mineralization process of epithermal gold deposits, we conducted a systematic study of the geology, fluid inclusions and H-O-S-Pb isotopes of the Ganhegou gold deposit, which is expected to be revealed as a medium-sized deposit in the latest exploration. We found the following: (1) The deposit occurs in Early Cretaceous continental andesites of the Jingouling Formation and granodiorite porphyry. The ore belts are controlled by NW-trending volcanic faults. The mineralization process can be divided into the quartz-hematite-arsenopyrite-pyrite stage (I), grey-white quartz-pyrite stage (II), smoky quartz-polymetallic sulfide stage (III), milky quartz-adularia stage (IV) and carbonate stage (V). Gold precipitated in stage III. (2) Vapour-rich-, liquid-rich-, pure-liquid- and pure-vapour-type FIs developed in quartz in stages II, III and IV, and the average homogenization temperatures in these stages are 325 ℃, 273 ℃ and 229 ℃, respectively. The ore-forming fluids belonged to the H₂O-NaCl ± CO₂ system. (3) The δ¹⁸O_H2O and δD_H2O values of stage II-IV range from −9.9 to −5.2‰ and −121.9 to −119.8‰, respectively, indicating that the ore-forming fluids were driven by intermediate-felsic magmatic water and mixed with meteoric water during mineralization. (4) The δ³⁴S values of pyrite in stages II and III range from −5.8 to −3.4‰, whereas the values of ²⁰⁶Pb/²⁰⁴Pb, ²⁰⁷Pb/²⁰⁴Pb and ²⁰⁸Pb/²⁰⁴Pb are 15.529–15.551, 18.239–18.257 and 38.075–38.153, respectively, implying that the ore-forming materials were derived from Neoproterozoic lower crust. These characteristics indicate that Ganhegou is a low-sulfidation epithermal gold deposit. Mineralization occurred via several main processes: (i) The ore-forming fluids migrated along volcanic faults to suitable positions driven by intermediate-felsic magmatic water. (ii) In stage I, the quartz-arsenopyrite-hematite assemblage formed under relatively high oxidation conditions. (iii) In stage II, the pyrite-hessite-galena-quartz veins formed in the near-neutral environment, which was slightly reduced relative to that of stage I due to the fluid boiling. (iv) In stage III, the gold-bearing quartz veins formed due to the fluid boiling and mixing. (v) In stage IV, the precipitation of quartz-adularia-pyrite veins occurred under near-neutral conditions (pH≈5). (iv) Small-scale carbonate veinlets formed in stage V, signalling the end of mineralization.

延边矿区位于中亚造山带的东端，在西太平洋大陆边缘成矿带的东北部。它是与中生代大陆火山喷发和下伏岩浆作用有关的斑岩-上热铜金矿区。为了探索超热金矿床的成因和成矿过程，我们对赣河沟金矿床的地质，流体包裹体和HOS-Pb同位素进行了系统的研究，有望在最新勘探中作为中型矿床揭示出来。 。我们发现：（1）沉积物存在于金沟岭组早白垩世陆安山岩和花岗闪长斑岩中。矿带受西北走向的火山岩断层控制。矿化过程可分为石英-赤铁矿-毒砂-黄铁矿阶段（I），灰白色石英-黄铁矿阶段（II），烟熏石英-多金属硫化物阶段（III），乳状石英-金刚砂阶段（IV）和碳酸盐阶段（V）。金在阶段III中沉淀。（2）在第II，III和IV阶段在石英中开发的富蒸气，富液体，纯液体和纯蒸气型FIs，这些阶段的平均均质温度为325 ℃，273  ℃和229  ℃。成矿流体属于H ₂ O-NaCl±CO ₂系统。（3）δ ^18个ö _H2O和δD _H2O阶段II-IV范围的值从-9.9到-5.2‰和-121.9至-119.8‰，分别指示成矿流体通过中间英质岩浆水驱动并在矿化过程中与流星水混合。（4）δ ³⁴在从-5.8到-3.4‰第二和第三阶段范围黄铁矿的价值观，而值²⁰⁶的Pb / ²⁰⁴的Pb，²⁰⁷的Pb / ²⁰⁴ Pb和²⁰⁸的Pb / ²⁰⁴铅分别为15.529–15.551、18.239–18.257和38.075–38.153，这表明成矿物质来自新元古代下地壳。这些特征表明赣河沟是一种低硫化超热金矿床。成矿是通过几个主要过程发生的：（i）成矿流体沿着火山断层迁移到中长生质岩浆水驱动的合适位置。（ii）在阶段I中，在相对较高的氧化条件下形成了石英-亚砷铁矿-赤铁矿集合体。（iii）在阶段II中，在接近中性的环境中形成了黄铁矿-黄铁矿-方铅矿-石英脉，由于流体沸腾，与阶段I相比，其略有减少。（iv）在第三阶段，由于流体沸腾和混合，形成了含金石英脉。（v）在第四阶段，石英-黄铁矿-黄铁矿脉的沉淀发生在接近中性的条件下（pH≈5）。（iv）在第五阶段中形成了小规模的碳酸盐矿脉，这标志着矿化的结束。