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中国西南右江盆地的卡林型金矿矿集区和三都-丹寨汞矿带，位于扬子地块西南缘，该地区是中国最重要的金汞资源产地之一。右江盆地中的卡林型金矿被区域性的大断裂限制在近三角形的地质构造中，因而被称之为“金三角”。右江盆地东北部的三都-丹寨地区，是我国黔西南地区最大的汞矿带。右江盆地中的卡林型金矿和盆地外围的汞矿在矿床地质特征方面既有相似之处，也有不同之处。本文以右江盆地内的水银洞、紫木凼、烂泥沟、八渡、者桑等卡林型金矿和滥木厂铊-汞矿以及丹寨地区的四相厂汞矿为研究对象，通过详细的野外地质与岩石学观察，并结合室内显微镜、电子探针（EPMA）、阴极发光（CL）等方面的研究，确定了矿床的矿物共生关系及生成顺序。在此基础上，运用激光剥蚀等离子体质谱（LA-ICP-MS）和二次离子探针（SIMS）等技术，系统研究了矿物的微量元素和碳氧同位素地球化学，并进行了碳酸盐矿物的原位U-Pb定年研究。通过对右江盆地卡林型金矿和汞矿的对比研究，主要取得以下成果：1、确定了矿床的矿物组合特征右江盆地卡林型金矿中的碳酸盐矿物以方解石为主，且方解石可以分为三期，成矿前期方解石（Cal 1），成矿晚期方解石（Cal 2），成矿期后方解石（Cal 3）。三丹地区汞矿中的碳酸盐矿物则以白云石为主，白云石可以分为两期，成矿早期团块状白云石（Dol 1期），成矿晚期白云石脉（Dol 2）和成矿晚期方解石脉（Cal 2 期）。卡林型金矿中出现的常见矿物为含砷黄铁矿、黄铁矿、毒砂、辉锑矿、雄黄、雌黄、石英、方解石、白云石、绢云母，而汞矿中的常见矿物为辰砂、黄铁矿、辉锑矿、石英、方解石、白云石，很难见到雄黄和雌黄。卡林型金矿的蚀变类型丰富多样，主要有黄铁矿化、雄黄和雌黄化、硅化、碳酸盐化等，汞矿则主要为白云石化。2、确定了矿物的稀土元素组成特征和控制因素右江盆地卡林型金矿的围岩和雄黄样品中的稀土元素低于热液成因碳酸盐矿物的稀土元素含量。卡林型金矿成矿前期和成矿期后的大部分方解石样品的稀土配分形式为轻稀土富集型，而成矿晚期大部分方解石样品的稀土配分形式为中重稀土富集型。三丹地区汞矿中碳酸盐矿物的稀土配分形式则为轻稀土富集型和平坦型。可见，金矿和汞矿碳酸盐矿物稀土配分形式不同。右江盆地卡林型金矿床与矿化相关的方解石富集中重稀主要受成矿流体组成和性质的影响，方解石的晶体化学性质对稀土含量和分配的控制作用不明显。3、确定了成矿流体成因和来源右江盆地内部的卡林型金矿（含滥木厂铊汞矿）的成矿流体非单一来源，表现为流体混合特征：成矿早期以岩浆流体混合变质流体为主，成矿晚期以盆地卤水混合大气降水为主。而盆地外围汞矿的成矿流体则以盆地卤水混合大气降水为特征，无岩浆水参与。这种差异表明，盆地内部的金矿和外部的汞矿具有相对独立的成矿流体系统。卡林型金矿的成矿物质主要来自于盆地基底地层，而汞矿的成矿物质则主要来自赋矿地层。4、确定了成矿流体性质相对于卡林型金矿，汞矿成矿流体的温度较低，但盐度更高。卡林型金矿的成矿温度为120-280℃，盐度变化范围为0.2-8.6（wt% NaCleq.）。而汞矿成矿温度一般为90-170℃，盐度主要集中在2-26（wt% NaCleq.）范围内。5、确定了成矿时代丹寨四相厂汞矿中白云石的原位U-Pb年龄为454±21Ma，属于加里东期成矿。滥木厂铊-汞矿中方解石的原位U-Pb年龄为97-106.2Ma，属于燕山晚期。烂泥沟金矿中方解石的原位U-Pb年龄为120.8±4.0Ma，为燕山晚期成矿。三丹汞矿带汞矿床的成矿主要集中在400-454Ma和114-129Ma两个时期，分别对应加里东期和燕山期。

The Carlin-type gold deposit and the Sandu-Danzhai mercury deposit belt in Youjiang basin, southwest China, are located in the southwest margin of the Yangtze block, which is one of the most important sources of gold and mercury resources in China. The Carlin-type gold deposit in Youjiang basin is restricted by regional large faults in near-triangular geological structure, so it is called golden triangle. The Sandu-Danzhai area in the northeast of Youjiang basin is the largest mercury deposit in southwest Guizhou. The Carlin-gold deposit in Youjiang basin and the mercury deposit in the periphery of the basin are similar and different in geological characteristics. Based on the research of Shuiyindong, Zimudang, Lannigou, Badu, Zhesang, Lanmuchang thallium - mercury deposit and Sixiangchang, through detailed field geological and petrological observation, combined with the indoor microscope, electron microprobe (EPMA) and cathodoluminescence (CL), and other aspects of the study, we determined the mineral symbiosis and formation of ore deposits. On this basis, the microelement and carbon and oxygen isotope geochemistry of minerals were systematically studied by laser denudation plasma mass spectrometry (LA-ICP-MS) and secondary ion probe (SIMS), and the in-situ U-Pb dating of carbonate minerals was studied. Through the comparative study of Carlin-type gold deposit and mercury deposit in Youjiang basin, the following results are obtained:1. Determined the mineral association characteristics of the depositThe carbonate minerals in the Carlin-type gold deposits in Youjiang basin are mainly calcite, which can be divided into three stages: calcite at the pre-ore stage (Cal 1), calcite at the late-ore stage (Cal 2), and calcite at the late-ore stage (Cal 3). The carbonate minerals in mercury deposits in Sandan area are mainly dolomite, which can be divided into two stages: early massive dolomite (Dol 1), late dolomite vein (Dol 2) and late calcite vein (Cal 2). The common minerals in Carlin-type gold deposits are arsenopyrite, pyrite, arsenopyrite, stibnite, realgar, dioecious, quartz, calcite, dolomite and sericite, while the common minerals in mercury deposits are chensha, pyrite, stibnite, quartz, calcite and dolomite. The alteration types of Carlin-type gold deposits are rich and varied, mainly including pyritization, realgar and pistil, silicification and carbonation, etc., while mercury deposits are mainly dolomitization.2. Determined the composition characteristics and control factors of rare earth elements of mineralsThe content of rare earth elements in the host-rocks and realgar samples of Carlin-type gold deposits in Youjiang basin is lower than that of carbonate minerals. The rare earth elements distribution forms of most calcite samples in the early and late metallogenic period of Carlin-type gold deposit are light rare earth elements enrichment type, while the rare earth elements distribution forms of most calcite samples in the late metallogenic period are medium and heavy rare earth elements enrichment type. The rare earth elements distribution forms of carbonate minerals in mercury deposits in Sandan area are light rare earth elements enrichment type and flat type. The distribution forms of the carbonate minerals in Youjiang basin are different from those in the periphery of Youjiang basin. The Carlin-type gold deposit in youjiang basin is mainly affected by the ore-forming fluid, while the crystal chemical properties of calcite have no obvious effect on the control of rare earth content.3. Determined the origin and source of ore-forming fluidThe ore-forming fluids of Carlin-type gold deposits in Youjiang basin are not single source but mixed fluids. The ore-forming fluid of Carlin-type gold deposit was magmatic fluid mixed metamorphic fluid in the early ore-forming period, and the fluid of late ore-forming period was dominated by brine mixed meteoric water in the basin. The metallogenic fluid of mercury deposit is basin brine mixed with meteoric water without the participation of magma water. The gold deposit in Youjiang basin and the mercury deposit outside the basin have relatively independent ore-forming fluid system. The major difference between them is that there is magma fluid in the basin, while there is no magma fluid outside the basin. The metallogenic materials of carlin-type gold deposits are mainly from the basement of the basin, while the metallogenic materials of mercury deposits are mainly from the ore formation.4. Determined the metallogenic fluid properties The temperature of metallogenic fluid in mercury deposit was lower than that of Carlin-type gold deposit, but the salinity was higher. Carling-type gold deposit mineralization temperature is 120-280℃, the range of salinity is 0.2-8.6 (wt.% NaCleq). And mercury metallogenic temperature is 90-170℃, salinity is mainly focused on the 2-26 (wt. % NaCleq).5. Determined the metallogenic ageThe in situ U-Pb age of dolomite is 454±21Ma in Sixiangchang mercury deposit. The in-situ U-Pb age of the calcite vein in the Lanmuchang thallium-mercury deposit is 97-106.2Ma, which is the late yanshanian mineralization. The in-situ U-Pb age of the calcite in the Lannigou gold deposit is 120.8±4.0Ma, which is the ore-forming stage of yanshanian. The metallogenic time of mercury deposit in Sandan mercury belt was mainly in two periods, 400-454Ma and 114-129Ma, respectively corresponding to Caledonian and Yanshanian.