CAJ | 학술논문

陕西省煎茶岭金矿床位于勉-略-阳三角区东北部，勉略缝合带南侧。矿体受 F1-45断裂及次级断裂控制。根据矿物共生组合及脉体穿切关系，可将成矿期划分为三个阶段：(Ⅰ)石英-黄铁矿-白云石细脉，含少量硫化物，变形强烈，形成于变形早期或同构造变形期；(Ⅱ)石英-多金属硫化物-碳酸盐细脉，发育大量铬云母；(Ⅲ)白云石-方解石-石英-雄黄-雌黄细脉，形成于张性环境。H、O同位素数据显示，早阶段成矿流体的δD值平均为-76.5‰，δ18OW值变化于7.5‰~21.1‰，类似于变质水，晚阶段δD值为-81‰，δ18OW变化于2.5‰~7.7‰，接近大气降水线，指示初始成矿流体为变质流体，晚阶段向大气降水演化。C同位素研究显示，早阶段成矿流体δ13CCO2为-2.4‰~2.6‰，中阶段成矿流体δ13CCO2为-1.9‰~0.4‰，晚阶段为-5.0‰~1.6‰，指示早阶段成矿流体来源于碳酸盐岩地层的变质分解，晚阶段有大气降水的混入。矿石S同位素显示较高的正值，集中于10‰~15‰，与断头崖组地层一致，指示成矿物质与断头崖组地层有关。相比于赋矿围岩，矿石Pb同位素具有更低的放射性成因铅，指示成矿物质需要有另一更低放射性成因铅的物质端元，即地幔物质的加入。总之，初始成矿流体以变质流体为主，成矿流体及成矿物质可能主要来源于围岩，另有少量深部(地幔)物质加入。
합서성전다령금광상위우면-략-양삼각구동북부，면략봉합대남측。광체수 F1-45단렬급차급단렬공제。근거광물공생조합급맥체천절관계，가장성광기화분위삼개계단：(Ⅰ)석영-황철광-백운석세맥，함소량류화물，변형강렬，형성우변형조기혹동구조변형기；(Ⅱ)석영-다금속류화물-탄산염세맥，발육대량락운모；(Ⅲ)백운석-방해석-석영-웅황-자황세맥，형성우장성배경。H、O동위소수거현시，조계단성광류체적δD치평균위-76.5‰，δ18OW치변화우7.5‰~21.1‰，유사우변질수，만계단δD치위-81‰，δ18OW변화우2.5‰~7.7‰，접근대기강수선，지시초시성광류체위변질류체，만계단향대기강수연화。C동위소연구현시，조계단성광류체δ13CCO2위-2.4‰~2.6‰，중계단성광류체δ13CCO2위-1.9‰~0.4‰，만계단위-5.0‰~1.6‰，지시조계단성광류체래원우탄산염암지층적변질분해，만계단유대기강수적혼입。광석S동위소현시교고적정치，집중우10‰~15‰，여단두애조지층일치，지시성광물질여단두애조지층유관。상비우부광위암，광석Pb동위소구유경저적방사성성인연，지시성광물질수요유령일경저방사성성인연적물질단원，즉지만물질적가입。총지，초시성광류체이변질류체위주，성광류체급성광물질가능주요래원우위암，령유소량심부(지만)물질가입。
The Jianchaling gold deposit in Shaanxi province, China, is located to the south of the Mianlue suture zone. The ore bodies were controlled by fault F1-45 and the secondary faults. The hydrothermal ore-forming processes can be divided into three stages according to the mineral assemblages and the crosscutting relationships of the veinlets as follows: (I) quartz-pyrite-dolomite vein with poor sulfides which was strongly deformed in a compressional or transcompressional setting; (II) quartz-polymetallic sulfides vein, characterized by large amount of fuchsite; and (III) dolomite-calcite-quartz-orpiment-realgar veinlets. The δ18OW and δD values of early stage fluids range from 7.5‰ to 21.1‰, with an average of 13.3‰, and from-85‰to-70‰, with an average of-77‰, respectively;while theδ18OW of late stage fluids range from 2.5‰to 7.7‰, with an average of 6.5‰, and the average value of δD is-81‰. This H-O isotopic signature suggests a shift from metamorphic water towards meteoric water. δ13CCO2 values of the ore-forming fluid range from -2.4‰ to 2.6‰ in stage I, from -1.9‰ to 0.4‰ in stage II, and from -5.0‰ to 1.6‰ in stage III, respectively, indicating that the ore-forming fluids were derived from metamorphic devolatilisation of carbonate strata. The δ34S values of the Jianchaling ores (10.0‰~14.3‰) suggest that the sulfur was mainly sourced from evaporation strata. The Pb isotope ratios of the ores have less radiogenic Pb isotope than the host rocks, and suggest that the ore-forming fluids, which interacted with the wallrocks to form ores, must have been sourced from a depleted mantle or a depleted subducting oceanic slab. In combination with the H, O, C, S and Pb geochemical signatures of the mineral systems, we argue that the initial ore-forming fluid is mainly metamorphic extracted from the dehydration of the wall rocks, and the ore-forming materials might have derived mainly from the wall rocks with mantle input.