大兴安岭中北部热液铜矿床的成矿机制与资源预测
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摘要
中国东北部的大兴安岭地区是我国重要的铜、钼和铅锌等多金属热液矿床发育区，至今已发现大中型铜矿13座，超大型钼矿床1座，大中型钼矿22座，大中型铅锌银矿11座，现已成为我国重要内生金属矿产勘查战略选区。鉴于此，为了揭示制约大兴安岭内生金属成矿、找矿的基础地质问题、成矿规律和找矿方向，本文在前人研究的基础上，以区域成矿背景为前提，针对区内发育的内生热液铜矿床开展了系统的矿床地质、流体演化、地球化学以及成矿年代学等方面研究，取得了如下重要进展。
1．在区域成矿地质背景研究的基础上，通过各类铜矿床的矿床地质研究，确立研究区热液铜矿床主要有三种成因类型，分别为斑岩型铜矿床（如：乌奴格吐山、多宝山和铜山铜（钼）矿床等）、浅成热液高硫化型铜矿床（如：莲花山、闹牛山铜（银）矿床等）和接触交代型铜多金属矿床（如：小多宝山、三矿沟铜铁矿床等）。（1）斑岩型：矿体多呈不规则状、扁豆状和透镜状，产于多宝山组与花岗闪长（斑）岩或二长花岗岩与黑云母花岗岩的断裂体系内，围岩蚀变主要是钾化、硅化、绢英岩化、青磐岩化、泥化及碳酸盐化等，矿化阶段可划分为（Ⅰ）黄铁矿-石英阶段，（Ⅱ）磁黄铁矿-黄铁矿-石英阶段，（Ⅲ）石英-辉钼矿阶段，（Ⅳ）石英-黄铜矿阶段，（Ⅴ）石英-碳酸盐阶段。（2）浅成热液高硫化型：矿体以脉状、网脉状为主，其次为透镜状，产于火山断裂体系中，围岩蚀变主要是硅化、电气石化、阳起石化、绿泥石化、高岭土化和碳酸盐化等，矿化阶段可划分为（Ⅰ）黄铁矿-石英阶段，（Ⅱ）石英-磁铁矿-黄铁矿-黄铜矿阶段，（Ⅲ）纯硫化物脉阶段，（Ⅳ）石英-多金属硫化物阶段和（Ⅴ）石英-碳酸盐阶段。（3）接触交代型：矿体呈扁豆状、透镜状和脉状，产于花岗岩岩体与古生代地层接触带上，围岩蚀变以矽卡岩化为主，发育硅化、绿泥石化、绿帘石化、碳酸盐化等；可划分（Ⅰ）干矽卡岩阶段、（Ⅱ）湿矽卡岩阶段、（Ⅲ）氧化阶段，（Ⅳ）早期硫化物阶段，（Ⅴ）晚期硫化物阶段及（Ⅵ）石英-碳酸盐阶段。
2．各类主要矿床的矿物流体包裹体研究揭示：斑岩型铜矿床的均一温度分别为＞500～470℃、470～420℃、420～330℃、330～220℃、220～110℃，盐度为＞11.8～7.44%NaCleq、7.2～4.0%NaCleq、52.0～3.2%NaCleq、39.6～2.89%NaCleq和3.4～12.4%NaCleq。浅成热液高硫化型铜矿床的均一温度和盐度分别为＞420～310℃、310～270℃、270～200℃、200～160℃、160～80℃，48.9～1.39%NaCleq、6.14～1.39%NaCleq、8.81～1.22%NaCleq、8.54～2.23%NaCleq和5.55～4.17%NaCleq。接触交代型铜矿床的硫化物阶段的均一温度和盐度依次为470～230℃、230～110℃，50.1～8.8%NaCleq、5.59～1.22%NaCleq。
3．拉曼分析和子晶矿物表明：斑岩型铜矿床的初始成矿流体为富CO_2的高氧逸度的岩浆流体，成矿阶段CO_2逃逸，氧逸度降低，流体具有贫CO_2的还原性质，晚期逐渐转为弱酸性（CO_3~(2-)）。浅成热液高硫化型铜矿床初始流体为含CO_2的高氧化性、酸性流体，成矿期演化为还原流体，晚期具有弱酸性（CO_3~(2-)）的特征。接触交代型铜矿床初始流体为贫CO_2的岩浆流体，演化为弱酸性的还原流体。
4.成岩成矿年代学研究表明，斑岩型铜矿床有两个成矿期，分别是480±13Ma（锆石U-Pb谐和定年）或482～486Ma（辉钼矿Re-Os等时线），成矿与早古生代花岗闪长岩岩浆作用密切相关（多宝山铜（钼）矿床）；188Ma（单颗粒锆石U-Pb定年）或178±10Ma（辉钼矿Re-Os等时线），以乌奴格吐山铜（钼）矿床为代表，成矿与早侏罗世二长花岗斑岩岩浆活动密切相关。浅成热液高硫化型铜矿床形成于242.9±2.7Ma或222±5Ma（锆石U-Pb谐和定年），以莲花山、闹牛山铜（银）矿床为代表，成矿与三叠纪的花岗闪长斑岩和英安岩密切相关。接触交代型铜矿床形成于171.9±1.7Ma（锆石U-Pb谐和定年），以小多宝山和三矿沟铜铁矿为代表，成矿与早侏罗世花岗闪长岩岩浆作用密切。
5.与成矿密切相关的岩浆热事件的岩石成因研究揭示，奥陶纪、早侏罗世斑岩型铜矿床的成矿岩石组合分别为高钾钙碱性的花岗闪长（斑）岩和多宝山组地层、二长花岗斑岩和黑云母花岗岩，三叠纪浅成热液高硫化型铜矿床的成矿岩石组合为钠质钙碱性的花岗闪长斑岩、英安岩、闪长玢岩和安山岩，早侏罗世接触交代型铜矿床的岩石组合为高钾钙碱性的花岗闪长岩和多宝山组的碳酸岩及碎屑岩等。成矿相关的侵入岩体均为高硅、高铝、富碱的I型花岗岩，富集大离子亲石元素和轻稀土元素，亏损高场强元素，轻重分馏较明显，无Eu异常或具有轻微的负Eu异常。Sr-Nd同位素显示：它们均具有低初始锶、正钕和年轻的两阶段模式年龄的特征，结合它们的成岩年龄，多宝山、莲花山和闹牛山的源区应为与古亚洲洋板块俯冲有关的被交代的地幔楔，而乌奴格吐山与小多宝山为新生的亚洲洋壳与下地壳减压部分熔融所致。
6．成矿机制：多宝山斑岩型铜矿床中初始成矿流体的温度和压力下降至360℃与38.6MPa时，流体沸腾，并冲破围岩，导致围岩中富含金属元素的低温流体进入斑岩流体系统，发生流体混合，随后金属硫化物以浸染状或细脉浸染状充填于岩石或裂隙中。莲花山浅成热液高硫化型铜矿床成矿流体的温度降低到420℃，压力下降为38.8Mpa时，发生沸腾，但并没有导致金属元素大量卸载，当温度和压力继续下降至300℃与25.7MPa时，大气降水开始混入，金属络合物或卤化物的溶解度急剧降低，形成角砾状、脉状或细脉浸染状硫化物矿石。接触交代型小多宝山铜（铁）矿床的初始成矿流体在410℃、80MPa时与低温低盐度的地层流体发生混合，与此同时间歇性剪切挤压引起的片理化活动直接破坏了混合流体的平衡体系，流体发生强烈的沸腾，金属大量卸载，形成块状与浸染状矿体。
7．热液铜矿床的成岩成矿作用与古亚洲洋、鄂霍次克洋及古太平洋的演化密切相关。早中奥陶世—晚泥盆-早石炭世佳木斯-松嫩微板块与额尔古纳-兴安微板块拼合，导致兴安地块上产生了早古生代岛弧火山岩和加里东期闪长岩—花岗闪长岩组合，形成了以多宝山、铜山铜（钼）矿床为代表的塔木察格-牙克石-黑河铜钼成矿带。二叠纪末—早三叠世，华北板块与黑龙江板块沿西拉木伦-长春-延吉-线呈自西向东的“剪刀式”碰撞对接，同时在缝合线的西侧产生大量与俯冲或碰撞造山相关的岩浆活动，伴生大量的金属矿化作用，形成了以莲花山、闹牛山浅成热液高硫化型铜矿床为主的一系列铜多金属矿床。另一方面自晚二叠世—晚侏罗-早白垩世，鄂霍次克洋向北侧俯冲，产生了大量与俯冲造山或造山后相关的花岗岩与火山岩，形成了以乌奴格吐山、八八一和八大关铜（钼）为代表的一系列铜钼矿床。此后，在太平洋板块斜向俯冲的影响下，早期因洋盆消失而造成的加厚下地壳的部分熔融物质沿断裂上涌，最终在适当的条件下形成一系列中小型金属矿床，如小多宝山和三矿沟铜矿床。
在综合研究的基础上，对研究区的成矿规律进行了分析，嫩江-多宝山成矿区与得尔布干成矿区遭受了强烈的剥蚀，一般剥蚀大于2km，导致这两个区内的浅成低温高硫化矿床遭受了巨大的破坏，因此不发育该类型的矿床；而乌兰浩特成矿区因剥蚀较浅，使得包括低温热液型在内的三类矿床均得以保存，因此该区具有继续寻找大型的斑岩型或接触交代型等深成矿床的潜力。
The Great Xing’an Range of NE China hosts many hydrothermal Cu and other base andprecious metal mineral deposits and mineralization, is an important part of the giant CentralAsian endogenous metallogenic belt, and has been the focus of many recent studies. Mineralexploration in this area has discovered numerous large-, middle-, and small-sized Pb–Zn, Cu,and Mo deposits, including the Errentaolegai and Jiawula Pb–Zn deposits, the Duobaoshan andWunugetushan Cu–Mo deposits, the Lianhuashan and Naoniushan Cu–Ag deposits, and theMaodeng and Aonaodaba Cu–Sn deposits. The genetic types, timing of mineralization, anddynamic setting of mineral deposits in the Great Xing’an Range remain largely unknown. Thisstudy focuses on the geological characteristics, mineral deposit classification, fluid inclusion,geochemistry, and geochronology of hydrothermal Copper deposits in the Great Xing’an Range,and discusses the fluid evolution, the timing of ore formation and the source of magmas thatformed mineralization-associated plutons in this area. In addition, we seek to identify importantmetallogenic events and processes that affected the Great Xing’an Range.
Here, we classify the Cu deposits in the region into three types: porphyry Cu–Mo,high-sulfidation epithermal Cu–Ag, and skarn Cu–Fe. The porphyry Cu-Mo deposits isexemplified by the Wunugetushan, Duobaoshan and Tongshan, these orebodies are hosted byDuobaoshan Formation and granodiorite (porphyry) or biobite granite, controlled byNW–SE-trending compressive shear faults or volcanic ring fracture and are tubular, lenticularand irregular forms in shape. Mineralization-related alteration is dominated by quartz–potassic,quartz–sericite, argillic, carbonate alteration, and propylitization. Ore minerals within the depositare dominantly pyrite, chalcopyrite, molybdenite, and bornite, with minor galena, sphalerite,pyrrhotite, tetrahedrite, and arsenopyrite.The formation of this deposit involved the followingfive mineralization stages, as deduced from mineral paragenetic relationships:(I) pyrite–quartz,(II) pyrrhotite–pyrite-quartz,(III) quartz–molybdenite,(IV) quartz–chalcopyrite, and (V)quartz–carbonate. The high-sulfidation epithermal Cu–Ag deposits are hosted by volcanic ringfracture, and orebodies have vein and lenticular forms. Alteration in the deposit is associated with vuggy/residual quartz, kaolin, chlorite, epidote, carbonate, and minor tourmaline, and apartially developed potassic alteration zone. The main ore minerals are pyrite, chalcopyrite, andpyrrhotite, with minor galena, sphalerite, arsenopyrite, molybdenite, and magnetite. Five stagesof ore formation have been identified based on paragenetic relationships:(I) pyrite–quartz,(II)quartz–magnetite–pyrite–chalcopyrite,(III) sulfide veins,(IV) quartz–polymetallic sulfides, and(V) quartz–carbonate. The skarn Cu–Fe deposits is associated with skarns and an EarlyYanshanian granodiorite, and the locations of individual vertical lenticular orebody locations arecontrolled by the intersections between skarns and bedding planes. Alteration is dominated byskarnification, with minor silicification, and chlorite, epidote, and carbonate development. Oreminerals within the deposit consist of magnetite and chalcopyrite with minor pyrite andmolybdenite. Six mineralization stages during deposit formation have been identified based onparagenetic relationships:(I) a dry skarn stage,(II) a wet skarn stage,(III) an oxidized stage,(IV)an early sulfide stage,(V) a late sulfide stage, and (VI) a quartz–carbonate stage.
Fluid inclusions studies of mineralization-associated quartz within these deposits revealsthat homogenization temperatures for porphyry Cu deposits are＞500-470℃,470-420℃,420-330℃,330-220℃, and220-110℃; and salinity are＞11.8-7.44%NaCleq,7.2-4.0%NaCleq,52.0-3.2%NaCleq,39.6-2.89%NaCleq, and3.4-12.4%NaCleq, respectively.Homogenization temperatures for high-sulfidation epithermal Cu–Ag deposits are＞420-310℃,310-270℃,270-200℃,200-160℃, and160-80℃; and salinity are48.9-1.39%NaCleq,6.14-1.39%NaCleq,8.81-1.22%NaCleq,8.54-2.23%NaCleq, and5.55-4.17%NaCleq,respectively. Homogenization temperatures of sulfide stage for skarn Cu–Fe deposits are470-230℃230-110℃; and salinity are50.1-8.8%NaCleq,5.59-1.22%NaCleq.
Daughter minerals hosted by fluid inclusions and raman anysis results indicated that initialore-forming fluid for porphyry Cu-Mo deposits is derived from magma, characterized by rich inCO_2and high oxygen fugacity; then CO_2escaped, oxygen fugacity reduced in mineralizationstage, fluid tranfered to reduction performance with poor in CO_2, and weak acid （CO_3~(2-)） inadvanced stage. The initial ore-forming fluid for high-sulfidation epithermal Cu–Ag deposits isderived from magma, characterized by contain CO_2, high oxidative and acid; then fluid tranferedto reduction performance, and weak acid （CO_3~(2-)） in advanced stage. The initial ore-formingfluid for skarn Cu–Fe deposits is derived from magma with little of CO_2, and tranfered to weakacid and reduction performance.
Porphyry Cu-Mo deposits have two mineralization, the one is located in the east of theregion, around the Nengjiang and Heihe area, as exemplified by the Duobaoshan and Tongshan (480±13Ma or482～486Ma and), and the mineralization is related to paleozoic granodiorite;another is generally located along the Deerbugan Fault in the northeastern Great Xing’an Range,represented by Wunugetushan, associated with Early Jurassic porphyritic monzogranite (188Maor178±10Ma). High-sulfidation epithermal Cu–Ag deposits are located in the middle of theGreat Xing’an Range, as exemplified by the Lianhuashan and Naoniushan, and the oldest zirconU–Pb concordia ages from mineralization-related granodiorite and dacite in the study area are242.9±2.7Ma and222±5Ma, suggesting that significant Cu mineralization occurred duringthe Triassic. Skarn Cu–Fe deposits are located in the southeast of the region, as exemplified bythe Xiaoduobaoshan, and mineralization is largely related to Early Jurassic granodiorite(171.9±1.7Ma).
Mineralization-associated intrusions all are I type granites with high SiO_2, Al2O3, and totalalkali (K2O+Na2O) contents, and generally enriched in the light rare earth elements (LREE),incompatible trace element (LILE: Rb, Ba, K, Th, and U), depleted in the heavy rare earthelements (HREE). They have weak or negligible Eu anomalies [Eu=2EuN/(SmN+GdN)] thatrange between0.77and1.05, and chondrite-normalized REE patterns that decrease from left toright. Most intrusions are characterized by low initial Sr values ((87Sr/86Sr)i=0.7011–0.7079),positive Nd values (Nd(t)=0.3–6.7), and old two-stage model ages (TDM2=486–945Ma),together with their diagenetic age, suggest that magmas from Duobaoshan, Lianhuashan andNaoniushan that were generated during partial melting of the lower crust after subduction ofPaleo-Asian ocean and a region of Neoproterozoic depleted mantle, the magmas ofWunugetushan and Xiaoduobaoshan originated during partial melting of both juvenilePaleo-Asian oceanic crust and lower crustal material after collision between the NCC and theSiberian Craton.
Based the studies of fluid inclusion and origin of magma, the fluid evolution andore-forming process are summarized as following. When the temperature and pressure dropdown to360℃and38.6MPa in Duobaoshan, initial ore-forming fluid boiled and break throughthe wall rocks, which directly resulted in metal-rich cryogenic fluid went into porphyry fliudsysterm, mixing with high-temperature magma hydrothermal, and sunsequently metal sulphidestarted to unloading and filled in rocks and fractures as disseminated or veinlet. Wheras, whentemperature and pressure drop down to420℃and38.8MPa in Lianhuashan, the initial fluid tookplace boiling, however the boiling did’t cause large-scale minerlization, as temperature andpressure continued to fell down at300℃and25.7MPa, and subquently mixing with meteoricwater, which caused solubility of metal complexes or halide drastically reduce, huge metal When temperature and pressure drop down to410℃and80MPa in Xiaoduobaoshan, mixingoccurred between initial ore-forming fluid and low-temperature and low-salinity formation fluid,at the same time balance of mixed fluid broke by intermittent activity of schistose, andsubquently took place strongly boiling, numerous metal unloading, and formed massive anddisseminated orebodies.
Hydrothermal Cu deposits in this area are closely related to subduction of the Paleo-AsianOcean, subduction of the Paleo-Pacific Plate, and closure of the Mongolia–Okhotsk Ocean. TheJiamusi–Songnen and Erguna–Xing’an microplates began to amalgamate after the MiddleOrdovician, with final collision occurring between the Late Devonian and the EarlyCarboniferous along the Hegenshan–Heihe suture zone, forming the Heilongjiang Plate. SeveralEarly Paleozoic island arc assemblages have been identified in the Xing’an Terrane, includingthe paleozoic arc and caledonian granites, and is associated with the Duobaoshan and TongshanCu deposits. Subsequent suturing of the NCC and the Heilongjiang Plate took place along theSolonker–Xar Moron–Changchun Fault, with final closure of the Paleo-Asian Ocean betweenthe Late Permian and Early Triassic. Contemporaneous subduction-or collision-relatedmagmatism occurred in the southern Xing’an Terrane, associated with the formation ofnumerous mineral deposits, including the Lianhuashan and Naoniushan Cu–Ag deposits.Subduction of the Mongolia–Okhotsk Ocean started in the Late Permian, and the ocean wasclosed between the Late Jurassic and the Early Cretaceous associated with suturing of the NCCand the Siberian Craton. Many subduction-or orogenic-related granites were intruded during thisperiod, leading to the formation of many Cu deposits, including the Wunugetushan, Babayi, andBadaguan Cu–Mo deposits. Afterward, under influence of subduction of Paciffic plate, thickenedlower crust that caused by the early disappeared ocean basin occured partial melting, andupwelling along the faults, and finally formed a series of metal deposits, such as theXiaoduobaoshan and Sankunggou Cu-Fe deposits.
As discussed above, the Great Xian’an Range can be divided into three metallogenicprovince: Nenjiang-Duobaoshan, Deerbugan and Wulanhaote. The first two province had beensuffered intense erosion, and generally erosion depth is grearer than2km, which causedhigh-sulfidation epithermal deposits almost destroyed; whereas, because of shallow erosion,three types of deposits are all preserved in the latter province.
1．在区域成矿地质背景研究的基础上，通过各类铜矿床的矿床地质研究，确立研究区热液铜矿床主要有三种成因类型，分别为斑岩型铜矿床（如：乌奴格吐山、多宝山和铜山铜（钼）矿床等）、浅成热液高硫化型铜矿床（如：莲花山、闹牛山铜（银）矿床等）和接触交代型铜多金属矿床（如：小多宝山、三矿沟铜铁矿床等）。（1）斑岩型：矿体多呈不规则状、扁豆状和透镜状，产于多宝山组与花岗闪长（斑）岩或二长花岗岩与黑云母花岗岩的断裂体系内，围岩蚀变主要是钾化、硅化、绢英岩化、青磐岩化、泥化及碳酸盐化等，矿化阶段可划分为（Ⅰ）黄铁矿-石英阶段，（Ⅱ）磁黄铁矿-黄铁矿-石英阶段，（Ⅲ）石英-辉钼矿阶段，（Ⅳ）石英-黄铜矿阶段，（Ⅴ）石英-碳酸盐阶段。（2）浅成热液高硫化型：矿体以脉状、网脉状为主，其次为透镜状，产于火山断裂体系中，围岩蚀变主要是硅化、电气石化、阳起石化、绿泥石化、高岭土化和碳酸盐化等，矿化阶段可划分为（Ⅰ）黄铁矿-石英阶段，（Ⅱ）石英-磁铁矿-黄铁矿-黄铜矿阶段，（Ⅲ）纯硫化物脉阶段，（Ⅳ）石英-多金属硫化物阶段和（Ⅴ）石英-碳酸盐阶段。（3）接触交代型：矿体呈扁豆状、透镜状和脉状，产于花岗岩岩体与古生代地层接触带上，围岩蚀变以矽卡岩化为主，发育硅化、绿泥石化、绿帘石化、碳酸盐化等；可划分（Ⅰ）干矽卡岩阶段、（Ⅱ）湿矽卡岩阶段、（Ⅲ）氧化阶段，（Ⅳ）早期硫化物阶段，（Ⅴ）晚期硫化物阶段及（Ⅵ）石英-碳酸盐阶段。
2．各类主要矿床的矿物流体包裹体研究揭示：斑岩型铜矿床的均一温度分别为＞500～470℃、470～420℃、420～330℃、330～220℃、220～110℃，盐度为＞11.8～7.44%NaCleq、7.2～4.0%NaCleq、52.0～3.2%NaCleq、39.6～2.89%NaCleq和3.4～12.4%NaCleq。浅成热液高硫化型铜矿床的均一温度和盐度分别为＞420～310℃、310～270℃、270～200℃、200～160℃、160～80℃，48.9～1.39%NaCleq、6.14～1.39%NaCleq、8.81～1.22%NaCleq、8.54～2.23%NaCleq和5.55～4.17%NaCleq。接触交代型铜矿床的硫化物阶段的均一温度和盐度依次为470～230℃、230～110℃，50.1～8.8%NaCleq、5.59～1.22%NaCleq。
3．拉曼分析和子晶矿物表明：斑岩型铜矿床的初始成矿流体为富CO_2的高氧逸度的岩浆流体，成矿阶段CO_2逃逸，氧逸度降低，流体具有贫CO_2的还原性质，晚期逐渐转为弱酸性（CO_3~(2-)）。浅成热液高硫化型铜矿床初始流体为含CO_2的高氧化性、酸性流体，成矿期演化为还原流体，晚期具有弱酸性（CO_3~(2-)）的特征。接触交代型铜矿床初始流体为贫CO_2的岩浆流体，演化为弱酸性的还原流体。
4.成岩成矿年代学研究表明，斑岩型铜矿床有两个成矿期，分别是480±13Ma（锆石U-Pb谐和定年）或482～486Ma（辉钼矿Re-Os等时线），成矿与早古生代花岗闪长岩岩浆作用密切相关（多宝山铜（钼）矿床）；188Ma（单颗粒锆石U-Pb定年）或178±10Ma（辉钼矿Re-Os等时线），以乌奴格吐山铜（钼）矿床为代表，成矿与早侏罗世二长花岗斑岩岩浆活动密切相关。浅成热液高硫化型铜矿床形成于242.9±2.7Ma或222±5Ma（锆石U-Pb谐和定年），以莲花山、闹牛山铜（银）矿床为代表，成矿与三叠纪的花岗闪长斑岩和英安岩密切相关。接触交代型铜矿床形成于171.9±1.7Ma（锆石U-Pb谐和定年），以小多宝山和三矿沟铜铁矿为代表，成矿与早侏罗世花岗闪长岩岩浆作用密切。
5.与成矿密切相关的岩浆热事件的岩石成因研究揭示，奥陶纪、早侏罗世斑岩型铜矿床的成矿岩石组合分别为高钾钙碱性的花岗闪长（斑）岩和多宝山组地层、二长花岗斑岩和黑云母花岗岩，三叠纪浅成热液高硫化型铜矿床的成矿岩石组合为钠质钙碱性的花岗闪长斑岩、英安岩、闪长玢岩和安山岩，早侏罗世接触交代型铜矿床的岩石组合为高钾钙碱性的花岗闪长岩和多宝山组的碳酸岩及碎屑岩等。成矿相关的侵入岩体均为高硅、高铝、富碱的I型花岗岩，富集大离子亲石元素和轻稀土元素，亏损高场强元素，轻重分馏较明显，无Eu异常或具有轻微的负Eu异常。Sr-Nd同位素显示：它们均具有低初始锶、正钕和年轻的两阶段模式年龄的特征，结合它们的成岩年龄，多宝山、莲花山和闹牛山的源区应为与古亚洲洋板块俯冲有关的被交代的地幔楔，而乌奴格吐山与小多宝山为新生的亚洲洋壳与下地壳减压部分熔融所致。
6．成矿机制：多宝山斑岩型铜矿床中初始成矿流体的温度和压力下降至360℃与38.6MPa时，流体沸腾，并冲破围岩，导致围岩中富含金属元素的低温流体进入斑岩流体系统，发生流体混合，随后金属硫化物以浸染状或细脉浸染状充填于岩石或裂隙中。莲花山浅成热液高硫化型铜矿床成矿流体的温度降低到420℃，压力下降为38.8Mpa时，发生沸腾，但并没有导致金属元素大量卸载，当温度和压力继续下降至300℃与25.7MPa时，大气降水开始混入，金属络合物或卤化物的溶解度急剧降低，形成角砾状、脉状或细脉浸染状硫化物矿石。接触交代型小多宝山铜（铁）矿床的初始成矿流体在410℃、80MPa时与低温低盐度的地层流体发生混合，与此同时间歇性剪切挤压引起的片理化活动直接破坏了混合流体的平衡体系，流体发生强烈的沸腾，金属大量卸载，形成块状与浸染状矿体。
7．热液铜矿床的成岩成矿作用与古亚洲洋、鄂霍次克洋及古太平洋的演化密切相关。早中奥陶世—晚泥盆-早石炭世佳木斯-松嫩微板块与额尔古纳-兴安微板块拼合，导致兴安地块上产生了早古生代岛弧火山岩和加里东期闪长岩—花岗闪长岩组合，形成了以多宝山、铜山铜（钼）矿床为代表的塔木察格-牙克石-黑河铜钼成矿带。二叠纪末—早三叠世，华北板块与黑龙江板块沿西拉木伦-长春-延吉-线呈自西向东的“剪刀式”碰撞对接，同时在缝合线的西侧产生大量与俯冲或碰撞造山相关的岩浆活动，伴生大量的金属矿化作用，形成了以莲花山、闹牛山浅成热液高硫化型铜矿床为主的一系列铜多金属矿床。另一方面自晚二叠世—晚侏罗-早白垩世，鄂霍次克洋向北侧俯冲，产生了大量与俯冲造山或造山后相关的花岗岩与火山岩，形成了以乌奴格吐山、八八一和八大关铜（钼）为代表的一系列铜钼矿床。此后，在太平洋板块斜向俯冲的影响下，早期因洋盆消失而造成的加厚下地壳的部分熔融物质沿断裂上涌，最终在适当的条件下形成一系列中小型金属矿床，如小多宝山和三矿沟铜矿床。
在综合研究的基础上，对研究区的成矿规律进行了分析，嫩江-多宝山成矿区与得尔布干成矿区遭受了强烈的剥蚀，一般剥蚀大于2km，导致这两个区内的浅成低温高硫化矿床遭受了巨大的破坏，因此不发育该类型的矿床；而乌兰浩特成矿区因剥蚀较浅，使得包括低温热液型在内的三类矿床均得以保存，因此该区具有继续寻找大型的斑岩型或接触交代型等深成矿床的潜力。
The Great Xing’an Range of NE China hosts many hydrothermal Cu and other base andprecious metal mineral deposits and mineralization, is an important part of the giant CentralAsian endogenous metallogenic belt, and has been the focus of many recent studies. Mineralexploration in this area has discovered numerous large-, middle-, and small-sized Pb–Zn, Cu,and Mo deposits, including the Errentaolegai and Jiawula Pb–Zn deposits, the Duobaoshan andWunugetushan Cu–Mo deposits, the Lianhuashan and Naoniushan Cu–Ag deposits, and theMaodeng and Aonaodaba Cu–Sn deposits. The genetic types, timing of mineralization, anddynamic setting of mineral deposits in the Great Xing’an Range remain largely unknown. Thisstudy focuses on the geological characteristics, mineral deposit classification, fluid inclusion,geochemistry, and geochronology of hydrothermal Copper deposits in the Great Xing’an Range,and discusses the fluid evolution, the timing of ore formation and the source of magmas thatformed mineralization-associated plutons in this area. In addition, we seek to identify importantmetallogenic events and processes that affected the Great Xing’an Range.
Here, we classify the Cu deposits in the region into three types: porphyry Cu–Mo,high-sulfidation epithermal Cu–Ag, and skarn Cu–Fe. The porphyry Cu-Mo deposits isexemplified by the Wunugetushan, Duobaoshan and Tongshan, these orebodies are hosted byDuobaoshan Formation and granodiorite (porphyry) or biobite granite, controlled byNW–SE-trending compressive shear faults or volcanic ring fracture and are tubular, lenticularand irregular forms in shape. Mineralization-related alteration is dominated by quartz–potassic,quartz–sericite, argillic, carbonate alteration, and propylitization. Ore minerals within the depositare dominantly pyrite, chalcopyrite, molybdenite, and bornite, with minor galena, sphalerite,pyrrhotite, tetrahedrite, and arsenopyrite.The formation of this deposit involved the followingfive mineralization stages, as deduced from mineral paragenetic relationships:(I) pyrite–quartz,(II) pyrrhotite–pyrite-quartz,(III) quartz–molybdenite,(IV) quartz–chalcopyrite, and (V)quartz–carbonate. The high-sulfidation epithermal Cu–Ag deposits are hosted by volcanic ringfracture, and orebodies have vein and lenticular forms. Alteration in the deposit is associated with vuggy/residual quartz, kaolin, chlorite, epidote, carbonate, and minor tourmaline, and apartially developed potassic alteration zone. The main ore minerals are pyrite, chalcopyrite, andpyrrhotite, with minor galena, sphalerite, arsenopyrite, molybdenite, and magnetite. Five stagesof ore formation have been identified based on paragenetic relationships:(I) pyrite–quartz,(II)quartz–magnetite–pyrite–chalcopyrite,(III) sulfide veins,(IV) quartz–polymetallic sulfides, and(V) quartz–carbonate. The skarn Cu–Fe deposits is associated with skarns and an EarlyYanshanian granodiorite, and the locations of individual vertical lenticular orebody locations arecontrolled by the intersections between skarns and bedding planes. Alteration is dominated byskarnification, with minor silicification, and chlorite, epidote, and carbonate development. Oreminerals within the deposit consist of magnetite and chalcopyrite with minor pyrite andmolybdenite. Six mineralization stages during deposit formation have been identified based onparagenetic relationships:(I) a dry skarn stage,(II) a wet skarn stage,(III) an oxidized stage,(IV)an early sulfide stage,(V) a late sulfide stage, and (VI) a quartz–carbonate stage.
Fluid inclusions studies of mineralization-associated quartz within these deposits revealsthat homogenization temperatures for porphyry Cu deposits are＞500-470℃,470-420℃,420-330℃,330-220℃, and220-110℃; and salinity are＞11.8-7.44%NaCleq,7.2-4.0%NaCleq,52.0-3.2%NaCleq,39.6-2.89%NaCleq, and3.4-12.4%NaCleq, respectively.Homogenization temperatures for high-sulfidation epithermal Cu–Ag deposits are＞420-310℃,310-270℃,270-200℃,200-160℃, and160-80℃; and salinity are48.9-1.39%NaCleq,6.14-1.39%NaCleq,8.81-1.22%NaCleq,8.54-2.23%NaCleq, and5.55-4.17%NaCleq,respectively. Homogenization temperatures of sulfide stage for skarn Cu–Fe deposits are470-230℃230-110℃; and salinity are50.1-8.8%NaCleq,5.59-1.22%NaCleq.
Daughter minerals hosted by fluid inclusions and raman anysis results indicated that initialore-forming fluid for porphyry Cu-Mo deposits is derived from magma, characterized by rich inCO_2and high oxygen fugacity; then CO_2escaped, oxygen fugacity reduced in mineralizationstage, fluid tranfered to reduction performance with poor in CO_2, and weak acid （CO_3~(2-)） inadvanced stage. The initial ore-forming fluid for high-sulfidation epithermal Cu–Ag deposits isderived from magma, characterized by contain CO_2, high oxidative and acid; then fluid tranferedto reduction performance, and weak acid （CO_3~(2-)） in advanced stage. The initial ore-formingfluid for skarn Cu–Fe deposits is derived from magma with little of CO_2, and tranfered to weakacid and reduction performance.
Porphyry Cu-Mo deposits have two mineralization, the one is located in the east of theregion, around the Nengjiang and Heihe area, as exemplified by the Duobaoshan and Tongshan (480±13Ma or482～486Ma and), and the mineralization is related to paleozoic granodiorite;another is generally located along the Deerbugan Fault in the northeastern Great Xing’an Range,represented by Wunugetushan, associated with Early Jurassic porphyritic monzogranite (188Maor178±10Ma). High-sulfidation epithermal Cu–Ag deposits are located in the middle of theGreat Xing’an Range, as exemplified by the Lianhuashan and Naoniushan, and the oldest zirconU–Pb concordia ages from mineralization-related granodiorite and dacite in the study area are242.9±2.7Ma and222±5Ma, suggesting that significant Cu mineralization occurred duringthe Triassic. Skarn Cu–Fe deposits are located in the southeast of the region, as exemplified bythe Xiaoduobaoshan, and mineralization is largely related to Early Jurassic granodiorite(171.9±1.7Ma).
Mineralization-associated intrusions all are I type granites with high SiO_2, Al2O3, and totalalkali (K2O+Na2O) contents, and generally enriched in the light rare earth elements (LREE),incompatible trace element (LILE: Rb, Ba, K, Th, and U), depleted in the heavy rare earthelements (HREE). They have weak or negligible Eu anomalies [Eu=2EuN/(SmN+GdN)] thatrange between0.77and1.05, and chondrite-normalized REE patterns that decrease from left toright. Most intrusions are characterized by low initial Sr values ((87Sr/86Sr)i=0.7011–0.7079),positive Nd values (Nd(t)=0.3–6.7), and old two-stage model ages (TDM2=486–945Ma),together with their diagenetic age, suggest that magmas from Duobaoshan, Lianhuashan andNaoniushan that were generated during partial melting of the lower crust after subduction ofPaleo-Asian ocean and a region of Neoproterozoic depleted mantle, the magmas ofWunugetushan and Xiaoduobaoshan originated during partial melting of both juvenilePaleo-Asian oceanic crust and lower crustal material after collision between the NCC and theSiberian Craton.
Based the studies of fluid inclusion and origin of magma, the fluid evolution andore-forming process are summarized as following. When the temperature and pressure dropdown to360℃and38.6MPa in Duobaoshan, initial ore-forming fluid boiled and break throughthe wall rocks, which directly resulted in metal-rich cryogenic fluid went into porphyry fliudsysterm, mixing with high-temperature magma hydrothermal, and sunsequently metal sulphidestarted to unloading and filled in rocks and fractures as disseminated or veinlet. Wheras, whentemperature and pressure drop down to420℃and38.8MPa in Lianhuashan, the initial fluid tookplace boiling, however the boiling did’t cause large-scale minerlization, as temperature andpressure continued to fell down at300℃and25.7MPa, and subquently mixing with meteoricwater, which caused solubility of metal complexes or halide drastically reduce, huge metal When temperature and pressure drop down to410℃and80MPa in Xiaoduobaoshan, mixingoccurred between initial ore-forming fluid and low-temperature and low-salinity formation fluid,at the same time balance of mixed fluid broke by intermittent activity of schistose, andsubquently took place strongly boiling, numerous metal unloading, and formed massive anddisseminated orebodies.
Hydrothermal Cu deposits in this area are closely related to subduction of the Paleo-AsianOcean, subduction of the Paleo-Pacific Plate, and closure of the Mongolia–Okhotsk Ocean. TheJiamusi–Songnen and Erguna–Xing’an microplates began to amalgamate after the MiddleOrdovician, with final collision occurring between the Late Devonian and the EarlyCarboniferous along the Hegenshan–Heihe suture zone, forming the Heilongjiang Plate. SeveralEarly Paleozoic island arc assemblages have been identified in the Xing’an Terrane, includingthe paleozoic arc and caledonian granites, and is associated with the Duobaoshan and TongshanCu deposits. Subsequent suturing of the NCC and the Heilongjiang Plate took place along theSolonker–Xar Moron–Changchun Fault, with final closure of the Paleo-Asian Ocean betweenthe Late Permian and Early Triassic. Contemporaneous subduction-or collision-relatedmagmatism occurred in the southern Xing’an Terrane, associated with the formation ofnumerous mineral deposits, including the Lianhuashan and Naoniushan Cu–Ag deposits.Subduction of the Mongolia–Okhotsk Ocean started in the Late Permian, and the ocean wasclosed between the Late Jurassic and the Early Cretaceous associated with suturing of the NCCand the Siberian Craton. Many subduction-or orogenic-related granites were intruded during thisperiod, leading to the formation of many Cu deposits, including the Wunugetushan, Babayi, andBadaguan Cu–Mo deposits. Afterward, under influence of subduction of Paciffic plate, thickenedlower crust that caused by the early disappeared ocean basin occured partial melting, andupwelling along the faults, and finally formed a series of metal deposits, such as theXiaoduobaoshan and Sankunggou Cu-Fe deposits.
As discussed above, the Great Xian’an Range can be divided into three metallogenicprovince: Nenjiang-Duobaoshan, Deerbugan and Wulanhaote. The first two province had beensuffered intense erosion, and generally erosion depth is grearer than2km, which causedhigh-sulfidation epithermal deposits almost destroyed; whereas, because of shallow erosion,three types of deposits are all preserved in the latter province.
引文
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