华北克拉通北缘赤峰—朝阳地区中生代构造岩浆演化与金成矿
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摘要
华北克拉通北接兴蒙造山带,南邻扬子克拉通,演化历史大于3.8Ga。进入中生代以后,华北克拉通经历了广泛的构造-热活化及岩石圈破坏,导致大于100km的岩石圈丢失,并在岩石圈破坏的峰期早白垩世时发育强烈岩浆作用及大规模金成矿作用,同时伴随着大量拉分盆地和变质核杂岩的出现。但是,关于克拉通与北侧蒙古弧地体最终碰撞闭合的时限、克拉通岩石圈减薄机制、大规模金成矿与岩石圈减薄的内在成因联系等科学问题到目前仍未获得一致认识。本文以华北克拉通北缘赤峰-朝阳金矿集中区为研究对象,以详细的野外地质调查为基础,通过高精度年代学研究揭示了区内三叠纪及白垩纪两期成岩、成矿事件具有时间上的高度耦合性。对区内三叠纪金厂沟梁脉岩、白垩纪鸡冠子及对面沟石英二长岩和其内的暗色包体开展了矿物化学、全岩地球化学、Sr-Nd-Pb-Hf同位素地球化学研究,探讨了两期岩浆作用的源区性质、壳幔交换机制和成岩过程。对区内安家营子、金厂沟梁及排山楼等典型金矿床开展了成矿流体、成矿物质来源的多元联合示踪研究,分析了金矿成矿流体及成矿物质来源,结合各金矿区及变质核杂岩形成时的应力场匹配结果讨论了区内金成矿、岩浆作用及变质核杂岩形成等地质事件之间的内在成因联系。主要成果和结论如下：
1.研究区主要分布太古代建平群变质基底及侏罗系-白垩系火山-沉积岩系；区域构造以晚古生代-早中生代形成的东西向深大断裂及晚中生代形成的北东走向变质核杂岩为主；受区域构造影响,区内主要岩浆岩及金矿床均就位于变质核杂岩内部,其中金矿与白垩纪岩体空间上密切伴生。区内金矿体主要以以脉状、透镜状赋存在岩体或变质基底内的北东、北西及近东西向断裂内,严格受断裂控制,含矿断裂主压应力为近南北-北西向。矿石构造以块状、浸染状、脉状、角砾状、条带状为主,矿石结构主要为包含结构、交代结构、碎裂结构及固溶体分解结构。各典型金矿区均发育黄铁矿、黄铜矿、方铅矿及闪锌矿等金属矿物,金以自然金或银金矿形式赋存于黄铁矿及黄铜矿中；另硅化、黄铁矿化、绿泥石化、绢云母化及碳酸盐化等围岩蚀变普遍发育。成矿过程可分为粗粒石英-黄铁矿、多金属硫化物、低温热液作用及表生作用四个阶段,其中多金属硫化物阶段为主要的金沉淀阶段。
2.金厂沟梁地区发育大量规模不等的脉岩,岩性以闪长岩、闪长玢岩为主。脉岩锆石LA-ICP-MS U-Pb年龄值可分为三组：2458～2524Ma、253±6Ma (MSWD=3.1)及227±1Ma(MSWD=0.4)。2.5Ga锆石与华北克拉通主要的地壳增长时代一致,反映成岩过程中有古老地壳物质参与；253Ma锆石可能与古亚洲洋闭合时的岩浆事件有关,227Ma则为脉岩的形成年龄。脉岩SiO2(51.22%～68.48%)、MgO(1.35%～8.13%)含量变化较大,且具有高Na2O+K2O Al2O3及低的TiO2、P2O5含量等特征。岩石LREE及LILE富集,HFSE亏损,可定义为钾玄质系列岩石。脉岩(87Sr/86Sr)i比值较为一致(0.70394-0.70592),而εNd(t)(1.1～-9.8)及T2DM(913-1972Ma)值变化范围较大,Pb同位素组成则介于1型富集地幔(EM1)与下地壳之间。主微量元素及同位素研究结果表明：金厂沟梁三叠纪脉岩来源于造山后拉张背景下下地壳,克拉通下岩石圈地幔及上升的软流圈地幔熔体的多源混合。结合区域上同时代ENE向退变质榴辉岩、蛇绿岩、弧岩浆岩带、A型花岗岩、碱性侵入岩及变质核杂岩等的出现,本文认为古亚洲洋的最终封闭发生在晚二叠-早三叠时期,随后研究区进入造山后伸展背景。脉岩岩浆源区软流圈熔体的出现暗示着华北克拉通北缘岩石圈地幔破坏在中-晚三叠世已经开始。
3. LA-ICP-MS分析结果显示金厂沟梁地区对面沟石英二长岩(128±Ma, MSWD=1.3)、安家营子地区鸡冠子石英二长岩(133±Ma, MSWD=0.6)及其内部包体(133±1Ma, MSWD=0.4)均形成于早白垩世。上述三类地质体中角闪石均属镁角闪石,以富镁为特征,分属地幔型,壳幔混合型及壳幔混合型-地幔型；三者之间的黑云母成分也极为类似,均为镁质黑云母。两个岩体内斜长石均以奥长石为主,An集中在15-26。鸡冠子岩体内包体中斜长石大多发育熔蚀结构及明显的反环带。角闪石-斜长石温压计算结果显示对面沟岩体、鸡冠子岩体及包体就位时岩浆房平均压力分别为0.77kbar、2.19kbar及1.59kbar,对应形成深度分别为2.7km、7.7km、5.6km,分别属于浅成及中深成相侵入岩,结晶温度分别为742℃、647℃及647℃。据黑云母成分计算的岩浆log fO2分别为-14.8--16.3、-17.8--18.7、-18.0--18.7,位于铁橄榄石-磁铁矿-石英及Ni-NiO缓冲曲线之间。
4.全岩地球化学分析结果显示,对面沟及鸡冠子岩体SiO2、Al2O、Na2O、K2O等主量元素含量较高,而MgO及Mg#相对较低,均属亚碱性准铝质石英二长岩。与寄主岩石鸡冠子岩体相比包体全碱含量相对较低,而MgO、CaO、FeO等氧化物含量较高,属亚碱性-碱性准铝质二长闪长岩-闪长岩。对面沟岩体、鸡冠子岩体及其内包体均富集大离子亲石元素,亏损高场强元素,具无-弱负Eu异常(0.89～1.10,0.61～0.83,0.79～0.93),(La/Yb)N比值较高(20.5～31.0,12.6～40.2,14.1～37.8),(Dy/Yb)N比值较低且稳定(0.87～1.60,1.12～1.35,1.31～1.63)。对面沟及鸡冠子岩体具有adakitic岩石的地球化学特征,与变质核杂岩及拉分盆地共存这一现象表明这类岩石亦可形成于陆内伸展环境。上述岩体及包体具有一致的Sr((87Sr/86Sr)i分别为0.7059～0.7066,0.7055～0.7060,0.7059)、Nd(εNd(t)分别为--6.2～-7.2,--8.2,-11.0)同位素组成。对面沟岩体Pb ((206Pb/204Pb)i=17.289～17.375,(207Pb/204Pb)i=15.359～15.463,(208Pb/204Pb)i=37.130～37.472)同位素组成较为均一。鸡冠子岩体及包体SHf(t)分别介于-9.2--12.0及-4.5～-10.0。矿物化学、主微量元素、Sr-Nd-Pb-Hf同位素综合对比研究表明区内早白垩世adakitic侵入岩为软流圈地幔来源的岩浆遭受地壳混染的产物；鸡冠子岩体内的暗色包体则可能代表了岩浆房演化晚期不断补给的分异程度较低的深部岩浆；因此区内白垩纪岩浆作用可能记录了陆内伸展环境下与软流圈底侵作用相关的岩浆事件。另外,岩浆演化过程中同时存在钾长石、黑云母、磷灰石及少量角闪石和斜长石等矿物的分离结晶作用。结合区域上榴辉岩的发现,笔者认为软流圈岩浆底侵及岩石圈拆沉在华北克拉通岩石圈破坏过程中均起着重要的作用。
5.安家营子金矿成矿流体均一温度为180～402℃(峰值301℃),冰点为-11.6～-0.8℃,盐度为1.3～15.6wt%NaCl,成矿压力为319×105Pa,δD为-80.3‰～-96.5‰,δ180H2O为3.7‰-5.5‰；金厂沟梁金矿均—温度为205～390℃(峰值323℃),冰点为-19.1--0.8℃,盐度为1.3～21.7wt%NaCl,成矿压力为422×105Pa,δD为-54.0‰～-110.9‰,δ18OH2O为1.9‰-8.9‰；排山楼金矿均一温度介于187～337℃,盐度为4.6～12.2wt%NaCl,δD为-87.3‰自～116.2‰,δ18OH2O为0.7‰～6.9‰。综合估计各金矿成矿深度约为2-2.5km,成矿流体主要来源于岩浆水,流体不混溶及温度降低是金沉淀的主要因素。
安家营子、金厂沟梁-二道沟及排山楼金矿硫化物δ34S分别为-0.5-7.6‰、-2.8～2.3‰和0.3～6.5‰。赤峰-朝阳地区变质岩校正后(206Pb/204Pb)i=15.040～18.090,(207Pb/204Pb)i=15.065～15.655、(208Pb/204Pb)i=34.897～38.571,早白垩世岩体校正后(206Pb/204Pb)i=15.742～17.375、(207Pb/204Pb)i=15.237～15.665、(208Pb/204Pb)i=36.908～38.547。典型矿床54件硫化物(206Pb/204Pb)i=16.400～17.591、(207Pb/204Pb)j=15.210～15.578、(208Pb/204Pb)i=36.690～38.091。区内金矿硫源为深源的岩浆硫,校正后的岩体Pb同位素与硫化物Pb同位素组成一致,表明成矿物质亦来源于岩浆活动。
6.研究区中部金厂沟梁西矿区石英脉中辉钼矿Re-Os同位素加权平均年龄为243.5±1.3Ma,确证研究区存在三叠纪含钼(金?)成矿作用,属蒙古弧地体和华北克拉通碰撞造山后拉张动力学背景下产物。研究区相关地质体锆石U-Pb年龄、黑云母及钾长石40Ar-39Ar年代学综合研究结果表明金成矿作用主要发生在早白垩世时期(133-117Ma),与区内白垩纪岩浆作用(133Ma～124Ma)及变质核杂岩的形成基本同时(130-100Ma),金矿成矿流体和成矿物质来源与岩浆活动关系密切。根据区内成岩成矿事件与构造演化之间的匹配关系,论文建立了赤峰-朝阳地区三叠纪及早白垩世两阶段成矿模型。
The North China Craton (NCC) is bounded to the north by the Hingan-Mongolian Orogenic Belt (HMOB) and to the southeast by the Yangtze Craton, and it is an Archean craton as indicated by the presence of≥3.8Ga crustal remnants. However, the lithospheric mantle beneath the Eastern Block of the NCC experienced widespread reactivation and thinning peaking in the Early Cretaceous, contemporaneous with extensional basin formation, the development of metamorphic core complexes (MCC), intense magmatism and large-scale gold metallogenesis. Until now, there are still many controversies concerning the timing of suturing between the NCC and HMOB, the thinning mechanism of NCC, and the genesis of the large-scale gold metallogenesis. Based on the detailed field investigation about the Chifeng-Chaoyang gold district, we present zircon U-Pb ages, mineralogy, major and trace element geochemistry, and Sr-Nd-Pb-Hf isotope compositions for the dykes from Jinchanggouliang (JCGL), the Duimiangou (DMG) and Jiguanzi (JGZ) intrusions, and the enclaves from JGZ to (1) document the Triassic and Cretaceous periodic magmatisms and mineralizing events,(2) investigate their magma sources and petrogenesis, and (3) provide potential information about crust-mantle interaction beneath the northern NCC. Moreover, we discussed the magmatic sources for the ore fluids and metal concerning the cretaceous gold ore systems according to the H-O-S-Pb isotopes, and analyzed the genetic links between gold metallogenesis, adakitic magmatism and formation of MCC. The main results are summarized herein:
1. The Chifeng-Chaoyang region is underlain by the Archean Jianping Group gneiss with a metamorphic age of about2.5Ga, and the Jurassic-Cretaceous volcanic-sedimentary rocks. The regional structures are dominated by the Late Paleozoic-Early Mesozoic EW-striking faults and the Late Mesozoic NE-striking MCC. Nearly all intrusions and gold deposits are located in the lower-plate of the MCC, and these intrusions and gold deposits always cluster together. Gold veins are hosted by the NE-trending faults, which are developed in the metamorphic basement or intrusions, and the maximum principal compressive stress is SN-NW oriented. Pyrite, chalcopyrite, galena and sphalerite are common sulfides in different gold deposit, and the gold often occurs as native gold or electrum in pyrite and chalcopyrite. Moreover, the quartz, pyrite, chlorite, sericite and carbonate are prevalent ore-related hydrothermal alteration minerals. Three stages of hydrothermal alteration and hypogene mineralization are recognized, largely on the basis of megascopic and microscopic textural relationships, and mineral assemblages:coarse grained quartz-pyrite stage, Polymetallic sulfide stage and the low-temperature quartz-pyrite-carbonate stage.
2. LA-ICP-MS zircon U-Pb dating reveals three major age groups of2500Ma (n=2),253±6Ma (n=5) and227±1Ma(n=9) of dykes. The inherited ages of2500Ma, contemporary with the Archean NCC continental growth, imply that crustal material was involved in the magma source. The igneous zircons with concordia age of227±1Ma may record the emplacement age of the JCGL dykes. Both diorite and diorite porphyry exhibit a wide range of SiO2and MgO contents and are characterized by high concentrations of Na2O+K2O and Al2O3and low abundances of P2O5and TiO2. They are enriched in large ion lithophile elements (LILE) and light rare earth elements (LREE) without significant Eu anomalies, depleted in high field strength elements (HFSE), and all are categorized as shoshonitic rocks. All samples show a narrow range of Sr isotope compositions with initial87Sr/86Sr ratios from0.70394to0.70592, variable εNd(t) values (1.1to-9.8) and TDM2ages (913～1972Ma). Their Pb isotope compositions form continuous variation trends and plot in the fields between EMI and LCC. The above results suggest that the JCGL dykes studied could have been derived from mixing of lower crust, lithospheric mantle of the NCC and ascending asthenospheric melt, in a post-orogenic extensional geodynamic setting. These shoshonitic dykes, together with the geochronologic data of regional ENE-trending retrograded eclogites, ophiolites, continental arc magmatic belt, A-type granite, alkaline intrusions and metamorphic core complex from the northern NCC and Central Asian Orogenic Belt (CAOB) suggest that closure of the Paleo-Asian Ocean (i.e. stage of pre-collision to collision) had completed during the latest Permian to earliest Triassic, and that the CAOB was subsequently tectonically dominated by post-orogenic extensional regimes. The involvement of asthenospheric melt in the magma source implies that the sub-continental lithospheric mantle (SCLM) of the NCC had been modified and the onset of lithospheric destruction and thinning beneath the northern NCC may have occurred in the Middle-Late Triassic as a result of post-orogenic subducting slab detachment and lithospheric delamination.
3. LA-ICP-MS zircon U-Pb dating reveals that the DMG quartz monzonite from JCGL (128±1Ma), the JGZ quartz monzonite from the Anjiayingzi (133±1Ma), and enclaves from the host JGZ intrusion (133±1Ma) all formed in the Early Cretaceous. All amphiboles from these quartz monzonite and enclaves belong to magnesiohornblende, and all micas can be classified as magnesian biotite. The 'An' of plagioclase from DMG and JGZ intrusion ranges from15to26, thus they are defined as oligoclase. The reversely-zoned plagioclases are common in enclaves from JGZ intrusion. Calculated results from aluminum-in-hornblende geobarometry show that the DMG intrusion, the JGZ intrusion and enclaves from the JGZ host intrusion emplaced at0.77kbar,2.19kbar and1.59kbar respectively, and corresponding depth at2.7km,7.7km,5.6km. Temperatures of emplacement calculated with the hornblende-plagioclase thermometer are742C,647℃and647℃respectively. The log fo2estimated from biotite ranges from-14.8～-16.3,-17.8～-18.7and-18.0～-18.7, located between quartz-fayalite-magnetite and the Ni-NiO buffer assemblages.
4. Bulk-rock analyses show that the DMG and JGZ intrusion are characterized by high contents of SiO2, Al2O3, Na2O, K2O and low abundance of MgO and Mg#, defining their subalkaline and metaluminous characteristics. The enclaves from JGZ intrusion has relatively low concentrations of SiO2and total alkaline, and higher MgO, CaO and FeO, and can be classified as subalkaline-alkaline metaluminous monzodiorite-diorite. The DMG intrusion, JGZ intrusion and the enclaves from it are all enriched in LILE and LREE, and depleted in heavy rare earth elements (HREE) and HFSE, without significant Eu anomalies (0.89～1.10,0.61～0.83,0.79～0.93). They have high (La/Yb)N ratios (20.5～31.0,12.6～40.2,14.1～37.8), and low and constant (Dy/Yb)N ratios (0.87～1.60,1.12～1.35,1.31～1.63). The DMG and JGZ adakitic intrusions formed in an intracontinental extensional setting contemporaneous with the formation of pull-apart basins, metamorphic core complexes and intense magmatism, rather than in a convergent margin. The DMG intrusion, JGZ intrusion and the enclaves from it have homogeneous (87Sr/86Sr)i ratios (0.7059～0.7066,0.7055～0.7060,0.7059) and εNd(t)(-6.2～-7.2,-8.2,-11.0). The Pb isotope compositions of DMG intrusion are also homogeneous ((206Pb/204Pb)i=17.289～17.375,(207Pb/204Pb)i=15.359～15.463,(208Pb/204Pb)i=37.130～37.472). Moreover, the εHf(t) of JGZ intrusion and enclaves from it ranges from-9.2～-12.0and-4.5～-10.0respectively. In combination with the mineralogy, geochemistry and Sr-Nd-Pb-Hf isotope compositions of these rocks, we contend that the DMG and JGZ intrusions could have originated from crustal contamination of newly formed basaltic melts derived from asthenospheric mantle, accompanied by fractional crystallization of K-feldspar, biotite, apatite, Fe-Ti oxides and minor hornblende and plagioclase, and the enclaves from the JGZ intrusion could denote the feeder system during the late stage of host magma evolution. Thus, the DMG and JGZ adakitic intrusions may record the magmatic event associated with underplating of asthenospheric amgma in an intracontinental extensional environment, and both asthenospheric magma underplating and lithospheric delamination may have played important roles in the lithospheric thinning of the northern NCC.
5. The fluid inclusions from Anjiayingzi gold deposit have final homogenization temperatures (Th) of180～402℃, ice-melting temperatures (Tm, ice) of-11.6～-0.8℃, salinities of1.3～15.6wt%NaCl and fluid pressures of319×105Pa with δD of-80.3‰～-96.5‰and δi8OH2O of3.7‰-5.5‰. The fluid inclusions from JCGL gold deposit have Th of205～390℃, Tm, ice of-19.1～0.8℃, salinities of1.3～21.7wt%NaCl and fluid pressures of422×105Pa with δD of-54.0‰～-110.9‰and δ18OH2O of1.9‰～8.9‰. The fluid inclusions from Paishanlou gold deposit have Th of187～337℃and salinities of4.6～12.2wt%NaCl with5D of-87.3‰～-116.2‰and518OH2O of0.7‰～6.9‰. The mineralization depths of gold deposits from the Chifeng-Chaoyang region calculated fluid inclusions parameters range from2-2.5km. The ore fluids derived from the Early Cretaceous intrusions dominantly, and the fluid unmixing and temperature drop controlled the gold deposition jointly.
The Anjiayingzi, JCGL-Erdaogou and Paishanlou gold deposits have δ34S of-0.5～7.6‰,-2.8～2.3‰and0.3～6.5‰respectively. The corrected Pb isotope composition of metamorphic basement from Chifeng-Chaoyang region is highly variable, with (206Pb/204Pb)i=15.040～18.090,(207Pb/204Pb)i=15.065～15.655and (208Pb/204Pb)i=34.897～38.571. The corrected Pb isotope composition of the Early Cretaceous adakitic intrusions is relatively homogeneous with (206Pb/204Pb);=15.742～17.375,(207Pb/204Pb)i=15.237～15.665and (208Pb/204Pb)i=36.908～38.547. The Pb isotope of ore sulfides from regional gold deposits is nearly the same as that of the Early Cretaceous intrusions with (206Pb/204Pb)i=16.400～17.591,(207Pb/204Pb)i=15.210～15.578and (208Pb/204Pb)i=36.690～38.091, indicating their magmatic origin.
6. The Triassic Mo (gold?) mineralizing event is confirmed by the Re-Os age of243.5±1.3from the JCGL Mo-bearing quartz veins, and it was developed in the post-orogenic extensional regime as the result of Paleo-Asian Ocean closure. The zircon U-Pb, biotite and K-feldspar40Ar-39Ar ages reveal that gold deposits from Chifeng-Chaoyang region mainly formed during the Early Cretaceous (133～117Ma), contemporaneous with the development of MCC (130～100Ma) and intense magmatism (133Ma～124Ma). Most importantly, the ore fluids and metals also derived from the Early Cretaceous intrusions. In combination with these results described above, this paper presents a two-stage mineralizing model.
1.研究区主要分布太古代建平群变质基底及侏罗系-白垩系火山-沉积岩系；区域构造以晚古生代-早中生代形成的东西向深大断裂及晚中生代形成的北东走向变质核杂岩为主；受区域构造影响,区内主要岩浆岩及金矿床均就位于变质核杂岩内部,其中金矿与白垩纪岩体空间上密切伴生。区内金矿体主要以以脉状、透镜状赋存在岩体或变质基底内的北东、北西及近东西向断裂内,严格受断裂控制,含矿断裂主压应力为近南北-北西向。矿石构造以块状、浸染状、脉状、角砾状、条带状为主,矿石结构主要为包含结构、交代结构、碎裂结构及固溶体分解结构。各典型金矿区均发育黄铁矿、黄铜矿、方铅矿及闪锌矿等金属矿物,金以自然金或银金矿形式赋存于黄铁矿及黄铜矿中；另硅化、黄铁矿化、绿泥石化、绢云母化及碳酸盐化等围岩蚀变普遍发育。成矿过程可分为粗粒石英-黄铁矿、多金属硫化物、低温热液作用及表生作用四个阶段,其中多金属硫化物阶段为主要的金沉淀阶段。
2.金厂沟梁地区发育大量规模不等的脉岩,岩性以闪长岩、闪长玢岩为主。脉岩锆石LA-ICP-MS U-Pb年龄值可分为三组：2458～2524Ma、253±6Ma (MSWD=3.1)及227±1Ma(MSWD=0.4)。2.5Ga锆石与华北克拉通主要的地壳增长时代一致,反映成岩过程中有古老地壳物质参与；253Ma锆石可能与古亚洲洋闭合时的岩浆事件有关,227Ma则为脉岩的形成年龄。脉岩SiO2(51.22%～68.48%)、MgO(1.35%～8.13%)含量变化较大,且具有高Na2O+K2O Al2O3及低的TiO2、P2O5含量等特征。岩石LREE及LILE富集,HFSE亏损,可定义为钾玄质系列岩石。脉岩(87Sr/86Sr)i比值较为一致(0.70394-0.70592),而εNd(t)(1.1～-9.8)及T2DM(913-1972Ma)值变化范围较大,Pb同位素组成则介于1型富集地幔(EM1)与下地壳之间。主微量元素及同位素研究结果表明：金厂沟梁三叠纪脉岩来源于造山后拉张背景下下地壳,克拉通下岩石圈地幔及上升的软流圈地幔熔体的多源混合。结合区域上同时代ENE向退变质榴辉岩、蛇绿岩、弧岩浆岩带、A型花岗岩、碱性侵入岩及变质核杂岩等的出现,本文认为古亚洲洋的最终封闭发生在晚二叠-早三叠时期,随后研究区进入造山后伸展背景。脉岩岩浆源区软流圈熔体的出现暗示着华北克拉通北缘岩石圈地幔破坏在中-晚三叠世已经开始。
3. LA-ICP-MS分析结果显示金厂沟梁地区对面沟石英二长岩(128±Ma, MSWD=1.3)、安家营子地区鸡冠子石英二长岩(133±Ma, MSWD=0.6)及其内部包体(133±1Ma, MSWD=0.4)均形成于早白垩世。上述三类地质体中角闪石均属镁角闪石,以富镁为特征,分属地幔型,壳幔混合型及壳幔混合型-地幔型；三者之间的黑云母成分也极为类似,均为镁质黑云母。两个岩体内斜长石均以奥长石为主,An集中在15-26。鸡冠子岩体内包体中斜长石大多发育熔蚀结构及明显的反环带。角闪石-斜长石温压计算结果显示对面沟岩体、鸡冠子岩体及包体就位时岩浆房平均压力分别为0.77kbar、2.19kbar及1.59kbar,对应形成深度分别为2.7km、7.7km、5.6km,分别属于浅成及中深成相侵入岩,结晶温度分别为742℃、647℃及647℃。据黑云母成分计算的岩浆log fO2分别为-14.8--16.3、-17.8--18.7、-18.0--18.7,位于铁橄榄石-磁铁矿-石英及Ni-NiO缓冲曲线之间。
4.全岩地球化学分析结果显示,对面沟及鸡冠子岩体SiO2、Al2O、Na2O、K2O等主量元素含量较高,而MgO及Mg#相对较低,均属亚碱性准铝质石英二长岩。与寄主岩石鸡冠子岩体相比包体全碱含量相对较低,而MgO、CaO、FeO等氧化物含量较高,属亚碱性-碱性准铝质二长闪长岩-闪长岩。对面沟岩体、鸡冠子岩体及其内包体均富集大离子亲石元素,亏损高场强元素,具无-弱负Eu异常(0.89～1.10,0.61～0.83,0.79～0.93),(La/Yb)N比值较高(20.5～31.0,12.6～40.2,14.1～37.8),(Dy/Yb)N比值较低且稳定(0.87～1.60,1.12～1.35,1.31～1.63)。对面沟及鸡冠子岩体具有adakitic岩石的地球化学特征,与变质核杂岩及拉分盆地共存这一现象表明这类岩石亦可形成于陆内伸展环境。上述岩体及包体具有一致的Sr((87Sr/86Sr)i分别为0.7059～0.7066,0.7055～0.7060,0.7059)、Nd(εNd(t)分别为--6.2～-7.2,--8.2,-11.0)同位素组成。对面沟岩体Pb ((206Pb/204Pb)i=17.289～17.375,(207Pb/204Pb)i=15.359～15.463,(208Pb/204Pb)i=37.130～37.472)同位素组成较为均一。鸡冠子岩体及包体SHf(t)分别介于-9.2--12.0及-4.5～-10.0。矿物化学、主微量元素、Sr-Nd-Pb-Hf同位素综合对比研究表明区内早白垩世adakitic侵入岩为软流圈地幔来源的岩浆遭受地壳混染的产物；鸡冠子岩体内的暗色包体则可能代表了岩浆房演化晚期不断补给的分异程度较低的深部岩浆；因此区内白垩纪岩浆作用可能记录了陆内伸展环境下与软流圈底侵作用相关的岩浆事件。另外,岩浆演化过程中同时存在钾长石、黑云母、磷灰石及少量角闪石和斜长石等矿物的分离结晶作用。结合区域上榴辉岩的发现,笔者认为软流圈岩浆底侵及岩石圈拆沉在华北克拉通岩石圈破坏过程中均起着重要的作用。
5.安家营子金矿成矿流体均一温度为180～402℃(峰值301℃),冰点为-11.6～-0.8℃,盐度为1.3～15.6wt%NaCl,成矿压力为319×105Pa,δD为-80.3‰～-96.5‰,δ180H2O为3.7‰-5.5‰；金厂沟梁金矿均—温度为205～390℃(峰值323℃),冰点为-19.1--0.8℃,盐度为1.3～21.7wt%NaCl,成矿压力为422×105Pa,δD为-54.0‰～-110.9‰,δ18OH2O为1.9‰-8.9‰；排山楼金矿均一温度介于187～337℃,盐度为4.6～12.2wt%NaCl,δD为-87.3‰自～116.2‰,δ18OH2O为0.7‰～6.9‰。综合估计各金矿成矿深度约为2-2.5km,成矿流体主要来源于岩浆水,流体不混溶及温度降低是金沉淀的主要因素。
安家营子、金厂沟梁-二道沟及排山楼金矿硫化物δ34S分别为-0.5-7.6‰、-2.8～2.3‰和0.3～6.5‰。赤峰-朝阳地区变质岩校正后(206Pb/204Pb)i=15.040～18.090,(207Pb/204Pb)i=15.065～15.655、(208Pb/204Pb)i=34.897～38.571,早白垩世岩体校正后(206Pb/204Pb)i=15.742～17.375、(207Pb/204Pb)i=15.237～15.665、(208Pb/204Pb)i=36.908～38.547。典型矿床54件硫化物(206Pb/204Pb)i=16.400～17.591、(207Pb/204Pb)j=15.210～15.578、(208Pb/204Pb)i=36.690～38.091。区内金矿硫源为深源的岩浆硫,校正后的岩体Pb同位素与硫化物Pb同位素组成一致,表明成矿物质亦来源于岩浆活动。
6.研究区中部金厂沟梁西矿区石英脉中辉钼矿Re-Os同位素加权平均年龄为243.5±1.3Ma,确证研究区存在三叠纪含钼(金?)成矿作用,属蒙古弧地体和华北克拉通碰撞造山后拉张动力学背景下产物。研究区相关地质体锆石U-Pb年龄、黑云母及钾长石40Ar-39Ar年代学综合研究结果表明金成矿作用主要发生在早白垩世时期(133-117Ma),与区内白垩纪岩浆作用(133Ma～124Ma)及变质核杂岩的形成基本同时(130-100Ma),金矿成矿流体和成矿物质来源与岩浆活动关系密切。根据区内成岩成矿事件与构造演化之间的匹配关系,论文建立了赤峰-朝阳地区三叠纪及早白垩世两阶段成矿模型。
The North China Craton (NCC) is bounded to the north by the Hingan-Mongolian Orogenic Belt (HMOB) and to the southeast by the Yangtze Craton, and it is an Archean craton as indicated by the presence of≥3.8Ga crustal remnants. However, the lithospheric mantle beneath the Eastern Block of the NCC experienced widespread reactivation and thinning peaking in the Early Cretaceous, contemporaneous with extensional basin formation, the development of metamorphic core complexes (MCC), intense magmatism and large-scale gold metallogenesis. Until now, there are still many controversies concerning the timing of suturing between the NCC and HMOB, the thinning mechanism of NCC, and the genesis of the large-scale gold metallogenesis. Based on the detailed field investigation about the Chifeng-Chaoyang gold district, we present zircon U-Pb ages, mineralogy, major and trace element geochemistry, and Sr-Nd-Pb-Hf isotope compositions for the dykes from Jinchanggouliang (JCGL), the Duimiangou (DMG) and Jiguanzi (JGZ) intrusions, and the enclaves from JGZ to (1) document the Triassic and Cretaceous periodic magmatisms and mineralizing events,(2) investigate their magma sources and petrogenesis, and (3) provide potential information about crust-mantle interaction beneath the northern NCC. Moreover, we discussed the magmatic sources for the ore fluids and metal concerning the cretaceous gold ore systems according to the H-O-S-Pb isotopes, and analyzed the genetic links between gold metallogenesis, adakitic magmatism and formation of MCC. The main results are summarized herein:
1. The Chifeng-Chaoyang region is underlain by the Archean Jianping Group gneiss with a metamorphic age of about2.5Ga, and the Jurassic-Cretaceous volcanic-sedimentary rocks. The regional structures are dominated by the Late Paleozoic-Early Mesozoic EW-striking faults and the Late Mesozoic NE-striking MCC. Nearly all intrusions and gold deposits are located in the lower-plate of the MCC, and these intrusions and gold deposits always cluster together. Gold veins are hosted by the NE-trending faults, which are developed in the metamorphic basement or intrusions, and the maximum principal compressive stress is SN-NW oriented. Pyrite, chalcopyrite, galena and sphalerite are common sulfides in different gold deposit, and the gold often occurs as native gold or electrum in pyrite and chalcopyrite. Moreover, the quartz, pyrite, chlorite, sericite and carbonate are prevalent ore-related hydrothermal alteration minerals. Three stages of hydrothermal alteration and hypogene mineralization are recognized, largely on the basis of megascopic and microscopic textural relationships, and mineral assemblages:coarse grained quartz-pyrite stage, Polymetallic sulfide stage and the low-temperature quartz-pyrite-carbonate stage.
2. LA-ICP-MS zircon U-Pb dating reveals three major age groups of2500Ma (n=2),253±6Ma (n=5) and227±1Ma(n=9) of dykes. The inherited ages of2500Ma, contemporary with the Archean NCC continental growth, imply that crustal material was involved in the magma source. The igneous zircons with concordia age of227±1Ma may record the emplacement age of the JCGL dykes. Both diorite and diorite porphyry exhibit a wide range of SiO2and MgO contents and are characterized by high concentrations of Na2O+K2O and Al2O3and low abundances of P2O5and TiO2. They are enriched in large ion lithophile elements (LILE) and light rare earth elements (LREE) without significant Eu anomalies, depleted in high field strength elements (HFSE), and all are categorized as shoshonitic rocks. All samples show a narrow range of Sr isotope compositions with initial87Sr/86Sr ratios from0.70394to0.70592, variable εNd(t) values (1.1to-9.8) and TDM2ages (913～1972Ma). Their Pb isotope compositions form continuous variation trends and plot in the fields between EMI and LCC. The above results suggest that the JCGL dykes studied could have been derived from mixing of lower crust, lithospheric mantle of the NCC and ascending asthenospheric melt, in a post-orogenic extensional geodynamic setting. These shoshonitic dykes, together with the geochronologic data of regional ENE-trending retrograded eclogites, ophiolites, continental arc magmatic belt, A-type granite, alkaline intrusions and metamorphic core complex from the northern NCC and Central Asian Orogenic Belt (CAOB) suggest that closure of the Paleo-Asian Ocean (i.e. stage of pre-collision to collision) had completed during the latest Permian to earliest Triassic, and that the CAOB was subsequently tectonically dominated by post-orogenic extensional regimes. The involvement of asthenospheric melt in the magma source implies that the sub-continental lithospheric mantle (SCLM) of the NCC had been modified and the onset of lithospheric destruction and thinning beneath the northern NCC may have occurred in the Middle-Late Triassic as a result of post-orogenic subducting slab detachment and lithospheric delamination.
3. LA-ICP-MS zircon U-Pb dating reveals that the DMG quartz monzonite from JCGL (128±1Ma), the JGZ quartz monzonite from the Anjiayingzi (133±1Ma), and enclaves from the host JGZ intrusion (133±1Ma) all formed in the Early Cretaceous. All amphiboles from these quartz monzonite and enclaves belong to magnesiohornblende, and all micas can be classified as magnesian biotite. The 'An' of plagioclase from DMG and JGZ intrusion ranges from15to26, thus they are defined as oligoclase. The reversely-zoned plagioclases are common in enclaves from JGZ intrusion. Calculated results from aluminum-in-hornblende geobarometry show that the DMG intrusion, the JGZ intrusion and enclaves from the JGZ host intrusion emplaced at0.77kbar,2.19kbar and1.59kbar respectively, and corresponding depth at2.7km,7.7km,5.6km. Temperatures of emplacement calculated with the hornblende-plagioclase thermometer are742C,647℃and647℃respectively. The log fo2estimated from biotite ranges from-14.8～-16.3,-17.8～-18.7and-18.0～-18.7, located between quartz-fayalite-magnetite and the Ni-NiO buffer assemblages.
4. Bulk-rock analyses show that the DMG and JGZ intrusion are characterized by high contents of SiO2, Al2O3, Na2O, K2O and low abundance of MgO and Mg#, defining their subalkaline and metaluminous characteristics. The enclaves from JGZ intrusion has relatively low concentrations of SiO2and total alkaline, and higher MgO, CaO and FeO, and can be classified as subalkaline-alkaline metaluminous monzodiorite-diorite. The DMG intrusion, JGZ intrusion and the enclaves from it are all enriched in LILE and LREE, and depleted in heavy rare earth elements (HREE) and HFSE, without significant Eu anomalies (0.89～1.10,0.61～0.83,0.79～0.93). They have high (La/Yb)N ratios (20.5～31.0,12.6～40.2,14.1～37.8), and low and constant (Dy/Yb)N ratios (0.87～1.60,1.12～1.35,1.31～1.63). The DMG and JGZ adakitic intrusions formed in an intracontinental extensional setting contemporaneous with the formation of pull-apart basins, metamorphic core complexes and intense magmatism, rather than in a convergent margin. The DMG intrusion, JGZ intrusion and the enclaves from it have homogeneous (87Sr/86Sr)i ratios (0.7059～0.7066,0.7055～0.7060,0.7059) and εNd(t)(-6.2～-7.2,-8.2,-11.0). The Pb isotope compositions of DMG intrusion are also homogeneous ((206Pb/204Pb)i=17.289～17.375,(207Pb/204Pb)i=15.359～15.463,(208Pb/204Pb)i=37.130～37.472). Moreover, the εHf(t) of JGZ intrusion and enclaves from it ranges from-9.2～-12.0and-4.5～-10.0respectively. In combination with the mineralogy, geochemistry and Sr-Nd-Pb-Hf isotope compositions of these rocks, we contend that the DMG and JGZ intrusions could have originated from crustal contamination of newly formed basaltic melts derived from asthenospheric mantle, accompanied by fractional crystallization of K-feldspar, biotite, apatite, Fe-Ti oxides and minor hornblende and plagioclase, and the enclaves from the JGZ intrusion could denote the feeder system during the late stage of host magma evolution. Thus, the DMG and JGZ adakitic intrusions may record the magmatic event associated with underplating of asthenospheric amgma in an intracontinental extensional environment, and both asthenospheric magma underplating and lithospheric delamination may have played important roles in the lithospheric thinning of the northern NCC.
5. The fluid inclusions from Anjiayingzi gold deposit have final homogenization temperatures (Th) of180～402℃, ice-melting temperatures (Tm, ice) of-11.6～-0.8℃, salinities of1.3～15.6wt%NaCl and fluid pressures of319×105Pa with δD of-80.3‰～-96.5‰and δi8OH2O of3.7‰-5.5‰. The fluid inclusions from JCGL gold deposit have Th of205～390℃, Tm, ice of-19.1～0.8℃, salinities of1.3～21.7wt%NaCl and fluid pressures of422×105Pa with δD of-54.0‰～-110.9‰and δ18OH2O of1.9‰～8.9‰. The fluid inclusions from Paishanlou gold deposit have Th of187～337℃and salinities of4.6～12.2wt%NaCl with5D of-87.3‰～-116.2‰and518OH2O of0.7‰～6.9‰. The mineralization depths of gold deposits from the Chifeng-Chaoyang region calculated fluid inclusions parameters range from2-2.5km. The ore fluids derived from the Early Cretaceous intrusions dominantly, and the fluid unmixing and temperature drop controlled the gold deposition jointly.
The Anjiayingzi, JCGL-Erdaogou and Paishanlou gold deposits have δ34S of-0.5～7.6‰,-2.8～2.3‰and0.3～6.5‰respectively. The corrected Pb isotope composition of metamorphic basement from Chifeng-Chaoyang region is highly variable, with (206Pb/204Pb)i=15.040～18.090,(207Pb/204Pb)i=15.065～15.655and (208Pb/204Pb)i=34.897～38.571. The corrected Pb isotope composition of the Early Cretaceous adakitic intrusions is relatively homogeneous with (206Pb/204Pb);=15.742～17.375,(207Pb/204Pb)i=15.237～15.665and (208Pb/204Pb)i=36.908～38.547. The Pb isotope of ore sulfides from regional gold deposits is nearly the same as that of the Early Cretaceous intrusions with (206Pb/204Pb)i=16.400～17.591,(207Pb/204Pb)i=15.210～15.578and (208Pb/204Pb)i=36.690～38.091, indicating their magmatic origin.
6. The Triassic Mo (gold?) mineralizing event is confirmed by the Re-Os age of243.5±1.3from the JCGL Mo-bearing quartz veins, and it was developed in the post-orogenic extensional regime as the result of Paleo-Asian Ocean closure. The zircon U-Pb, biotite and K-feldspar40Ar-39Ar ages reveal that gold deposits from Chifeng-Chaoyang region mainly formed during the Early Cretaceous (133～117Ma), contemporaneous with the development of MCC (130～100Ma) and intense magmatism (133Ma～124Ma). Most importantly, the ore fluids and metals also derived from the Early Cretaceous intrusions. In combination with these results described above, this paper presents a two-stage mineralizing model.
引文
①李建威.矿床学前沿讲义.中国地质大学(武汉),2008.
②李永刚等.内蒙古喀喇沁旗金蟾山金矿成矿规律和找矿预测研究.金蟾山金矿内部资料,2000.
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