吉林省海沟金矿矿床地质特征及成矿模式
|
摘要
海沟金矿床位于吉林省延边自治州安图县两江镇境内，是一个大型的石英脉型金矿床。矿床在大地构造位置上位于华北地台北缘东段与兴蒙—吉黑造山带接壤的构造区内，是中生代太平洋构造域NE向构造与海西期古亚洲域NW向构造叠加十分明显的地区。海沟金矿即产于NW向金银别—清茶馆断裂和NE向两江断裂交汇部位。
矿区出露的地层主要为元古界集安群、色洛河群变质岩系和青白口系沉积岩，以及中新生界火山—沉积岩系；研究区断裂构造发育，主要形成大量NE向和NW向展布的断裂构造，矿区内分别以两江断裂及海沟—荒沟农场断裂为代表。矿区内侵入岩以中酸性花岗质岩石为主，主要由晚古生代中酸性花岗质侵入岩和中生代花岗质、闪长质侵入岩等组成；火山岩仅见于局部地段，多为零星分布的中、新生代安山岩、玄武岩等。
海沟金矿矿区范围内已经探明50余条矿脉，主矿脉带有28号、38号、43号3条。矿脉主要分布在海沟二长岩—二长花岗岩岩体中，少部分在岩体外围的色洛河群，受NE-NNE向断裂构造带控制。矿石类型以含金石英脉型为主，少量蚀变岩型。矿石矿物主要有自然金、黄铁矿、方铅矿、黄铜矿、辉钼矿、闪锌矿、赤铁矿等，脉石矿物有石英、方解石、重晶石、高岭土等。矿石结构以结晶结构、交代结构、碎裂结构为主，矿石构造以脉状、网脉状最为发育，其次有团块构造、浸染状构造和星散状构造等。根据矿物生成顺序和组合特点，海沟金矿可划分为5个成矿阶段：Ⅰ、石英-赤铁矿-沥青铀矿阶段，Ⅱ、白色石英脉阶段，Ⅲ、金-烟灰色石英脉-黄铁矿阶段，Ⅳ、金-多金属硫化物阶段，Ⅴ、方解石阶段；第Ⅲ、Ⅳ阶段为矿化主要阶段。矿床围岩蚀变以钾化、黄铁矿化和硅化为主。
海沟金矿床的流体包裹体可以分为气液两相包裹体、富气相(主要为CO_2)包裹体两类，大小较小，多在2~8μm之间。海沟金矿成矿流体成分为富CO_2型CO_2-H_2O-CH_4体系，具―低盐富碳‖的特点，与典型造山型金矿流体成分特点相似。主矿化阶段（第Ⅲ、Ⅳ矿化阶段）成矿温度集中在200~300℃。碳、氢、氧同位素研究结果显示成矿流体以岩浆水为主，有大气水参与，且后期有增加趋势，具幔源特点。硫、铅同位素研究显示成矿物质具壳幔混合来源的特点，主要来源于元古宙色洛河群和太古宙地壳。
海沟岩体是矿区内金矿脉的直接赋矿围岩，可分为中心相二长花岗岩和边缘相二长岩两个岩相，岩石常量元素显示海沟岩体为低硅富铝的钾玄岩系列-高钾钙碱性系列，稀土元素分馏明显、轻稀土富集（71.36×10~(-6)~220.97×10~(-6)），重稀土亏损（9.05×10~(-6)~35.7×10~(-6)），δEu=0.81~1.26，平均1.01，无明显铕异常。微量元素富Ba、Sr等大离子亲石元素和U、Th、Pb等高场强元素，亏损P、Ti等。
通过对二长花岗岩（HG11）、二长岩（HG12）的锆石CL图像分析和岩浆锆石LA-ICP-MS U-Pb测年研究，认为海沟岩体成岩年代为晚古生代海西期（322.4-326.1Ma）。其中所捕获的太古代（2802±37Ma）和元古代（2320±32Ma、2305±32Ma）继承锆石可能反映了元古宙及太古宙地层对海沟岩体岩浆来源的贡献，结合稀土、微量元素及其Sr、Nd、Hf同位素研究，认为其岩浆来源以壳源为主，并有较多幔源物质混入，产出大地构造环境为与古亚洲板块俯冲作用有关的陆缘火山弧环境。
本次测得正长闪长斑岩岩浆结晶锆石LA-ICP-MS U-Pb年龄为132.4Ma，结合前人对海沟金矿成矿时代研究结果，限定海沟金矿成矿作用发生在142.3~128Ma之间，矿化峰期时间为130Ma。结合海沟矿区的成矿动力学背景，其成矿模式可总结如下：
在142.3~128Ma之间，海沟金矿区所在地区受到太平洋板块由俯冲碰撞挤压向伸展构造体制转换过渡的影响，古老的地幔岩石圈发生大规模拆沉和快速减薄，软流圈地幔向上底侵，导致下地壳部分熔融，为成矿提供初始的热源和早期高盐度岩浆热液；同时，随着底侵作用的发生，富CO_2的地幔流体与板下基性岩浆沿深大断裂上侵，提供部分幔源成矿物质，并引起一系列中基性岩浆活动，海沟矿区主要表现为侵入至海西期海沟岩体中的辉石闪长岩体和大量基性脉岩。地幔流体在上升运移过程中，萃取地壳中成矿物质，形成含矿热液。在其温度、压力、pH值、Eh值等物理化学条件发生改变的情况下，含矿热液中的金在海沟岩体中的NE-NEE向有利构造部位沉淀成矿。
Haigou gold deposit is located in Liangjiang town, Antu country of JilinProvince. It is in the transitional tectonic area between the northern margin of theNorth China Plate and the Xing'an-Mongolia orogenic belt (Jilin-Heilongjiangportion). The study area is in a tectonic region where the Mesozoic Pacific tectonicdomain superposed on Hercynian Paleo-Asian Ocean tectonic domain. The Haigougold deposit exsits in the place where NW trending Jinyinbie-Qingchaguan Faultcrosscuts with NE trending Liangjiang Fault.
The strata exposed in the region mainly include Ji’an Group and Seluohe Groupmetamorphic rock series, Qingbaikou System sedimentary strata of Proterozoic, andvolcanic-sedimentary rock series of Mesozoic-Cenozoic. NE trending and NWtrending faults are seen in and nearby the Haigou mine, for example, the LiangjiangFault and the Haigou-Huanggou Fault. The regional magmatic activities were alsostrong in the area and the intrusions are mainly Late Hercynian intermediate-acidgranitoids, and Mesozoic granitic and dioritic intrusions. The intermediate-basicvolcanic rocks of Mesozoic-Cenozoic are locally developped in the area.
Haigou gold deposit contains more than50ore veins, and the28th,38thand43thvein are the main vein groups of them. The veins are mainly controlled by NE-NNEtrending structure belts in monzonite and monzogranite, a few in Seluohe complex.The mineralization type are auriferous quartz veins principally, and a few altered rocktype. The ore minerals are native gold, pyrite, galena, chalcopyrite, molybdenite,sphalerite and hematite etc, and the gangue minerals are mainly quartz, calcite, barite,kaolin, etc. There are many types of ore structures, mainly include crystallinestructure, replacement texture, cataclastic structure etc. Ore textures mainly includevein, reticulate vein texture, in addition to developing massive texture, disseminated texture and scattered texture, etc. In accordance with formation orders, themineralization of Haigou gold deposit can be divided into five phases:Ⅰ.quartzvein-hematite-pitchblende stage,Ⅱ. white quartz vein stage, Ⅲ. gold-gray quartzvein-pyrite stage, Ⅳ. gold-polymetallic sulfide stage, and Ⅴ.calcite stage. Amongthem the stage Ⅲ, Ⅳ are the principal mineralization stages. The types of wall-rockalteration include alteration to K-feldspar, pyrite, and silicification etc.
The types of fluid inclusions can be divided into two phases: gas-liquidtwo-phase inclusions and gas-rich(mainly CO_2) inclusions, whose size ranges from2to8μm. The components of ore-forming fluid are CO_2-H_2O-CH_4system, which ischaracterized by CO_2-rich and salinity-low, similar to the fluid composition of typicalorogenic gold deposits. The temperature of the main mineralization stage(Ⅲ,Ⅳ)focused on200~300℃. The results of carbon-hydrogen-oxygen isotopes researchindicate that the ore-forming fluids are mostly magmatic water, a little meteoric waterand a few mantle-derived fluids in addition. Sulfur and lead isotopes research revealthat the ore-forming material resources mainly come from Seluohe group of LateProterozoic and Archean Strata, with crust-mantle mixing characteristics.
The Haigou intrusion consists mainly of central monzogranite, and marginalmonzonite. Study on major elements shows that Haigou intrusive rocks are alkali-richand aluminum-rich shoshonite-serieshigh-K calc-alkaline series granitic rocks,characterized by enrichment in LREE(71.36×10~(-6)~220.97×10~(-6)) and depletion inHREE(9.05×10~(-6)~35.7×10~(-6)), unconspicuous anomalies of Eu(δEu=0.81~1.26,averaged at1.01). The rocks are characterized by the enrichment of LILE(Ba, Sr) andHFSE(Th, U, Pb)，depletion of Pand Ti, etc.
According to the CL image analysis and LA-ICP-MS U-Pb age of testing ofzircon in adamellite(HG11), monzonite(HG12), the petrogenic age of Haigouintrusion is Hercynian period(322.4-326.1Ma), with inherited zircon of Archeanera(2802±37Ma) and Proterozoic era(2320±32Ma,2305±32Ma). Combining the REEs,trace elements, and Sr, Nd, Hf isotopes research, the paper suggests that the sources ofHaigou intrusion are mainly derived from crust source, with a great amount of mantlematerial, its tectonic environment belongs a continental margin setting related toPaleo-Asian Ocean plate subduction..
The geologic age of syn-mineralization granodiorite porphyry is132.4Ma.Considering the former studies about metallogenic epoch of the Haigou gold deposit, its mineralization time should be limited to142.3~128Ma, mainly130Ma.
The metallogenic model of the deposit is suggested as the followings:
In142.3~128Ma, the area was in the period of conversion of tectonic regimes.The ancient mantle lithospheric delamination and extension, asthenosphere upwelling,caused the lower crust partial melting, provided the initial heat source and highsalinity magmatic hydrothermal for mineralization. And with the occurrence anddevelopment of underplating, the CO_2-rich mantle fluids and the basic magma intrudeupwards along the deep-large fault, carrying partial mantle-derived ore-formingmaterial and caused the formation of the Dahaigou gabbro-diorite stock and largenumber of intermediate-basic dikes in the mine. During the mantle-derived fluidsascending, they extracted the ore-forming materials from the crust and formedore-bearing hydrothermal fluids. Gold was deposited in the NE-NEE extending faultsin the Haigou intrusion where favorable physicochemical conditions (for instance, P, T,Ph, Eh) are met.
矿区出露的地层主要为元古界集安群、色洛河群变质岩系和青白口系沉积岩，以及中新生界火山—沉积岩系；研究区断裂构造发育，主要形成大量NE向和NW向展布的断裂构造，矿区内分别以两江断裂及海沟—荒沟农场断裂为代表。矿区内侵入岩以中酸性花岗质岩石为主，主要由晚古生代中酸性花岗质侵入岩和中生代花岗质、闪长质侵入岩等组成；火山岩仅见于局部地段，多为零星分布的中、新生代安山岩、玄武岩等。
海沟金矿矿区范围内已经探明50余条矿脉，主矿脉带有28号、38号、43号3条。矿脉主要分布在海沟二长岩—二长花岗岩岩体中，少部分在岩体外围的色洛河群，受NE-NNE向断裂构造带控制。矿石类型以含金石英脉型为主，少量蚀变岩型。矿石矿物主要有自然金、黄铁矿、方铅矿、黄铜矿、辉钼矿、闪锌矿、赤铁矿等，脉石矿物有石英、方解石、重晶石、高岭土等。矿石结构以结晶结构、交代结构、碎裂结构为主，矿石构造以脉状、网脉状最为发育，其次有团块构造、浸染状构造和星散状构造等。根据矿物生成顺序和组合特点，海沟金矿可划分为5个成矿阶段：Ⅰ、石英-赤铁矿-沥青铀矿阶段，Ⅱ、白色石英脉阶段，Ⅲ、金-烟灰色石英脉-黄铁矿阶段，Ⅳ、金-多金属硫化物阶段，Ⅴ、方解石阶段；第Ⅲ、Ⅳ阶段为矿化主要阶段。矿床围岩蚀变以钾化、黄铁矿化和硅化为主。
海沟金矿床的流体包裹体可以分为气液两相包裹体、富气相(主要为CO_2)包裹体两类，大小较小，多在2~8μm之间。海沟金矿成矿流体成分为富CO_2型CO_2-H_2O-CH_4体系，具―低盐富碳‖的特点，与典型造山型金矿流体成分特点相似。主矿化阶段（第Ⅲ、Ⅳ矿化阶段）成矿温度集中在200~300℃。碳、氢、氧同位素研究结果显示成矿流体以岩浆水为主，有大气水参与，且后期有增加趋势，具幔源特点。硫、铅同位素研究显示成矿物质具壳幔混合来源的特点，主要来源于元古宙色洛河群和太古宙地壳。
海沟岩体是矿区内金矿脉的直接赋矿围岩，可分为中心相二长花岗岩和边缘相二长岩两个岩相，岩石常量元素显示海沟岩体为低硅富铝的钾玄岩系列-高钾钙碱性系列，稀土元素分馏明显、轻稀土富集（71.36×10~(-6)~220.97×10~(-6)），重稀土亏损（9.05×10~(-6)~35.7×10~(-6)），δEu=0.81~1.26，平均1.01，无明显铕异常。微量元素富Ba、Sr等大离子亲石元素和U、Th、Pb等高场强元素，亏损P、Ti等。
通过对二长花岗岩（HG11）、二长岩（HG12）的锆石CL图像分析和岩浆锆石LA-ICP-MS U-Pb测年研究，认为海沟岩体成岩年代为晚古生代海西期（322.4-326.1Ma）。其中所捕获的太古代（2802±37Ma）和元古代（2320±32Ma、2305±32Ma）继承锆石可能反映了元古宙及太古宙地层对海沟岩体岩浆来源的贡献，结合稀土、微量元素及其Sr、Nd、Hf同位素研究，认为其岩浆来源以壳源为主，并有较多幔源物质混入，产出大地构造环境为与古亚洲板块俯冲作用有关的陆缘火山弧环境。
本次测得正长闪长斑岩岩浆结晶锆石LA-ICP-MS U-Pb年龄为132.4Ma，结合前人对海沟金矿成矿时代研究结果，限定海沟金矿成矿作用发生在142.3~128Ma之间，矿化峰期时间为130Ma。结合海沟矿区的成矿动力学背景，其成矿模式可总结如下：
在142.3~128Ma之间，海沟金矿区所在地区受到太平洋板块由俯冲碰撞挤压向伸展构造体制转换过渡的影响，古老的地幔岩石圈发生大规模拆沉和快速减薄，软流圈地幔向上底侵，导致下地壳部分熔融，为成矿提供初始的热源和早期高盐度岩浆热液；同时，随着底侵作用的发生，富CO_2的地幔流体与板下基性岩浆沿深大断裂上侵，提供部分幔源成矿物质，并引起一系列中基性岩浆活动，海沟矿区主要表现为侵入至海西期海沟岩体中的辉石闪长岩体和大量基性脉岩。地幔流体在上升运移过程中，萃取地壳中成矿物质，形成含矿热液。在其温度、压力、pH值、Eh值等物理化学条件发生改变的情况下，含矿热液中的金在海沟岩体中的NE-NEE向有利构造部位沉淀成矿。
Haigou gold deposit is located in Liangjiang town, Antu country of JilinProvince. It is in the transitional tectonic area between the northern margin of theNorth China Plate and the Xing'an-Mongolia orogenic belt (Jilin-Heilongjiangportion). The study area is in a tectonic region where the Mesozoic Pacific tectonicdomain superposed on Hercynian Paleo-Asian Ocean tectonic domain. The Haigougold deposit exsits in the place where NW trending Jinyinbie-Qingchaguan Faultcrosscuts with NE trending Liangjiang Fault.
The strata exposed in the region mainly include Ji’an Group and Seluohe Groupmetamorphic rock series, Qingbaikou System sedimentary strata of Proterozoic, andvolcanic-sedimentary rock series of Mesozoic-Cenozoic. NE trending and NWtrending faults are seen in and nearby the Haigou mine, for example, the LiangjiangFault and the Haigou-Huanggou Fault. The regional magmatic activities were alsostrong in the area and the intrusions are mainly Late Hercynian intermediate-acidgranitoids, and Mesozoic granitic and dioritic intrusions. The intermediate-basicvolcanic rocks of Mesozoic-Cenozoic are locally developped in the area.
Haigou gold deposit contains more than50ore veins, and the28th,38thand43thvein are the main vein groups of them. The veins are mainly controlled by NE-NNEtrending structure belts in monzonite and monzogranite, a few in Seluohe complex.The mineralization type are auriferous quartz veins principally, and a few altered rocktype. The ore minerals are native gold, pyrite, galena, chalcopyrite, molybdenite,sphalerite and hematite etc, and the gangue minerals are mainly quartz, calcite, barite,kaolin, etc. There are many types of ore structures, mainly include crystallinestructure, replacement texture, cataclastic structure etc. Ore textures mainly includevein, reticulate vein texture, in addition to developing massive texture, disseminated texture and scattered texture, etc. In accordance with formation orders, themineralization of Haigou gold deposit can be divided into five phases:Ⅰ.quartzvein-hematite-pitchblende stage,Ⅱ. white quartz vein stage, Ⅲ. gold-gray quartzvein-pyrite stage, Ⅳ. gold-polymetallic sulfide stage, and Ⅴ.calcite stage. Amongthem the stage Ⅲ, Ⅳ are the principal mineralization stages. The types of wall-rockalteration include alteration to K-feldspar, pyrite, and silicification etc.
The types of fluid inclusions can be divided into two phases: gas-liquidtwo-phase inclusions and gas-rich(mainly CO_2) inclusions, whose size ranges from2to8μm. The components of ore-forming fluid are CO_2-H_2O-CH_4system, which ischaracterized by CO_2-rich and salinity-low, similar to the fluid composition of typicalorogenic gold deposits. The temperature of the main mineralization stage(Ⅲ,Ⅳ)focused on200~300℃. The results of carbon-hydrogen-oxygen isotopes researchindicate that the ore-forming fluids are mostly magmatic water, a little meteoric waterand a few mantle-derived fluids in addition. Sulfur and lead isotopes research revealthat the ore-forming material resources mainly come from Seluohe group of LateProterozoic and Archean Strata, with crust-mantle mixing characteristics.
The Haigou intrusion consists mainly of central monzogranite, and marginalmonzonite. Study on major elements shows that Haigou intrusive rocks are alkali-richand aluminum-rich shoshonite-serieshigh-K calc-alkaline series granitic rocks,characterized by enrichment in LREE(71.36×10~(-6)~220.97×10~(-6)) and depletion inHREE(9.05×10~(-6)~35.7×10~(-6)), unconspicuous anomalies of Eu(δEu=0.81~1.26,averaged at1.01). The rocks are characterized by the enrichment of LILE(Ba, Sr) andHFSE(Th, U, Pb)，depletion of Pand Ti, etc.
According to the CL image analysis and LA-ICP-MS U-Pb age of testing ofzircon in adamellite(HG11), monzonite(HG12), the petrogenic age of Haigouintrusion is Hercynian period(322.4-326.1Ma), with inherited zircon of Archeanera(2802±37Ma) and Proterozoic era(2320±32Ma,2305±32Ma). Combining the REEs,trace elements, and Sr, Nd, Hf isotopes research, the paper suggests that the sources ofHaigou intrusion are mainly derived from crust source, with a great amount of mantlematerial, its tectonic environment belongs a continental margin setting related toPaleo-Asian Ocean plate subduction..
The geologic age of syn-mineralization granodiorite porphyry is132.4Ma.Considering the former studies about metallogenic epoch of the Haigou gold deposit, its mineralization time should be limited to142.3~128Ma, mainly130Ma.
The metallogenic model of the deposit is suggested as the followings:
In142.3~128Ma, the area was in the period of conversion of tectonic regimes.The ancient mantle lithospheric delamination and extension, asthenosphere upwelling,caused the lower crust partial melting, provided the initial heat source and highsalinity magmatic hydrothermal for mineralization. And with the occurrence anddevelopment of underplating, the CO_2-rich mantle fluids and the basic magma intrudeupwards along the deep-large fault, carrying partial mantle-derived ore-formingmaterial and caused the formation of the Dahaigou gabbro-diorite stock and largenumber of intermediate-basic dikes in the mine. During the mantle-derived fluidsascending, they extracted the ore-forming materials from the crust and formedore-bearing hydrothermal fluids. Gold was deposited in the NE-NEE extending faultsin the Haigou intrusion where favorable physicochemical conditions (for instance, P, T,Ph, Eh) are met.
引文
[1]长春地质学院,吉林省地矿局第六地质调查所.吉林省安图县海沟金矿区及其外围控矿机制和找矿靶区优选[R].1996.6
[2]海沟黄金矿业有限责任公司生产部,海沟金矿区以往地质工作及开采现状汇报[R].2010
[3]吉林省地质矿产局.吉林省区域地质志[M].北京:地质出版社,1988:1-605
[4]方文昌.吉林省花岗岩类及成矿作用[M].长春:吉林科学技术出版社.1992:9-16
[5]迟清华,鄢明才.应用地球化学元素丰度数据手册[M].地质出版社.2007:5-25
[6]李昌年.火成岩微量元素岩石学[M].北京:中国地质大学出版社.1992:104-109
[7]肖庆辉,邓晋福,马大铨等.花岗岩研究思维与方法[M].北京:地质出版社.2002:12-63
[8]程裕淇.中国区域地质概论[M].北京:地质出版社.1994:416-424
[9]卢焕章,范宏瑞,倪培,等.流体包裹体[M].北京:科学出版社,2004:1-492
[10]邱家骧主编.岩浆岩岩石学[M].北京:地质出版社.1985:207-311
[11]邱家骧主编.应用岩浆岩岩石学[M].北京:中国地质大学出版社.1991:38-265
[12]杨忠芳,徐景奎等.胶东区域地壳演化与金矿作用地球化学[M]北京:地质出版社.1998:112-117
[13]常艳.吉林省海沟大型金矿床的成矿动力学模式[D].硕士学位论文.长春:吉林大学,2009
[14]聂喜涛.黑龙江省团结沟金矿床成矿地质背景与成矿模式研究[D].硕士学位论文.长春:吉林大学,2010
[15]曹花花.珲春地区晚海西期辉长岩——闪长岩的形成时代和地球化学[D].硕士学位论文.长春:吉林大学,2010
[16]丰成友.青海东昆仑地区的复合造山过程及造山型金矿床成矿作用[D].博士学位论文.北京:中国地质科学院矿产资源研究所,2002
[17]陈衍景.造山型矿床、成矿模式及找矿潜力[J].中国地质.2006,33(6):1181-1196
[18] Thompson J F H, Sillitoe R H, Baker T et al. Intrusion-related gold deposits associated withtungstentin provinces[J]. Mieralium Deposita.1999,34:323-334
[19] Lang J R, Baker T. Intrusion-related gold systems: the present level of understanding[J].Mieralium Deposita.2001,36:477-489
[20] Terry P, Memagh, et al. Comparison of fluid inclusion data and mineralization processes forAustralian orogenic gold and intrusion-related gold systems[J].Acta PetrologicaSinica.2007,23(1):21-32
[21]胡朋,聂凤军,江思宏.与侵入岩有关金矿床的研究现状、存在问题及在中国的前景[J].地质论评.2006,52(4):539-549
[22]李存有(编译).与侵入岩有关的脉型金矿:类型、构造岩浆背景及与造山带金矿的区别[J].内蒙古地质.2000,2(95):24-30
[23]刘裕庆.吉林海沟金矿床同位素地球化学和成矿规律研究[J].矿床地质.1991,10(2):132-142
[24]李荫清.吉林海沟金矿床成矿流体的地球化学特征[J].地质学报.1994,68(1):48-61
[25]曾庆栋,戴薪义,金蓬洙.吉林省安图县海沟金矿床控矿构造特征[J].吉林地质.1996,15(2):36-44
[26]戴薪义,曾庆栋.吉林省安图县海沟花岗岩体的地质特征及其与金矿关系[J].吉林地质.1996,15(1):30-37
[27]曾庆栋,沈远超.海沟金矿区脉岩特征及其与金矿成矿关系[J].贵金属地质.1999.8(2):70-75
[28]沈远超,曾庆栋,谢宏远.吉林省夹皮沟—海沟成矿带金矿定位时代[J].黄金科学技术.1999,7(2):19-26
[29]孙忠实,冯亚民,孟庆丽等.吉林海沟金矿成矿预测新思路——控矿构造层次[J].吉林地质.1998,17(3):43-50
[30]彭向东,张梅生,李晓敏.吉黑造山带古生代构造古地理演化[J].世界地质.1999,18(3):24-28
[31]冯守忠.吉林海沟金矿床地质特征及成矿模式[J].地质与勘探.1999,35(1):10-15
[32]孙岳,雷时斌,卿敏,等.吉林省海沟金矿断裂地球化学预测研究[J].地质与勘探,2002,38(3):23-27
[33]张传乐,张希友,金艳峰.吉林省安图县海沟金矿床地质特征及其形成机制[J].吉林地质.2005,24(3):5-10
[34]李志明,张长江,廖宗廷,等.海沟金矿地质-地球化学特征及其成矿机制探讨[J].地质与资源.2005,14(2):111-116
[35]冯明,王好均,曹国等.吉林海沟金矿控矿构造特征及其演化[J].长春工程学院学报.2005,16(24):44-47
[36]冯明,吕建生.延边海沟金矿控矿构造类型及成矿动力学机制探讨[J].世界地质.2007,26(3):275-281
[37]焦保权,李世平,王艳萍等.海沟岩体的成岩时代及成因探讨[J].吉林地质.2008,27(2):1-4
[38]李绪俊,范振华,范文亮等.海沟金矿28#脉深部隐伏矿体地球化学预测[J].世界地质.2011,30(3):359-367
[39]汪志刚,牛继辉,朱文丰.吉林安图海沟金矿成矿流体特征及成矿机制[J].世界地质.2011,30(3):313-322
[40]张松,曾庆栋,刘建明等.吉林省海沟石英脉型金矿床流体包裹体特征及地质意义[J].岩石学报.2011,27(5):1287-1298
[41]吴尚全.吉林省主要金矿床的石英气液包裹体特征[J].1994,2(5):8-16
[42]陈衍景,倪培,范宏瑞等.不同类型热液金矿系统的流体包裹体特征[J].2007,23(9):2085-2108
[43]范振华,李绪俊,梁本胜等.吉林安图海沟岩体岩石地球化学特征及其成岩构造环境[J].世界地质,2012,31(1):9-19
[44]张松,王永彬,褚少雄.华北克拉通北缘东段海沟岩体的锆石U-Pb年龄、Sr-Nd-Hf同位素组成及其动力学背景[J].岩石学报.2012,28(2):544-556
[45]綦远江,李凤阁,胡文国.夹皮沟色洛河群中金矿地质特征及找矿方向[J].黄金科学技术,2002,10(3):26-31
[46]张艳斌,吴福元,李惠民,等.吉林黄泥岭花岗岩体的单颗粒锆石U-Pb年龄[J].岩石学报,2002,18(4):475-481
[47]陈跃军,孙春林,刘跃文等.吉林延边安图县海沟地区海沟岩群的建立及其意义[J].地层学杂志.2006,3(3):237-242.
[48]李承东,张福勤,苗来成等.吉林色洛河群的重新认识[J].吉林大学学报(地球科学版).2007,37(05):841-848.
[49]吴克隆,严炳铨,陆振球等.福建省晶洞（钾长）花岗岩一般特征及成因初步探讨[J].福建地质,1982,2:1-28
[50] M.P.Roberts, J.D.Clemens,董传万.高钾钙碱性Ⅰ型花岗岩类的成因[J].世界地质.1994,13(4):8-12.
[51]吴元保,郑永飞.锆石成因矿物学研究及其对U-Pb年龄解释的制约[J].科学通报.2004,49(16):1589-1604
[52]吴荣新.锆石阴极发光和U-Pb年龄特征研究[J].安徽理工大学学报(自然科学版).2008,28(4):1-7
[53]简平,程裕淇,刘敦一.变质锆石成因的岩相学研究——高级变质岩U-Pb年龄解释的基本依据[J]地学前缘(中国地质大学,北京).2001,8(3):183-191
[54] Cynthia D B. Joseph L W, Melanie J H. U-Pb zircon and geochemical evidence for bimodalmid-Paleozoic magmatism and syngenetic base-metal mineralization in the Yukon-Tananaterrane, Alaska [J]. Geological Survey of Amevica Bulletin.2004,116(7/8):989-1015
[55] Arvin M, Dargahi S, Babaei A A. Mafic microgranular enclave swarms in the Chenargranitoid stock, NW of Kerman, Iran:evidence for magma mingling[J].Journal of Asian EarthSciences.2004,24:105-113
[56] QIN J F, LAI S C, Grapes R, et al. Geochemical evidence for origin of magma mixing for theTriassic monzonitic graniteand its enclaves at Mishuling in the Qinling orogen(centralChina)[J].Lithos.2009,112:259-276
[57]张旗,王云龙,金惟俊等.造山前、造山和造山后花岗岩的识别[J].地质通报.2008,27(1):1-18
[58]李晶,陈衍景,李强之.甘肃阳山金矿碳氢氧同位素与成矿流体来源[J].岩石学报.2008,24(4):817-826
[59]毛景文,赫英,丁悌平.胶东金矿形成期间地幔流体参与成矿过程的碳氧氢同位素证据[J].矿床地质.2002,21(2):121-128
[60]毛景文,李厚民,王义天等.地幔流体参与胶乐金矿成矿作用的氢氧碳硫同位素证据[J].地质学报.2005,79(6):839-850
[61]刘丛强,黄智龙,李和平等.地幔流体及其成矿作用[J].地学前缘.2001,8(4):231-243
[62]卢焕章,J.Guha等.山东玲珑金矿的成矿流体特征[J]地球化学.1999,28(5):421-437
[63]卢焕章,袁万春,张国平等.玲珑—焦家地区主要金矿床稳定同位素及同位素年代学[J].桂林工学院学报.1999,19(1):1-8
[64]陕亮,郑有业,许荣科等.硫同位素示踪与热液成矿作用研究[J].地质与资源.2009,18(3):197-203
[65]汪在聪,刘建明,刘红涛等.稳定同位素热液来源示踪的复杂性和多解性评述——以造山型金矿为例[J].岩石矿物学杂志.2010,29(5):563-576
[66]侯明兰,蒋少涌,姜耀辉等.胶东蓬莱金成矿区的S-Pb同位素地球化学和Rb-Sr同位素年代学研究[J].岩石学报.2006,22(10):2525-2533
[67]林文蔚,赵一鸣,赵国红等.胶东金矿铅同位素地质特征及成矿年代讨论[J].长春科技大学学报.1999,29(2):116-121
[68]王义文.夹皮沟金矿床同位素地质学研究[J].地球科学(武汉地质学院学报).1984,4:25-36
[69]王力,孙丰月等.山东金岭金矿床成矿流体地球化学特征[J].岩石学报.2010,26(12):3735-3744
[70]马振东.论铅同位素的地质指示作用[J].地球科学(武汉地质学院学报).1988,11(4):437-443
[71]谭俊,魏俊浩,谭文娟等.同源岩浆成因金矿成岩成矿时差的统计研究[J].地质论评.2006,52(1):54-60
[72]谢荣举.暗色岩脉与成矿关系[J].现代地质.1997:130
[73]孙德有,吴福元,张艳斌等.西拉木伦河—长春—延吉板块缝合带的最后闭合时间——来自吉林大玉山花岗岩体的证据[J].吉林大学学院(地球科学版).2004,34(2):174-181
[74]罗镇宽,苗来成,关康等.中国大地构造演化与金矿成矿作用[J].1998,13(3):24-34
[75]李双林,欧阳自远.兴蒙造山带及邻区的构造格局与构造演化[J].海洋地质与第四纪地质.1998,18(3):45-54
[76]唐克东,王莹,何国琦等.中国东北及邻区大陆边缘构造[J].地质学报.1995,69(1):16-30
[77]隋振民.吉林省中生代花岗岩成因系列及其构造环境[J].吉林地质.1995,14(1):15-22
[78]赵振华.关于岩石微量元素构造环境判别图解使用的有关问题[J].大地构造与成矿学.2007,31(1):92-103
[79]张旗,潘国强,李承东等.花岗岩构造环境问题:关于花岗岩研究的思考之三[J].岩石学报.2007,23(11):683-698
[80]张旗,李承东,王焰等.中国东部中生代高Sr低Yb和低Sr高Yb型花岗岩对比及其地质意义[J].岩石学报.2005,21(06):1527-1537
[81] Pearce J A, Harris N B W, Tindle A G. Trace element discrimination diagrams for thetectonic interpretation of granitic rocks [J]. Petrology.1984,25(4):956-983
[82]肖庆辉,邢作云,张昱等.当代花岗岩研究的几个重要前沿[J].地学前缘(中国地质大学,北京).2003,10(3):221-229
[83]肖庆辉,邱瑞照,邓晋福等.中国花岗岩与大陆地壳生长方式初步研究[J].中国地质.2005,32(3):343-352
[84]肖庆辉,邓晋福,邱瑞照等.花岗岩类与大陆地壳生长初探——以中国典型造山带花岗岩类岩石的形成为例[J].中国地质.2009,36(3):594-622
[85] YANG J H, WU F Y, CHUNG S L, et al. Multiple sources for the origin of granites:Geochemical and Nd/Sr isotopic evidence from the Gudaoling granite and its mafic enclaves,northeast China [J].Geochimica et Cosmochimica Acta.2004,68(21):4469-4483.
[86] YANG J H, WU F Y, Wilde S A. A review of the geodynamic setting of large-scale LateMesozoic gold mineralization in the North China Craton: an association with lithosphericthinning[J]. Ore Geology Reviews.2003(23):125-152
[87] Barbarin, B.A review of the relationships between granitoid types, their origins and theirgeodynamic environments[J].Lithos.1999,46:605-626
[88]吴福元,孙德有,林强.东北地区显生宙花岗岩的成因与地壳演化[J].岩石学报.1999(15):181-189
[89]赵成弼,靳克,齐成栋等.珲春地区早印支期I-A型花岗岩系的特征及其大地构造意义[J].吉林地质.2001,20(1):1-11
[90]李莉,白云山,牛志军等.藏北羌塘中部劳日特错花岗斑岩体的特征及构造意义[J].地质通报.2004,23(9/10):40-45
[91] Barbarin, B. Granitoids: main petrogenetic classifications in relation to origin and tectonicsetting [J]. Geology.1990,25:227-238
[92] Barbarin, B. Genesis of the two main types of peraluminousgranitoids[J].Geology.1996,24(4):295-298
[93]孙忠实,邓军,翟裕生等.吉林钾长花岗岩构造背景及铀对大型金矿床的控制[J].地球学报.1999,20(2):460-465
[94]孙忠实,邓军,冯亚民等.吉林古陆成岩背景及边缘金构造—成矿系统[J].地质地球化学.2000,28(4):1-6
[95]隋振民.吉林省中生代花岗岩成因系列及其构造环境[J].吉林地质.1995,14(1):15-21
[96]徐公愉,方文昌.吉林省两类花岗岩及其形成的构造背景[J].矿物岩石地球化学通报.1990,1:1-3
[97]葛肖虹.吉林东部大地构造环境与构造演化轮廓[J].现代地质.1990,4(1):107-113
[98]陈殿芬,孙淑琼.吉林海沟金矿床石英的研究[J].矿物岩石.1991,11(1):4-8
[99]李永军,刘志武,付国民等.花岗岩类I型S型分类在造山带实践中存在的问题——以西秦岭地区为例[J].华南地质与矿产.2002,2:1-7
[100] Roberts M P, Clemens J D. Origin of high plassium, calc-alkaline, I-typegranitoids[J].Geology.1993,21:825-828
[101]瞿泓滢,裴荣富,李进文.安徽铜陵凤凰山石英二长闪长岩和花岗闪长岩锆石SHRIMPU-Pb年龄及其地质意义[J].吉林大学学报(地球科学版).2010,40(3):581-590
[102]李印,韩峰,凌明星.蚌埠荆山和涂山岩体的年代学、地球化学特征及其动力学意义[J].大地构造与成矿学.2010,34(1):114-124
[103]赵俊伟.青海东昆仑造山带造山型金矿床成矿系列研究[D].硕士学位论文.长春:吉林大学,2008
[104]李厚民,沈远超,胡正国等.青海东昆仑五龙沟金矿床成矿条件及成矿机理[J].地质与勘探.2011,37(1):65-69
[105]梁业恒,孙晓明,石贵勇等.云南哀牢山老王寨大型造山型金矿成矿流体地球化学[J].岩石学报.2011,27(9):2533-2540
[106]张作衡.西秦岭地区造山型金矿床成矿作用和成矿过程[D].博士学位论文.北京:中国地质科学院
[107]李强,王兵岐,马治国等.南秦岭凤太盆地金矿与铅锌矿的成矿模式[J].地球科学与环境学院.2007,29(1):15-21
[108]韦龙明.陕西八卦庙金矿成矿流体初步研究[J].岩石学报.2007,23(9):2257-2262
[109] WU F Y, SUN D Y, GE W C, et al. Geochronolygy of the Phanerozoic granitoids innortheastern China[J]. Journal of Asian Earth Sciences.2011,(41):1-30
[110] MAO J W, WANG Y T, LI H M, et al. The relationship of mantle-derived fluids to goldmetallogenesis in the Jiaodong Peninsula: Evidence from D-O-C-S isotope systematics[J].Ore Geology Reviews.2007:1-21.
[2]海沟黄金矿业有限责任公司生产部,海沟金矿区以往地质工作及开采现状汇报[R].2010
[3]吉林省地质矿产局.吉林省区域地质志[M].北京:地质出版社,1988:1-605
[4]方文昌.吉林省花岗岩类及成矿作用[M].长春:吉林科学技术出版社.1992:9-16
[5]迟清华,鄢明才.应用地球化学元素丰度数据手册[M].地质出版社.2007:5-25
[6]李昌年.火成岩微量元素岩石学[M].北京:中国地质大学出版社.1992:104-109
[7]肖庆辉,邓晋福,马大铨等.花岗岩研究思维与方法[M].北京:地质出版社.2002:12-63
[8]程裕淇.中国区域地质概论[M].北京:地质出版社.1994:416-424
[9]卢焕章,范宏瑞,倪培,等.流体包裹体[M].北京:科学出版社,2004:1-492
[10]邱家骧主编.岩浆岩岩石学[M].北京:地质出版社.1985:207-311
[11]邱家骧主编.应用岩浆岩岩石学[M].北京:中国地质大学出版社.1991:38-265
[12]杨忠芳,徐景奎等.胶东区域地壳演化与金矿作用地球化学[M]北京:地质出版社.1998:112-117
[13]常艳.吉林省海沟大型金矿床的成矿动力学模式[D].硕士学位论文.长春:吉林大学,2009
[14]聂喜涛.黑龙江省团结沟金矿床成矿地质背景与成矿模式研究[D].硕士学位论文.长春:吉林大学,2010
[15]曹花花.珲春地区晚海西期辉长岩——闪长岩的形成时代和地球化学[D].硕士学位论文.长春:吉林大学,2010
[16]丰成友.青海东昆仑地区的复合造山过程及造山型金矿床成矿作用[D].博士学位论文.北京:中国地质科学院矿产资源研究所,2002
[17]陈衍景.造山型矿床、成矿模式及找矿潜力[J].中国地质.2006,33(6):1181-1196
[18] Thompson J F H, Sillitoe R H, Baker T et al. Intrusion-related gold deposits associated withtungstentin provinces[J]. Mieralium Deposita.1999,34:323-334
[19] Lang J R, Baker T. Intrusion-related gold systems: the present level of understanding[J].Mieralium Deposita.2001,36:477-489
[20] Terry P, Memagh, et al. Comparison of fluid inclusion data and mineralization processes forAustralian orogenic gold and intrusion-related gold systems[J].Acta PetrologicaSinica.2007,23(1):21-32
[21]胡朋,聂凤军,江思宏.与侵入岩有关金矿床的研究现状、存在问题及在中国的前景[J].地质论评.2006,52(4):539-549
[22]李存有(编译).与侵入岩有关的脉型金矿:类型、构造岩浆背景及与造山带金矿的区别[J].内蒙古地质.2000,2(95):24-30
[23]刘裕庆.吉林海沟金矿床同位素地球化学和成矿规律研究[J].矿床地质.1991,10(2):132-142
[24]李荫清.吉林海沟金矿床成矿流体的地球化学特征[J].地质学报.1994,68(1):48-61
[25]曾庆栋,戴薪义,金蓬洙.吉林省安图县海沟金矿床控矿构造特征[J].吉林地质.1996,15(2):36-44
[26]戴薪义,曾庆栋.吉林省安图县海沟花岗岩体的地质特征及其与金矿关系[J].吉林地质.1996,15(1):30-37
[27]曾庆栋,沈远超.海沟金矿区脉岩特征及其与金矿成矿关系[J].贵金属地质.1999.8(2):70-75
[28]沈远超,曾庆栋,谢宏远.吉林省夹皮沟—海沟成矿带金矿定位时代[J].黄金科学技术.1999,7(2):19-26
[29]孙忠实,冯亚民,孟庆丽等.吉林海沟金矿成矿预测新思路——控矿构造层次[J].吉林地质.1998,17(3):43-50
[30]彭向东,张梅生,李晓敏.吉黑造山带古生代构造古地理演化[J].世界地质.1999,18(3):24-28
[31]冯守忠.吉林海沟金矿床地质特征及成矿模式[J].地质与勘探.1999,35(1):10-15
[32]孙岳,雷时斌,卿敏,等.吉林省海沟金矿断裂地球化学预测研究[J].地质与勘探,2002,38(3):23-27
[33]张传乐,张希友,金艳峰.吉林省安图县海沟金矿床地质特征及其形成机制[J].吉林地质.2005,24(3):5-10
[34]李志明,张长江,廖宗廷,等.海沟金矿地质-地球化学特征及其成矿机制探讨[J].地质与资源.2005,14(2):111-116
[35]冯明,王好均,曹国等.吉林海沟金矿控矿构造特征及其演化[J].长春工程学院学报.2005,16(24):44-47
[36]冯明,吕建生.延边海沟金矿控矿构造类型及成矿动力学机制探讨[J].世界地质.2007,26(3):275-281
[37]焦保权,李世平,王艳萍等.海沟岩体的成岩时代及成因探讨[J].吉林地质.2008,27(2):1-4
[38]李绪俊,范振华,范文亮等.海沟金矿28#脉深部隐伏矿体地球化学预测[J].世界地质.2011,30(3):359-367
[39]汪志刚,牛继辉,朱文丰.吉林安图海沟金矿成矿流体特征及成矿机制[J].世界地质.2011,30(3):313-322
[40]张松,曾庆栋,刘建明等.吉林省海沟石英脉型金矿床流体包裹体特征及地质意义[J].岩石学报.2011,27(5):1287-1298
[41]吴尚全.吉林省主要金矿床的石英气液包裹体特征[J].1994,2(5):8-16
[42]陈衍景,倪培,范宏瑞等.不同类型热液金矿系统的流体包裹体特征[J].2007,23(9):2085-2108
[43]范振华,李绪俊,梁本胜等.吉林安图海沟岩体岩石地球化学特征及其成岩构造环境[J].世界地质,2012,31(1):9-19
[44]张松,王永彬,褚少雄.华北克拉通北缘东段海沟岩体的锆石U-Pb年龄、Sr-Nd-Hf同位素组成及其动力学背景[J].岩石学报.2012,28(2):544-556
[45]綦远江,李凤阁,胡文国.夹皮沟色洛河群中金矿地质特征及找矿方向[J].黄金科学技术,2002,10(3):26-31
[46]张艳斌,吴福元,李惠民,等.吉林黄泥岭花岗岩体的单颗粒锆石U-Pb年龄[J].岩石学报,2002,18(4):475-481
[47]陈跃军,孙春林,刘跃文等.吉林延边安图县海沟地区海沟岩群的建立及其意义[J].地层学杂志.2006,3(3):237-242.
[48]李承东,张福勤,苗来成等.吉林色洛河群的重新认识[J].吉林大学学报(地球科学版).2007,37(05):841-848.
[49]吴克隆,严炳铨,陆振球等.福建省晶洞（钾长）花岗岩一般特征及成因初步探讨[J].福建地质,1982,2:1-28
[50] M.P.Roberts, J.D.Clemens,董传万.高钾钙碱性Ⅰ型花岗岩类的成因[J].世界地质.1994,13(4):8-12.
[51]吴元保,郑永飞.锆石成因矿物学研究及其对U-Pb年龄解释的制约[J].科学通报.2004,49(16):1589-1604
[52]吴荣新.锆石阴极发光和U-Pb年龄特征研究[J].安徽理工大学学报(自然科学版).2008,28(4):1-7
[53]简平,程裕淇,刘敦一.变质锆石成因的岩相学研究——高级变质岩U-Pb年龄解释的基本依据[J]地学前缘(中国地质大学,北京).2001,8(3):183-191
[54] Cynthia D B. Joseph L W, Melanie J H. U-Pb zircon and geochemical evidence for bimodalmid-Paleozoic magmatism and syngenetic base-metal mineralization in the Yukon-Tananaterrane, Alaska [J]. Geological Survey of Amevica Bulletin.2004,116(7/8):989-1015
[55] Arvin M, Dargahi S, Babaei A A. Mafic microgranular enclave swarms in the Chenargranitoid stock, NW of Kerman, Iran:evidence for magma mingling[J].Journal of Asian EarthSciences.2004,24:105-113
[56] QIN J F, LAI S C, Grapes R, et al. Geochemical evidence for origin of magma mixing for theTriassic monzonitic graniteand its enclaves at Mishuling in the Qinling orogen(centralChina)[J].Lithos.2009,112:259-276
[57]张旗,王云龙,金惟俊等.造山前、造山和造山后花岗岩的识别[J].地质通报.2008,27(1):1-18
[58]李晶,陈衍景,李强之.甘肃阳山金矿碳氢氧同位素与成矿流体来源[J].岩石学报.2008,24(4):817-826
[59]毛景文,赫英,丁悌平.胶东金矿形成期间地幔流体参与成矿过程的碳氧氢同位素证据[J].矿床地质.2002,21(2):121-128
[60]毛景文,李厚民,王义天等.地幔流体参与胶乐金矿成矿作用的氢氧碳硫同位素证据[J].地质学报.2005,79(6):839-850
[61]刘丛强,黄智龙,李和平等.地幔流体及其成矿作用[J].地学前缘.2001,8(4):231-243
[62]卢焕章,J.Guha等.山东玲珑金矿的成矿流体特征[J]地球化学.1999,28(5):421-437
[63]卢焕章,袁万春,张国平等.玲珑—焦家地区主要金矿床稳定同位素及同位素年代学[J].桂林工学院学报.1999,19(1):1-8
[64]陕亮,郑有业,许荣科等.硫同位素示踪与热液成矿作用研究[J].地质与资源.2009,18(3):197-203
[65]汪在聪,刘建明,刘红涛等.稳定同位素热液来源示踪的复杂性和多解性评述——以造山型金矿为例[J].岩石矿物学杂志.2010,29(5):563-576
[66]侯明兰,蒋少涌,姜耀辉等.胶东蓬莱金成矿区的S-Pb同位素地球化学和Rb-Sr同位素年代学研究[J].岩石学报.2006,22(10):2525-2533
[67]林文蔚,赵一鸣,赵国红等.胶东金矿铅同位素地质特征及成矿年代讨论[J].长春科技大学学报.1999,29(2):116-121
[68]王义文.夹皮沟金矿床同位素地质学研究[J].地球科学(武汉地质学院学报).1984,4:25-36
[69]王力,孙丰月等.山东金岭金矿床成矿流体地球化学特征[J].岩石学报.2010,26(12):3735-3744
[70]马振东.论铅同位素的地质指示作用[J].地球科学(武汉地质学院学报).1988,11(4):437-443
[71]谭俊,魏俊浩,谭文娟等.同源岩浆成因金矿成岩成矿时差的统计研究[J].地质论评.2006,52(1):54-60
[72]谢荣举.暗色岩脉与成矿关系[J].现代地质.1997:130
[73]孙德有,吴福元,张艳斌等.西拉木伦河—长春—延吉板块缝合带的最后闭合时间——来自吉林大玉山花岗岩体的证据[J].吉林大学学院(地球科学版).2004,34(2):174-181
[74]罗镇宽,苗来成,关康等.中国大地构造演化与金矿成矿作用[J].1998,13(3):24-34
[75]李双林,欧阳自远.兴蒙造山带及邻区的构造格局与构造演化[J].海洋地质与第四纪地质.1998,18(3):45-54
[76]唐克东,王莹,何国琦等.中国东北及邻区大陆边缘构造[J].地质学报.1995,69(1):16-30
[77]隋振民.吉林省中生代花岗岩成因系列及其构造环境[J].吉林地质.1995,14(1):15-22
[78]赵振华.关于岩石微量元素构造环境判别图解使用的有关问题[J].大地构造与成矿学.2007,31(1):92-103
[79]张旗,潘国强,李承东等.花岗岩构造环境问题:关于花岗岩研究的思考之三[J].岩石学报.2007,23(11):683-698
[80]张旗,李承东,王焰等.中国东部中生代高Sr低Yb和低Sr高Yb型花岗岩对比及其地质意义[J].岩石学报.2005,21(06):1527-1537
[81] Pearce J A, Harris N B W, Tindle A G. Trace element discrimination diagrams for thetectonic interpretation of granitic rocks [J]. Petrology.1984,25(4):956-983
[82]肖庆辉,邢作云,张昱等.当代花岗岩研究的几个重要前沿[J].地学前缘(中国地质大学,北京).2003,10(3):221-229
[83]肖庆辉,邱瑞照,邓晋福等.中国花岗岩与大陆地壳生长方式初步研究[J].中国地质.2005,32(3):343-352
[84]肖庆辉,邓晋福,邱瑞照等.花岗岩类与大陆地壳生长初探——以中国典型造山带花岗岩类岩石的形成为例[J].中国地质.2009,36(3):594-622
[85] YANG J H, WU F Y, CHUNG S L, et al. Multiple sources for the origin of granites:Geochemical and Nd/Sr isotopic evidence from the Gudaoling granite and its mafic enclaves,northeast China [J].Geochimica et Cosmochimica Acta.2004,68(21):4469-4483.
[86] YANG J H, WU F Y, Wilde S A. A review of the geodynamic setting of large-scale LateMesozoic gold mineralization in the North China Craton: an association with lithosphericthinning[J]. Ore Geology Reviews.2003(23):125-152
[87] Barbarin, B.A review of the relationships between granitoid types, their origins and theirgeodynamic environments[J].Lithos.1999,46:605-626
[88]吴福元,孙德有,林强.东北地区显生宙花岗岩的成因与地壳演化[J].岩石学报.1999(15):181-189
[89]赵成弼,靳克,齐成栋等.珲春地区早印支期I-A型花岗岩系的特征及其大地构造意义[J].吉林地质.2001,20(1):1-11
[90]李莉,白云山,牛志军等.藏北羌塘中部劳日特错花岗斑岩体的特征及构造意义[J].地质通报.2004,23(9/10):40-45
[91] Barbarin, B. Granitoids: main petrogenetic classifications in relation to origin and tectonicsetting [J]. Geology.1990,25:227-238
[92] Barbarin, B. Genesis of the two main types of peraluminousgranitoids[J].Geology.1996,24(4):295-298
[93]孙忠实,邓军,翟裕生等.吉林钾长花岗岩构造背景及铀对大型金矿床的控制[J].地球学报.1999,20(2):460-465
[94]孙忠实,邓军,冯亚民等.吉林古陆成岩背景及边缘金构造—成矿系统[J].地质地球化学.2000,28(4):1-6
[95]隋振民.吉林省中生代花岗岩成因系列及其构造环境[J].吉林地质.1995,14(1):15-21
[96]徐公愉,方文昌.吉林省两类花岗岩及其形成的构造背景[J].矿物岩石地球化学通报.1990,1:1-3
[97]葛肖虹.吉林东部大地构造环境与构造演化轮廓[J].现代地质.1990,4(1):107-113
[98]陈殿芬,孙淑琼.吉林海沟金矿床石英的研究[J].矿物岩石.1991,11(1):4-8
[99]李永军,刘志武,付国民等.花岗岩类I型S型分类在造山带实践中存在的问题——以西秦岭地区为例[J].华南地质与矿产.2002,2:1-7
[100] Roberts M P, Clemens J D. Origin of high plassium, calc-alkaline, I-typegranitoids[J].Geology.1993,21:825-828
[101]瞿泓滢,裴荣富,李进文.安徽铜陵凤凰山石英二长闪长岩和花岗闪长岩锆石SHRIMPU-Pb年龄及其地质意义[J].吉林大学学报(地球科学版).2010,40(3):581-590
[102]李印,韩峰,凌明星.蚌埠荆山和涂山岩体的年代学、地球化学特征及其动力学意义[J].大地构造与成矿学.2010,34(1):114-124
[103]赵俊伟.青海东昆仑造山带造山型金矿床成矿系列研究[D].硕士学位论文.长春:吉林大学,2008
[104]李厚民,沈远超,胡正国等.青海东昆仑五龙沟金矿床成矿条件及成矿机理[J].地质与勘探.2011,37(1):65-69
[105]梁业恒,孙晓明,石贵勇等.云南哀牢山老王寨大型造山型金矿成矿流体地球化学[J].岩石学报.2011,27(9):2533-2540
[106]张作衡.西秦岭地区造山型金矿床成矿作用和成矿过程[D].博士学位论文.北京:中国地质科学院
[107]李强,王兵岐,马治国等.南秦岭凤太盆地金矿与铅锌矿的成矿模式[J].地球科学与环境学院.2007,29(1):15-21
[108]韦龙明.陕西八卦庙金矿成矿流体初步研究[J].岩石学报.2007,23(9):2257-2262
[109] WU F Y, SUN D Y, GE W C, et al. Geochronolygy of the Phanerozoic granitoids innortheastern China[J]. Journal of Asian Earth Sciences.2011,(41):1-30
[110] MAO J W, WANG Y T, LI H M, et al. The relationship of mantle-derived fluids to goldmetallogenesis in the Jiaodong Peninsula: Evidence from D-O-C-S isotope systematics[J].Ore Geology Reviews.2007:1-21.