黑龙江省团结沟金矿床成矿地质背景与成矿模式研究
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摘要
团结沟金矿床位于黑龙江省伊春市嘉荫县乌拉嘎镇境内,是东北地区主要的大型-超大型岩金矿床。本论文主要从成矿地质背景、矿床地质特征、流体包裹体、同位素特征、与成矿有关的地球化学特征、成矿环境讨论以及锆石U-Pb年龄等方面对团结沟金矿进行研究,从而总结出团结沟金矿的成矿规律和成矿模式。
团结沟金矿矿石的类型主要包括含金胶状玉髓状石英-黄铁矿型、碳酸盐-黄铁矿型、含金胶状-玉髓状石英-辉锑矿型和富硫化物型。该矿床的矿石结构类主要有胶状结构、镶嵌结构、细粒状结构、细晶质结构、包含结构。矿石构造以脉状、网脉状构造、角砾状构造最为发育。矿区围岩蚀变主要有黄铁绢英岩化、冰长石化、硅化、碳酸盐化、泥化等。
本次包裹体的均一温度主要集中在150~220℃。成矿流体的盐度主要集中在3.0-4.1wt%NaCl范围。成矿流体的密度范围为0.78~0.93g/ cm3。成矿压力为10.2~14.1MPa。含矿热液成分是岩浆水和大气降水混合源。成矿物质来源于岩浆岩,有少量生物硫的加入;花岗岩类岩浆不仅提供了成矿热液,也提供了部分的成矿物质。成矿作用发生在早白垩世晚期(106Ma),成矿发生在火山岩喷发、花岗斑岩浅成就位的晚期,建立了团结沟金矿的成矿模式。
结合火山岩和花岗斑岩的地质、地球化学特征和年代学研究,确立成矿环境与晚中生代太平洋板块俯冲作用密切相关。
Tuanjiegou gold deposit is located in wulaga town,Jiayin county,Heilongjiang province.It is in the east of wulaga basin,verge of Hegang border uplift and fault. The deep NNE trend fault devide the wulaga.Rift of Hegang and basin into two part.
The strata exposed in the region mainly include Proterozoic and Cenozoic.Intrusive rocks are exposed extensively and complexly.Intrusive rocks consists of acid intrusive rocks of Proterozoic, ultramafic rocks of Paleozoic, granitic intrusive rocks of Late Triassic, Late Triassic - Early Jurassic and early Cretaceous From old to new,the intrusion age are Luliang,Jinningian, Indo-China and Yanshanian period
Regional volcanism is well developed.They are mainly exposed in wulaga town - Willow River sub-area of the east of Wulaga basin,while a small amount of them exposed in Shangmaqihe on the west side of the basin.It can be divided into two periods: Ningyuan Village period and Fumin River period.Folds and faults are development in the region. Fold in Proterozoic metamorphic rocks formed for the deformed Maljan station, the center channel complex anticline and syncline between the complex, were en echelon arrangement, the overall inclined to back the North East - Southwest. Faults can be divided according to NNE, from east to west, north and south to breakage.
Tuanjiegou gold deposit has explored more than 80 ore bodies.and 6 main ore bodies. They are controlled by breccia belt in plagioclase granitic porphyry,and they are mainly distributed in it.Only a small number of them are associated with scattered and fragmented pieces lean ore rock between the fracture zones, alteration zones.
Primary types of gold ore include colloidal chalcedonic quartz - pyrite, carbonate - pyrite, gold jelly - chalcedony-like quartz - stibnite type and rich sulfide. Secondary ore is limonite type,and this type is contained in the oxidized zone. Ore minerals include are gold, pyrite, small amounts of stibnite, silver, sphalerite, mercury, galena, chalcopyrite, realgar, orpiment and jarosite. The secondary mineral is brown iron.Gangue minerals include chalcedony quartz, micro granular quartz ,comb quartz, calcite, colloidal opal, dolomite, feldspar, quartz, kaolin,and so on.
There are many types of ore structures, mainly include colloidal structure, mosaic structure, fine granular structure, fine crystalline structure,inclusion structure and droplet-like structure.The development of low temperature structure is an important feature of unity GOLD one.Ore textures mainly include vein, stockwork texture,and most developed brecciated texture, in addition to developing a disseminated texture, gel-like and crystal and other hole textures.Complex wall-rock alteration apperes in the area, mainly pyrite phyllic, ice Petro-Chemical, silicification, carbonate, clay and so on.Silicification is most closely with mineralization.
The temperature of fluid inclusions ranges from 150℃to 280℃. The main value is between 150℃and 220℃. The salinity ranges from 1.39~5.99 wt%NaCl, with the average 3.4wt%NaCl. The main salinity is between 3.0~4.1wt%NaCl. The value of density is between 0.78 and 0.93g/ cm3. The value of pressure ranges from 10.2~14.1MPa.
Thus determine that Tuanjiegou gold deposit has characteristics of low salinity , low temperature and low density. According to the Characteristics of laser Raman and Isotopic liquid. Major components of mineralizing fluid is water; S isotope studies show that Mineralization from granite; Pb isotope studies show Tuanjiegou magmatic plagioclase granite plaque not only provides the mineralizing fluid, also provided some of the forming materials.
Study on major elements shows the intrusive rocks of this area are all calc-alkaline granitic porphyry, while the volcanic lava and pyroclastic rocks are also shown the nature of calc-alkaline igneous rocks.The characteristics of the rare earth and trace elements suggest that the volcanic rocks and igneous rocks are the product of Comagmatic Evolution.
The zircons from granodiorite-porphyry give U-Pb ages of 119-100Ma, with a weighted mean value of 109.7±3.8Ma, shows that is the production of early Cretaceous magmatism. Its formation is closely related to the subduction of the Mesozoic Pacific plate towards the Asian continent, this caused the formation of acid magma, and intruded upward along NNE-NE deep faults passively, this belong to production of fault expansion or calderas in passive mechanism. The age of single grain zircon from dacite cuttings crystal tuff is 121-102Ma, with a weighted mean value of 108±2Ma. On the formation environment discrimination diagrams, the composition points of typical volcanic fall under the area of continental margin, this feature reflects the volcanic rocks of Ningyuan village period formed at continental margin environment.
Late Mesozoic Early Cretaceous, the subduction of the Mesozoic Pacific plate towards the Asian plate formed the NNE-NE trending Wulaga deep fault. Under the continental margin environment, series of calc-alkaline volcanic lava and pyroclastic rocks magma, which was caused by partial melting of the basement, migrated upward along Wulaga deep fault, and emitted surface, as the pressure in magma chamber reduced continuously, the magma was unable to erupt to the surface, and crystallized rapidly in shallow crust, thus formed the shallow plagioclase-granite porphyry, granodiorite porphyry and granite porphyry intrusions, which output as stocks. The sub-volcanic hydrothermal caused by differentiation in magma chamber migrated upward along Wulaga deep fault, while extracted the minerals of plagioclase granite porphyry, granodiorite porphyry, granite-porphyry intrusions and the old base rocks, was gradually enriched to form the ore-bearing hydrothermal, meanwhile mixed meteoric water. The formation of the gold deposit underwent mainly two main stage: one stage is brecciated gold mineralization period, which outputs in the tectonic breccia zone. Another stage is the vein, stockwork gold mineralization, the enrichment and precipitation happen at the NW-NWW trending secondary fault of the NNE-NE trending Wulaga deep fault.Thus form this typical low sulphidation epithermal gold deposit.
团结沟金矿矿石的类型主要包括含金胶状玉髓状石英-黄铁矿型、碳酸盐-黄铁矿型、含金胶状-玉髓状石英-辉锑矿型和富硫化物型。该矿床的矿石结构类主要有胶状结构、镶嵌结构、细粒状结构、细晶质结构、包含结构。矿石构造以脉状、网脉状构造、角砾状构造最为发育。矿区围岩蚀变主要有黄铁绢英岩化、冰长石化、硅化、碳酸盐化、泥化等。
本次包裹体的均一温度主要集中在150~220℃。成矿流体的盐度主要集中在3.0-4.1wt%NaCl范围。成矿流体的密度范围为0.78~0.93g/ cm3。成矿压力为10.2~14.1MPa。含矿热液成分是岩浆水和大气降水混合源。成矿物质来源于岩浆岩,有少量生物硫的加入;花岗岩类岩浆不仅提供了成矿热液,也提供了部分的成矿物质。成矿作用发生在早白垩世晚期(106Ma),成矿发生在火山岩喷发、花岗斑岩浅成就位的晚期,建立了团结沟金矿的成矿模式。
结合火山岩和花岗斑岩的地质、地球化学特征和年代学研究,确立成矿环境与晚中生代太平洋板块俯冲作用密切相关。
Tuanjiegou gold deposit is located in wulaga town,Jiayin county,Heilongjiang province.It is in the east of wulaga basin,verge of Hegang border uplift and fault. The deep NNE trend fault devide the wulaga.Rift of Hegang and basin into two part.
The strata exposed in the region mainly include Proterozoic and Cenozoic.Intrusive rocks are exposed extensively and complexly.Intrusive rocks consists of acid intrusive rocks of Proterozoic, ultramafic rocks of Paleozoic, granitic intrusive rocks of Late Triassic, Late Triassic - Early Jurassic and early Cretaceous From old to new,the intrusion age are Luliang,Jinningian, Indo-China and Yanshanian period
Regional volcanism is well developed.They are mainly exposed in wulaga town - Willow River sub-area of the east of Wulaga basin,while a small amount of them exposed in Shangmaqihe on the west side of the basin.It can be divided into two periods: Ningyuan Village period and Fumin River period.Folds and faults are development in the region. Fold in Proterozoic metamorphic rocks formed for the deformed Maljan station, the center channel complex anticline and syncline between the complex, were en echelon arrangement, the overall inclined to back the North East - Southwest. Faults can be divided according to NNE, from east to west, north and south to breakage.
Tuanjiegou gold deposit has explored more than 80 ore bodies.and 6 main ore bodies. They are controlled by breccia belt in plagioclase granitic porphyry,and they are mainly distributed in it.Only a small number of them are associated with scattered and fragmented pieces lean ore rock between the fracture zones, alteration zones.
Primary types of gold ore include colloidal chalcedonic quartz - pyrite, carbonate - pyrite, gold jelly - chalcedony-like quartz - stibnite type and rich sulfide. Secondary ore is limonite type,and this type is contained in the oxidized zone. Ore minerals include are gold, pyrite, small amounts of stibnite, silver, sphalerite, mercury, galena, chalcopyrite, realgar, orpiment and jarosite. The secondary mineral is brown iron.Gangue minerals include chalcedony quartz, micro granular quartz ,comb quartz, calcite, colloidal opal, dolomite, feldspar, quartz, kaolin,and so on.
There are many types of ore structures, mainly include colloidal structure, mosaic structure, fine granular structure, fine crystalline structure,inclusion structure and droplet-like structure.The development of low temperature structure is an important feature of unity GOLD one.Ore textures mainly include vein, stockwork texture,and most developed brecciated texture, in addition to developing a disseminated texture, gel-like and crystal and other hole textures.Complex wall-rock alteration apperes in the area, mainly pyrite phyllic, ice Petro-Chemical, silicification, carbonate, clay and so on.Silicification is most closely with mineralization.
The temperature of fluid inclusions ranges from 150℃to 280℃. The main value is between 150℃and 220℃. The salinity ranges from 1.39~5.99 wt%NaCl, with the average 3.4wt%NaCl. The main salinity is between 3.0~4.1wt%NaCl. The value of density is between 0.78 and 0.93g/ cm3. The value of pressure ranges from 10.2~14.1MPa.
Thus determine that Tuanjiegou gold deposit has characteristics of low salinity , low temperature and low density. According to the Characteristics of laser Raman and Isotopic liquid. Major components of mineralizing fluid is water; S isotope studies show that Mineralization from granite; Pb isotope studies show Tuanjiegou magmatic plagioclase granite plaque not only provides the mineralizing fluid, also provided some of the forming materials.
Study on major elements shows the intrusive rocks of this area are all calc-alkaline granitic porphyry, while the volcanic lava and pyroclastic rocks are also shown the nature of calc-alkaline igneous rocks.The characteristics of the rare earth and trace elements suggest that the volcanic rocks and igneous rocks are the product of Comagmatic Evolution.
The zircons from granodiorite-porphyry give U-Pb ages of 119-100Ma, with a weighted mean value of 109.7±3.8Ma, shows that is the production of early Cretaceous magmatism. Its formation is closely related to the subduction of the Mesozoic Pacific plate towards the Asian continent, this caused the formation of acid magma, and intruded upward along NNE-NE deep faults passively, this belong to production of fault expansion or calderas in passive mechanism. The age of single grain zircon from dacite cuttings crystal tuff is 121-102Ma, with a weighted mean value of 108±2Ma. On the formation environment discrimination diagrams, the composition points of typical volcanic fall under the area of continental margin, this feature reflects the volcanic rocks of Ningyuan village period formed at continental margin environment.
Late Mesozoic Early Cretaceous, the subduction of the Mesozoic Pacific plate towards the Asian plate formed the NNE-NE trending Wulaga deep fault. Under the continental margin environment, series of calc-alkaline volcanic lava and pyroclastic rocks magma, which was caused by partial melting of the basement, migrated upward along Wulaga deep fault, and emitted surface, as the pressure in magma chamber reduced continuously, the magma was unable to erupt to the surface, and crystallized rapidly in shallow crust, thus formed the shallow plagioclase-granite porphyry, granodiorite porphyry and granite porphyry intrusions, which output as stocks. The sub-volcanic hydrothermal caused by differentiation in magma chamber migrated upward along Wulaga deep fault, while extracted the minerals of plagioclase granite porphyry, granodiorite porphyry, granite-porphyry intrusions and the old base rocks, was gradually enriched to form the ore-bearing hydrothermal, meanwhile mixed meteoric water. The formation of the gold deposit underwent mainly two main stage: one stage is brecciated gold mineralization period, which outputs in the tectonic breccia zone. Another stage is the vein, stockwork gold mineralization, the enrichment and precipitation happen at the NW-NWW trending secondary fault of the NNE-NE trending Wulaga deep fault.Thus form this typical low sulphidation epithermal gold deposit.
引文
[1] Anderson M R.Fluid mixing in the generation of Mesothermal gold mineralization in the Transval Sequence[M]. Transval,Souh Africa. Eur J. Mineral.1992.(4): 993- 948.
[2] BergerB R, Henley RW. A davances in the understanding of ep ithermal gold-silver deposits, with special reference to theWestern United States [J ]. Econ. Geo l. , 1989, Monograph 6,405-423.
[3] CrawfordM L .Fluid inclusion--what can we learn? Earth Science Reviews, 1992, (32) : 137-139.
[4] Groves D I.A rchean lode gold deposits. In: Foster R, ed. Gold Metallogeny and Exploration. 1991.63- 103.
[5] Heald P, Foley N K, Hayba D O. Comparative anatomy of volcanic-hosted epithermal deposits: acid-sulfate and adularia-sericite types [J].Economic Geology , 1987, 82 (2) :1-26
[6] Hedenquist J W, et al.The role of magmas in the formation of hydrotherm al ore deposits[J].Nature,1994, 370(18).
[7] Kesler S E. Nature and composition of mineralizing solutons. In: Robert F, et al1ed1Greenstone Gold and Crustal Evou2tion. 1990.86-90.
[8] Nesbitt BE, Murowchich J B, Muehlenbacks K, Dual origin of lode gold deposits in the Canadian Co rdillera.Geology,1986, (14) : 506-509.
[9] Sillitoe R H, et a1.High sulfidation deposit in the volcanogenic massive sulfide environment [J].Economic Geology,1996, 91(2):2O4-212.
[10] Scoot A M, Watanabe Y.“Extreme boiling model for variable salinity of the Hokko low-sulfidation epithermal Au prospect , south-western Hokkaido , Japan[J ] . Mineralium Deposita , 1998 , 33(6):568-578.
[11] Takahiro Hosono, Takanori Nakano. Pb–Sr isotopic evidence for contribution of deep crustal fluid to the Hishikari epithermal gold deposit, southwestern Japan [J]. Earth and Planetary Science,2004,222 (2004) 61– 69.
[12] White N C, Hendenquist J W. Epithermal environment and styles of mineralization: variations and their causes and guide-lines for exploration [J]. Journal of Geochemical Exploration.1990, 36(3): 445- 474.
[13] White N C,Leake S N,McCaughey,Parris B W.Epithermal gold deposits of the southwest Pacific[J].Journal of Geochemical Exploration,1995,54:87-136
[14]胡朋,赫英,张义,等.浅成低温热液金矿床研究进展[J].黄金地质,2004, 10(1):48-54.
[15]池国祥,周义明,卢焕章.当前流体包裹体研究和应用概况[J].岩石学报,2003,19(2):201-212.
[16]邓军,高帮飞,王庆飞等.成矿流体系统的形成与演化[J].地质科技情报,2005,24(1):49-54.
[17]范宏瑞,谢奕汉,王英兰.流体包裹体与金矿床的成矿及勘探评价[J].地质与资源,1997,6(3):204-213.
[18]费红彩,肖荣阁.成矿流体演化与成矿物理化学[J].矿物岩石地球化学通报,2002,21(2):139-144.
[19]丰成友.火山岩区浅成低温热液金矿床研究进展[J].地学工程进展,1998,15(1):10-15.
[20]张德全,李大新,赵一鸣,等.福建紫金山矿床-我国大陆首例石英-明矾石型浅成低温热液铜-金矿床[J].地质论评,1991, 37(6):481-491.
[21]张德会,刘伟.流体包裹体成分与成矿流体来源[J].地质科技情报,1998,17:67-71.
[22]应汉龙.浅成低温热液金矿床的全球背景[J].贵金属地质,1999,12:241-248.
[23]林宝钦.中国东部冰长石-绢云母型低温浅成热液金矿[J].贵金属地质,1992,1(4):199~206.
[24] .沙德铭,苑丽华.浅成低温热液型金矿特点、分布和找矿前景[J].地质与资源,2003,6:115-122.
[25]毋瑞身.低温浅成热液金矿若干问题探讨[J]贵金属地质,1993,2(1):47~53.
[26]李之彤.我国东部中(新)生代火山热液型金矿地质特征[A].见金矿地质论文集[C]北京:地质出版社.1982.
[27]陈满,聂朝晖,王献忠,等.上黑龙江断陷火山岩特征及岩金找矿方向[J].黄金地质,2002,8(4):37-42.
[28]曹圣恩.黑龙江省金矿地质特征及找矿方向[J].黄金地质科技,1994,39(1):31-35.
[29]孙凤兴,吴国学,杨鹏.团结沟金矿床地质模型[J].吉林地质,1996,15(2):52-60.
[30]武警黄金指挥部.黑龙江省团结沟斑岩金矿地质[M].北京:地震出版社,1995,134.
[31]姜泽阳,王晓勇,梁海军,等.吉东火山岩型金矿地质特征及流体包裹体研究[J].黄金地质,2002,8(2):26-30.
[32]姚凤良,孙丰月.矿床学教程[M].北京:地质出版社,2006.
[33]吴国学.团结沟金矿床综合找矿标志研究[J].长春地质学院学报,1994,24(4):397-403.
[34]吴尚全.团结沟斑岩金矿床多源成因的同位素地质学证据[J].地质与勘探,1984,20(2):28-31.
[35]吴尚全.团结沟斑岩金矿床自然金的成因矿物学研究[J].地质论评,1984,30(1):42-48.
[36]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].岩石学报,2007,23(9):2085-2108.
[37]杨天奇,魏仪方,何高文.中国陆相火山岩区特大型金矿床模型[M].北京:冶金工业出版社,1994.
[38]魏仪方,刘春华.团结沟金矿床地质地球化学模型[J].黄金,1996,17(2):3-11.
[39]魏菊英,王关玉等.同位素地球化学[M].地质出版社,1988.
[40]孟宪伟.团结沟金矿床的地球化学找矿模型[J].地质与勘探,1994,3:63-66.
[41]李碧乐,王健.黑龙江团结沟金矿区花岗斑岩体与金矿化的关系[J].黄金,1998,19(3):3-6.
[42]李凤友.乌拉嘎金矿床找矿模型及其应用[J].黄金,2001,22(6):11-13.
[43]孙丰月.王力.豁亮,等.黑龙江乌拉嘎大型金矿床流体包裹体特征及矿床成因研究[J].中国地质,2008,12:1267-1272.
[44]王永祥,吴国学,白士俊,等.乌拉嘎金矿床地质地球化学特征研究[J].世界地质,2005,24(4):338-343.
[45]张文淮,陈紫英.流体包裹体地质学[M].武汉:中国地质大学出版社,1993:1-246.
[2] BergerB R, Henley RW. A davances in the understanding of ep ithermal gold-silver deposits, with special reference to theWestern United States [J ]. Econ. Geo l. , 1989, Monograph 6,405-423.
[3] CrawfordM L .Fluid inclusion--what can we learn? Earth Science Reviews, 1992, (32) : 137-139.
[4] Groves D I.A rchean lode gold deposits. In: Foster R, ed. Gold Metallogeny and Exploration. 1991.63- 103.
[5] Heald P, Foley N K, Hayba D O. Comparative anatomy of volcanic-hosted epithermal deposits: acid-sulfate and adularia-sericite types [J].Economic Geology , 1987, 82 (2) :1-26
[6] Hedenquist J W, et al.The role of magmas in the formation of hydrotherm al ore deposits[J].Nature,1994, 370(18).
[7] Kesler S E. Nature and composition of mineralizing solutons. In: Robert F, et al1ed1Greenstone Gold and Crustal Evou2tion. 1990.86-90.
[8] Nesbitt BE, Murowchich J B, Muehlenbacks K, Dual origin of lode gold deposits in the Canadian Co rdillera.Geology,1986, (14) : 506-509.
[9] Sillitoe R H, et a1.High sulfidation deposit in the volcanogenic massive sulfide environment [J].Economic Geology,1996, 91(2):2O4-212.
[10] Scoot A M, Watanabe Y.“Extreme boiling model for variable salinity of the Hokko low-sulfidation epithermal Au prospect , south-western Hokkaido , Japan[J ] . Mineralium Deposita , 1998 , 33(6):568-578.
[11] Takahiro Hosono, Takanori Nakano. Pb–Sr isotopic evidence for contribution of deep crustal fluid to the Hishikari epithermal gold deposit, southwestern Japan [J]. Earth and Planetary Science,2004,222 (2004) 61– 69.
[12] White N C, Hendenquist J W. Epithermal environment and styles of mineralization: variations and their causes and guide-lines for exploration [J]. Journal of Geochemical Exploration.1990, 36(3): 445- 474.
[13] White N C,Leake S N,McCaughey,Parris B W.Epithermal gold deposits of the southwest Pacific[J].Journal of Geochemical Exploration,1995,54:87-136
[14]胡朋,赫英,张义,等.浅成低温热液金矿床研究进展[J].黄金地质,2004, 10(1):48-54.
[15]池国祥,周义明,卢焕章.当前流体包裹体研究和应用概况[J].岩石学报,2003,19(2):201-212.
[16]邓军,高帮飞,王庆飞等.成矿流体系统的形成与演化[J].地质科技情报,2005,24(1):49-54.
[17]范宏瑞,谢奕汉,王英兰.流体包裹体与金矿床的成矿及勘探评价[J].地质与资源,1997,6(3):204-213.
[18]费红彩,肖荣阁.成矿流体演化与成矿物理化学[J].矿物岩石地球化学通报,2002,21(2):139-144.
[19]丰成友.火山岩区浅成低温热液金矿床研究进展[J].地学工程进展,1998,15(1):10-15.
[20]张德全,李大新,赵一鸣,等.福建紫金山矿床-我国大陆首例石英-明矾石型浅成低温热液铜-金矿床[J].地质论评,1991, 37(6):481-491.
[21]张德会,刘伟.流体包裹体成分与成矿流体来源[J].地质科技情报,1998,17:67-71.
[22]应汉龙.浅成低温热液金矿床的全球背景[J].贵金属地质,1999,12:241-248.
[23]林宝钦.中国东部冰长石-绢云母型低温浅成热液金矿[J].贵金属地质,1992,1(4):199~206.
[24] .沙德铭,苑丽华.浅成低温热液型金矿特点、分布和找矿前景[J].地质与资源,2003,6:115-122.
[25]毋瑞身.低温浅成热液金矿若干问题探讨[J]贵金属地质,1993,2(1):47~53.
[26]李之彤.我国东部中(新)生代火山热液型金矿地质特征[A].见金矿地质论文集[C]北京:地质出版社.1982.
[27]陈满,聂朝晖,王献忠,等.上黑龙江断陷火山岩特征及岩金找矿方向[J].黄金地质,2002,8(4):37-42.
[28]曹圣恩.黑龙江省金矿地质特征及找矿方向[J].黄金地质科技,1994,39(1):31-35.
[29]孙凤兴,吴国学,杨鹏.团结沟金矿床地质模型[J].吉林地质,1996,15(2):52-60.
[30]武警黄金指挥部.黑龙江省团结沟斑岩金矿地质[M].北京:地震出版社,1995,134.
[31]姜泽阳,王晓勇,梁海军,等.吉东火山岩型金矿地质特征及流体包裹体研究[J].黄金地质,2002,8(2):26-30.
[32]姚凤良,孙丰月.矿床学教程[M].北京:地质出版社,2006.
[33]吴国学.团结沟金矿床综合找矿标志研究[J].长春地质学院学报,1994,24(4):397-403.
[34]吴尚全.团结沟斑岩金矿床多源成因的同位素地质学证据[J].地质与勘探,1984,20(2):28-31.
[35]吴尚全.团结沟斑岩金矿床自然金的成因矿物学研究[J].地质论评,1984,30(1):42-48.
[36]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].岩石学报,2007,23(9):2085-2108.
[37]杨天奇,魏仪方,何高文.中国陆相火山岩区特大型金矿床模型[M].北京:冶金工业出版社,1994.
[38]魏仪方,刘春华.团结沟金矿床地质地球化学模型[J].黄金,1996,17(2):3-11.
[39]魏菊英,王关玉等.同位素地球化学[M].地质出版社,1988.
[40]孟宪伟.团结沟金矿床的地球化学找矿模型[J].地质与勘探,1994,3:63-66.
[41]李碧乐,王健.黑龙江团结沟金矿区花岗斑岩体与金矿化的关系[J].黄金,1998,19(3):3-6.
[42]李凤友.乌拉嘎金矿床找矿模型及其应用[J].黄金,2001,22(6):11-13.
[43]孙丰月.王力.豁亮,等.黑龙江乌拉嘎大型金矿床流体包裹体特征及矿床成因研究[J].中国地质,2008,12:1267-1272.
[44]王永祥,吴国学,白士俊,等.乌拉嘎金矿床地质地球化学特征研究[J].世界地质,2005,24(4):338-343.
[45]张文淮,陈紫英.流体包裹体地质学[M].武汉:中国地质大学出版社,1993:1-246.