红旗岭地区构造特征及对铜镍硫化物矿床的控制意义
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摘要
吉林红旗岭矿区是我国典型的岩浆铜镍硫化物矿床。呈北东向展布的辉发河断裂是矿区的主要导矿构造,北西向的断裂构造控制着该区镁铁-超镁铁质岩体分布。矿区内发育30多个镁铁-超镁铁质岩体,其中形成于印支期的1号和7号岩体中的铜镍硫化物矿体构成大、中型矿床。与国内其它矿床一样,这些矿床空间上受大地构造条件的制约性非常明显。本文以矿田构造为研究内容,着重对1号和7号控岩控矿构造特征、性质、成因、规模及对岩体的控制作用进行深入研究,为矿区与外围进一步的找矿工作提供理论支持。
Magmatic sulfide deposits is the main source of nickel production in the world today. As this kind of ore deposit besides produces the nickel, but also coexists with the copper, the cobalt, the platinum race, the gold and so on metals. So people pay attention to them because of the enormous economic value.
Cu-Ni sulphide deposits of our country are in large quantity and in small scale.Most of them are hosted in the belt area or in Orogenic Belt of different times and spatial distribution of the transitional zone. (Tang Zhong li, 1996).
Hongqiling and other deposits-Piaohaichuan,Changren and Zhangxiang of Jilin Province are with the similar geological back-ground,so they areConsidered to be the thing that has serial copper nickel sulphide mineral deposit of the same cause under the same structure environment (Chen Zi cheng,1984; Fu-yuan W u et al ,2004).
Hongqiling area is located in the flanking of the Hufahe Fracture Zone.In this area ,there are more than 30 basic ultrabasic rocks. These rocks were emplaced in the NW structure of the sub-Huifahe fracture,and their diagenesis and mineralization were strictly controlled by stuctural structures, therefore, the research of the environment and the construction of the diagenesis and mineralization has to be of significance.
At present,the research of geological characteristics, metallogenic model, mineral geochemical characteristics and genesis of the deposits of nickel sulphide deposit in Hongqiling is more detailed, but the research about diagenesis and mineralization structure of the main rocks is relatively less.
During master,I was privileged to participate in the project,which is responsible by Hao libo pro and Lu Jilong pro,that taking over resource prospecting of national crisis mine- The metallogenic regularity conclusion of Jilin Hongqiling nickel deposit.I carried out a large amount of field observations and laboratory consolidation studies about metall -ogenic geological background,regional structural feature diagenesis and mineralization structure of the typical rocks of Hongqiling Cu-Ni sulphide mineral deposit,so I have accumulated the abundant basic materials.
This paper studies the formation age and mechanism of Hongqiling mining area based on the field observations of structural characteristics, petrography with mic -roscope and microstructure studies,and combined with previous structure,and furtherly studies their control significance to Cu-Ni sulfide deposit.
Main faults in this area is the EW, NW, NE, SN direction. According to gravity anomaly and the distribution of to the anomalous relationship of the mining area ,it can be determined that faults from early to late is EW,NW,NE→SN. Huifa River deep fault is the NE direction, with the characteristics of many repeated activities. In addition, there are some late faults with the formation of parallel NE trending,and they have a destructive effect on the rock and the ore body. The main control structure of rocks and deposit is the NW trending faults.Field observations show that the direction of the fault are mostly pressure-shear, and they also show a tensional features in a certain period.Such as F1 which controlsⅠr ock belt overally shows Compression and Torsion,but it shows both Compression and Torsion and tensional characteristics . In the vicinity of NO.7rock mass.It can be seen from 1:10 000 gravity anomaly level 90°of derivative map of the Hong qiling that SN trending faults are generally shorter, and is the tensional fault, so the principal compressive stress is north-south.X joints are well developed In the region, and their strike mainly is 40°-50°, 310°-320°.The area mainly was squeezed by north-south compression when X joints formated.Field observations show that the joints is not affected by later tectonic transformation,and they have no penetration of dike. So,we judge that SN faults and X joints formed in the same period.
Ore-bearing rocks mainly distribute inⅠrock belt and they are contonrolled by F1 fault. F1 fault has multiple repeated activities.The early activity was the sinistral piezotropy; When Ore-bearing magma invades the position,it was dextral tensional; However ,it transfered the sinistral movement in the later period.
From the plane distribution ofⅠrock belt ,from northwest (NO.2→NO.1→NO.3→NO.9→NO.7 rock mass) to the southeast ,the rock mass have the echelon distri-bution roughly, and they are belt-shaped,the arteries shape,and they distributes approximately in the identical fault zone.they have the characteristic of pinch-out reappearance. The compression and torsion fault which contonroled this rock belt showed waving characteristic in the forming initial period, and the two walls of fault had the horizontal direction dislocation in the later period .It formed a series of arteries shape, belt-shaped, the bean pod shape space, and it provided the place for the upper mantle mafic-ultramafic magma .
According to mirror under microstructures, EBSD quartz fabric chart and heavy magnetism unusual distribution map, and unifies predecessor's material and the geostructure background, I think that the structure evolution activity divided into four issues at least in this area. late caledonian, it formed north west control structure of rocks and deposit under areal structure stress field function;.at the same time ,Huifa River had intensifies moving and the cutting depth further enlarged, so the curtain magma frommantle taking the opportunity invaded and emplaced in the faults of NWⅡrock belt. Late hercynian- early indo-chinese, it had the medium degree deterioration distortion function and formed the Hulan group deterioration rock series in this area under the northern east 50°near horizontal direction's extrusion.Late Indo-Chinese, Huifa River had a large-scale left strike-slip movement and had traction function to enable it to have tensional wrench characteristic to a certain extent. It provided the space for rochs ofⅠrock belt. Early cretaceous-tertiary, the whole area was in an extensional environment and Huifa River had intensifies moving once again .NW faults had a sinistral movement, and the magma from mantle invaded once more at the same time formedⅢbelt rock masses.
In summary, each belt rock mass's formation had the extremely close relationship with the Huifa River deep fault and the activity in Hongqiling.
Magmatic sulfide deposits is the main source of nickel production in the world today. As this kind of ore deposit besides produces the nickel, but also coexists with the copper, the cobalt, the platinum race, the gold and so on metals. So people pay attention to them because of the enormous economic value.
Cu-Ni sulphide deposits of our country are in large quantity and in small scale.Most of them are hosted in the belt area or in Orogenic Belt of different times and spatial distribution of the transitional zone. (Tang Zhong li, 1996).
Hongqiling and other deposits-Piaohaichuan,Changren and Zhangxiang of Jilin Province are with the similar geological back-ground,so they areConsidered to be the thing that has serial copper nickel sulphide mineral deposit of the same cause under the same structure environment (Chen Zi cheng,1984; Fu-yuan W u et al ,2004).
Hongqiling area is located in the flanking of the Hufahe Fracture Zone.In this area ,there are more than 30 basic ultrabasic rocks. These rocks were emplaced in the NW structure of the sub-Huifahe fracture,and their diagenesis and mineralization were strictly controlled by stuctural structures, therefore, the research of the environment and the construction of the diagenesis and mineralization has to be of significance.
At present,the research of geological characteristics, metallogenic model, mineral geochemical characteristics and genesis of the deposits of nickel sulphide deposit in Hongqiling is more detailed, but the research about diagenesis and mineralization structure of the main rocks is relatively less.
During master,I was privileged to participate in the project,which is responsible by Hao libo pro and Lu Jilong pro,that taking over resource prospecting of national crisis mine- The metallogenic regularity conclusion of Jilin Hongqiling nickel deposit.I carried out a large amount of field observations and laboratory consolidation studies about metall -ogenic geological background,regional structural feature diagenesis and mineralization structure of the typical rocks of Hongqiling Cu-Ni sulphide mineral deposit,so I have accumulated the abundant basic materials.
This paper studies the formation age and mechanism of Hongqiling mining area based on the field observations of structural characteristics, petrography with mic -roscope and microstructure studies,and combined with previous structure,and furtherly studies their control significance to Cu-Ni sulfide deposit.
Main faults in this area is the EW, NW, NE, SN direction. According to gravity anomaly and the distribution of to the anomalous relationship of the mining area ,it can be determined that faults from early to late is EW,NW,NE→SN. Huifa River deep fault is the NE direction, with the characteristics of many repeated activities. In addition, there are some late faults with the formation of parallel NE trending,and they have a destructive effect on the rock and the ore body. The main control structure of rocks and deposit is the NW trending faults.Field observations show that the direction of the fault are mostly pressure-shear, and they also show a tensional features in a certain period.Such as F1 which controlsⅠr ock belt overally shows Compression and Torsion,but it shows both Compression and Torsion and tensional characteristics . In the vicinity of NO.7rock mass.It can be seen from 1:10 000 gravity anomaly level 90°of derivative map of the Hong qiling that SN trending faults are generally shorter, and is the tensional fault, so the principal compressive stress is north-south.X joints are well developed In the region, and their strike mainly is 40°-50°, 310°-320°.The area mainly was squeezed by north-south compression when X joints formated.Field observations show that the joints is not affected by later tectonic transformation,and they have no penetration of dike. So,we judge that SN faults and X joints formed in the same period.
Ore-bearing rocks mainly distribute inⅠrock belt and they are contonrolled by F1 fault. F1 fault has multiple repeated activities.The early activity was the sinistral piezotropy; When Ore-bearing magma invades the position,it was dextral tensional; However ,it transfered the sinistral movement in the later period.
From the plane distribution ofⅠrock belt ,from northwest (NO.2→NO.1→NO.3→NO.9→NO.7 rock mass) to the southeast ,the rock mass have the echelon distri-bution roughly, and they are belt-shaped,the arteries shape,and they distributes approximately in the identical fault zone.they have the characteristic of pinch-out reappearance. The compression and torsion fault which contonroled this rock belt showed waving characteristic in the forming initial period, and the two walls of fault had the horizontal direction dislocation in the later period .It formed a series of arteries shape, belt-shaped, the bean pod shape space, and it provided the place for the upper mantle mafic-ultramafic magma .
According to mirror under microstructures, EBSD quartz fabric chart and heavy magnetism unusual distribution map, and unifies predecessor's material and the geostructure background, I think that the structure evolution activity divided into four issues at least in this area. late caledonian, it formed north west control structure of rocks and deposit under areal structure stress field function;.at the same time ,Huifa River had intensifies moving and the cutting depth further enlarged, so the curtain magma frommantle taking the opportunity invaded and emplaced in the faults of NWⅡrock belt. Late hercynian- early indo-chinese, it had the medium degree deterioration distortion function and formed the Hulan group deterioration rock series in this area under the northern east 50°near horizontal direction's extrusion.Late Indo-Chinese, Huifa River had a large-scale left strike-slip movement and had traction function to enable it to have tensional wrench characteristic to a certain extent. It provided the space for rochs ofⅠrock belt. Early cretaceous-tertiary, the whole area was in an extensional environment and Huifa River had intensifies moving once again .NW faults had a sinistral movement, and the magma from mantle invaded once more at the same time formedⅢbelt rock masses.
In summary, each belt rock mass's formation had the extremely close relationship with the Huifa River deep fault and the activity in Hongqiling.
引文
[1]贾大成,卢焱等.对辉发河断裂带构造运动的再认识[J].吉林地质,1991.9(3):36-41.
[2]秦宽.红旗岭地区硫化铜镍矿床地质特征[J].吉林地质,1995.9(3):18-29.
[3]杨言辰,孙德有等.红旗岭镁铁—超镁铁岩侵入体及铜镍硫化物矿床的成岩成矿机制[J].吉林大学报:地球科学版,2005.
[4]蒋图治.林省红旗岭地区古地热场地质特征及对基性岩侵入体前缘石墨化带地质意义的探讨[J].地构造学与成矿,1992:148-149.
[5]张广良,吴福元等.林红旗岭镁铁—超镁铁岩地球化学特征及构造动力学意义[J].科技大学学报,2001.
[6]唐文龙,杨言辰等.吉林红旗岭镁铁—超镁铁质岩的地球化学特征及地质意义[J].世界地质,2007.6(2):165-170.
[7]王好均.显微构造及构造岩的研究与应用[J].长春工程学院学报,2002.
[8]汤中立.中国主要镍矿类型及其与古板块构造的关系[J].矿床地质,1983.
[9]曹淑云,刘俊来等.岩石显微构造分析现代技术—EBSD技术及应用[J].地球科学进展,2006.10.
[10]郗爱华,顾连兴等.中国北方造山带岩浆铜镍硫化物矿床及地球动力学背景[J].地质学报,2006.11(11):1721-1727.
[11]李述靖,张维杰等.古弧地质构造特征及形成演化概论[M].北京:地质出版社,1998.
[12]张岳桥,董树文等.郯庐断裂带中生代构造演化史:进展与新认识[J].地质通报,2008.9(9):1372-1387.
[13]任纪顺,牛宝贵等.碰撞、叠覆造山和多旋回缝合作用[J].地学前缘,1999,3期:85-93.
[14]池永一.中呼兰镇地区呼兰群的划分及时代[J].地球科学,1997(2):205-214.
[15]林强.中国东北地区中生代火山岩的大地构造意义[J].地质科学,1998
[16]向必伟,朱广等.棱岩化过程中矿物变形温度计[J].地球科学进展,2007.2(2):126-133.
[17]徐海军,金淑燕等.岩石组构学研究的最新技术—电子背散射衍射(EBSD)[J].现代地质,2007.6.
[18]吴小奇,刘德良等.确定变形温度和应变速率分形法的探讨—以郯庐断裂浮槎山构造岩为例[J].中国地质,2006.2.
[19]吕素林,毛景文等.华北克拉通北缘岩浆Ni—Cu(PGE)硫化物矿床地质特征、形成时代及其地球动力学背景[J].地球学报,2007.4.
[20]路孝平,吴福元等.吉林南部通化地区古元古代辽吉花岗岩的侵位年代与形成构造背景[J].岩石学报,2004
[21]郗爱华,顾连兴等.吉林省红旗岭铜镍硫化物矿床的成矿时代讨论[J].矿床地质,2005.
[22]郗爱华,葛玉辉等.中亚蒙古造山带东段造山事件的40Ar-39Ar同位素年代学证据[J].中国地质,2006
[23]吴香尧著,岩组学导论[M].重庆出版社,1984
[24]孙德有,吴福元等.吉林中部晚三叠世和早侏罗世两期铝质A型花岗岩的厘定及对吉黑东部构造格局的制约[J].地学前沿,2005.4
[25]彭玉鲸,赵成弼等.古吉黑造山带的演化与陆壳的增生.吉林地质2001
[26]翟安民,沈保丰等.吉辽古裂谷地质演化与成矿[J].地质调查与研究,2005
[27]胡玲.显微构造地质学概论「M」.北京地质出版社,1998
[28]郑亚东,常志忠主编.岩石有限应变测量及韧性剪切带「M」.北京:地质出版社,1985
[29]王宇明.丹东韧性剪切带内岩石的有限应变测量及其地质找矿意义[J].地质找矿丛书,1991
[30]程裕淇主编.中国区域地质概论[M].北京地质出版社,1994
[31]孙德有,吴福元等.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] .吉林大学学报(地球科学版),2004
[32]颉颃强张福勤等.吉林中部漂河川镁铁—超镁铁质杂岩带的特征:对华北东北缘构造带性质和演化的约束[J].地质通报,2007.7(7):810-823.
[33]周树亮,孙英华等.吉林省红旗岭镍矿区3号岩体成矿地质特征及找矿方向[J].吉林地质,2009.6(2):38-44.
[34]冯光英,刘燊等.吉林红旗岭与Cu-Ni硫化物矿床有关的超基性岩体的时代和地球化学特征[J].矿物学报,2009.12
[35] Xi Aihua, Ge Yuhui .Gnetic mineralogy of the Hongqiling Cu-Ni sulphide deposit: Implications for ore genesis[J].Progress in Natural Science,2007.12.
[36] Zhang Guangliang,Wu Fuyuan.Gochronological Significance of the Post- Orogenic MaficUltramafic Rocks in the Hongqiling Area of Jilin Province, Northeast China[J]. Earthquake Research in China.2006.6
[37] Tang Zhongli.Gmatic Sulfide Ni Cu Deposits in China[J]. Journal of China Univer- sity of Geosciences.199.3
[38] Naldrret. The composition of Ni-sulfide ores with particular reference to their content of PGE and Au[J]. Canadian Mineralogist.1979
[39] Dingley D J, Randle V. Microtexture determination by electron back-scatter diffraction [J]. Journal of Material Science.1992
[40] Buffett. Role reversal in geomag- netism[J].. Nature,1999
[41] Pruner P.. Paleomagnitism and paleogeography of Mongolia in the Cretaceous, Permian and Carboniferous- prelim- inary data[J]. Tectonophysics.1987
[42] Walshe JL.A six-component chlorite solid solutionmodel and the ystems[J]. Economical Geology.1986
[43] Tang Zhongli.Main Mineralization Mechanism of Magmatic Sulphide Deposits in China[J].Acta Geologica Sinica.1997
[44] Tang Zhongli.Classification of Magmatic Sulphide Deposits in China and Mineralization of Small Intrusions[J]. Acta Geologica Sinica .2006.6
[45]汤中立.关于矿田构造研究的若干问题「M」.地质评论.1984
[46]支学军.吉林红旗岭铜镍矿床成矿规律及找矿远景评价「D」.长春:吉林大学地球科学学院,2005.
[47]刘默.吉林红旗岭铜镍硫化物矿床地质特征及成因研究「D」.长春:吉林大学地球科学学院,2005.
[48]李碧乐,孙丰月,姚凤良.中生代敦化-密山断裂大规模左旋平移及其对金矿床形成的控制作用[J].大地构造与成矿学2002(4):390-395.
[49]董南庭,吴水波.密山-抚顺断裂带及其牵引构造对成矿物控制作用[J].吉林地质1982(1):1-11.
[50]蒋图治等.红旗岭铜镍矿区地质背景、成岩成矿规律及找矿方向(R)1993.
[51]王鸿祯.中国地壳发展的主要特征[M].武汉地质学院,1982
[52]王书丹.吉林省铜镍硫化矿床的地质规律[J].吉林地质,1982 1期.
[53]骆华宝.中国主要的铜镍矿床及其成因研究[M].中国地质科学院,1990.
[54]马醒华,杨振宇.中国三大地块的碰撞拼合与古欧亚大陆的重建.地球物理学报1993,4期:476-488.
[55]汤中立.中国硫化铜镍矿床类型及成矿模式.地质学报,1987,4期:350-361
[56]郗爱华,任洪茂,张宝福,王永详.吉林省红旗岭铜镍硫化物矿床矿石学特征[J].吉林大学学报2004(3):338-343.
[57]齐金忠,戚学祥,陈方远.南苏鲁高压变质带南岗"高公岛韧性剪切带特征及EBSD石英组构分析「J」.中国地质,2005,第3期:287—296.
[58]葛肖虹,马文璞,刘俊来等.对中国大陆构造格架的讨论[J].中国地质,2009,第5期:951-959.
[59]葛肖红.吉林省东部的大地构造环境与构造演化轮廓[J].现代地质,1990.3,第1期:107-112.
[60]葛肖虹,马文璞.东北亚南区中—新生代大地构造轮廓[J].中国地质,2007.4,第2期,213-225.
[2]秦宽.红旗岭地区硫化铜镍矿床地质特征[J].吉林地质,1995.9(3):18-29.
[3]杨言辰,孙德有等.红旗岭镁铁—超镁铁岩侵入体及铜镍硫化物矿床的成岩成矿机制[J].吉林大学报:地球科学版,2005.
[4]蒋图治.林省红旗岭地区古地热场地质特征及对基性岩侵入体前缘石墨化带地质意义的探讨[J].地构造学与成矿,1992:148-149.
[5]张广良,吴福元等.林红旗岭镁铁—超镁铁岩地球化学特征及构造动力学意义[J].科技大学学报,2001.
[6]唐文龙,杨言辰等.吉林红旗岭镁铁—超镁铁质岩的地球化学特征及地质意义[J].世界地质,2007.6(2):165-170.
[7]王好均.显微构造及构造岩的研究与应用[J].长春工程学院学报,2002.
[8]汤中立.中国主要镍矿类型及其与古板块构造的关系[J].矿床地质,1983.
[9]曹淑云,刘俊来等.岩石显微构造分析现代技术—EBSD技术及应用[J].地球科学进展,2006.10.
[10]郗爱华,顾连兴等.中国北方造山带岩浆铜镍硫化物矿床及地球动力学背景[J].地质学报,2006.11(11):1721-1727.
[11]李述靖,张维杰等.古弧地质构造特征及形成演化概论[M].北京:地质出版社,1998.
[12]张岳桥,董树文等.郯庐断裂带中生代构造演化史:进展与新认识[J].地质通报,2008.9(9):1372-1387.
[13]任纪顺,牛宝贵等.碰撞、叠覆造山和多旋回缝合作用[J].地学前缘,1999,3期:85-93.
[14]池永一.中呼兰镇地区呼兰群的划分及时代[J].地球科学,1997(2):205-214.
[15]林强.中国东北地区中生代火山岩的大地构造意义[J].地质科学,1998
[16]向必伟,朱广等.棱岩化过程中矿物变形温度计[J].地球科学进展,2007.2(2):126-133.
[17]徐海军,金淑燕等.岩石组构学研究的最新技术—电子背散射衍射(EBSD)[J].现代地质,2007.6.
[18]吴小奇,刘德良等.确定变形温度和应变速率分形法的探讨—以郯庐断裂浮槎山构造岩为例[J].中国地质,2006.2.
[19]吕素林,毛景文等.华北克拉通北缘岩浆Ni—Cu(PGE)硫化物矿床地质特征、形成时代及其地球动力学背景[J].地球学报,2007.4.
[20]路孝平,吴福元等.吉林南部通化地区古元古代辽吉花岗岩的侵位年代与形成构造背景[J].岩石学报,2004
[21]郗爱华,顾连兴等.吉林省红旗岭铜镍硫化物矿床的成矿时代讨论[J].矿床地质,2005.
[22]郗爱华,葛玉辉等.中亚蒙古造山带东段造山事件的40Ar-39Ar同位素年代学证据[J].中国地质,2006
[23]吴香尧著,岩组学导论[M].重庆出版社,1984
[24]孙德有,吴福元等.吉林中部晚三叠世和早侏罗世两期铝质A型花岗岩的厘定及对吉黑东部构造格局的制约[J].地学前沿,2005.4
[25]彭玉鲸,赵成弼等.古吉黑造山带的演化与陆壳的增生.吉林地质2001
[26]翟安民,沈保丰等.吉辽古裂谷地质演化与成矿[J].地质调查与研究,2005
[27]胡玲.显微构造地质学概论「M」.北京地质出版社,1998
[28]郑亚东,常志忠主编.岩石有限应变测量及韧性剪切带「M」.北京:地质出版社,1985
[29]王宇明.丹东韧性剪切带内岩石的有限应变测量及其地质找矿意义[J].地质找矿丛书,1991
[30]程裕淇主编.中国区域地质概论[M].北京地质出版社,1994
[31]孙德有,吴福元等.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] .吉林大学学报(地球科学版),2004
[32]颉颃强张福勤等.吉林中部漂河川镁铁—超镁铁质杂岩带的特征:对华北东北缘构造带性质和演化的约束[J].地质通报,2007.7(7):810-823.
[33]周树亮,孙英华等.吉林省红旗岭镍矿区3号岩体成矿地质特征及找矿方向[J].吉林地质,2009.6(2):38-44.
[34]冯光英,刘燊等.吉林红旗岭与Cu-Ni硫化物矿床有关的超基性岩体的时代和地球化学特征[J].矿物学报,2009.12
[35] Xi Aihua, Ge Yuhui .Gnetic mineralogy of the Hongqiling Cu-Ni sulphide deposit: Implications for ore genesis[J].Progress in Natural Science,2007.12.
[36] Zhang Guangliang,Wu Fuyuan.Gochronological Significance of the Post- Orogenic MaficUltramafic Rocks in the Hongqiling Area of Jilin Province, Northeast China[J]. Earthquake Research in China.2006.6
[37] Tang Zhongli.Gmatic Sulfide Ni Cu Deposits in China[J]. Journal of China Univer- sity of Geosciences.199.3
[38] Naldrret. The composition of Ni-sulfide ores with particular reference to their content of PGE and Au[J]. Canadian Mineralogist.1979
[39] Dingley D J, Randle V. Microtexture determination by electron back-scatter diffraction [J]. Journal of Material Science.1992
[40] Buffett. Role reversal in geomag- netism[J].. Nature,1999
[41] Pruner P.. Paleomagnitism and paleogeography of Mongolia in the Cretaceous, Permian and Carboniferous- prelim- inary data[J]. Tectonophysics.1987
[42] Walshe JL.A six-component chlorite solid solutionmodel and the ystems[J]. Economical Geology.1986
[43] Tang Zhongli.Main Mineralization Mechanism of Magmatic Sulphide Deposits in China[J].Acta Geologica Sinica.1997
[44] Tang Zhongli.Classification of Magmatic Sulphide Deposits in China and Mineralization of Small Intrusions[J]. Acta Geologica Sinica .2006.6
[45]汤中立.关于矿田构造研究的若干问题「M」.地质评论.1984
[46]支学军.吉林红旗岭铜镍矿床成矿规律及找矿远景评价「D」.长春:吉林大学地球科学学院,2005.
[47]刘默.吉林红旗岭铜镍硫化物矿床地质特征及成因研究「D」.长春:吉林大学地球科学学院,2005.
[48]李碧乐,孙丰月,姚凤良.中生代敦化-密山断裂大规模左旋平移及其对金矿床形成的控制作用[J].大地构造与成矿学2002(4):390-395.
[49]董南庭,吴水波.密山-抚顺断裂带及其牵引构造对成矿物控制作用[J].吉林地质1982(1):1-11.
[50]蒋图治等.红旗岭铜镍矿区地质背景、成岩成矿规律及找矿方向(R)1993.
[51]王鸿祯.中国地壳发展的主要特征[M].武汉地质学院,1982
[52]王书丹.吉林省铜镍硫化矿床的地质规律[J].吉林地质,1982 1期.
[53]骆华宝.中国主要的铜镍矿床及其成因研究[M].中国地质科学院,1990.
[54]马醒华,杨振宇.中国三大地块的碰撞拼合与古欧亚大陆的重建.地球物理学报1993,4期:476-488.
[55]汤中立.中国硫化铜镍矿床类型及成矿模式.地质学报,1987,4期:350-361
[56]郗爱华,任洪茂,张宝福,王永详.吉林省红旗岭铜镍硫化物矿床矿石学特征[J].吉林大学学报2004(3):338-343.
[57]齐金忠,戚学祥,陈方远.南苏鲁高压变质带南岗"高公岛韧性剪切带特征及EBSD石英组构分析「J」.中国地质,2005,第3期:287—296.
[58]葛肖虹,马文璞,刘俊来等.对中国大陆构造格架的讨论[J].中国地质,2009,第5期:951-959.
[59]葛肖红.吉林省东部的大地构造环境与构造演化轮廓[J].现代地质,1990.3,第1期:107-112.
[60]葛肖虹,马文璞.东北亚南区中—新生代大地构造轮廓[J].中国地质,2007.4,第2期,213-225.