江南—雪峰构造带西南缘构造特征研究
|
摘要
江南-雪峰构造带出露大范围的新元古界板溪群浅变质岩,震旦系-下古生界不整合于其上。目前普遍认为雪峰构造带是上扬子大陆东南边缘的加里东期隆起。
论文以江南-雪峰构造带西南缘凯里-从江-融水-融安-独山一带的地质构造为主要研究对象,从不同时代沉积相空间变化和沉积盆地演化的角度研究大地构造问题。在沉积学研究的同时,辅助以岩浆岩的地球化学和同位素地质年代学研究,主要取得以下初步认识:
1、上扬子地块东南部与江南-雪峰构造带西南缘凯里-黎平-融水地区出露新元古界板溪群至中三叠统,上三叠统、下-中侏罗统和上白垩统局部出露,古近系与新近系在研究区基本不发育。从下向上可以把研究区划分为四个构造层,即:前震旦系基底构造层、震旦系-下古生界构造层、泥盆系-三叠系构造层和三叠系以上构造层,它们分别反映了研究区内经历了4个比较大的地质发展阶段。从下向上,沉积中心有规律地由南东向北西迁移。
2、研究区构造变形方面最显著的一个特点是,大致以凯里—独山一线为界,东西两侧具有不同的构造变形特点。
凯里—独山一线以东的加里东运动表现为褶皱运动,导致在下古生界中形成近东西向的褶皱,泥盆系角度不整合覆盖在下伏被褶皱的下古生界之上;凯里—独山以西的加里东运动则表现为垂直隆升,导致晚志留世基本缺失沉积,以及泥盆系与下伏下古生界之间的平行不整合接触关系。西部的燕山运动表现为强烈的褶皱运动,导致侏罗-白垩系的大范围缺失,以及零星发育的上白垩统茅台群粗碎屑岩与下伏地层之间的角度不整合;东部的燕山运动则表现为强烈的伸展运动,导致华南花岗岩大范围发生。研究区内缺失古近系和新近系,根据第四纪河流阶地和溶洞发育情况来看,喜马拉雅运动在研究区主要表现为垂直的升降运动。
3、研究区内各期构造变形之间有一定的继承关系,多条长期活动的区域性大断裂和复活断层不仅破坏了基底构造,而且还控制了盖层的沉积。
研究区内断裂和褶皱比较发育,研究区东部融安一带的断裂主要形成于加里东期,后期又叠加了燕山期的改造作用;研究区西部的断裂主要形成于燕山期。按照研究区内的断层和褶皱大体走向方位来划分,区内主要有四组断裂、褶皱系,即北东向、北西向、南北向和少量的近东西向断裂系。
4、论文对黔东南从江县秀塘河口花岗质岩石进行的激光等离子体质谱(La-ICP-MS)锆石U-Pb同位素地质年代学测定获得该花岗质岩石的年龄值为836±5.1Ma。黔东南-桂北地区新元古代早-中期中酸性岩浆活动在时间上发生于江南造山带的峰期碰撞造山作用之后,应该形成于江南造山带峰期碰撞后伸展阶段的岩浆活动中,它是黔东南-桂北地区同时代大规模中酸性岩浆活动的一部分。江南-雪峰构造带西南缘在南华纪-早古生代的区域沉降作用和巨厚的沉积建造就形成在从青白口纪开始的区域伸展背景之下。
5、江南-雪峰构造带西南缘及邻区新元古代以来经历了四个阶段的沉积-构造演化
(1)青白口纪早期Rodinia古陆形成阶段:扬子与华夏地块拼合,江南造山带形成;
(2)青白口纪晚期-志留纪:Rodinia古陆裂解与聚敛阶段:江南-雪峰带裂陷沉降(青白口纪晚期-中奥陶世)与隆升剥蚀(晚奥陶世-志留纪)。又可以分为4个次级阶段:青白口纪晚期-震旦纪(820-680Ma)江南-雪峰裂陷盆地、震旦系-中奥陶统江南-雪峰坳陷盆地和晚奥陶世-志留纪研究区东部的褶皱变形与西部的隆升剥蚀。
(3)泥盆纪-三叠纪:扬子克拉通内坳陷与NW向紫云-罗甸-南丹裂陷槽叠加演化阶段。包括4个次级阶段:泥盆纪紫云-罗甸-南丹裂陷槽拉张和其它地区坳陷、石炭-二叠纪克拉通内碳酸盐岩台地、早-中三叠世海退背景下的浅海台盆和晚三叠世的洋陆转换。
(4)燕山-喜马拉雅期:盆、山演化与强烈改造阶段。包括3个次级阶段:晚侏罗世-早白垩世(早燕山期)江南-雪峰陆内构造变形作用、晚白垩世-古近纪(晚燕山期-早喜马拉雅期)岩石圈伸展减薄作用与A型花岗岩作用和新近纪至今(晚喜马拉雅期)强烈的陆内变形阶段。
6、论文在野外地质考察及对地层、构造和岩浆岩等资料分析研究的基础上,充分结合当前关于扬子地块与江南-雪峰构造带等大地构造单元的的最新研究成果,支持前人关于雪峰构造带是扬子大陆东南边缘的加里东期隆起的观点。
Low grade metamorphic rocks of the Neoproterozoic Banxi Group disconformatively overlain by the Sinian and Paleozoic are extensively exposed in the Jiangnan-Xuefeng structural belt.At present it is generally considered that the Xuefeng structural belt is a Caledonian uplift at southeast margin of the Yangtze continent.
In this paper,we mainly studied geological structure of the Kaili-Congjiang-Rongshui-Rongan-Dushan belt at the southwest margin of the Jiangnan-Xuefeng structural belt,and discussed the tectonics according to spacial changes of sedimentary facies of different ages and evolution of sedimentary basins.In addition, geochemical test of magmatic rocks and isotope geochronological analysis were also conducted.On the basis of these studies,some primary conclusions were summarized as following:
1.Outcrops of ages ranging from the Neoproterozoic Banxi Group to the Middle Triassic are fully exposed at the southeastern Upper Yangtze continent and southwest margin of the Jiangnan-Xuefeng structural belt,wile the Upper Triassic,Lower-Middle Jurassic,and Upper Cretaceous are partially exposed.However,the Paleogene and Neogene are invisible in the study area.The study area can be sub-divided into four structural layers,in chronological order,the pre-Sinian,Sinian and Lower Paleozoic,Devonian-Triassic,and post-Triassic structural layers,which reflect four main geologically developmental stages in the study area, respectively.Stratigraphically,the depocenter migrates from southeast to northwest.
2.It is notable that the study area is divisible by the Kaili-Dushan structural belt. Eastern and western wings of this belt show distinctive character of deformation.Vertical uplift occurs in western Kaili-Dushan structural belt,causing deletion of the Upper Silurian and parallel unconformity between the Devonian and Lower Paleozoic.In the west,Yanshan movement exhibits strong folding,causing extensive deletion of the Jurassic and Cretaceous as well as angular unconformity between clastic rocks of the Upper Cretaceous Maotai Group and the underlying strata.In the east,Yanshan movement exhibits strong extension,causing the occurrence of extensive granites in South China.The Paleogene and Neogene is absent from the study area.According to the development of Quaternary fluvial terrace and dissolved cavern,Himalayan movement mainly exhibits vertical movement in the study area.
3.Deformations of a variety of age developed in the study area are,in chronological order,inherited from the younger stages of deformation.Multiple,long-term activated large faults and revived faults have together destroyed structure of the basement and controlled deposition of the capping bed.
4.A U-Pb age of 836±5.1 Ma is obtained using La-ICP-MS dating method from zircon. The zircon-host granitic rock is sampled from Hekou of Xiutang,eastern Guizhou.In southeastern Guizhou-northern Guangxi area,early-middle stage activities of Neoproterozoic acidic magmatism occurred after collision of the Jiangnan orogenic belt,which may have occurred during tension stage of the magmatism.This magmatism is part of the large-scaled, southeastern Guizhou-northern Guangxi acidic magmatism.
5.Four stages of structural evolution occurred in the Jiangnan-Xuefeng structural belt:
(1)Formation Rodinia ancient land stage(Early Qingbaikou):the Yangtze and Cathaysia continents merged together;Jiangnan orogenic belt formed.
(2) Detachment and re-assemblage of the Rodinia ancient land stage(Early Qingbaikou-Silurian):depression(Qingbaikou-Middle Ordovician) and uplift and erosion (Late Ordovician-Silurian) of the Jiangnan-Xuefeng structural belt.Four sub-stages can be identified:late Qingbaikou-Sinian(820-680Ma) Jiangnan-Xuefeng depression basin, Sinian-Middle Ordovician Jiangnan-Xuefeng depression basin,Late Ordovician-Silurian folding and deformation of the eastern study area,and uplift and erosion of the western study area.
(3) Devonian-Triassic:Inner-Yangtze Craton depression and superimposed evolution of the NW-trending Ziyun-Luodian-Nandan depressed trough.Four sub-stages can be identified: Tension of the Ziyun-Luodian-Nandan depressed trough(Devonian) and depression of other area,formation of inner-craton carbonate platform(Carboniferous-Permian),shallow water basin under regression(Early-Middle Triassic),and transition of oceanic to terrestrial environments(Late Triassic).
(4) Basin and orogenic belt evolution stage(Yanshan-Himalayan):Three sub-stages can be identified:Jiangnan-Xuefeng inner-continent deformation during Late Jurassic-Early Cretaceous(early Yanshan),tension and thinning of lithosphere and A-type magmatism during Late Cretaceou-Paleogene(late Yanshan to early Himalayan),and inner-continent deformation during Neogene afterward(late Himalayan).
6.On the basis of filed observation,detailed investigations of strata and previous publications,we suggest,as proposed by previous workers,that the Xuefeng structural belt is the result from a Caledonian uplift of the southeastern margin of the Yangtze Continent.
论文以江南-雪峰构造带西南缘凯里-从江-融水-融安-独山一带的地质构造为主要研究对象,从不同时代沉积相空间变化和沉积盆地演化的角度研究大地构造问题。在沉积学研究的同时,辅助以岩浆岩的地球化学和同位素地质年代学研究,主要取得以下初步认识:
1、上扬子地块东南部与江南-雪峰构造带西南缘凯里-黎平-融水地区出露新元古界板溪群至中三叠统,上三叠统、下-中侏罗统和上白垩统局部出露,古近系与新近系在研究区基本不发育。从下向上可以把研究区划分为四个构造层,即:前震旦系基底构造层、震旦系-下古生界构造层、泥盆系-三叠系构造层和三叠系以上构造层,它们分别反映了研究区内经历了4个比较大的地质发展阶段。从下向上,沉积中心有规律地由南东向北西迁移。
2、研究区构造变形方面最显著的一个特点是,大致以凯里—独山一线为界,东西两侧具有不同的构造变形特点。
凯里—独山一线以东的加里东运动表现为褶皱运动,导致在下古生界中形成近东西向的褶皱,泥盆系角度不整合覆盖在下伏被褶皱的下古生界之上;凯里—独山以西的加里东运动则表现为垂直隆升,导致晚志留世基本缺失沉积,以及泥盆系与下伏下古生界之间的平行不整合接触关系。西部的燕山运动表现为强烈的褶皱运动,导致侏罗-白垩系的大范围缺失,以及零星发育的上白垩统茅台群粗碎屑岩与下伏地层之间的角度不整合;东部的燕山运动则表现为强烈的伸展运动,导致华南花岗岩大范围发生。研究区内缺失古近系和新近系,根据第四纪河流阶地和溶洞发育情况来看,喜马拉雅运动在研究区主要表现为垂直的升降运动。
3、研究区内各期构造变形之间有一定的继承关系,多条长期活动的区域性大断裂和复活断层不仅破坏了基底构造,而且还控制了盖层的沉积。
研究区内断裂和褶皱比较发育,研究区东部融安一带的断裂主要形成于加里东期,后期又叠加了燕山期的改造作用;研究区西部的断裂主要形成于燕山期。按照研究区内的断层和褶皱大体走向方位来划分,区内主要有四组断裂、褶皱系,即北东向、北西向、南北向和少量的近东西向断裂系。
4、论文对黔东南从江县秀塘河口花岗质岩石进行的激光等离子体质谱(La-ICP-MS)锆石U-Pb同位素地质年代学测定获得该花岗质岩石的年龄值为836±5.1Ma。黔东南-桂北地区新元古代早-中期中酸性岩浆活动在时间上发生于江南造山带的峰期碰撞造山作用之后,应该形成于江南造山带峰期碰撞后伸展阶段的岩浆活动中,它是黔东南-桂北地区同时代大规模中酸性岩浆活动的一部分。江南-雪峰构造带西南缘在南华纪-早古生代的区域沉降作用和巨厚的沉积建造就形成在从青白口纪开始的区域伸展背景之下。
5、江南-雪峰构造带西南缘及邻区新元古代以来经历了四个阶段的沉积-构造演化
(1)青白口纪早期Rodinia古陆形成阶段:扬子与华夏地块拼合,江南造山带形成;
(2)青白口纪晚期-志留纪:Rodinia古陆裂解与聚敛阶段:江南-雪峰带裂陷沉降(青白口纪晚期-中奥陶世)与隆升剥蚀(晚奥陶世-志留纪)。又可以分为4个次级阶段:青白口纪晚期-震旦纪(820-680Ma)江南-雪峰裂陷盆地、震旦系-中奥陶统江南-雪峰坳陷盆地和晚奥陶世-志留纪研究区东部的褶皱变形与西部的隆升剥蚀。
(3)泥盆纪-三叠纪:扬子克拉通内坳陷与NW向紫云-罗甸-南丹裂陷槽叠加演化阶段。包括4个次级阶段:泥盆纪紫云-罗甸-南丹裂陷槽拉张和其它地区坳陷、石炭-二叠纪克拉通内碳酸盐岩台地、早-中三叠世海退背景下的浅海台盆和晚三叠世的洋陆转换。
(4)燕山-喜马拉雅期:盆、山演化与强烈改造阶段。包括3个次级阶段:晚侏罗世-早白垩世(早燕山期)江南-雪峰陆内构造变形作用、晚白垩世-古近纪(晚燕山期-早喜马拉雅期)岩石圈伸展减薄作用与A型花岗岩作用和新近纪至今(晚喜马拉雅期)强烈的陆内变形阶段。
6、论文在野外地质考察及对地层、构造和岩浆岩等资料分析研究的基础上,充分结合当前关于扬子地块与江南-雪峰构造带等大地构造单元的的最新研究成果,支持前人关于雪峰构造带是扬子大陆东南边缘的加里东期隆起的观点。
Low grade metamorphic rocks of the Neoproterozoic Banxi Group disconformatively overlain by the Sinian and Paleozoic are extensively exposed in the Jiangnan-Xuefeng structural belt.At present it is generally considered that the Xuefeng structural belt is a Caledonian uplift at southeast margin of the Yangtze continent.
In this paper,we mainly studied geological structure of the Kaili-Congjiang-Rongshui-Rongan-Dushan belt at the southwest margin of the Jiangnan-Xuefeng structural belt,and discussed the tectonics according to spacial changes of sedimentary facies of different ages and evolution of sedimentary basins.In addition, geochemical test of magmatic rocks and isotope geochronological analysis were also conducted.On the basis of these studies,some primary conclusions were summarized as following:
1.Outcrops of ages ranging from the Neoproterozoic Banxi Group to the Middle Triassic are fully exposed at the southeastern Upper Yangtze continent and southwest margin of the Jiangnan-Xuefeng structural belt,wile the Upper Triassic,Lower-Middle Jurassic,and Upper Cretaceous are partially exposed.However,the Paleogene and Neogene are invisible in the study area.The study area can be sub-divided into four structural layers,in chronological order,the pre-Sinian,Sinian and Lower Paleozoic,Devonian-Triassic,and post-Triassic structural layers,which reflect four main geologically developmental stages in the study area, respectively.Stratigraphically,the depocenter migrates from southeast to northwest.
2.It is notable that the study area is divisible by the Kaili-Dushan structural belt. Eastern and western wings of this belt show distinctive character of deformation.Vertical uplift occurs in western Kaili-Dushan structural belt,causing deletion of the Upper Silurian and parallel unconformity between the Devonian and Lower Paleozoic.In the west,Yanshan movement exhibits strong folding,causing extensive deletion of the Jurassic and Cretaceous as well as angular unconformity between clastic rocks of the Upper Cretaceous Maotai Group and the underlying strata.In the east,Yanshan movement exhibits strong extension,causing the occurrence of extensive granites in South China.The Paleogene and Neogene is absent from the study area.According to the development of Quaternary fluvial terrace and dissolved cavern,Himalayan movement mainly exhibits vertical movement in the study area.
3.Deformations of a variety of age developed in the study area are,in chronological order,inherited from the younger stages of deformation.Multiple,long-term activated large faults and revived faults have together destroyed structure of the basement and controlled deposition of the capping bed.
4.A U-Pb age of 836±5.1 Ma is obtained using La-ICP-MS dating method from zircon. The zircon-host granitic rock is sampled from Hekou of Xiutang,eastern Guizhou.In southeastern Guizhou-northern Guangxi area,early-middle stage activities of Neoproterozoic acidic magmatism occurred after collision of the Jiangnan orogenic belt,which may have occurred during tension stage of the magmatism.This magmatism is part of the large-scaled, southeastern Guizhou-northern Guangxi acidic magmatism.
5.Four stages of structural evolution occurred in the Jiangnan-Xuefeng structural belt:
(1)Formation Rodinia ancient land stage(Early Qingbaikou):the Yangtze and Cathaysia continents merged together;Jiangnan orogenic belt formed.
(2) Detachment and re-assemblage of the Rodinia ancient land stage(Early Qingbaikou-Silurian):depression(Qingbaikou-Middle Ordovician) and uplift and erosion (Late Ordovician-Silurian) of the Jiangnan-Xuefeng structural belt.Four sub-stages can be identified:late Qingbaikou-Sinian(820-680Ma) Jiangnan-Xuefeng depression basin, Sinian-Middle Ordovician Jiangnan-Xuefeng depression basin,Late Ordovician-Silurian folding and deformation of the eastern study area,and uplift and erosion of the western study area.
(3) Devonian-Triassic:Inner-Yangtze Craton depression and superimposed evolution of the NW-trending Ziyun-Luodian-Nandan depressed trough.Four sub-stages can be identified: Tension of the Ziyun-Luodian-Nandan depressed trough(Devonian) and depression of other area,formation of inner-craton carbonate platform(Carboniferous-Permian),shallow water basin under regression(Early-Middle Triassic),and transition of oceanic to terrestrial environments(Late Triassic).
(4) Basin and orogenic belt evolution stage(Yanshan-Himalayan):Three sub-stages can be identified:Jiangnan-Xuefeng inner-continent deformation during Late Jurassic-Early Cretaceous(early Yanshan),tension and thinning of lithosphere and A-type magmatism during Late Cretaceou-Paleogene(late Yanshan to early Himalayan),and inner-continent deformation during Neogene afterward(late Himalayan).
6.On the basis of filed observation,detailed investigations of strata and previous publications,we suggest,as proposed by previous workers,that the Xuefeng structural belt is the result from a Caledonian uplift of the southeastern margin of the Yangtze Continent.
引文
[1]许效松。雪峰古隆起沉积构造演化与油气成藏关系。中扬子-雪峰地区油气勘探研讨会,2006年8月。
[1] Bea R, Arzamastsev A., Montero P., et al. Aonmalous alkaline rocks of Soustov, Kola: Evidengce of mantle-drived matasomatic fluids crustal material[J] . Contributions to Mineralogy and Petrology, 2001,140: 554-566
[2] Boynton W V. Geochemistry of the rare earth elements: meteorite studies. In: Henderson P, Rare earth element geochemistry[J]. Elsevier, 1984, 63-114
[3] Grabau A. W. Migration of Geosyelines[J] . The National Gelogical Survey of China, 1924,208-237
[4] Grabau A. W. Seratigraphy of China. The Geological Survey, Ministry of Agriculture and Commerce[J]. Peking, 1923-1924, 8-9
[5] Hou K. J. et al. Reply to Gopts.et al(1989). On "Mesozoic overthrust tectonics in South China" [J]. Geology, 1988,17: 672-673
[6] Hou K.J., et al. Mesosoic overthrust tectonics in South China[J] .Geology, 1985, 16: 418-421
[7] Li W X, Li XH, Li ZX. Neoproterozoic bimodal magmatism in the Cathaysia Block of South China and its tectonic significance[J]. Precam.Res., 2005,136: 51-66
[8] Li X H, Li Z X, Zhou H W, Liu Y, Kinny, P. U-Pb zircon geochronology, geochemistry and Nd isotopic study of Neoproterozoic bimodal volcanic rocks in the Kangdiam Rift of South China: implications for the initial rifting of Rodinia[J] . Precam. Res., 2002, 113: 135-155
[9] Li Z X, Li X H, Kinny P D, et al. Geochronology of Neoproterozoic syn-rift magmatism in the Yangtze Cration, south China and correlations with other continents: evience for a mantle supperplume that broke up Rodinia[J] . Precambrian Res., 2003, 122: 85-109
[10] Li ZX, Li X H, Kinny P D, Wang J. The breakup of Rodinia: did it start with a mantle plume beneath South China? [J]. Earth Planet Sci Lett, 1999,173: 171-181
[11] Ling W L, Gao S, Zhang B R, Li H M, Liu Y, Cheng J P. Neoproterozoic tectonic evolution of the northwestern Yangtze Craton, South China: implications for amalgamation and break-up of the Rodinia Supercontinent[J] . Precam. Res., 2003, 122: 111-140
[12] Rudnick R L, Fountain D M. Nature and composition of the Continental rust: a lower crustal perspective[J]. Reviews of Geophysics, 1995, 33(3): 267-309
[13] Rudnick R L., Gao S. Composition of the Continental crust. In: Rudnick RL(eds.). The Crust.Treaties on Geochemistry,3rd[J].Oxford:Elsevier Pergamon,2003,1-64
[14]Rubatto D.Zircon trace element geochemistry:Partitioning with garnet and the link between U-Pb ages and metamorphism.Chemical Geology,2002,184:123-138
[15]Sun S S.,McDonough W F.,Geo.Soc.London Spec.Publ.,1989,42:313-345
[16]Wang X L,Zhou J C,Qiu J S,et al.Geochemistry of the Meso-to Neoproterozoic basic-acid rocks from Hunan Province,South China:implication for the evolution of the western Jiangnan orogen[J].Precambrian Research,2004,135:79-103
[17]Zhao G C,Cawood P A.Tectonothemal evolution of the Mayuan assemblage in the Cathaysia block:implications for Neoproterozoic collision-related assembley of the South China craton[J].Am.J.Sci.,1999,299:309-339
[18]蔡明海,梁婷,吴德成,皇惠民.广西大厂矿田花岗岩地球化学特征及其构造环境[J].地质科技情报,2004,23(2):57-62
[19]车自成,刘良等.中国及其邻区区域大地构造学[M].北京:科学出版社,2002,395-432
[20]陈海泓,孙枢,李继亮等.雪峰山大地构造的基本特征初探[J].地质科学,1993,28(3):201-210
[21]陈旭,周志毅.奥陶系全球界线层型剖面和点位(GSSP)的研究[J].地层学杂志,2005,29(2):165-170
[22]陈毓川,王登红.广西大厂层状花岗质岩石地质、地球化学特征及成因初探[J].地质论评,1996,42(6):523-530
[23]丁道桂,郭彤楼,刘运黎,翟常博.对江南-雪峰带构造属性的讨论[J].地质通报,2007,26(7):801-809
[24]丁道桂,朱樱,陈凤良等.中下扬子区古生代盆地基底拆离改造与油气领域[J].石油与天然气地质,1991,12(4):376-384
[25]冯增昭,杨玉卿,鲍志东.中国南方石炭纪岩相古地理[J].古地理学报,1999,1(1):75-86
[26]冯增昭,金振奎,柯玉卿等.滇黔桂地区二叠纪岩相古地理[J].北京:地质出版社,1994,217
[27]广西壮族自治区地质局区域地质测量队五分队.区域地质测量报告书[M].南宁:1967,7-72
[28]贵州省地质局.榕江幅1:20万地质图.1963
[29]贵州省地质局.都云幅1:20万地质图.1963
[30]贵州省地质局.罗甸幅1:20万地质图.1965
[31]贵州省地质局.独山幅1:20万地质图.1965
[32]贵州省地质局.江口幅1:20万地质图.1971
[33]贵州省地质局.贵阳幅1:20万地质图.1976
[34]贵州省地质局.黎平幅1:20万地质图.1978
[35]贵州省地矿局.贵州省区域地质志[M].北京:地质出版社,1987,26-48
[36]贵州省地质矿产局.贵州省区域地质志[M].北京:地质出版社,1987,194-226
[37]贵州省地质志[M].北京:地质出版社,1987,13-26,514-525
[38]广西壮族自治区地质局.融安幅1:20万地质图.1967
[39]广西壮族自治区地质局.南丹幅1:20万地质图.1969
[40]葛文春,李献华,李正祥,周汉文,李寄嵎.桂北新元古代两类过铝花岗岩地球化学研究[J].地球化学,2001,30(1):24-35
[41]郭令智等.华南板块构造[M].北京:地质出版社,2001:1-6
[42]郭正吾,邓康龄,韩永辉等.四川盆地形成与演化[M].北京:地质出版社,1996,57-78
[43]韩世庆,王守德,胡惟元.黔东麻江古油藏的发现及其意义[J].石油与天然气地质,1982,3(4):316-327
[44]贺自爱,杨宏,周经才.贵州中三叠世生物礁[J].地质科学,1980,(3):256-264
[45]侯方浩,方少仙,陈景山等.西南地区上古生界海相碳酸盐岩沉积模式及其在油气勘探中的应用[M].成都:成都科技大学出版社,1991,1-20
[46]黄汲清.中国主要地质构造单位.中央地质调查所地质专报[R],甲种 1945,20:1-165
[47]姜月华,岳文浙,业治铮.华南下古生界缺氧事件与黑色页岩及有关矿产[J].有色金属矿产与勘查,1994,3:272-278
[48]李胜荣,高振敏.湘黔寒武系底部黑色岩系贵金属元素来源示踪[J].中国科学(D 辑),2000,30(2):169-174
[49]李曙光,HartSR,郑双根等.中国华北、华南陆块碰撞时代的钐-钕同位素年龄证据[J].中国科学(B辑),1989,19(3):312-319
[50]李钟模.滇黔桂地区二叠纪生物礁[J].贵州地质,1988,5(1):31-42
[51]梁祥济,王福生,乔莉.桂北雪峰期含锡黑云母花岗岩成因的见证[J].地球学报, 1995,1:55-68
[52]廖士范.“黔中隆起”的发生发展与古风化壳铝土矿的形成问题[J].贵州工学院学报,1990,19(1):81-82
[53]林广春,李献华,李武显.川西新元古代基性岩墙群的SHRIMP锆石U-Pb年龄、元素和Nd-Hf同位素地球化学:岩石成因与构造意义[J].中国科D辑地球科学,2006,36(7):630-645
[54]林启祥.贵州紫云晚古生代生物礁的性质和演化[J].地球科学-中国地质大学学报,1992,17(1):301-307
[55]刘特民.黔中何时隆起[J].贵州地质,1987,4(1):65-71
[56]刘育燕,杨巍然,森永速男,等.华北、秦岭及扬子陆块的若干古地磁研究结果[J].地球科学-中国地质大学学报,1993,18(5):635-641
[57]卢华夏.关于华夏古陆[J].高校地质学报,2006,12(4):413-417
[58]吕炳全,王红罡,胡望水,等.扬子地块东南古生代上升流沉积相及其与烃源岩的关系[J].海洋地质与第四纪地质,2004,24(4):29-35
[59]罗志立.四川盆地基底结构的新认识[J].成都理工学院学报,1998,25(2):191-200
[60]马力,陈焕疆,甘克文,等.中国南方大地构造和海相油气地质[J].北京:地质出版社,2004,502-567
[61]马文璞,丘元禧,何丰盛.江南隆起上的下古生界缺失带-华南加里东前陆褶冲带的标志[J].现代地质,1995,9(3):320-324
[62]毛景文,谢贵青,李晓峰,等.华南地区中生代大规模成矿作用与岩石圈多阶段伸展[J].地学前缘(中国地质大学,北京),2004,11(1):45-55
[63]毛景文,张宗清,董宝林.江南古陆南缘四堡群钐钕同位素年龄研究[J].地质论评,1990,36(3):264-268
[64]毛景文、陈毓川.关于桂北四堡期花岗闪长岩成因的探讨[J].岩石矿物学杂志,1988,7(4):289-298
[65]梅冥相.论“黔中古陆”[J].贵州地质,1994,11(3):0-5
[66]牛新生,冯常茂,刘进.黔中隆起的形成时间及形成机制探讨[J].海相油气地质,2007,12(2):46-50
[67]彭军,陈景山,陈洪德,等.黔桂地区石炭纪Ⅰ型层序界面沉积记录及成因分析[J].地球学报,2000,21(4):433-440
[68]丘元禧,马文璞,范小林,等.“雪峰古陆”加里东期的构造性质和构造演化[J].中 国区域地质,1996,(2):150-160
[69]邱检生,周金城,张光辉,凌文黎.桂北前寒武纪花岗岩类岩石的地球化学与成因[J].岩石矿物学杂志,2002,20(3):197-208.
[70]沙庆安,吴望始,傅家谟.黔桂地区二叠系综合研究-兼论含油气性.北京:科学出版社,1990,207
[71]沈志达,梅冥相,曾羽.贵州太康运动的地层学效应-兼论“黔中古陆”的形成[J].贵州地质,1990,7(2):91-97
[72]舒良树,周国庆,施央申,等.江南造山带东段高压变质蓝片及其地质时代研究[J].科学通报,1993,38(20):1879-1882
[73]孙涛.新编华南花岗岩分布图及其说明.地质通报,2006,25(3):332-335
[74]腾格尔,胡凯,高长林,等.上扬子东南缘下组合优质烃源岩的发育及生烃潜力评价[J].石油实验地质,2006,28(4):359-365
[75]田海芹,沃玉进,郑磊,等.中国南方中、古生界油气勘探方向之思考-近源深埋逆断带可能是今后中国南方中、古生界油气勘探的主战场[J].南方油气,2002,15(3):236-243
[76]涂光炽.华南花岗岩类的地球化学[J].科学出版社,1979,357-373.
[77]汪啸风,IanMetcalfe,简平.金沙江缝合带构造地层划分及时代厘定[J].中国科学(D辑),1999,29(4):289-297
[78]王德滋,周新民,孙幼群.华南前寒武纪慢源花岗岩类的基本特征[J].桂林冶金地质学院学报,1982,(4):1-9
[79]王鸿祯,乔秀夫.中国元古代构造单元及其边界性质[J].前寒武纪地质,1986,(3):1-14
[80]王练成,李达周,张旗,等.四川理塘蛇绿混杂岩-一个以火山岩为基质的蛇绿混杂岩[J].岩石学报,1985,1(2):17-27
[81]王懋基.黑水-泉州地学断而的重磁解释[J].地球物理学报,1994,37(3):321-329
[82]王小多.雪峰山构造带及其邻区磁性结构研究[D].西安:西北大学,2008
[83]王晓青,刘祖彝.湖南长常区地质志,前湖南地质调查所.1936,乙种:(1)
[84]王孝磊,周金城,邱检生,等.桂北新元古代强过铝花岗岩的成因:锆石年代学和Hf同位素制约[J].岩石学报,2006,22(2):326-342
[85]吴汉宁,常承法,刘椿,等.依据古地磁资料探讨华北和华南快体运动及其对秦岭 造山带构造演化的影响[J].地质科学,1990,25(3):201-214
[86]吴浩若.重新解释广西运动[J].科学通报,2000,45(5):555-558
[87]许靖华,孙枢,李继亮.是华南造山带而不是华南地台[J].中国科学(B辑),1987,17(10):1107-1115
[88]许靖华,孙枢.寒武纪生物爆发前的海洋[J].地质科学,1986,1:1-10
[89]许靖华.薄壳板块构造模式与冲撞型造山运动[J].中国科学,B辑.1980,(1):1081-1089
[90]许靖华.中国南方大地构造的几个问题[J].(武汉地质学院)地质科技情报,1987,6(2):13-27
[91]杨斌,廖宗廷.广西大厂礁灰岩区碳沥青的产状特征及其与多金属成矿关系探讨[J].沉积学报,1999,17(增刊):668-674
[92]尹赞勋.中国南部志留纪地层之分类与对比[J].中国地质学会志,1949,29:162
[93]袁照令,李大明,易顺华.对保靖-慈利逆冲断裂带的一些认识[J].地质与勘探,2000,36(5):59-61
[94]袁正新,谢岩豹.华南地区加里东期构造运动时空分布的新认识.华南地质与矿产,1997,V4
[95]曾雯,周汉文,钟增球,等.黔东南新元古代岩浆岩单颗粒锆石U-Pb年龄及其构造意义[J].地球化学,2005,34(6):548-556
[96]曾昭光,唐云辉,彭慈刚,等.黔桂边界四堡群中高压变质矿物的发现及其地质意义[J].贵州省地质,2005,22(1):46-49
[97]张桂林,梁金城,刘之葵,等.桂北元古代本洞花岗闪长岩体中发现左旋-正滑型韧性剪切带[J].桂林工学院学报,2003,23(1):1-4
[98]张永刚,马宗晋,王国力,等.中国南方海相油气成藏模式分析[J].地质学报,2007,81(2):236-243
[99]张正华,王治华,李昌全.黔南二叠纪地层[J].贵阳:贵州人民出版社,1988,113
[100]赵志东,王炯章,李载沃,等.中国石油地质志,第十一卷(滇黔桂油气区)[M].北京:石油工业出版社,1987,81-116
[101]赵子杰,马大铨.桂北前寒武纪花岗岩本洞、三防岩体的研究[A].宜昌地质矿产研究所.南岭地质矿产科研报告集(一)[C].武汉:武汉地质学院出版社,1987,1-27
[102]赵宗举,朱琰,李大成,等.中国南方构造变形对油气藏的控制作用[J].石油与 天然气地质,2002,23(1):19-25
[103]赵宗举,朱琰,徐云俊.中国南方古生界-中生界油气藏成藏规律及勘探方向[J].地质学报,2004,78(5):710-720
[104]赵宗举.中国南方古隆起对中、古生界原生油气藏的控制作用[J].石油实验地质,2003,25(1):20-25
[105]周金城,王孝磊,邱检生.江南造山带是否格林威尔期造山带?—关于华南前寒武纪地质的几个问题[J].高校地质学报,2008,14(1):64-72
[106]周金城,王孝磊,邱检生.江南造山带西段岩浆作用特征[J].高校地质学报,2005,11(4):527-533
[107]周金城,王孝磊,裘检生,等.南桥高度亏损N-MORB的发现及其地质意义[J].岩石矿物杂志,2003,22(3):211-216
[1] Bea R, Arzamastsev A., Montero P., et al. Aonmalous alkaline rocks of Soustov, Kola: Evidengce of mantle-drived matasomatic fluids crustal material[J] . Contributions to Mineralogy and Petrology, 2001,140: 554-566
[2] Boynton W V. Geochemistry of the rare earth elements: meteorite studies. In: Henderson P, Rare earth element geochemistry[J]. Elsevier, 1984, 63-114
[3] Grabau A. W. Migration of Geosyelines[J] . The National Gelogical Survey of China, 1924,208-237
[4] Grabau A. W. Seratigraphy of China. The Geological Survey, Ministry of Agriculture and Commerce[J]. Peking, 1923-1924, 8-9
[5] Hou K. J. et al. Reply to Gopts.et al(1989). On "Mesozoic overthrust tectonics in South China" [J]. Geology, 1988,17: 672-673
[6] Hou K.J., et al. Mesosoic overthrust tectonics in South China[J] .Geology, 1985, 16: 418-421
[7] Li W X, Li XH, Li ZX. Neoproterozoic bimodal magmatism in the Cathaysia Block of South China and its tectonic significance[J]. Precam.Res., 2005,136: 51-66
[8] Li X H, Li Z X, Zhou H W, Liu Y, Kinny, P. U-Pb zircon geochronology, geochemistry and Nd isotopic study of Neoproterozoic bimodal volcanic rocks in the Kangdiam Rift of South China: implications for the initial rifting of Rodinia[J] . Precam. Res., 2002, 113: 135-155
[9] Li Z X, Li X H, Kinny P D, et al. Geochronology of Neoproterozoic syn-rift magmatism in the Yangtze Cration, south China and correlations with other continents: evience for a mantle supperplume that broke up Rodinia[J] . Precambrian Res., 2003, 122: 85-109
[10] Li ZX, Li X H, Kinny P D, Wang J. The breakup of Rodinia: did it start with a mantle plume beneath South China? [J]. Earth Planet Sci Lett, 1999,173: 171-181
[11] Ling W L, Gao S, Zhang B R, Li H M, Liu Y, Cheng J P. Neoproterozoic tectonic evolution of the northwestern Yangtze Craton, South China: implications for amalgamation and break-up of the Rodinia Supercontinent[J] . Precam. Res., 2003, 122: 111-140
[12] Rudnick R L, Fountain D M. Nature and composition of the Continental rust: a lower crustal perspective[J]. Reviews of Geophysics, 1995, 33(3): 267-309
[13] Rudnick R L., Gao S. Composition of the Continental crust. In: Rudnick RL(eds.). The Crust.Treaties on Geochemistry,3rd[J].Oxford:Elsevier Pergamon,2003,1-64
[14]Rubatto D.Zircon trace element geochemistry:Partitioning with garnet and the link between U-Pb ages and metamorphism.Chemical Geology,2002,184:123-138
[15]Sun S S.,McDonough W F.,Geo.Soc.London Spec.Publ.,1989,42:313-345
[16]Wang X L,Zhou J C,Qiu J S,et al.Geochemistry of the Meso-to Neoproterozoic basic-acid rocks from Hunan Province,South China:implication for the evolution of the western Jiangnan orogen[J].Precambrian Research,2004,135:79-103
[17]Zhao G C,Cawood P A.Tectonothemal evolution of the Mayuan assemblage in the Cathaysia block:implications for Neoproterozoic collision-related assembley of the South China craton[J].Am.J.Sci.,1999,299:309-339
[18]蔡明海,梁婷,吴德成,皇惠民.广西大厂矿田花岗岩地球化学特征及其构造环境[J].地质科技情报,2004,23(2):57-62
[19]车自成,刘良等.中国及其邻区区域大地构造学[M].北京:科学出版社,2002,395-432
[20]陈海泓,孙枢,李继亮等.雪峰山大地构造的基本特征初探[J].地质科学,1993,28(3):201-210
[21]陈旭,周志毅.奥陶系全球界线层型剖面和点位(GSSP)的研究[J].地层学杂志,2005,29(2):165-170
[22]陈毓川,王登红.广西大厂层状花岗质岩石地质、地球化学特征及成因初探[J].地质论评,1996,42(6):523-530
[23]丁道桂,郭彤楼,刘运黎,翟常博.对江南-雪峰带构造属性的讨论[J].地质通报,2007,26(7):801-809
[24]丁道桂,朱樱,陈凤良等.中下扬子区古生代盆地基底拆离改造与油气领域[J].石油与天然气地质,1991,12(4):376-384
[25]冯增昭,杨玉卿,鲍志东.中国南方石炭纪岩相古地理[J].古地理学报,1999,1(1):75-86
[26]冯增昭,金振奎,柯玉卿等.滇黔桂地区二叠纪岩相古地理[J].北京:地质出版社,1994,217
[27]广西壮族自治区地质局区域地质测量队五分队.区域地质测量报告书[M].南宁:1967,7-72
[28]贵州省地质局.榕江幅1:20万地质图.1963
[29]贵州省地质局.都云幅1:20万地质图.1963
[30]贵州省地质局.罗甸幅1:20万地质图.1965
[31]贵州省地质局.独山幅1:20万地质图.1965
[32]贵州省地质局.江口幅1:20万地质图.1971
[33]贵州省地质局.贵阳幅1:20万地质图.1976
[34]贵州省地质局.黎平幅1:20万地质图.1978
[35]贵州省地矿局.贵州省区域地质志[M].北京:地质出版社,1987,26-48
[36]贵州省地质矿产局.贵州省区域地质志[M].北京:地质出版社,1987,194-226
[37]贵州省地质志[M].北京:地质出版社,1987,13-26,514-525
[38]广西壮族自治区地质局.融安幅1:20万地质图.1967
[39]广西壮族自治区地质局.南丹幅1:20万地质图.1969
[40]葛文春,李献华,李正祥,周汉文,李寄嵎.桂北新元古代两类过铝花岗岩地球化学研究[J].地球化学,2001,30(1):24-35
[41]郭令智等.华南板块构造[M].北京:地质出版社,2001:1-6
[42]郭正吾,邓康龄,韩永辉等.四川盆地形成与演化[M].北京:地质出版社,1996,57-78
[43]韩世庆,王守德,胡惟元.黔东麻江古油藏的发现及其意义[J].石油与天然气地质,1982,3(4):316-327
[44]贺自爱,杨宏,周经才.贵州中三叠世生物礁[J].地质科学,1980,(3):256-264
[45]侯方浩,方少仙,陈景山等.西南地区上古生界海相碳酸盐岩沉积模式及其在油气勘探中的应用[M].成都:成都科技大学出版社,1991,1-20
[46]黄汲清.中国主要地质构造单位.中央地质调查所地质专报[R],甲种 1945,20:1-165
[47]姜月华,岳文浙,业治铮.华南下古生界缺氧事件与黑色页岩及有关矿产[J].有色金属矿产与勘查,1994,3:272-278
[48]李胜荣,高振敏.湘黔寒武系底部黑色岩系贵金属元素来源示踪[J].中国科学(D 辑),2000,30(2):169-174
[49]李曙光,HartSR,郑双根等.中国华北、华南陆块碰撞时代的钐-钕同位素年龄证据[J].中国科学(B辑),1989,19(3):312-319
[50]李钟模.滇黔桂地区二叠纪生物礁[J].贵州地质,1988,5(1):31-42
[51]梁祥济,王福生,乔莉.桂北雪峰期含锡黑云母花岗岩成因的见证[J].地球学报, 1995,1:55-68
[52]廖士范.“黔中隆起”的发生发展与古风化壳铝土矿的形成问题[J].贵州工学院学报,1990,19(1):81-82
[53]林广春,李献华,李武显.川西新元古代基性岩墙群的SHRIMP锆石U-Pb年龄、元素和Nd-Hf同位素地球化学:岩石成因与构造意义[J].中国科D辑地球科学,2006,36(7):630-645
[54]林启祥.贵州紫云晚古生代生物礁的性质和演化[J].地球科学-中国地质大学学报,1992,17(1):301-307
[55]刘特民.黔中何时隆起[J].贵州地质,1987,4(1):65-71
[56]刘育燕,杨巍然,森永速男,等.华北、秦岭及扬子陆块的若干古地磁研究结果[J].地球科学-中国地质大学学报,1993,18(5):635-641
[57]卢华夏.关于华夏古陆[J].高校地质学报,2006,12(4):413-417
[58]吕炳全,王红罡,胡望水,等.扬子地块东南古生代上升流沉积相及其与烃源岩的关系[J].海洋地质与第四纪地质,2004,24(4):29-35
[59]罗志立.四川盆地基底结构的新认识[J].成都理工学院学报,1998,25(2):191-200
[60]马力,陈焕疆,甘克文,等.中国南方大地构造和海相油气地质[J].北京:地质出版社,2004,502-567
[61]马文璞,丘元禧,何丰盛.江南隆起上的下古生界缺失带-华南加里东前陆褶冲带的标志[J].现代地质,1995,9(3):320-324
[62]毛景文,谢贵青,李晓峰,等.华南地区中生代大规模成矿作用与岩石圈多阶段伸展[J].地学前缘(中国地质大学,北京),2004,11(1):45-55
[63]毛景文,张宗清,董宝林.江南古陆南缘四堡群钐钕同位素年龄研究[J].地质论评,1990,36(3):264-268
[64]毛景文、陈毓川.关于桂北四堡期花岗闪长岩成因的探讨[J].岩石矿物学杂志,1988,7(4):289-298
[65]梅冥相.论“黔中古陆”[J].贵州地质,1994,11(3):0-5
[66]牛新生,冯常茂,刘进.黔中隆起的形成时间及形成机制探讨[J].海相油气地质,2007,12(2):46-50
[67]彭军,陈景山,陈洪德,等.黔桂地区石炭纪Ⅰ型层序界面沉积记录及成因分析[J].地球学报,2000,21(4):433-440
[68]丘元禧,马文璞,范小林,等.“雪峰古陆”加里东期的构造性质和构造演化[J].中 国区域地质,1996,(2):150-160
[69]邱检生,周金城,张光辉,凌文黎.桂北前寒武纪花岗岩类岩石的地球化学与成因[J].岩石矿物学杂志,2002,20(3):197-208.
[70]沙庆安,吴望始,傅家谟.黔桂地区二叠系综合研究-兼论含油气性.北京:科学出版社,1990,207
[71]沈志达,梅冥相,曾羽.贵州太康运动的地层学效应-兼论“黔中古陆”的形成[J].贵州地质,1990,7(2):91-97
[72]舒良树,周国庆,施央申,等.江南造山带东段高压变质蓝片及其地质时代研究[J].科学通报,1993,38(20):1879-1882
[73]孙涛.新编华南花岗岩分布图及其说明.地质通报,2006,25(3):332-335
[74]腾格尔,胡凯,高长林,等.上扬子东南缘下组合优质烃源岩的发育及生烃潜力评价[J].石油实验地质,2006,28(4):359-365
[75]田海芹,沃玉进,郑磊,等.中国南方中、古生界油气勘探方向之思考-近源深埋逆断带可能是今后中国南方中、古生界油气勘探的主战场[J].南方油气,2002,15(3):236-243
[76]涂光炽.华南花岗岩类的地球化学[J].科学出版社,1979,357-373.
[77]汪啸风,IanMetcalfe,简平.金沙江缝合带构造地层划分及时代厘定[J].中国科学(D辑),1999,29(4):289-297
[78]王德滋,周新民,孙幼群.华南前寒武纪慢源花岗岩类的基本特征[J].桂林冶金地质学院学报,1982,(4):1-9
[79]王鸿祯,乔秀夫.中国元古代构造单元及其边界性质[J].前寒武纪地质,1986,(3):1-14
[80]王练成,李达周,张旗,等.四川理塘蛇绿混杂岩-一个以火山岩为基质的蛇绿混杂岩[J].岩石学报,1985,1(2):17-27
[81]王懋基.黑水-泉州地学断而的重磁解释[J].地球物理学报,1994,37(3):321-329
[82]王小多.雪峰山构造带及其邻区磁性结构研究[D].西安:西北大学,2008
[83]王晓青,刘祖彝.湖南长常区地质志,前湖南地质调查所.1936,乙种:(1)
[84]王孝磊,周金城,邱检生,等.桂北新元古代强过铝花岗岩的成因:锆石年代学和Hf同位素制约[J].岩石学报,2006,22(2):326-342
[85]吴汉宁,常承法,刘椿,等.依据古地磁资料探讨华北和华南快体运动及其对秦岭 造山带构造演化的影响[J].地质科学,1990,25(3):201-214
[86]吴浩若.重新解释广西运动[J].科学通报,2000,45(5):555-558
[87]许靖华,孙枢,李继亮.是华南造山带而不是华南地台[J].中国科学(B辑),1987,17(10):1107-1115
[88]许靖华,孙枢.寒武纪生物爆发前的海洋[J].地质科学,1986,1:1-10
[89]许靖华.薄壳板块构造模式与冲撞型造山运动[J].中国科学,B辑.1980,(1):1081-1089
[90]许靖华.中国南方大地构造的几个问题[J].(武汉地质学院)地质科技情报,1987,6(2):13-27
[91]杨斌,廖宗廷.广西大厂礁灰岩区碳沥青的产状特征及其与多金属成矿关系探讨[J].沉积学报,1999,17(增刊):668-674
[92]尹赞勋.中国南部志留纪地层之分类与对比[J].中国地质学会志,1949,29:162
[93]袁照令,李大明,易顺华.对保靖-慈利逆冲断裂带的一些认识[J].地质与勘探,2000,36(5):59-61
[94]袁正新,谢岩豹.华南地区加里东期构造运动时空分布的新认识.华南地质与矿产,1997,V4
[95]曾雯,周汉文,钟增球,等.黔东南新元古代岩浆岩单颗粒锆石U-Pb年龄及其构造意义[J].地球化学,2005,34(6):548-556
[96]曾昭光,唐云辉,彭慈刚,等.黔桂边界四堡群中高压变质矿物的发现及其地质意义[J].贵州省地质,2005,22(1):46-49
[97]张桂林,梁金城,刘之葵,等.桂北元古代本洞花岗闪长岩体中发现左旋-正滑型韧性剪切带[J].桂林工学院学报,2003,23(1):1-4
[98]张永刚,马宗晋,王国力,等.中国南方海相油气成藏模式分析[J].地质学报,2007,81(2):236-243
[99]张正华,王治华,李昌全.黔南二叠纪地层[J].贵阳:贵州人民出版社,1988,113
[100]赵志东,王炯章,李载沃,等.中国石油地质志,第十一卷(滇黔桂油气区)[M].北京:石油工业出版社,1987,81-116
[101]赵子杰,马大铨.桂北前寒武纪花岗岩本洞、三防岩体的研究[A].宜昌地质矿产研究所.南岭地质矿产科研报告集(一)[C].武汉:武汉地质学院出版社,1987,1-27
[102]赵宗举,朱琰,李大成,等.中国南方构造变形对油气藏的控制作用[J].石油与 天然气地质,2002,23(1):19-25
[103]赵宗举,朱琰,徐云俊.中国南方古生界-中生界油气藏成藏规律及勘探方向[J].地质学报,2004,78(5):710-720
[104]赵宗举.中国南方古隆起对中、古生界原生油气藏的控制作用[J].石油实验地质,2003,25(1):20-25
[105]周金城,王孝磊,邱检生.江南造山带是否格林威尔期造山带?—关于华南前寒武纪地质的几个问题[J].高校地质学报,2008,14(1):64-72
[106]周金城,王孝磊,邱检生.江南造山带西段岩浆作用特征[J].高校地质学报,2005,11(4):527-533
[107]周金城,王孝磊,裘检生,等.南桥高度亏损N-MORB的发现及其地质意义[J].岩石矿物杂志,2003,22(3):211-216