南黄海盆地北部坳陷构造演化及沉积相研究
|
摘要
南黄海盆地是叠合于下扬子地台前震旦系变质岩基底之上的一个多旋回叠合盆地。北部坳陷是南黄海盆地的次级构造单元,北以千里岩隆起为界,南部地层超覆于南黄海盆地中部隆起之上,整体结构为北断南超,总面积约51000Km2。北部坳陷又可分为九个三级构造单元,包括六个负向构造单元(东北凹、北凹、中凹、西凹、南凹、东凹)和三个正向构造单元(北凸、西凸、南凸)。
南黄海盆地北部坳陷自1975年钻探黄二井以来,已经有约三十年的勘探历史。我国在北凹的泰州组岩芯裂隙中见到了液体原油,韩国有2口井见到了气显示,但均未获得商业性油气发现。
本文以构造地质学、沉积学、石油地质学理论为基础,利用地震剖面、钻井等地球物理资料,通过构造样式分析、平衡剖面恢复、沉降史分析、沉积相分析等方法,研究该区域的构造演化过程与沉积特征,并进行初步的油气远景分析。
研究表明,南黄海盆地北部坳陷构造演化可分为三个阶段,即海相盆地演化阶段(Z-T),陆相断陷盆地演化阶段(K-E)和坳陷盆地演化阶段(N-Q)。在海相盆地演化阶段,南黄海盆地北部坳陷沉积了扬子型基底盖层。地层发育较为齐全,基本无沉积间断。在陆相断陷盆地演化阶段,由于张性断裂的发展,产生了活动性强、分布局限的陆相断陷盆地。到了坳陷盆地演化阶段,南黄海盆地北部坳陷区域性沉降。
南黄海盆地北部坳陷的构造样式主要有两类,一类是压性断块和基底逆冲断层,另一类是张性断块,这两类均为基底卷入型构造样式。基底逆冲断层主要位于千里岩隆起南缘,张性断块在坳陷内广泛发育。
正、负反转构造在南黄海盆地北部坳陷内均有发育。负反转构造主要分布于千里岩隆起南侧。正反转构造主要分布于东北凹、北凹、中凹和南凹。反转期主要有渐新世和上新世末两期,后者的影响相对较小。构造反转与太平洋板块与欧亚板块的汇聚速率变化有关。
南黄海盆地北部坳陷沉降曲线呈两段式,第一段曲线较陡,沉降速率快,对应于断陷阶段；第二段曲线变缓,对应于坳陷阶段。断陷阶段又可进一步分为初始裂陷阶段,强裂陷阶段,裂陷萎缩阶段,反转隆升阶段,整体上具有伸展作用控制下的幕式旋回演化特征。北凹、中凹、南凹有着近似的沉降史,晚白垩世即进入快速沉降期,一直到古新世保持着较高的沉积速率,东北凹则是在古新世进入裂陷高峰期。
南黄海盆地北部坳陷从晚白垩世到始新世呈现河流相—湖泊相—河流相的沉积演化特征。晚白垩世时主要发育河流相沉积,至上白垩统泰州组,沉积范围缩小,主要分布于北凹和东北凹,发育有河流相和湖相沉积。阜宁组沉积时期,从阜一段到阜四段,随着水体的加深,沉积物由河流相沉积逐渐转变为湖相沉积。戴南组沉积时期,沉积范围比阜宁组有所缩小,以河流相沉积为主。到三垛组沉积时期,地形逐渐被夷平,主要发育河流相沉积。
不同构造阶段的构造格局对盆地的沉积充填具有明显的控制作用。初始裂陷期和强裂陷期的沉积充填,沉降速率快,沉积厚度大,沉积区域受同沉积断裂控制,呈近东西向条带状分布。总体上沉积中心位于北凹和东北凹北界断裂陡坡带。同沉积断裂的差异活动和演化导致沉积中心的迁移。初始裂陷期沉积以河流相为主,随着水体加深湖相沉积逐渐发育。裂陷萎缩期的沉积充填,沉降速率慢,沉积厚度小,沉积范围大。由于遭受了广泛的剥蚀,局部构造活动的差异、次级地堑和地垒等可造成局部残余厚度的明显变化。裂陷萎缩期水体较浅,以河流相沉积为主。
South Yellow Sea Basin is a multicycle superimposed basin forming on the pre-Sinian metamorphic rock basement of the Lower Yangtze Platform.North Depression is the secondary structual unit of South Yellow Sea Basin,making Qianliyan Uplift as the northern boundary.Its southern stratum overlaps the Middle Uplift of South Yellow Sea Basin,and on the whole it downfaults to north and overlaps to the south,with a total area of about 51,000 km2.North Depression can be devided into 9 third-level structural units,including 6 negative structural units(Northeast Sag,North Sag,Middle Sag,West Sag,South Sag and East Sag) and 3 positive structural units(North Salient,West Salient and South Salient).
Since well Huang 2 was drilled in 1975 in North Depression of South Yellow Sea Basin,it has been almost 30 years already.China has found liquid crude oil in the crack of Taizhou Formation in North Sag,and Korea has found gas show in its 2 wells,but neither of the two countries get commercial gas and oil flows so far.
On the base of structural geology,sendimentology and petroleum geology,geophysical data such as seismic profiles and wells are used to study the structural evolution,sedimentary characteristics and hydrocarbon potential of this region by means of structural style analysis,balanced cross-section restoration,subsidence history analysis and sedimentary facies analysis.
The result shows that the structural evolution of North Depression of South Yellow Sea Basin can be divided into three stages:the marine basin stage,the continental rift basin stage and depression basin stage. Basement cover of Yangtze style was deposited in North Depression of South Yellow Sea Basin in the marine basin stage.The sequence of the strata was well developed and there was basically no hiatus. Owing to the development of tensional faults,active continental rift basion with limited distribution was developed in the continental rift basin stage. The depression basin stage was the regional subsidence stage of North Depression of South Yellow Sea Basin.
There are mainly two kinds of structural styles in the North Depression of South Yellow Sea Basin:compressive block and basement-involved thrust style and tensional block style.Both of them are basement-involved type.The basement-involved thrust is mainly located in the southern edge of Qianliyan Uplift,and the tensional blocks are widely developed.
Both positive inversion tectonics and negative inversion tectonics can be identified in the North Depression of South Yellow Sea Basin.The negative inversion tectonics are mailly distributed to the south of Qianliyan Uplift.The positive inversion tectonics are mainly distributed in northeast sag,north sag,middle sag and south sag.The inversion period is Oligocene and late Pliocene.The inversion is related to the convergence rate between Paciffic plate and Eurasia plate.
The subsidence curve of North Depression of South Yellow Sea Basin can be divided into two sections.The steep section corresponds to the rift phase in which subsidence rate is high,and the slow section corresponds to the depression phase in which subsidence rate is low.The rift phase can further be diveded into initial rifting stage(Late Cretaceous),high rifting stage(Palaeocene),rifting atrophy stage(Eocene) and inversion-uplifting stage(Oligocene).On the whole it shows the characteristic of episodic rift basin cycle evolution under the control of extensional action.
The sedimentary evolution characteristic of North Depression of South Yellow Sea Basin from Late Cretaceous to Eocene can be summarized to river facies-lacustrine facies-river facies.Sedimentation of river facies was well developed in Late Cretaceous.The Late Cretaceous Taizhou Formation which developed sedimentation of river facies and lacustrine facies was districted only in North Sag and Northeast Sag.With the deepening of water,the sedimentary facies of Palaeocene Funing-1 Member to Palaeocene Funing-4 Member gradually changed from river facies to lacustrine facies.The Eocene Dainan Formation developed sedimentation of river facies in a smaller area compared with Funing Formation. The Eocene Sanduo Formation developed sedimentation of river facies after planation.
The structural framework has control action on depositional filling of the basin.In the initial rifting stage and high rifting stage the subsidence rate is high and the sedimentation is thick.The sedimentation is distributed in EW trending belts controlled by synsedimentary faults.The depocenter is mainly located in steep slope zone of the northern border fault of north sag and northeast sag.The differential activity and evolution of the synsedimentary fault makes the transfer of depocenter.The sedimentation of river facies is well developed in the initial rifting stage. With the deepening of water,the sedimentary facies gradually changes to lacustrine facies. In the rifting atrophy stage the subsidence rate is low and the sedimentation is thin and wide.Owing to wide-ranging denudation,the difference of local structural activities,secondary horsts and grabens can make obvious differerce of local residual thickness.The river facies are well developed in the rifting atrophy stage.
南黄海盆地北部坳陷自1975年钻探黄二井以来,已经有约三十年的勘探历史。我国在北凹的泰州组岩芯裂隙中见到了液体原油,韩国有2口井见到了气显示,但均未获得商业性油气发现。
本文以构造地质学、沉积学、石油地质学理论为基础,利用地震剖面、钻井等地球物理资料,通过构造样式分析、平衡剖面恢复、沉降史分析、沉积相分析等方法,研究该区域的构造演化过程与沉积特征,并进行初步的油气远景分析。
研究表明,南黄海盆地北部坳陷构造演化可分为三个阶段,即海相盆地演化阶段(Z-T),陆相断陷盆地演化阶段(K-E)和坳陷盆地演化阶段(N-Q)。在海相盆地演化阶段,南黄海盆地北部坳陷沉积了扬子型基底盖层。地层发育较为齐全,基本无沉积间断。在陆相断陷盆地演化阶段,由于张性断裂的发展,产生了活动性强、分布局限的陆相断陷盆地。到了坳陷盆地演化阶段,南黄海盆地北部坳陷区域性沉降。
南黄海盆地北部坳陷的构造样式主要有两类,一类是压性断块和基底逆冲断层,另一类是张性断块,这两类均为基底卷入型构造样式。基底逆冲断层主要位于千里岩隆起南缘,张性断块在坳陷内广泛发育。
正、负反转构造在南黄海盆地北部坳陷内均有发育。负反转构造主要分布于千里岩隆起南侧。正反转构造主要分布于东北凹、北凹、中凹和南凹。反转期主要有渐新世和上新世末两期,后者的影响相对较小。构造反转与太平洋板块与欧亚板块的汇聚速率变化有关。
南黄海盆地北部坳陷沉降曲线呈两段式,第一段曲线较陡,沉降速率快,对应于断陷阶段；第二段曲线变缓,对应于坳陷阶段。断陷阶段又可进一步分为初始裂陷阶段,强裂陷阶段,裂陷萎缩阶段,反转隆升阶段,整体上具有伸展作用控制下的幕式旋回演化特征。北凹、中凹、南凹有着近似的沉降史,晚白垩世即进入快速沉降期,一直到古新世保持着较高的沉积速率,东北凹则是在古新世进入裂陷高峰期。
南黄海盆地北部坳陷从晚白垩世到始新世呈现河流相—湖泊相—河流相的沉积演化特征。晚白垩世时主要发育河流相沉积,至上白垩统泰州组,沉积范围缩小,主要分布于北凹和东北凹,发育有河流相和湖相沉积。阜宁组沉积时期,从阜一段到阜四段,随着水体的加深,沉积物由河流相沉积逐渐转变为湖相沉积。戴南组沉积时期,沉积范围比阜宁组有所缩小,以河流相沉积为主。到三垛组沉积时期,地形逐渐被夷平,主要发育河流相沉积。
不同构造阶段的构造格局对盆地的沉积充填具有明显的控制作用。初始裂陷期和强裂陷期的沉积充填,沉降速率快,沉积厚度大,沉积区域受同沉积断裂控制,呈近东西向条带状分布。总体上沉积中心位于北凹和东北凹北界断裂陡坡带。同沉积断裂的差异活动和演化导致沉积中心的迁移。初始裂陷期沉积以河流相为主,随着水体加深湖相沉积逐渐发育。裂陷萎缩期的沉积充填,沉降速率慢,沉积厚度小,沉积范围大。由于遭受了广泛的剥蚀,局部构造活动的差异、次级地堑和地垒等可造成局部残余厚度的明显变化。裂陷萎缩期水体较浅,以河流相沉积为主。
South Yellow Sea Basin is a multicycle superimposed basin forming on the pre-Sinian metamorphic rock basement of the Lower Yangtze Platform.North Depression is the secondary structual unit of South Yellow Sea Basin,making Qianliyan Uplift as the northern boundary.Its southern stratum overlaps the Middle Uplift of South Yellow Sea Basin,and on the whole it downfaults to north and overlaps to the south,with a total area of about 51,000 km2.North Depression can be devided into 9 third-level structural units,including 6 negative structural units(Northeast Sag,North Sag,Middle Sag,West Sag,South Sag and East Sag) and 3 positive structural units(North Salient,West Salient and South Salient).
Since well Huang 2 was drilled in 1975 in North Depression of South Yellow Sea Basin,it has been almost 30 years already.China has found liquid crude oil in the crack of Taizhou Formation in North Sag,and Korea has found gas show in its 2 wells,but neither of the two countries get commercial gas and oil flows so far.
On the base of structural geology,sendimentology and petroleum geology,geophysical data such as seismic profiles and wells are used to study the structural evolution,sedimentary characteristics and hydrocarbon potential of this region by means of structural style analysis,balanced cross-section restoration,subsidence history analysis and sedimentary facies analysis.
The result shows that the structural evolution of North Depression of South Yellow Sea Basin can be divided into three stages:the marine basin stage,the continental rift basin stage and depression basin stage. Basement cover of Yangtze style was deposited in North Depression of South Yellow Sea Basin in the marine basin stage.The sequence of the strata was well developed and there was basically no hiatus. Owing to the development of tensional faults,active continental rift basion with limited distribution was developed in the continental rift basin stage. The depression basin stage was the regional subsidence stage of North Depression of South Yellow Sea Basin.
There are mainly two kinds of structural styles in the North Depression of South Yellow Sea Basin:compressive block and basement-involved thrust style and tensional block style.Both of them are basement-involved type.The basement-involved thrust is mainly located in the southern edge of Qianliyan Uplift,and the tensional blocks are widely developed.
Both positive inversion tectonics and negative inversion tectonics can be identified in the North Depression of South Yellow Sea Basin.The negative inversion tectonics are mailly distributed to the south of Qianliyan Uplift.The positive inversion tectonics are mainly distributed in northeast sag,north sag,middle sag and south sag.The inversion period is Oligocene and late Pliocene.The inversion is related to the convergence rate between Paciffic plate and Eurasia plate.
The subsidence curve of North Depression of South Yellow Sea Basin can be divided into two sections.The steep section corresponds to the rift phase in which subsidence rate is high,and the slow section corresponds to the depression phase in which subsidence rate is low.The rift phase can further be diveded into initial rifting stage(Late Cretaceous),high rifting stage(Palaeocene),rifting atrophy stage(Eocene) and inversion-uplifting stage(Oligocene).On the whole it shows the characteristic of episodic rift basin cycle evolution under the control of extensional action.
The sedimentary evolution characteristic of North Depression of South Yellow Sea Basin from Late Cretaceous to Eocene can be summarized to river facies-lacustrine facies-river facies.Sedimentation of river facies was well developed in Late Cretaceous.The Late Cretaceous Taizhou Formation which developed sedimentation of river facies and lacustrine facies was districted only in North Sag and Northeast Sag.With the deepening of water,the sedimentary facies of Palaeocene Funing-1 Member to Palaeocene Funing-4 Member gradually changed from river facies to lacustrine facies.The Eocene Dainan Formation developed sedimentation of river facies in a smaller area compared with Funing Formation. The Eocene Sanduo Formation developed sedimentation of river facies after planation.
The structural framework has control action on depositional filling of the basin.In the initial rifting stage and high rifting stage the subsidence rate is high and the sedimentation is thick.The sedimentation is distributed in EW trending belts controlled by synsedimentary faults.The depocenter is mainly located in steep slope zone of the northern border fault of north sag and northeast sag.The differential activity and evolution of the synsedimentary fault makes the transfer of depocenter.The sedimentation of river facies is well developed in the initial rifting stage. With the deepening of water,the sedimentary facies gradually changes to lacustrine facies. In the rifting atrophy stage the subsidence rate is low and the sedimentation is thin and wide.Owing to wide-ranging denudation,the difference of local structural activities,secondary horsts and grabens can make obvious differerce of local residual thickness.The river facies are well developed in the rifting atrophy stage.
引文
[1]蔡乾忠.中国海域油气地质学.北京：海洋出版社,2005.131～150
[2]尹延鸿,汪企浩,张训华等.黄东海地区及其邻域地质构造单元划分.我国专属经济区和大陆架勘测研究论文集.北京：海洋出版社,2002.22～53
[3]邢涛,张训华,张维冈.南黄海地球物理调查研究现状.海洋地质动态.2005，21(6)：1～4
[4]袁文光.渤海、黄海、东海的地球物理调查史.海洋地质与第四纪地质.1989.9(3)：19～27
[5]Proceedings of the second Korea-China international symposium on petroleum potential of the Yellow Sea and the East China Sea,Korea Petroleum Development Corp.and China National Offshore Oil Corp..9-106
[6]Korea/China Symposium Sedimentary Basins in Yellow Sea and Adjacent Areas Abatract, Korea,2001:2-17
[7]Sangheon Yi, Songsuk Yi, David J. Batten, Heysu Yun, Se-Jin Park. Cretaceous and Cenozoic non-marine deposits of the Northern South Yellow Sea Basin, offshore western Korea: palynostratigraphy and palaeoenvironments.Palaeogeography, Palaeoclimatology, Palaeoecology, 2003,191(1):15-44
[8]金翔龙,喻普之.黄海、东海地质构造.黄东海地质.北京：科学出版社,1982.12～26
[9]张文佑.中国及邻区海陆大地构造.北京：科学出版社,1986.3～15
[10]朱夏.关于中国大陆边缘构造演化.海洋地质与第四纪地质,1987,7(3)：115～120
[11]秦蕴珊,赵一阳,陈丽蓉.黄海地质.北京：海洋出版社,1989.9～17
[12]刘光鼎.中国海区及邻域地质地球物理系列图(1/500万).北京：地质出版社,1992
[13]郭玉贵,李延成,许东禹.黄东海大陆架及邻域大地构造演化史.海洋地质与第四纪地质.1997,17(1)：1～12
[14]许东禹,刘锡清,张训华.中国近海地质.北京：地质出版社,1997：210～239
[15]罗明.中国海洋石油总公司志.北京：改革出版社,1998.146～147
[16]李刚,陈建文,肖国林.南黄海海域的海相中-古生界油气远景.海洋地质动态.2003,19(8)：12～16
[17]刘守全,蔡乾忠,莫杰.中国海域油气勘探的新领域-应当重视海域中生界油气资源.中国地质.2001,28(11)：4～9
[18]戴春山,李刚.黄海海域前第三系及油气勘探.海洋地质动态,2002,18(11)：21～22
[19]戴春山,李刚,蔡峰.黄海前第三系及油气勘探方向.中国海上油气地质,2003,17(4)：225～231
[20]蔡乾忠.中国东部与朝鲜大地构造单元对应划分.海洋地质与第四纪地质,1995,15(1)：7～24
[21]蔡乾忠.黄海含油气盆地区域地质与大地构造环境.海洋地质动态,2002,18(11)：8～12
[22]马寅生.中国东部-朝鲜半岛海陆构造格局及含油气盆地特征.北京：地质出版社,2006.261～290
[23]Chough S. K.,Kwon S. T.,Ree J. H.,Choi D. K..Tectonic and sedimentary evolution of the Korean peninsula:a review and new view.Earth-Science Reviews,2000,52:175～235
Mancheol.黄海深部结构与中朝-扬子块体结合带在海区位置的地球物理研究.地学前缘,2004,11(3)：5～61
[25]黄福林.黄、渤海活动断裂初探.海洋地质与第四纪地质.1992,12(4)：21～28
[26]郝天珧,Suh Mancheol黄海中央断裂带的地球物理证据及其与边缘海演化的关系.地球物理学报.2003.46(2)：179～184
[27]郝天珧,Suh Mancheol.根据重力数据研究黄海周边断裂带在海区的延伸.地球物理学报,2002,45(3)：385～397
[28]Harding T.P.,Lowell J.D.,Structural styles,their plate-tectonic habitats,and hydrocarbon traps in petroleum provinces.AAPG.Bulletin,1983,63(7):1016～1085
[29]Lowell J.D..Structural styles in petroleum exploration.Tulsa:Oil and Gas Consultants International.Inc.1985.66～88
[30]胡见义,黄第藩.中国陆相石油地质理论基础.北京：石油工业出版社,1991.55～78
[31]姚永坚.南黄海构造样式的特征及含油气性.海洋地质动态.2002,18(11)：30～32
[32]汪泽成,刘和甫,段周芳.黄骅坳陷中新生代构造负反转分析.地球科学-中国地质大学学报,1998,23(3)：289～293
[33]陈洁,董冬,邱明文.1999.济阳坳陷内的负反转构造及其石油地质意义.石油实验地质,21(3)：201～206
[34]贾霍甫,徐思煌.东营凹陷通王地区负反转构造与断块型古潜山的形成.油气地质与采收率.2006,13(3)：19～21
[35]王同和,王根海,赵宗举.中国含油气盆地的反转构造样式及其油气聚集.海相油气地质,2001,6(3)：27～37
[36]周建生,杨长春.渤海湾地区前第三系构造样式分布特征研究.地球物理学进展2007,22(5)：1416～1426
[37]蔡希源,王根海,迟元林.中国油气区反转构造.北京：石油工业出版社,2001.17～21
[38]Glennie K. W.,P. L. Boeger.Sole pit inversion tectonics.Petroleum Geology of the Continental Shelf of Northwest Europe.1984:110～120
[39]Bally A. W..Tectogenese et sismique reflexion.Bulletin Societe Geologique France.1984,7: 279-285
[40]Harding T.P..Seismic characteristics and identification of negative flower structures,positive flower structures,and positive structural inversion.AAPG Bulletin,1985,69(4):582～600
[41]Williams G. D.,Powell C. M.,Cooper M. A..Geometry and kinematics of inversion tectonics.Inversion Tectonics.Geological society special publication.1989,44:3～15
[42]Cooper M. A.,Williams G. D..Inversion Tectonics.London:The Geo.Soc.,1989.5～11 [43]Mitra S.. Geometry and kinematic evoluation of inversion. AAPG Bulletin,1993,77(7):159-191
[44]胡望水.塔里木盆地反转构造与油气聚集.新疆石油地质,1995,16(2)：89～95
[45]胡望水,卫拥军,张自其.辽河盆地反转期构造特征.西安石油学院学报(自然科学版),2002,17(5)：5～13
[46]杨克绳.从地震信息划分三种不同程度的正、负反转构造样式.海相油气地质.2006,11(1)：21-29
[47]胡望水,周延军,刘学锋.正反转构造综合分析原理和方法.北京：石油工业出版社,2001.17～22
[48]McClay K.R.,Buchanan P.G..Thrust faults in inverted extensional basins.In:McClay K.R.ed.Thrust Tectonics.London:Chapman-Hall,1991.93～104
[49]Green P.F.,Duddy I.R.,Bray R.J..Application of thermal history reconstruction in inverted basins.Buchanan J.G.,Buchanan P,G.(eds)basin inversion.Geological Society Specical Publication,1995.88:149-166
[50]Uliana M.A.,Arteaga M.E.,Legarreta..Inversion structures and hydrocarbon occurrence in Argentina.Buchanan J.G..Buchanan P.G.(eds)basin inversion.Geological Society Specical Publication,1995.88:211-234
[51]汪新文.中国东北地区中-新生代盆地构造演化与油气关系.北京：地质出版社.2007.105～115
[52]陈志勇,葛和平.西湖凹陷反转构造与油气聚集.中国海上油气地质,2003,17(1)：21～24
[53]Hayward A. B., Graham H.R.. Some Geometrical characteristics of inversion. M. A. Cooper and G. D. Williams, eds, Inversion Tectonics.Geological Society Special Publication,1989.44: 34-56
[54]胡望水.正反转构造成因类型.江汉石油学院学报,1993,15(4)：19～25
[55]胡望水,刘学锋,吕新华.论正反转构造的分类.新疆石油地质,2000,21(1)：5～8
[56]刘和甫.伸展构造及其反转作用.地学前缘,1995,2(1)：113～123
[57]陈昭年,陈布科.松辽盆地反转构造与油气聚集成都理工学院学报,1996,23(4)：50～57
[58]吴珍汉.中国大陆及邻区新生代构造-地貌演化过程与机理.北京：地质出版社,2001.203～207
[59]任建业,李思田.西太平洋边缘海盆地的扩张过程和动力学背景.地学前缘,2000,7(3)：203-211
[60]Jurdy D.M.. Relative plate motions and the formation of marginal basins. J. Geophys. Res., 1979,84(B12):6796～6802
[61]Cox A., Engebretson D.. Change in motion of Pacific Plate at 5 Myr BP. Nature, 1985,313(6002):472-474
[62]Northrup C.J.,Royden L.H.,Burchfiel B.C.. Motion of the Pacific Plate relative to Eurasia and its potential relation to Cenozoic extension along the eastern margin of Eurasia. Geology.1995, 23(8):719-722
[63]陈昭年,陈发景.反转构造与油气圈闭.地学前缘,1995.2：96-102
[64]伊恩.勒奇.盆地分析的定量方法.第一卷.魏增璞,冷鹏华,张博闻译.北京：石油工业出版社,1996.7～41
[65]Allen P. A.,Allen J. R..Basin analysis principles & application.Oxford,London:Blackwell Scientific Publication,1990.349～366
[66]陆克政,朱筱敏,漆家福.含油气盆地分析.北京：石油大学出版社,2003.77～89
[67]Lawrence D.T.,M.Doyle,T.Aignef.Stratigraphic simulation of sedimentary basins:concepts and calibration.AAPG Bulletin,1990,74(3):273-295
[68]陈发景.伸展断陷盆地分析.北京：地质出版社,2004.93～107
[69]Steckler M. S.,Watts A. B..Subsidence of the Atlantic-type continental margin of New York.Earth Planetary Sci.,Letter,1978(41):1～13
[70]Bond G. C.,Komiz M. A.. Construction of tectonic subsidence curves for the early Paleozoic miogeocline,southern Canadian Rocky Mountains:Implications for subsidence mechanisms,age of breakup,and Crustal thinning.G.S.A.,Bull.,1984(95):155～173
[71]张功成.裂陷盆地分析原理和方法-以松辽盆地为例.北京：石油工业出版社,1996：162～176
[72]杨庚,钱祥麟,郭华.塔里木北缘库车陆内挠曲盆地构造演化与油气远景评价.北京：地质出版社,2003.29～39
[73]郝石生等.恢复地层剥蚀厚度的最优化方法.沉积学报,1988,6(4)：27～35
[74]何生,王青玲.关于用镜质体反射率恢复地层剥蚀厚度的讨论.地质论评,1989,35(2)：39～44
[75]张海军、曹强,孙建峰.地层剥蚀厚度恢复研究-以南黄海北部盆地东北凹陷为例.石油地质，2008(5)：21～25
[76]刘景彦,林畅松,肖建新.等著.东海西湖凹陷第三系主要不整合面的特征、剥蚀量的分布及其意义.现代地质.1999,13(4)：432～438
[77]陈伟.平衡剖面计算机模拟及其应用.北京：科学出版社,1993.4～26
[78]贾维民,杜秀霞,译.平衡地质剖面.武汉：中国地质大学出版社,1991.11～15
[79]王运所,刘亚洲,张孝义,等.平衡剖面的制作流程及其地质意义.长安大学学报：地球科学版,2003，25(1)：2832
[80]张明山,陈发景.平衡剖面技术应用的条件及实例分析.石油地球物理勘探,1998,33(4)：532～540
[81]Dahlen C.D.A.Balanced cross sections.Canadian Journal of Earth Sciences,1969(6):743-757
[82]Reks I. J., Gray D. R.. Strain patterns and shortening in a folded thrust sheet:an example from the southern Appalachians.Tectonophysics,1983,93(1):99～128
[83]Allen M. B.,Vincent S. J.,Wheeler P. J..Late Cenozoic tectonics of the Kepingtage thrust zone: interactions of the Tien Shan and Tarim Basin,Northwest China.Tectonics,1999,18(4):639-654
[84]Taboada A., Rivera L. A., Fuenzalida A., eta.l Geodynamics of the northern Andes: subductions and intracontinental deformation(Colombia).Tectonics,2000,19(5):787～813
[85]Depaor D. G. Balanced section in thrust belts:Part 1, Construction.AAPG Bulletin,1988, 72(1):73～90
[86]Thomas F,,Martin H.. Folded basement-cored tectonic wedges a long the northern edge of the Amadeus Basin,Central Australia:evaluation of orogenic shortening. Journal of Structural Geology,1999,21(4):399-412
[87]Shahram S., Jean L..Variation of structural style and basin evolution in the central Zagros(Izeh zone and Dezful Embayment),Iran.Marine and Petroleum Geology,2004,21(5):535～554
[88]Mouthereau F.,Lacombe O.,Deffontaines B.,eta.l Deformation history of the southwestern Taiwan foreland thrust belt:insights from tectono-sedimentary analyses and balanced cross-sections.Tectonophysics,2001,333(1):293～322
[89]Alain M., Bernard D. G.,Antonio T.D. R., eta.Structural geometry in the eastern Pyrenees and western Gulf of Lion (Western Mediterranean).Journal of Structural Geology,2001,23(11):1701～ 1726
[90]施泽进,彭大钧,施央申.苏北溱潼凹陷的拉张量研究及构造运动强度分析.大地构造与成矿学,1994,18(1)：43～52
[91]颜丹平,田崇鲁,孟令波.伸展构造盆地的平衡剖面及其构造意义-以松辽盆地南部为例.地球科学-中国地质大学学报,2003,28(3)：275～280
[92]Elliot D..The construction of balanced cross-sections.Journal of Structural Geology,1983(5): 101～103
[93]Woodward N. B.. Valley and ridge thrust belt:balanced structural sections, Pennsylvania to Alabma. Studies in Geology,1985.227～231
[94]Schonborn G.. Balancing cross sections with kinematic constraints:the dolomites (northern Italy).Tectonics,1999,18(3):527～545
[95]Gibbs A..Balanced cross-section construction from seismic sections in areas of extensional tectonics. Journal of Structural Geology,1983,5:153～160
[96]Park. Seismic stratigraphy of the Tertiary Eocene formation of the south Heuksan basin in the Yellow sea.Master's thesis. Kongju National University,1995.5～17
[97]徐万哲.南黄海Heuksan盆地的地震地层学研究,地球物理学进展.2003，18(4)：679～691
[98]徐怀大,王世凤,陈开远.地震地层学解释基础.武汉：中国地质大学出版社.1990.15～29
[99]张万选,张厚福,曾洪流.陆相断陷盆地区域地震地层学研究.东营：石油大学出版社.1998.12～26
[100]张万选,张厚福,曾洪流.陆相地震地层学.东营：石油大学出版社.1993.9～35
[101]Mitchum,R. M.,Vail,P. R.,J.B. Sangree.. Seismic Stratigraphy and Groval Changes of sea level. Part 6:Stratigraphic interpretation of seismic reflection patterns in deposition sequences. In: Payton, C. E. edited, Seismic stratigraphy applications to hydrocarbon exploration.1977,AAPG memoir 26.117～132
[102]孙家振,李兰斌.地震地质综合解释教程.武汉：中国地质大学出版社,2002.121～134
[103]于兴河.储层沉积学.武汉：中国地质大学出版社,2002.64～71
[104]杨琦,陈红宇.苏北-南黄海盆地构造演化.石油实验地质.2003,25(0)：562～565
[2]尹延鸿,汪企浩,张训华等.黄东海地区及其邻域地质构造单元划分.我国专属经济区和大陆架勘测研究论文集.北京：海洋出版社,2002.22～53
[3]邢涛,张训华,张维冈.南黄海地球物理调查研究现状.海洋地质动态.2005，21(6)：1～4
[4]袁文光.渤海、黄海、东海的地球物理调查史.海洋地质与第四纪地质.1989.9(3)：19～27
[5]Proceedings of the second Korea-China international symposium on petroleum potential of the Yellow Sea and the East China Sea,Korea Petroleum Development Corp.and China National Offshore Oil Corp..9-106
[6]Korea/China Symposium Sedimentary Basins in Yellow Sea and Adjacent Areas Abatract, Korea,2001:2-17
[7]Sangheon Yi, Songsuk Yi, David J. Batten, Heysu Yun, Se-Jin Park. Cretaceous and Cenozoic non-marine deposits of the Northern South Yellow Sea Basin, offshore western Korea: palynostratigraphy and palaeoenvironments.Palaeogeography, Palaeoclimatology, Palaeoecology, 2003,191(1):15-44
[8]金翔龙,喻普之.黄海、东海地质构造.黄东海地质.北京：科学出版社,1982.12～26
[9]张文佑.中国及邻区海陆大地构造.北京：科学出版社,1986.3～15
[10]朱夏.关于中国大陆边缘构造演化.海洋地质与第四纪地质,1987,7(3)：115～120
[11]秦蕴珊,赵一阳,陈丽蓉.黄海地质.北京：海洋出版社,1989.9～17
[12]刘光鼎.中国海区及邻域地质地球物理系列图(1/500万).北京：地质出版社,1992
[13]郭玉贵,李延成,许东禹.黄东海大陆架及邻域大地构造演化史.海洋地质与第四纪地质.1997,17(1)：1～12
[14]许东禹,刘锡清,张训华.中国近海地质.北京：地质出版社,1997：210～239
[15]罗明.中国海洋石油总公司志.北京：改革出版社,1998.146～147
[16]李刚,陈建文,肖国林.南黄海海域的海相中-古生界油气远景.海洋地质动态.2003,19(8)：12～16
[17]刘守全,蔡乾忠,莫杰.中国海域油气勘探的新领域-应当重视海域中生界油气资源.中国地质.2001,28(11)：4～9
[18]戴春山,李刚.黄海海域前第三系及油气勘探.海洋地质动态,2002,18(11)：21～22
[19]戴春山,李刚,蔡峰.黄海前第三系及油气勘探方向.中国海上油气地质,2003,17(4)：225～231
[20]蔡乾忠.中国东部与朝鲜大地构造单元对应划分.海洋地质与第四纪地质,1995,15(1)：7～24
[21]蔡乾忠.黄海含油气盆地区域地质与大地构造环境.海洋地质动态,2002,18(11)：8～12
[22]马寅生.中国东部-朝鲜半岛海陆构造格局及含油气盆地特征.北京：地质出版社,2006.261～290
[23]Chough S. K.,Kwon S. T.,Ree J. H.,Choi D. K..Tectonic and sedimentary evolution of the Korean peninsula:a review and new view.Earth-Science Reviews,2000,52:175～235
Mancheol.黄海深部结构与中朝-扬子块体结合带在海区位置的地球物理研究.地学前缘,2004,11(3)：5～61
[25]黄福林.黄、渤海活动断裂初探.海洋地质与第四纪地质.1992,12(4)：21～28
[26]郝天珧,Suh Mancheol黄海中央断裂带的地球物理证据及其与边缘海演化的关系.地球物理学报.2003.46(2)：179～184
[27]郝天珧,Suh Mancheol.根据重力数据研究黄海周边断裂带在海区的延伸.地球物理学报,2002,45(3)：385～397
[28]Harding T.P.,Lowell J.D.,Structural styles,their plate-tectonic habitats,and hydrocarbon traps in petroleum provinces.AAPG.Bulletin,1983,63(7):1016～1085
[29]Lowell J.D..Structural styles in petroleum exploration.Tulsa:Oil and Gas Consultants International.Inc.1985.66～88
[30]胡见义,黄第藩.中国陆相石油地质理论基础.北京：石油工业出版社,1991.55～78
[31]姚永坚.南黄海构造样式的特征及含油气性.海洋地质动态.2002,18(11)：30～32
[32]汪泽成,刘和甫,段周芳.黄骅坳陷中新生代构造负反转分析.地球科学-中国地质大学学报,1998,23(3)：289～293
[33]陈洁,董冬,邱明文.1999.济阳坳陷内的负反转构造及其石油地质意义.石油实验地质,21(3)：201～206
[34]贾霍甫,徐思煌.东营凹陷通王地区负反转构造与断块型古潜山的形成.油气地质与采收率.2006,13(3)：19～21
[35]王同和,王根海,赵宗举.中国含油气盆地的反转构造样式及其油气聚集.海相油气地质,2001,6(3)：27～37
[36]周建生,杨长春.渤海湾地区前第三系构造样式分布特征研究.地球物理学进展2007,22(5)：1416～1426
[37]蔡希源,王根海,迟元林.中国油气区反转构造.北京：石油工业出版社,2001.17～21
[38]Glennie K. W.,P. L. Boeger.Sole pit inversion tectonics.Petroleum Geology of the Continental Shelf of Northwest Europe.1984:110～120
[39]Bally A. W..Tectogenese et sismique reflexion.Bulletin Societe Geologique France.1984,7: 279-285
[40]Harding T.P..Seismic characteristics and identification of negative flower structures,positive flower structures,and positive structural inversion.AAPG Bulletin,1985,69(4):582～600
[41]Williams G. D.,Powell C. M.,Cooper M. A..Geometry and kinematics of inversion tectonics.Inversion Tectonics.Geological society special publication.1989,44:3～15
[42]Cooper M. A.,Williams G. D..Inversion Tectonics.London:The Geo.Soc.,1989.5～11 [43]Mitra S.. Geometry and kinematic evoluation of inversion. AAPG Bulletin,1993,77(7):159-191
[44]胡望水.塔里木盆地反转构造与油气聚集.新疆石油地质,1995,16(2)：89～95
[45]胡望水,卫拥军,张自其.辽河盆地反转期构造特征.西安石油学院学报(自然科学版),2002,17(5)：5～13
[46]杨克绳.从地震信息划分三种不同程度的正、负反转构造样式.海相油气地质.2006,11(1)：21-29
[47]胡望水,周延军,刘学锋.正反转构造综合分析原理和方法.北京：石油工业出版社,2001.17～22
[48]McClay K.R.,Buchanan P.G..Thrust faults in inverted extensional basins.In:McClay K.R.ed.Thrust Tectonics.London:Chapman-Hall,1991.93～104
[49]Green P.F.,Duddy I.R.,Bray R.J..Application of thermal history reconstruction in inverted basins.Buchanan J.G.,Buchanan P,G.(eds)basin inversion.Geological Society Specical Publication,1995.88:149-166
[50]Uliana M.A.,Arteaga M.E.,Legarreta..Inversion structures and hydrocarbon occurrence in Argentina.Buchanan J.G..Buchanan P.G.(eds)basin inversion.Geological Society Specical Publication,1995.88:211-234
[51]汪新文.中国东北地区中-新生代盆地构造演化与油气关系.北京：地质出版社.2007.105～115
[52]陈志勇,葛和平.西湖凹陷反转构造与油气聚集.中国海上油气地质,2003,17(1)：21～24
[53]Hayward A. B., Graham H.R.. Some Geometrical characteristics of inversion. M. A. Cooper and G. D. Williams, eds, Inversion Tectonics.Geological Society Special Publication,1989.44: 34-56
[54]胡望水.正反转构造成因类型.江汉石油学院学报,1993,15(4)：19～25
[55]胡望水,刘学锋,吕新华.论正反转构造的分类.新疆石油地质,2000,21(1)：5～8
[56]刘和甫.伸展构造及其反转作用.地学前缘,1995,2(1)：113～123
[57]陈昭年,陈布科.松辽盆地反转构造与油气聚集成都理工学院学报,1996,23(4)：50～57
[58]吴珍汉.中国大陆及邻区新生代构造-地貌演化过程与机理.北京：地质出版社,2001.203～207
[59]任建业,李思田.西太平洋边缘海盆地的扩张过程和动力学背景.地学前缘,2000,7(3)：203-211
[60]Jurdy D.M.. Relative plate motions and the formation of marginal basins. J. Geophys. Res., 1979,84(B12):6796～6802
[61]Cox A., Engebretson D.. Change in motion of Pacific Plate at 5 Myr BP. Nature, 1985,313(6002):472-474
[62]Northrup C.J.,Royden L.H.,Burchfiel B.C.. Motion of the Pacific Plate relative to Eurasia and its potential relation to Cenozoic extension along the eastern margin of Eurasia. Geology.1995, 23(8):719-722
[63]陈昭年,陈发景.反转构造与油气圈闭.地学前缘,1995.2：96-102
[64]伊恩.勒奇.盆地分析的定量方法.第一卷.魏增璞,冷鹏华,张博闻译.北京：石油工业出版社,1996.7～41
[65]Allen P. A.,Allen J. R..Basin analysis principles & application.Oxford,London:Blackwell Scientific Publication,1990.349～366
[66]陆克政,朱筱敏,漆家福.含油气盆地分析.北京：石油大学出版社,2003.77～89
[67]Lawrence D.T.,M.Doyle,T.Aignef.Stratigraphic simulation of sedimentary basins:concepts and calibration.AAPG Bulletin,1990,74(3):273-295
[68]陈发景.伸展断陷盆地分析.北京：地质出版社,2004.93～107
[69]Steckler M. S.,Watts A. B..Subsidence of the Atlantic-type continental margin of New York.Earth Planetary Sci.,Letter,1978(41):1～13
[70]Bond G. C.,Komiz M. A.. Construction of tectonic subsidence curves for the early Paleozoic miogeocline,southern Canadian Rocky Mountains:Implications for subsidence mechanisms,age of breakup,and Crustal thinning.G.S.A.,Bull.,1984(95):155～173
[71]张功成.裂陷盆地分析原理和方法-以松辽盆地为例.北京：石油工业出版社,1996：162～176
[72]杨庚,钱祥麟,郭华.塔里木北缘库车陆内挠曲盆地构造演化与油气远景评价.北京：地质出版社,2003.29～39
[73]郝石生等.恢复地层剥蚀厚度的最优化方法.沉积学报,1988,6(4)：27～35
[74]何生,王青玲.关于用镜质体反射率恢复地层剥蚀厚度的讨论.地质论评,1989,35(2)：39～44
[75]张海军、曹强,孙建峰.地层剥蚀厚度恢复研究-以南黄海北部盆地东北凹陷为例.石油地质，2008(5)：21～25
[76]刘景彦,林畅松,肖建新.等著.东海西湖凹陷第三系主要不整合面的特征、剥蚀量的分布及其意义.现代地质.1999,13(4)：432～438
[77]陈伟.平衡剖面计算机模拟及其应用.北京：科学出版社,1993.4～26
[78]贾维民,杜秀霞,译.平衡地质剖面.武汉：中国地质大学出版社,1991.11～15
[79]王运所,刘亚洲,张孝义,等.平衡剖面的制作流程及其地质意义.长安大学学报：地球科学版,2003，25(1)：2832
[80]张明山,陈发景.平衡剖面技术应用的条件及实例分析.石油地球物理勘探,1998,33(4)：532～540
[81]Dahlen C.D.A.Balanced cross sections.Canadian Journal of Earth Sciences,1969(6):743-757
[82]Reks I. J., Gray D. R.. Strain patterns and shortening in a folded thrust sheet:an example from the southern Appalachians.Tectonophysics,1983,93(1):99～128
[83]Allen M. B.,Vincent S. J.,Wheeler P. J..Late Cenozoic tectonics of the Kepingtage thrust zone: interactions of the Tien Shan and Tarim Basin,Northwest China.Tectonics,1999,18(4):639-654
[84]Taboada A., Rivera L. A., Fuenzalida A., eta.l Geodynamics of the northern Andes: subductions and intracontinental deformation(Colombia).Tectonics,2000,19(5):787～813
[85]Depaor D. G. Balanced section in thrust belts:Part 1, Construction.AAPG Bulletin,1988, 72(1):73～90
[86]Thomas F,,Martin H.. Folded basement-cored tectonic wedges a long the northern edge of the Amadeus Basin,Central Australia:evaluation of orogenic shortening. Journal of Structural Geology,1999,21(4):399-412
[87]Shahram S., Jean L..Variation of structural style and basin evolution in the central Zagros(Izeh zone and Dezful Embayment),Iran.Marine and Petroleum Geology,2004,21(5):535～554
[88]Mouthereau F.,Lacombe O.,Deffontaines B.,eta.l Deformation history of the southwestern Taiwan foreland thrust belt:insights from tectono-sedimentary analyses and balanced cross-sections.Tectonophysics,2001,333(1):293～322
[89]Alain M., Bernard D. G.,Antonio T.D. R., eta.Structural geometry in the eastern Pyrenees and western Gulf of Lion (Western Mediterranean).Journal of Structural Geology,2001,23(11):1701～ 1726
[90]施泽进,彭大钧,施央申.苏北溱潼凹陷的拉张量研究及构造运动强度分析.大地构造与成矿学,1994,18(1)：43～52
[91]颜丹平,田崇鲁,孟令波.伸展构造盆地的平衡剖面及其构造意义-以松辽盆地南部为例.地球科学-中国地质大学学报,2003,28(3)：275～280
[92]Elliot D..The construction of balanced cross-sections.Journal of Structural Geology,1983(5): 101～103
[93]Woodward N. B.. Valley and ridge thrust belt:balanced structural sections, Pennsylvania to Alabma. Studies in Geology,1985.227～231
[94]Schonborn G.. Balancing cross sections with kinematic constraints:the dolomites (northern Italy).Tectonics,1999,18(3):527～545
[95]Gibbs A..Balanced cross-section construction from seismic sections in areas of extensional tectonics. Journal of Structural Geology,1983,5:153～160
[96]Park. Seismic stratigraphy of the Tertiary Eocene formation of the south Heuksan basin in the Yellow sea.Master's thesis. Kongju National University,1995.5～17
[97]徐万哲.南黄海Heuksan盆地的地震地层学研究,地球物理学进展.2003，18(4)：679～691
[98]徐怀大,王世凤,陈开远.地震地层学解释基础.武汉：中国地质大学出版社.1990.15～29
[99]张万选,张厚福,曾洪流.陆相断陷盆地区域地震地层学研究.东营：石油大学出版社.1998.12～26
[100]张万选,张厚福,曾洪流.陆相地震地层学.东营：石油大学出版社.1993.9～35
[101]Mitchum,R. M.,Vail,P. R.,J.B. Sangree.. Seismic Stratigraphy and Groval Changes of sea level. Part 6:Stratigraphic interpretation of seismic reflection patterns in deposition sequences. In: Payton, C. E. edited, Seismic stratigraphy applications to hydrocarbon exploration.1977,AAPG memoir 26.117～132
[102]孙家振,李兰斌.地震地质综合解释教程.武汉：中国地质大学出版社,2002.121～134
[103]于兴河.储层沉积学.武汉：中国地质大学出版社,2002.64～71
[104]杨琦,陈红宇.苏北-南黄海盆地构造演化.石油实验地质.2003,25(0)：562～565
© 2004-2018 中国地质图书馆版权所有 京ICP备05064691号 京公网安备11010802017129号 地址：北京市海淀区学院路29号 邮编：100083 电话：办公室：(+86 10)66554848；文献借阅、咨询服务、科技查新：66554700 |