敦化盆地发育演化及其沉积响应
|
摘要
敦化盆地位于敦密地堑中段,为受敦密断裂控制的裂陷-断陷叠合盆地。敦密断裂带在中、新生代发生了一系列构造体系的转换,即在晚三叠世启动,中晚侏罗世为挤压性质,白垩纪—古近纪具左行平移并有一定规模的拉张,古近纪末有一次挤压,新近纪以后又转变为拉张状态。敦密断裂带的演化对敦化盆地的生成、发展及演化起着主要的控制作用。敦化盆地在中新生代的演化过程为:晚侏罗世—早白垩世的挤压造山-走滑拉分-初始张裂阶段(裂陷发育阶段)、晚白垩世—古新世的回返隆升剥蚀阶段、始新世—渐新世的断陷盆地发育阶段以及新近纪之后的拗陷和玄武岩喷发阶段。各个演化阶段具不同的沉积响应特征。
Dunhua Basin is located in the middle of Dunhua Mishan Graben.And it is a rift-fault depression superposed basin which is controlled by the Dunhua Mishan fracture zone.A series of tectonic system transitions happens during the Mesozoic and Cenozoic period in the Dunhua Mishan fracture zone.The transitions starts in the Late Triassic.In the Late Jurassic,it is compressional;during the Cretaceous-Paleogene,it has a left-lateral displacement and a certain scale of extension;there is a compression in the late Paleogene,which then turns into the extension state again after Neogene.The evolution of Dunhua Mishan fracture zone plays a controlling role in the generation,development and evolution of the Dunhua basin.The evolution of the Dunhua Basin in the Mesozoic-Cenozoic period is:the compressional orogeny,strike slip & pull-apart and the initial rifting stage in Late Jurassic-Early Cretaceous(rift development stage);the inversion,uplifting and exhumation stage in Late Cretaceous-Paleocene;rift basin development stages in the Eocene-Oligocene period and Depression and basalt eruption stage after the Neogene.Different evolution stages have different deposition response characteristics.
Dunhua Basin is located in the middle of Dunhua Mishan Graben.And it is a rift-fault depression superposed basin which is controlled by the Dunhua Mishan fracture zone.A series of tectonic system transitions happens during the Mesozoic and Cenozoic period in the Dunhua Mishan fracture zone.The transitions starts in the Late Triassic.In the Late Jurassic,it is compressional;during the Cretaceous-Paleogene,it has a left-lateral displacement and a certain scale of extension;there is a compression in the late Paleogene,which then turns into the extension state again after Neogene.The evolution of Dunhua Mishan fracture zone plays a controlling role in the generation,development and evolution of the Dunhua basin.The evolution of the Dunhua Basin in the Mesozoic-Cenozoic period is:the compressional orogeny,strike slip & pull-apart and the initial rifting stage in Late Jurassic-Early Cretaceous(rift development stage);the inversion,uplifting and exhumation stage in Late Cretaceous-Paleocene;rift basin development stages in the Eocene-Oligocene period and Depression and basalt eruption stage after the Neogene.Different evolution stages have different deposition response characteristics.
引文
[1]徐嘉炜.郯-庐断裂带的平移运动及其地质意义[C]//国际交流地质学术论文集为二十六届国际地质大会撰写(1).北京:地质出版社,1980:129-142.
[2]徐嘉炜.郯城—庐江平移断裂系统[M]//构造地质论丛(3).北京:地质出版社,1984:18-32.
[3]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,2002,26(4):390-395.
[4]吴根耀,梁兴,陈焕疆.试论郯城—庐江断裂带的形成、演化及其性质[J].地质科学,2007,42(1):160-175.
[5]吴根耀,马力,梁兴,等.从郯庐断裂带两侧的“盆”、“山”耦合演化看前白垩纪“郯庐断裂带”的性质[J].地质通报,2008,27(3):308-325.
[6]乔秀夫,张安棣.华北块体、胶辽朝块体与郯庐断裂[J].中国地质,2002,29(4):337-345.
[7]Zhang Z M,Liou J G,Coleman R G.An outline of theplate tectonics of China[J].Geological Society of AmericaBulletin,1984,95:2952-3120.
[8]徐嘉炜,马国锋.郯庐断裂带研究的十年回顾[J].地质论评,1992,38(4):316-324.
[9]Yin A,Nie S Y.An indentation model for the north andsouth China collision and the development of the Tan-LuandHonamfaultsystem,easternAsia[J].Tectonics,1993,12(4):801-813.
[10]Li Z X.Collision between the north and southblocks:Acrustdetachment model for suturing in the region east ofthe Tan-Lu fault[J].Geology,1994,22:739-742.
[11]万天丰.郯庐断裂带的演化与古应力场[J].地球科学:中国地质大学学报,1995,20(5):526-534.
[12]万天丰.郯庐断裂带的延伸与切割深度[J].现代地质,1996,10(4):518-525.
[13]万天丰,朱鸿,赵磊,等.郯庐断裂带的形成与演化:综述[J].现代地质,1996,10(2):159-168.
[14]万天丰,朱鸿.郯庐断裂的最大左行走滑断距及其形成时期[J].高校地质学报,1996,2(1):14-27.
[15]罗志立,姚军辉.试论松辽盆地新的成因模式及其地质构造和油气勘探意义[J].天然气地球科学,1992,3(1):1-10.
[16]罗志立,李景明,李小军,等.试论郯城—庐江断裂带形成、演化及问题[J].吉林大学学报:地球科学版,2005,35(6):699-706.
[17]Gilder S A,Leloup P H,Courtillotv,et al.Tectonic evo-lution of the Tancheng-Lujiang(Tan-Lu)fault via middleTriassic to Early Cenozoic paleomagnetic data[J].Journalof Geophysical Research,1999,104(B7):15365-15390.
[18]朱光,王道轩,刘国生,等.郯庐断裂带的演化及其对西太平洋板块运动的响应[J].地质科学,2004,39(1):36-49.
[19]朱光,王道轩,刘国生,等.郯庐断裂带的伸展活动及其动力学背景[J].地质科学,2001,36(3):269-278.
[20]朱光,刘国生,宋传中,等.郯庐断裂带的脉动式伸展活动[J].高校地质学报,2000,6(3):396-404.
[21]朱光,王勇生,王道轩,等.前陆沉积与变形对郯庐断裂带同造山运动的制约[J].地质科学,2006,41(1):102-121.
[22]王小凤,李中坚,陈柏林,等.郯庐走滑断裂系的形成演化及其地质意义[C]//郑亚东.第30届国际地质大会论文集.北京:地质出版社,1998:l76-l96.
[23]张云银.郯庐断裂带含油气性研究[J].石油实验地质,2003,25(1):28-32,38.
[24]宋传中,牛漫兰,刘国生,等.郯庐断裂带南段及邻区中、新生代盆地的反转机制[J].合肥工业大学学报:自然科学版,2002,25(3):325-330.
[25]胡望水,吕炳全,官大勇,等.郯庐断裂带及其周缘中新生代盆地发育特征[J].海洋地质与第四纪地质,2003,23(4):51-58.
[26]杨占宝.郯庐断裂带中新生代演化与含油气盆地形成分布综述[J].地质力学学报,2006,12(1):43-48,70.
[27]李宏伟,许坤.郯庐断裂走滑活动与辽河盆地构造古地理格局[J].地学前缘,2001,8(4):467-470.
[28]王金山.黑龙江省东部敦化—密山断裂带中的第三纪盆地[J].煤炭技术,2005,24(2):96-98.
[29]侯明金,Mercier J,Vergely P,等.海西至印支期郯庐断裂带的性质据中国东部石炭纪至三叠纪的岩相古地理特征分析[J].古地理学报,2004,6(4):459-468.
[30]Maruyama S,Isozaki Y,Kimura G,et al.Paleogeographicmaps of the Japanese Islands:plate tectonic systhesis from750 Ma to the present[J].Island Arc,1997,6:121-142.
[31]邵济安,唐克东.中国东北地体与东北亚大陆边缘演化[M].北京:地震出版社,1995.
[2]徐嘉炜.郯城—庐江平移断裂系统[M]//构造地质论丛(3).北京:地质出版社,1984:18-32.
[3]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,2002,26(4):390-395.
[4]吴根耀,梁兴,陈焕疆.试论郯城—庐江断裂带的形成、演化及其性质[J].地质科学,2007,42(1):160-175.
[5]吴根耀,马力,梁兴,等.从郯庐断裂带两侧的“盆”、“山”耦合演化看前白垩纪“郯庐断裂带”的性质[J].地质通报,2008,27(3):308-325.
[6]乔秀夫,张安棣.华北块体、胶辽朝块体与郯庐断裂[J].中国地质,2002,29(4):337-345.
[7]Zhang Z M,Liou J G,Coleman R G.An outline of theplate tectonics of China[J].Geological Society of AmericaBulletin,1984,95:2952-3120.
[8]徐嘉炜,马国锋.郯庐断裂带研究的十年回顾[J].地质论评,1992,38(4):316-324.
[9]Yin A,Nie S Y.An indentation model for the north andsouth China collision and the development of the Tan-LuandHonamfaultsystem,easternAsia[J].Tectonics,1993,12(4):801-813.
[10]Li Z X.Collision between the north and southblocks:Acrustdetachment model for suturing in the region east ofthe Tan-Lu fault[J].Geology,1994,22:739-742.
[11]万天丰.郯庐断裂带的演化与古应力场[J].地球科学:中国地质大学学报,1995,20(5):526-534.
[12]万天丰.郯庐断裂带的延伸与切割深度[J].现代地质,1996,10(4):518-525.
[13]万天丰,朱鸿,赵磊,等.郯庐断裂带的形成与演化:综述[J].现代地质,1996,10(2):159-168.
[14]万天丰,朱鸿.郯庐断裂的最大左行走滑断距及其形成时期[J].高校地质学报,1996,2(1):14-27.
[15]罗志立,姚军辉.试论松辽盆地新的成因模式及其地质构造和油气勘探意义[J].天然气地球科学,1992,3(1):1-10.
[16]罗志立,李景明,李小军,等.试论郯城—庐江断裂带形成、演化及问题[J].吉林大学学报:地球科学版,2005,35(6):699-706.
[17]Gilder S A,Leloup P H,Courtillotv,et al.Tectonic evo-lution of the Tancheng-Lujiang(Tan-Lu)fault via middleTriassic to Early Cenozoic paleomagnetic data[J].Journalof Geophysical Research,1999,104(B7):15365-15390.
[18]朱光,王道轩,刘国生,等.郯庐断裂带的演化及其对西太平洋板块运动的响应[J].地质科学,2004,39(1):36-49.
[19]朱光,王道轩,刘国生,等.郯庐断裂带的伸展活动及其动力学背景[J].地质科学,2001,36(3):269-278.
[20]朱光,刘国生,宋传中,等.郯庐断裂带的脉动式伸展活动[J].高校地质学报,2000,6(3):396-404.
[21]朱光,王勇生,王道轩,等.前陆沉积与变形对郯庐断裂带同造山运动的制约[J].地质科学,2006,41(1):102-121.
[22]王小凤,李中坚,陈柏林,等.郯庐走滑断裂系的形成演化及其地质意义[C]//郑亚东.第30届国际地质大会论文集.北京:地质出版社,1998:l76-l96.
[23]张云银.郯庐断裂带含油气性研究[J].石油实验地质,2003,25(1):28-32,38.
[24]宋传中,牛漫兰,刘国生,等.郯庐断裂带南段及邻区中、新生代盆地的反转机制[J].合肥工业大学学报:自然科学版,2002,25(3):325-330.
[25]胡望水,吕炳全,官大勇,等.郯庐断裂带及其周缘中新生代盆地发育特征[J].海洋地质与第四纪地质,2003,23(4):51-58.
[26]杨占宝.郯庐断裂带中新生代演化与含油气盆地形成分布综述[J].地质力学学报,2006,12(1):43-48,70.
[27]李宏伟,许坤.郯庐断裂走滑活动与辽河盆地构造古地理格局[J].地学前缘,2001,8(4):467-470.
[28]王金山.黑龙江省东部敦化—密山断裂带中的第三纪盆地[J].煤炭技术,2005,24(2):96-98.
[29]侯明金,Mercier J,Vergely P,等.海西至印支期郯庐断裂带的性质据中国东部石炭纪至三叠纪的岩相古地理特征分析[J].古地理学报,2004,6(4):459-468.
[30]Maruyama S,Isozaki Y,Kimura G,et al.Paleogeographicmaps of the Japanese Islands:plate tectonic systhesis from750 Ma to the present[J].Island Arc,1997,6:121-142.
[31]邵济安,唐克东.中国东北地体与东北亚大陆边缘演化[M].北京:地震出版社,1995.
版权所有：© 2023 中国地质图书馆 中国地质调查局地学文献中心