亚洲东部碰撞构造:郯庐—尚塔尔碰撞带研究
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摘要
沿郯城—庐江断裂带两侧各约500 km内发育的中生代以来白云母花岗岩、二云母花岗岩和A型花岗岩,五大连池、科洛和二克山火山岩带的强碱性富钾火山岩,高87Sr/86Sr值、低εNd值的中新生代玄武岩,沿郯庐断裂带两侧盆地广泛发育的磨拉石建造,稀土元素∑REE,∑LREE,∑LREE/∑HREE从老到新均逐渐增高;郯庐断裂带莫霍面深度明显大于两侧盆地;郯庐断裂带两侧地块的不连续与差异;沿郯城—庐江断裂带展布的华北地台北缘及东缘的高压麻粒岩、NNE向展布的日照、莒南、东海榴辉岩超高压带和安徽张八岭高压蓝片岩带;郯庐断裂带内表现的强烈挤压构造;郯庐断裂带东侧胶辽—苏北黄海负磁异常区不同于周围地质体(正磁异常区)等,所有证据都指示着南起安徽庐江,经山东郯城、黑龙江佳木斯,北至俄罗斯尚塔尔群岛的断裂带及其两侧构造带为一构造碰撞带:郯庐—尚塔尔碰撞带,郯庐—尚塔尔断裂带为碰撞带的缝合线。松辽盆地、华北盆地、苏北盆地等成煤、成油气等矿产的盆地是碰撞的结果。碰撞带的(突出)应力集中区鲁西—胶东超高压带碰撞区、燕山—辽东碰撞区是中国东部地震的高发区。碰撞的主要动力机制为日本海和鄂霍次克海的张开及菲律宾板块的俯冲。
Muscovite granite,two mica granite and A-type granite developed within 500km on the either sides of Tancheng-Lujiang fault zone since Mesozoic Era,strong alkali and K-rich volcanics of Wudalianchi,Keluo and Erke volcanic belt and the Mesozoic-Cenozoic basalts with high 87Sr/86Sr and low εNd value and molasses formation developed in basins on the either sides of Tancheng-Lujiang fault zone are all characterized by gradual∑REE、∑LREE、∑LREE/∑HREE increment from the old to young;Moho interface bellow Tancheng-Lujiang fault zone is evidently deeper than that bellow basins on the either sides of the fault zone;blocks on the either sides of the fault zone are not continuous and uniform;high pressure granulite along the fault zone occurs in the north and east margins of the north China platform and"Rizhao-Junan-Donghai" ultra-pressure NNW eclogite belt and Zhangbaling high pressure blue schist belt in Anhui province;strong compression structure is developed in the fault zone;the Jiaoliao-Subei-Huanghai negative magnetic anomaly zone in the eastern Tancheng-Lujiang Fault Zone is contrast with the surrounding positive magnetic anomaly.All these are the evidences to lineate a tectonic collision zone extended from south at Lujiang,Anhui province,through Tancheng,Shandong province and Jiamusi,Heilongjiang province to north at Shangtaer archipelago in Russia.Tancheng-Lujiang fault zone is the suture of the collision zone.The major dynamic mechanism of collision is the openning of Japanese Sea and Okhotsk sea and subduction of Philippine Plate.
Muscovite granite,two mica granite and A-type granite developed within 500km on the either sides of Tancheng-Lujiang fault zone since Mesozoic Era,strong alkali and K-rich volcanics of Wudalianchi,Keluo and Erke volcanic belt and the Mesozoic-Cenozoic basalts with high 87Sr/86Sr and low εNd value and molasses formation developed in basins on the either sides of Tancheng-Lujiang fault zone are all characterized by gradual∑REE、∑LREE、∑LREE/∑HREE increment from the old to young;Moho interface bellow Tancheng-Lujiang fault zone is evidently deeper than that bellow basins on the either sides of the fault zone;blocks on the either sides of the fault zone are not continuous and uniform;high pressure granulite along the fault zone occurs in the north and east margins of the north China platform and"Rizhao-Junan-Donghai" ultra-pressure NNW eclogite belt and Zhangbaling high pressure blue schist belt in Anhui province;strong compression structure is developed in the fault zone;the Jiaoliao-Subei-Huanghai negative magnetic anomaly zone in the eastern Tancheng-Lujiang Fault Zone is contrast with the surrounding positive magnetic anomaly.All these are the evidences to lineate a tectonic collision zone extended from south at Lujiang,Anhui province,through Tancheng,Shandong province and Jiamusi,Heilongjiang province to north at Shangtaer archipelago in Russia.Tancheng-Lujiang fault zone is the suture of the collision zone.The major dynamic mechanism of collision is the openning of Japanese Sea and Okhotsk sea and subduction of Philippine Plate.
引文
[1]杨建军.苏鲁榴辉岩及有关超基性岩[M].北京:地质出版社,1991.
[2]康迪K C(张雯华,李继亮,译).板块构造与地壳演化[M].北京:科学出版社,1986.
[3]高山,Yumin Qiu,凌文黎,等.大别山英山和熊店榴辉岩单颗粒锆石SHRIMP U-Pb年代学研究[J].地球科学———中国地质大学学报,2002,27(5):558-563.
[4]刘若新.中国新生代火山岩年代学与地球化学[M].北京:地震出版社,1992.
[5]许志琴,耿瑞伦,肖庆辉,等.中国大陆科学钻探先行研究[M].北京:冶金工业出版社,1996.
[6]凌贤长.中国鲁东造山带岩石圈动力学[M].香港:雅园出版社,2001.
[7]邱家骧.五大连池—科洛—二克山富钾火山岩[M].武汉:中国地质大学出版社,1991.
[8]王小风,李中坚,陈柏林,等.郯庐断裂带[M].北京:地质出版社,2000.
[9]考沃特M P,里斯A C(徐贵忠译).碰撞构造[M].北京:地质出版社,1990.
[10]邓晋福,赵海玲,莫宣学,等.中国大陆根-柱构造———大陆动力学钥匙[M].北京:地质出版社,1996.
[11]柴育成.碰撞造山带大地构造相的变形相及平衡剖面研究[M].北京:地质出版社,1995.
[12]王东坡,刘招君,刘立.松辽盆地演化与海平面上升[M].北京:地质出版社,1994.
[13]王沛成,刘建文,宋志勇,等.胶南—威海造山带与罗迪尼亚(Rodinia)超大陆相关问题的初步探讨[J].山东地质,2001,17(6):27-31.
[14]宋奠南.山东中新生代盆地基本特征及演化特征[J].山东地质,2001,17(5):5-10.
[15]徐嘉伟.初论大别山碰撞带[Z].合肥:合肥工业大学学术讨论会,1981.
[16]王鸿祯.中国古地理图集[M].北京:地图出版社,1985.
[17]邓晋福,莫宣学,罗照华,等.火成岩构造组合与壳-幔成矿系统[J].地学前缘,1999,6(2):259-270.
[18]乔秀夫,高林志,彭阳.古郯庐带新元古界———灾变.层序.生物[M].北京:地质出版社,2001.
[19]余钦范,马杏垣.华北地区航磁图像处理结果和地震构造解释[J].地震地质,1989,11(4),5-13.
[2]康迪K C(张雯华,李继亮,译).板块构造与地壳演化[M].北京:科学出版社,1986.
[3]高山,Yumin Qiu,凌文黎,等.大别山英山和熊店榴辉岩单颗粒锆石SHRIMP U-Pb年代学研究[J].地球科学———中国地质大学学报,2002,27(5):558-563.
[4]刘若新.中国新生代火山岩年代学与地球化学[M].北京:地震出版社,1992.
[5]许志琴,耿瑞伦,肖庆辉,等.中国大陆科学钻探先行研究[M].北京:冶金工业出版社,1996.
[6]凌贤长.中国鲁东造山带岩石圈动力学[M].香港:雅园出版社,2001.
[7]邱家骧.五大连池—科洛—二克山富钾火山岩[M].武汉:中国地质大学出版社,1991.
[8]王小风,李中坚,陈柏林,等.郯庐断裂带[M].北京:地质出版社,2000.
[9]考沃特M P,里斯A C(徐贵忠译).碰撞构造[M].北京:地质出版社,1990.
[10]邓晋福,赵海玲,莫宣学,等.中国大陆根-柱构造———大陆动力学钥匙[M].北京:地质出版社,1996.
[11]柴育成.碰撞造山带大地构造相的变形相及平衡剖面研究[M].北京:地质出版社,1995.
[12]王东坡,刘招君,刘立.松辽盆地演化与海平面上升[M].北京:地质出版社,1994.
[13]王沛成,刘建文,宋志勇,等.胶南—威海造山带与罗迪尼亚(Rodinia)超大陆相关问题的初步探讨[J].山东地质,2001,17(6):27-31.
[14]宋奠南.山东中新生代盆地基本特征及演化特征[J].山东地质,2001,17(5):5-10.
[15]徐嘉伟.初论大别山碰撞带[Z].合肥:合肥工业大学学术讨论会,1981.
[16]王鸿祯.中国古地理图集[M].北京:地图出版社,1985.
[17]邓晋福,莫宣学,罗照华,等.火成岩构造组合与壳-幔成矿系统[J].地学前缘,1999,6(2):259-270.
[18]乔秀夫,高林志,彭阳.古郯庐带新元古界———灾变.层序.生物[M].北京:地质出版社,2001.
[19]余钦范,马杏垣.华北地区航磁图像处理结果和地震构造解释[J].地震地质,1989,11(4),5-13.
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