东北地区上古生界变质特征研究
|
摘要
东北地区上古生界发育,研究东北地区上古生界的变质程度对确定东北地区上古生界是否具有勘探潜力有着重要的意义。本文在对古生代地层发育特征、大地构造背景、岩浆岩活动期次、等问题研究基础上,根据大量的露头和部分岩心的古生物鉴定、岩矿鉴定及有机质成熟度、裂隙包裹体测温、伊利石结晶度等测试分析手段,确认东北古生界部分地区遭受了极低级变质,部分地区未遭受变质,变质程度较高的地区主要出现于岩体和大型断裂带附近。变质作用类型主要有接触变质、气液变质、动力变质及区域低温动力变质,其中气液变质和区域低温动力变质又进一步划分为A型和B型,前三者皆为局部变质作用,后者是东北古生界发生面状变质的主要因素。经过详细分析变质动用进一步将东北地区的上古生界变质相划分为2大类、6亚类,变质相区可划分为6种类型8个区块。
There are marine facies strata in upper Paleozoic,Northeast China, especially in the Late Carboniferous and Early Permian marine strata in the Songliao, Erlian basins are widely developed. The tectonic position of the study area is located between Siberia Plate and the North China Plate, regional structure has undergone the orogeny plate mosaic from different directions and different periods before Mesozoic, and also undergone the tectonism later in Mesozoic and Cenozoic, these show a complex tectonic evolution. Late Paleozoic volcanic-sedimentary rocks are widely distributed in Northeast China, formations are mainly marine limestone, mainly carbonate rock, a little clastic rocks, volcanic rocks, rich in fossils which contain a number of categories.
According to the analysis by field, combinations of minerals, fluid inclusion thermometry, vitrinite reflectance, illite crystallinity in order to discuss the Upper Paleozoic metamorphic type characteristics, type of metamorphic facies, metamorphic grade and metamorphic phase partition Upper Paleozoic in Northeast China experienced varying degrees of thermodynamic and dynamic fields and other factors, some of later reformation is not obvious, basically remained the primary sedimentary - volcanic features; some stood post reconstruction, showing different types of metamorphic rocks, tectonite and so on. According to the transformation characteristics of these rocks in the research area, we divided four main types of metamorphism. The contact metamorphism; liquid metamorphism; dynamic metamorphism; regional low-temperature dynamic metamorphism. Based on the comprehensive identification of the samples collected in the research region, the metamorphic rocks in the area are involved in thermal contact metamorphic (no account of the role), the maximum metamorphic intensity to medium temperature, but the low-temperature contact metamorphism are still more common. The characteristics and the types of the gas-liquid alteration are very complex, the magma-liquid phenomenon is very obvious and the intensity is very strong in many Upper Paleozoic stratums in the research area. Upper Paleozoic stratigraphy and lithology changes in the region involved in gas-liquid samples primarily for low-temperature hydrothermal alteration. The characteristics of the alterations depend on the rock types. Some samples are cataclastic rock which turned from brittle rock in some fault zone of this area, but the ductile tectonism-mylonite, phyllonite, structure slate, and phyllite are the common rock types. Regional low-temperature dynamic metamorphism often has large areal or zonal distribution of the green schist facies metamorphism single-phase zone occurs in the shallow crust (typically no more than 7-8km), is a product under the strong stress deformation and low temperature conditions which turned by recrystallization and metamorphic crystallization. The regional low temperature-dynamic metamorphic rock which widely distributed in the study area can be further divided into very low grade metamorphic rocks(equivalent to low greenschist facies) and low grade metamorphic rocks(equivalent to low greenschist facies), the first three kinds of metamorphism is the regional metamorphism, the last one is the major factor about the metamorphism in the Northeast China.
In this paper we identified metamorphism into very low level, low level, middle level in the Upper Paleozoic. The very low level metamorphism we mentioned in this paper means a condition which changed between no obvious diagnostic metamorphic mineral and no metamorphism, especially the mud type metamorphic rocks. The basic metamorphic rock is not developed in the research area, the rock type is dominated by the metamorphic rock which have characteristics minerals like sericite, hydromica, while the vitrinite reflection Ro is between 2.5～4.0%,illite crystallinity ranged between 0.25～0.42. That shows the undergo maximum temperature is between 200～350℃. Then we further divided the very low grade metamorphism into very low grade metamorphism A and B period. The middle-low grade metamorphism mainly in the local contact metamorphism, liquid and dynamic metamorphism zone. Besides, we can find biotite,garnet, zoisite, actinolite as the characteristic minerals, in the other hand pumpellyite and lawsonite disappear. Meanwhile the vitrinite reflectance Ro>4.0%, illite crystallinity<0.25, the maximum temperature has been subjected to >350℃.
Higher degree of contact metamorphism metamorphic, liquid metamorphic, metamorphism is only partial, the metamorphic facies widely distributed in the study area can be divided into no result and sub-greenschist facies. Based on these classification of the metamorphic grade and the metamorphic mineral assemblage, we give a further description on the metamorphic facies. The study area is divided into the“overall no metamorphism(D0), the regional low-temperature dynamic metamorphism-sub-greenschist facies(D1)”two caegories. And further we divided the“overall no metamorphism(D0) into“no metamorphism”(D01),“no metamorphism-regional gas and liquid A type metamorphism”(D02),“no metamorphism-regional gas and liquid B type metamorphism(D03) there metamorphic facies area, and then divided the“regional low-temperature dynamic metamorphism-greenschist facies”(D1) into“regional low-temperature dynamic metamorphism-gas and liquid A type metamorphism(D11),“regional low-temperature dynamic metamorphism-local gas and liquid A type metamorphism(D12) and“regional low-temperature dynamic metamorphism-local gas and liquid B type metamorphism(D13) there facies areas. According to the basic parameters of metamorphic facies characteristics combined with the tectonic and environment evolution in different areas,Northeast China, through Paletology and mineral identification, vitrinite reflectance, illite crystallinity, fluid inclusion thermometry distribution characteristics, then remove rock contact zone, fault zone and other Highlevel metamorphims zone, finally we divided the Upper Pleozoic metamorphic zone into 6 types and 8 areas which are : no metamorphism area in the south of Songliao basin, Erlianhaote-Aershan no metamorphism-regional gas and liquid A type metamorphic zone, Jiamusi no metamorphism-regional gas and liquid A type metamorphic zone, Erguna no metamorphism-regional gas and liquid B type metamorphic zone, South of Daxinganling regional low-temperature dynamic-local gas and liquid A type metamorphic zone, North of Songliao basin regional low-temperature dynamic-local gas and liquid A type metamorphic zone, Daqing regional low-temperature dynamic-local gas and liquid B type metamorphic zone, east of Jilin regional ow-temperature dynamic-local gas and liquid B type metamorphic zone
There are marine facies strata in upper Paleozoic,Northeast China, especially in the Late Carboniferous and Early Permian marine strata in the Songliao, Erlian basins are widely developed. The tectonic position of the study area is located between Siberia Plate and the North China Plate, regional structure has undergone the orogeny plate mosaic from different directions and different periods before Mesozoic, and also undergone the tectonism later in Mesozoic and Cenozoic, these show a complex tectonic evolution. Late Paleozoic volcanic-sedimentary rocks are widely distributed in Northeast China, formations are mainly marine limestone, mainly carbonate rock, a little clastic rocks, volcanic rocks, rich in fossils which contain a number of categories.
According to the analysis by field, combinations of minerals, fluid inclusion thermometry, vitrinite reflectance, illite crystallinity in order to discuss the Upper Paleozoic metamorphic type characteristics, type of metamorphic facies, metamorphic grade and metamorphic phase partition Upper Paleozoic in Northeast China experienced varying degrees of thermodynamic and dynamic fields and other factors, some of later reformation is not obvious, basically remained the primary sedimentary - volcanic features; some stood post reconstruction, showing different types of metamorphic rocks, tectonite and so on. According to the transformation characteristics of these rocks in the research area, we divided four main types of metamorphism. The contact metamorphism; liquid metamorphism; dynamic metamorphism; regional low-temperature dynamic metamorphism. Based on the comprehensive identification of the samples collected in the research region, the metamorphic rocks in the area are involved in thermal contact metamorphic (no account of the role), the maximum metamorphic intensity to medium temperature, but the low-temperature contact metamorphism are still more common. The characteristics and the types of the gas-liquid alteration are very complex, the magma-liquid phenomenon is very obvious and the intensity is very strong in many Upper Paleozoic stratums in the research area. Upper Paleozoic stratigraphy and lithology changes in the region involved in gas-liquid samples primarily for low-temperature hydrothermal alteration. The characteristics of the alterations depend on the rock types. Some samples are cataclastic rock which turned from brittle rock in some fault zone of this area, but the ductile tectonism-mylonite, phyllonite, structure slate, and phyllite are the common rock types. Regional low-temperature dynamic metamorphism often has large areal or zonal distribution of the green schist facies metamorphism single-phase zone occurs in the shallow crust (typically no more than 7-8km), is a product under the strong stress deformation and low temperature conditions which turned by recrystallization and metamorphic crystallization. The regional low temperature-dynamic metamorphic rock which widely distributed in the study area can be further divided into very low grade metamorphic rocks(equivalent to low greenschist facies) and low grade metamorphic rocks(equivalent to low greenschist facies), the first three kinds of metamorphism is the regional metamorphism, the last one is the major factor about the metamorphism in the Northeast China.
In this paper we identified metamorphism into very low level, low level, middle level in the Upper Paleozoic. The very low level metamorphism we mentioned in this paper means a condition which changed between no obvious diagnostic metamorphic mineral and no metamorphism, especially the mud type metamorphic rocks. The basic metamorphic rock is not developed in the research area, the rock type is dominated by the metamorphic rock which have characteristics minerals like sericite, hydromica, while the vitrinite reflection Ro is between 2.5～4.0%,illite crystallinity ranged between 0.25～0.42. That shows the undergo maximum temperature is between 200～350℃. Then we further divided the very low grade metamorphism into very low grade metamorphism A and B period. The middle-low grade metamorphism mainly in the local contact metamorphism, liquid and dynamic metamorphism zone. Besides, we can find biotite,garnet, zoisite, actinolite as the characteristic minerals, in the other hand pumpellyite and lawsonite disappear. Meanwhile the vitrinite reflectance Ro>4.0%, illite crystallinity<0.25, the maximum temperature has been subjected to >350℃.
Higher degree of contact metamorphism metamorphic, liquid metamorphic, metamorphism is only partial, the metamorphic facies widely distributed in the study area can be divided into no result and sub-greenschist facies. Based on these classification of the metamorphic grade and the metamorphic mineral assemblage, we give a further description on the metamorphic facies. The study area is divided into the“overall no metamorphism(D0), the regional low-temperature dynamic metamorphism-sub-greenschist facies(D1)”two caegories. And further we divided the“overall no metamorphism(D0) into“no metamorphism”(D01),“no metamorphism-regional gas and liquid A type metamorphism”(D02),“no metamorphism-regional gas and liquid B type metamorphism(D03) there metamorphic facies area, and then divided the“regional low-temperature dynamic metamorphism-greenschist facies”(D1) into“regional low-temperature dynamic metamorphism-gas and liquid A type metamorphism(D11),“regional low-temperature dynamic metamorphism-local gas and liquid A type metamorphism(D12) and“regional low-temperature dynamic metamorphism-local gas and liquid B type metamorphism(D13) there facies areas. According to the basic parameters of metamorphic facies characteristics combined with the tectonic and environment evolution in different areas,Northeast China, through Paletology and mineral identification, vitrinite reflectance, illite crystallinity, fluid inclusion thermometry distribution characteristics, then remove rock contact zone, fault zone and other Highlevel metamorphims zone, finally we divided the Upper Pleozoic metamorphic zone into 6 types and 8 areas which are : no metamorphism area in the south of Songliao basin, Erlianhaote-Aershan no metamorphism-regional gas and liquid A type metamorphic zone, Jiamusi no metamorphism-regional gas and liquid A type metamorphic zone, Erguna no metamorphism-regional gas and liquid B type metamorphic zone, South of Daxinganling regional low-temperature dynamic-local gas and liquid A type metamorphic zone, North of Songliao basin regional low-temperature dynamic-local gas and liquid A type metamorphic zone, Daqing regional low-temperature dynamic-local gas and liquid B type metamorphic zone, east of Jilin regional ow-temperature dynamic-local gas and liquid B type metamorphic zone
引文
[1] Defant M J, Drummond M S. Derivation of some modern magmas by melting of young subduction lithosphere.Nature,1990,347:662-665.
[2] Vernik L..A new type of reservoir rock in volcaniclastic sequences[J]. 1999, AAPG ,74(6):830-836.
[3] Norton D L, Cathles L M. 1973. Breccia pipe products of exsolved vapor from magmas[J]. Econ. Geol.,68:540-546.
[4] Burnham C. W. Magmas and hydrothermal fluids.[A] In: Bames H. L. , Geochemistry of Hydrothermal Ore Deposites New York[M]. John Wiley and Sons, 1997, third edition ,63-124.
[5] Korzhinskv M. A, Tkachenko S. I, Shmulovich K.I, et al. Discovery of a pure rhenium mineral at Kudriavy volcano [J].NATURE, 2003,369 6475):51-52.
[6]李三忠,刘建忠.变质作用热模拟模型及模拟结果[J].世界地质. 1996. 15 (1):13-20.
[7]程裕淇,庄育勋,沈其韩.变质作用研究的回顾与展望[J].地学前缘(中国地质大学,北京). 1998. 5 (4):257-264.
[8]王璞珺,刘万洙,王东坡.沉积盆地热史研究方法[J].世界地质.1994. 13 (3):114-119.
[9]韩郁菁.当前高压变质作用研究中几个值得注意的动向[J].地学前缘(中国地质大学,北京). 1994. 1 (1-2):134-139.
[10]张开均.华北板块东缘晚古生代火山活动及其大地构造含义[J].中国煤田地质. 1998. 10 (3):10-11.
[11]黄雄南,李江海,陈征,刘志强;冀东遵化新太古代蛇绿混杂岩带岩石学与构造特征—古板块构造运动的证据[J];北京大学学报(自然科学版);2003年02期.
[12]徐仲元,刘正宏,杨振升.内蒙古大青山地区早前寒武纪变质地层的组成及特征[J];世界地质;2001年03期.
[13]赵宗溥.成岩作用、埋藏变质作用与近变质作用[J];地质论评;1984年05期
[14]张秋生.中国的变质旋回及其成矿作用[J];吉林大学学报(地球科学版);1981年03期.
[15]张翊钧,变质作用中岩石成分的变化[A];中国地质科学院天津地质矿产研究所文集(20)[C];1989年.
[16]娄玉行.桐柏山地区榴辉岩与石榴角闪岩的变质作用研究[D];中国地质科学院;2005年.
[17]徐学纯.内蒙古乌拉山地区变质作用演化及其动力学研究[J];吉林大学学报(地球科学版);1991年01期.
[18]靳是琴;北京密云群变质岩的矿物演化[J];岩石矿物学杂志;1986年01期
[19]张厚福,方朝亮,张枝焕等.石油地质学[M].北京:石油工业出版社, 1999.
[20]马文璞.区域构造解析[M].地质出版社. 1992.
[21]王东坡,刘招君,刘立.松辽盆地演化与海平面升降[M].地质出版社. 1994.
[22]谯汉生,方朝亮,牛嘉玉等.东北地区深层石油地质[M].北京:石油工业出版社, 2003.
[23]谯汉生,方朝亮,牛嘉玉等.中国东部深层石油地质[M].北京:石油工业出版社, 2002.
[24] M-SGT地质课题组.中国满洲里-绥芬河地学断面域内岩石圈结构及其演化的地质研究[M].地震出版社, 1994.
[25]刘招君,郭巍.松辽盆地及其邻区中新生代盆山动力学[R].吉林大学油气与盆地研究所, 2001-2003.
[26]彭玉鲸,唐守贤.吉林省区域地质志[M].地质出版社,1988.
[27]谯汉生,罗治斌,李先奇.中国东部深层石油勘探论文集[M].北京:石油工业出版社, 2001.
[28]赵政璋,李永铁,叶和飞.青藏高原海相烃源层的油气生成[M].北京:科学出版社, 2000.
[29]王东坡,薛林福,刘立,等.沉积盆地的地球动力学[J].石油与天然气地质. 1998, 19(3):181-185.
[30]王骏,王东坡.沉积盆地的地球动力学演化分类[J].长春科技大学学报. 1998, 28(1):50-52.
[31]杨春,戴金星,陈汉林等.浅变质岩热模拟实验及天然气成藏潜力[J].石油勘探与开发, 2009,36(2):200-208
[32]肖安成,杨树锋,陈汉林.二连盆地形成的地球动力学背景[J].石油与天然气地质. 2001, 22(2):137-140.
[33]罗震宇,金振民.岩石超塑性变形及其地球动力学意义综述[J].地质科技情报. 2003, 22(1):17-23.
[34]索书田,毕先梅,赵文霞,等.右江盆地三叠纪岩层极低级变质作用及地球动力学意义[J].地质科学. 1998, 33(4):395-405.
[35]张渝昌,高长林.大陆热覆盖效应和盆地变格[J].中国西部油气地质. 2006, 2 (1):1-7.
[36]邵济安,张履桥,储著银.冀北早白垩世火山-沉积作用及构造背景[J].地质通报. 2003, 22(6):384-390.
[37]朱建辉,江兴歌,徐旭辉,等.苏北盆地海安凹陷曲塘-李堡地区新生代演化和油气响应评价[J].石油实验地质. 2005, 27(2):138-144.
[38]徐旭辉.塔里木古生代原型盆地分析的油气勘探意义[J].石油与天然气地质. 2002, 23(3);224-229.
[39]周瑶琪,赵士宝.太平洋古陆的破碎消亡与中新生代华北克拉通板内构造岩浆活化[J].地球科学-中国地质大学学报. 2004, 29(5):575-582.
[40]徐旭辉,高长林,黄泽光,等.中国盆地形成的三大活动构造历史阶段[J].石油与天然气地质. 2005, 26(2):155-163.
[41]张忠民,李春生,龙胜祥,许化政.华北地区东部上古生界天然气勘探前景[J].天然气地球科学. 2006, 17 (3):330-334.
[42]赵孟为.划分成岩作用与埋藏变质作用的指标及其界线[J].地质论评. 1995, 41 (3):238-244.
[43]任战利,肖晖,刘丽等.沁水盆地中生代构造热事件发生时期的确定[J].石油勘探与开发. 2005, 32 (1):43-47.
[44]陶士振,刘德良.郯庐断裂带及邻区地热特征、温泉形成因素及气体组成[J].天然气工业. 2000,20(6):42-46.
[45]邱楠生,李慧莉,金之钧等.碳酸盐岩层系热历史恢复的有机质自由基古温标研究[J].地质学报. 2006, 80 (3):390-397.
[46]郝建荣,柳益群,冯乔等.新疆三塘湖盆地构造-热史研究[J].西北大学学报. 2006, 36 (2):290-294.
[47]赵靖舟.油气成藏年代学研究进展及发展趋势[J].地球科学进展. 2002, 17 (3):378-384.
[48]范小林.中国大陆岩石圈与中新生代盆地构造-热体制[J].勘探地球物理进展. 2005, 28 (5):330-334
[49]张梅生,彭向东,孙晓猛.中国东北区古生代构造古地理格局[J].辽宁地质1998, (2):91-96.
[50]张旗,赵太平,王焰等.中国东部燕山期岩浆活动的几个问题[J].岩石矿物学杂志. 2001, 20 (3):273-280.
[51]杨宝俊,等.中国东部陆缘主要盆地区及邻区区域构造和深层油气目标[R].长春科技大学科研报告,1999.
[52]许文良,孙德有.中国满洲里—绥芬河地学断面域内岩浆活动及其深部构造背景[R].长春地质学院,1993.
[53]孙加鹏.松辽盆地及其东缘深部构造与油气预测[D].长春:长春科技大学博士学位论文,1997.
[54]许文良,孙德有,周燕,等.满洲里—绥芬河地学断面域内晚海西-早印支期和晚印支期的花岗岩的形成环境[J].中国满洲里—绥芬河地学断面域内岩石圈结构及其演化的地质研究(M-SGT地质课题组).北京:地震出版社,1994,123-131.
[55]刘招君,汪筱林,刘万洙等满洲里-绥芬河地学断面域松辽-海拉尔中生代盆地形成机制[J].中国满洲里—绥芬河地学断面域内岩石圈结构及其演化的地质研究(M-SGT地质课题组).北京:地震出版社,1994,14-26.
[56]余和中,蔡希源,韩守华,徐云俊.松辽盆地石炭-二叠系烃源岩研究[J].沉积与特提斯地质. 2003, 23 (2):62-66.
[57]吴福元,孙德有,李惠民,汪筱林.松辽盆地基底岩石的锆石U-Pb年龄[J].科学通报. 2000, 45 (6):656-660.
[58]高福红,许文良,杨德彬等.松辽盆地南部基底花岗质岩石锆石LA-ICP-MS U-Pb定年:对盆地基底形成时代的制约[J].中国科学D辑:地球科学. 2007, 37 (3):331-335.
[59]胡大千、于介江,中国东北地区晚古生代区域成岩—极低级变质作用研究。东北亚地区油气地质与矿产资源学术研讨会,2008.5
[60]王成文,马志红,孙跃武,等.晚古生代海相地层———东北地区油气勘查的一个新层系[ J ] .世界地质,2008 ,27 (2) :1132118.
[61]董申葆,沈其韩,孙大中,等.中国变质地质图(1∶4 00万) [M] .北京:地质出版社,1996.
[62]董申保.中国变质作用及其与地壳演化关系.北京:地质出版社,1986.10～14
[63]贺高品,李应场.新疆准噶尔—北天山地区古生代的埋藏变质作用.见:长春地质学院地质研究所文集,北京:地震出版社,1992.48～61
[64]索书田,毕仙梅,周汉文.极低级变质作用.地质出版社,1999.
[65]董申保.中国变质作用及其与地壳演化关系.北京:地质出版社,1986.10～14
[2] Vernik L..A new type of reservoir rock in volcaniclastic sequences[J]. 1999, AAPG ,74(6):830-836.
[3] Norton D L, Cathles L M. 1973. Breccia pipe products of exsolved vapor from magmas[J]. Econ. Geol.,68:540-546.
[4] Burnham C. W. Magmas and hydrothermal fluids.[A] In: Bames H. L. , Geochemistry of Hydrothermal Ore Deposites New York[M]. John Wiley and Sons, 1997, third edition ,63-124.
[5] Korzhinskv M. A, Tkachenko S. I, Shmulovich K.I, et al. Discovery of a pure rhenium mineral at Kudriavy volcano [J].NATURE, 2003,369 6475):51-52.
[6]李三忠,刘建忠.变质作用热模拟模型及模拟结果[J].世界地质. 1996. 15 (1):13-20.
[7]程裕淇,庄育勋,沈其韩.变质作用研究的回顾与展望[J].地学前缘(中国地质大学,北京). 1998. 5 (4):257-264.
[8]王璞珺,刘万洙,王东坡.沉积盆地热史研究方法[J].世界地质.1994. 13 (3):114-119.
[9]韩郁菁.当前高压变质作用研究中几个值得注意的动向[J].地学前缘(中国地质大学,北京). 1994. 1 (1-2):134-139.
[10]张开均.华北板块东缘晚古生代火山活动及其大地构造含义[J].中国煤田地质. 1998. 10 (3):10-11.
[11]黄雄南,李江海,陈征,刘志强;冀东遵化新太古代蛇绿混杂岩带岩石学与构造特征—古板块构造运动的证据[J];北京大学学报(自然科学版);2003年02期.
[12]徐仲元,刘正宏,杨振升.内蒙古大青山地区早前寒武纪变质地层的组成及特征[J];世界地质;2001年03期.
[13]赵宗溥.成岩作用、埋藏变质作用与近变质作用[J];地质论评;1984年05期
[14]张秋生.中国的变质旋回及其成矿作用[J];吉林大学学报(地球科学版);1981年03期.
[15]张翊钧,变质作用中岩石成分的变化[A];中国地质科学院天津地质矿产研究所文集(20)[C];1989年.
[16]娄玉行.桐柏山地区榴辉岩与石榴角闪岩的变质作用研究[D];中国地质科学院;2005年.
[17]徐学纯.内蒙古乌拉山地区变质作用演化及其动力学研究[J];吉林大学学报(地球科学版);1991年01期.
[18]靳是琴;北京密云群变质岩的矿物演化[J];岩石矿物学杂志;1986年01期
[19]张厚福,方朝亮,张枝焕等.石油地质学[M].北京:石油工业出版社, 1999.
[20]马文璞.区域构造解析[M].地质出版社. 1992.
[21]王东坡,刘招君,刘立.松辽盆地演化与海平面升降[M].地质出版社. 1994.
[22]谯汉生,方朝亮,牛嘉玉等.东北地区深层石油地质[M].北京:石油工业出版社, 2003.
[23]谯汉生,方朝亮,牛嘉玉等.中国东部深层石油地质[M].北京:石油工业出版社, 2002.
[24] M-SGT地质课题组.中国满洲里-绥芬河地学断面域内岩石圈结构及其演化的地质研究[M].地震出版社, 1994.
[25]刘招君,郭巍.松辽盆地及其邻区中新生代盆山动力学[R].吉林大学油气与盆地研究所, 2001-2003.
[26]彭玉鲸,唐守贤.吉林省区域地质志[M].地质出版社,1988.
[27]谯汉生,罗治斌,李先奇.中国东部深层石油勘探论文集[M].北京:石油工业出版社, 2001.
[28]赵政璋,李永铁,叶和飞.青藏高原海相烃源层的油气生成[M].北京:科学出版社, 2000.
[29]王东坡,薛林福,刘立,等.沉积盆地的地球动力学[J].石油与天然气地质. 1998, 19(3):181-185.
[30]王骏,王东坡.沉积盆地的地球动力学演化分类[J].长春科技大学学报. 1998, 28(1):50-52.
[31]杨春,戴金星,陈汉林等.浅变质岩热模拟实验及天然气成藏潜力[J].石油勘探与开发, 2009,36(2):200-208
[32]肖安成,杨树锋,陈汉林.二连盆地形成的地球动力学背景[J].石油与天然气地质. 2001, 22(2):137-140.
[33]罗震宇,金振民.岩石超塑性变形及其地球动力学意义综述[J].地质科技情报. 2003, 22(1):17-23.
[34]索书田,毕先梅,赵文霞,等.右江盆地三叠纪岩层极低级变质作用及地球动力学意义[J].地质科学. 1998, 33(4):395-405.
[35]张渝昌,高长林.大陆热覆盖效应和盆地变格[J].中国西部油气地质. 2006, 2 (1):1-7.
[36]邵济安,张履桥,储著银.冀北早白垩世火山-沉积作用及构造背景[J].地质通报. 2003, 22(6):384-390.
[37]朱建辉,江兴歌,徐旭辉,等.苏北盆地海安凹陷曲塘-李堡地区新生代演化和油气响应评价[J].石油实验地质. 2005, 27(2):138-144.
[38]徐旭辉.塔里木古生代原型盆地分析的油气勘探意义[J].石油与天然气地质. 2002, 23(3);224-229.
[39]周瑶琪,赵士宝.太平洋古陆的破碎消亡与中新生代华北克拉通板内构造岩浆活化[J].地球科学-中国地质大学学报. 2004, 29(5):575-582.
[40]徐旭辉,高长林,黄泽光,等.中国盆地形成的三大活动构造历史阶段[J].石油与天然气地质. 2005, 26(2):155-163.
[41]张忠民,李春生,龙胜祥,许化政.华北地区东部上古生界天然气勘探前景[J].天然气地球科学. 2006, 17 (3):330-334.
[42]赵孟为.划分成岩作用与埋藏变质作用的指标及其界线[J].地质论评. 1995, 41 (3):238-244.
[43]任战利,肖晖,刘丽等.沁水盆地中生代构造热事件发生时期的确定[J].石油勘探与开发. 2005, 32 (1):43-47.
[44]陶士振,刘德良.郯庐断裂带及邻区地热特征、温泉形成因素及气体组成[J].天然气工业. 2000,20(6):42-46.
[45]邱楠生,李慧莉,金之钧等.碳酸盐岩层系热历史恢复的有机质自由基古温标研究[J].地质学报. 2006, 80 (3):390-397.
[46]郝建荣,柳益群,冯乔等.新疆三塘湖盆地构造-热史研究[J].西北大学学报. 2006, 36 (2):290-294.
[47]赵靖舟.油气成藏年代学研究进展及发展趋势[J].地球科学进展. 2002, 17 (3):378-384.
[48]范小林.中国大陆岩石圈与中新生代盆地构造-热体制[J].勘探地球物理进展. 2005, 28 (5):330-334
[49]张梅生,彭向东,孙晓猛.中国东北区古生代构造古地理格局[J].辽宁地质1998, (2):91-96.
[50]张旗,赵太平,王焰等.中国东部燕山期岩浆活动的几个问题[J].岩石矿物学杂志. 2001, 20 (3):273-280.
[51]杨宝俊,等.中国东部陆缘主要盆地区及邻区区域构造和深层油气目标[R].长春科技大学科研报告,1999.
[52]许文良,孙德有.中国满洲里—绥芬河地学断面域内岩浆活动及其深部构造背景[R].长春地质学院,1993.
[53]孙加鹏.松辽盆地及其东缘深部构造与油气预测[D].长春:长春科技大学博士学位论文,1997.
[54]许文良,孙德有,周燕,等.满洲里—绥芬河地学断面域内晚海西-早印支期和晚印支期的花岗岩的形成环境[J].中国满洲里—绥芬河地学断面域内岩石圈结构及其演化的地质研究(M-SGT地质课题组).北京:地震出版社,1994,123-131.
[55]刘招君,汪筱林,刘万洙等满洲里-绥芬河地学断面域松辽-海拉尔中生代盆地形成机制[J].中国满洲里—绥芬河地学断面域内岩石圈结构及其演化的地质研究(M-SGT地质课题组).北京:地震出版社,1994,14-26.
[56]余和中,蔡希源,韩守华,徐云俊.松辽盆地石炭-二叠系烃源岩研究[J].沉积与特提斯地质. 2003, 23 (2):62-66.
[57]吴福元,孙德有,李惠民,汪筱林.松辽盆地基底岩石的锆石U-Pb年龄[J].科学通报. 2000, 45 (6):656-660.
[58]高福红,许文良,杨德彬等.松辽盆地南部基底花岗质岩石锆石LA-ICP-MS U-Pb定年:对盆地基底形成时代的制约[J].中国科学D辑:地球科学. 2007, 37 (3):331-335.
[59]胡大千、于介江,中国东北地区晚古生代区域成岩—极低级变质作用研究。东北亚地区油气地质与矿产资源学术研讨会,2008.5
[60]王成文,马志红,孙跃武,等.晚古生代海相地层———东北地区油气勘查的一个新层系[ J ] .世界地质,2008 ,27 (2) :1132118.
[61]董申葆,沈其韩,孙大中,等.中国变质地质图(1∶4 00万) [M] .北京:地质出版社,1996.
[62]董申保.中国变质作用及其与地壳演化关系.北京:地质出版社,1986.10～14
[63]贺高品,李应场.新疆准噶尔—北天山地区古生代的埋藏变质作用.见:长春地质学院地质研究所文集,北京:地震出版社,1992.48～61
[64]索书田,毕仙梅,周汉文.极低级变质作用.地质出版社,1999.
[65]董申保.中国变质作用及其与地壳演化关系.北京:地质出版社,1986.10～14