鄂尔多斯盆地长7油层组深水重力流沉积分布特征及成因
|
摘要
鄂尔多斯盆地长7油层组广泛发育大规模重力流沉积砂体,对盆地周缘露头及几百口井取心井进行了系统沉积相综合研究。研究结果表明,长7油层组沉积期,湖盆西南及湖盆中部重力流沉积主要为滑塌、砂质碎屑流和浊流,以砂质碎屑流沉积为主;在纵向上,砂质碎屑流沉积和浊流沉积不同组合的多期叠置形成了6种纵向组合类型,并在平面上呈一定的规律性分布;受沉积底形控制,在斜坡区以砂质碎屑流沉积为主,顺斜坡呈带状分布,平面分布规模小;在湖盆中部的坡脚及湖底平原,由于能量减弱,沉积物大量沉积,形成以砂质碎屑流为主的大规模重力流沉积,构成湖盆中部砂体的主体;再往湖盆中心,则主要发育薄层的浊流沉积。成因分析认为,盆地西南较陡的湖盆底形、细粒沉积物的高速率供应和高频次地震促发是重力流砂体发育的重要条件。
The large scale of sand bodies of deep-water gravity flows are developed in Chang7 Reservoir of TriassicYanchang Formation in Ordos Basin.By researching the outcrop and hundreds of drilling corings,an integral study is systematically carried out in sedimentary facies.The result indicates that the sand deposits of deep water gravity flow of Chang7 can be subdivided into slump,sandy debris flow and turbidty flow,in which the sandy debris flow deposits are the main type and the turbidites take second place.The different ways of stacking of the sandy debris flows deposits and turbidites can form 6 styles of vertical architecture,which are regularly distributed in the plane.Controlled by sedimentary bottom shape,in the slope area,debris are the main styles and are banded along the slope.Its distributional scale is relatively small in plane.On the foot of slope and the lake floor plain,owing to the reduction of hydropower,the sedimentations are discharged greatly and formed large scale of gravity flow sedimentation,which mainly are sandy debris flow.It also are the mainly composition of the sand bodies in the center of the basin.Forward to the center of basin,the turbid current deposits of thin layers are mainly developed.The genesis analysis indicates that the high-rate supply of basin-bottom type,fine-grained sediments and high-frequency sub-seismic acceleration are an important condition for the development of gravity-flow sand bodies in the deeper slope area in the southwest of the basin.
The large scale of sand bodies of deep-water gravity flows are developed in Chang7 Reservoir of TriassicYanchang Formation in Ordos Basin.By researching the outcrop and hundreds of drilling corings,an integral study is systematically carried out in sedimentary facies.The result indicates that the sand deposits of deep water gravity flow of Chang7 can be subdivided into slump,sandy debris flow and turbidty flow,in which the sandy debris flow deposits are the main type and the turbidites take second place.The different ways of stacking of the sandy debris flows deposits and turbidites can form 6 styles of vertical architecture,which are regularly distributed in the plane.Controlled by sedimentary bottom shape,in the slope area,debris are the main styles and are banded along the slope.Its distributional scale is relatively small in plane.On the foot of slope and the lake floor plain,owing to the reduction of hydropower,the sedimentations are discharged greatly and formed large scale of gravity flow sedimentation,which mainly are sandy debris flow.It also are the mainly composition of the sand bodies in the center of the basin.Forward to the center of basin,the turbid current deposits of thin layers are mainly developed.The genesis analysis indicates that the high-rate supply of basin-bottom type,fine-grained sediments and high-frequency sub-seismic acceleration are an important condition for the development of gravity-flow sand bodies in the deeper slope area in the southwest of the basin.
引文
[1]Shanmugam G.Ten turbidite myths[J].Earth Science Reviews,2002,58:311～341.
[2] 李云,郑荣才,朱国金,等.沉积物重力流研究进展综述[J].地球科学进展,2011,26( 2) :157～164.
[3]李林,曲永强,孟庆仁,等.重力流沉积:理论研究与野外识别[J].沉积学报,2011,29(4):677～688.
[4] 邹才能,赵文智,张兴阳,等.大型敞流坳陷湖盆浅水三角洲与湖盆中心砂体的形成与分布[J].地质学报,2008,82(6):815～825.
[5]蒲秀刚,周立宏,韩文中,等.岐口凹陷沙一下亚段斜坡区重力流沉积于致密油勘探[J].石油勘探与开发,2014,41(2):138～149.
[6]陈广坡,李娟,吴海波,等.陆相断陷湖盆滑塌型深水重力流沉积特征、识别标志及形成机制——来自海拉尔盆地东明凹陷明D2井全井段连续取心的证据[J].石油学报,2018,39(10):1119～1129.
[7] 李顺明,沈平平,严耀祖.沾化凹陷桩西油田古近系东营组重力流水道的沉积特征及形成条件[J].沉积学报,2010,28(1):83～90.
[8]杨华,李士祥,刘显阳,等.鄂尔多斯盆地致密油、页岩油特征及资源潜力[J].石油学报,2013,34(1):1～11.
[9]付金华,喻建,徐黎明,等.鄂尔多斯盆地致密油勘探开发进展及规模富集可开发主控因素[J].中国石油勘探,2015,20(5):9～19.
[10]杨华,窦伟坦,刘显阳,等.鄂尔多斯盆地三叠系延长组长7沉积相分析[J].沉积学报,2010,28(2):254～263.
[11]杨华,牛小兵,罗顺社,等.鄂尔多斯盆地陇东地区长7段致密砂体重力流沉积模拟实验研究[J].地学前缘,2015,22(3):322～332.
[12]刘芬,朱筱敏,李洋,等.鄂尔多斯盆地西南部延长组重力流沉积特征及相模式[J].石油勘探与开发,2015,42(5):577～588.
[13]李相博,陈启林,刘化清,等.鄂尔多斯盆地延长组3种沉积物重力流及其含油气性[J].岩性油气藏,2010,22(3):16～21.
[14]付金华,罗顺社,牛小兵,等.鄂尔多斯盆地陇东地区长7段沟道型重力流沉积特征研究[J].矿物岩石地球化学通报,2015,34(1):18～24.
[15]廖纪佳,朱筱敏,邓秀芹,等.鄂尔多斯盆地陇东地区延长组重力流沉积特征及其模式[J].地学前缘,2013,20(2):29～39.
[16]李相博,付金华,陈启林,等.砂质碎屑流概念及其在鄂尔多斯盆地延长组深水沉积研究中的应用[J].地球科学进展,2011,26(3):286～294.
[17]邹才能,赵政璋,杨华,等.陆相湖盆深水砂质碎屑流成因机制与分布特征——以鄂尔多斯盆地为例[J].沉积学报,2009,27(6):1065～1075.
[18]庞军刚,李赛,杨友运,等.湖盆深水区细粒沉积成因研究进展——以鄂尔多斯盆地延长组为例[J].石油实验地质,2014,36(6):706～711.
[19]魏斌,魏红红,陈全红,等.鄂尔多斯盆地上三叠统延长组物源分析[J].西北大学学报(自然科学版),2003,33(4):447～450.
[20]何自新.鄂尔多斯盆地演化与油气[M].北京:石油工业出版社,2003:1～153.
[21] 赵俊兴,李凤杰,申晓莉,等.鄂尔多斯盆地南部长6 和长7 油层浊流事件的沉积特征及发育模式[J].石油学报,2008,29(3):389～394.
[22] Rdading H G.Sedimentary Environments:Processes,Fadices and Stratigraphy[M].Oxford :Blackwell Science,1996:407～418.
[23]赵振宇,郭彦如,王艳,等.鄂尔多斯盆地构造演化及古地理特征研究进展[J].特种油气藏,2012,19(5):15～20.
[24]夏义平,徐礼贵,郑良合,等.鄂尔多斯盆地西缘逆冲断裂带构造特征及油气勘探方向[J].石油地质,2005,13(5):13～19.
[25]张天舒,吴因业,郭彬程,等.鄂尔多斯盆地西南缘晚三叠世前陆冲断活动控制的沉积层序特征[J].地学前缘,2012,19(1):40～50.
[27]邓秀芹,蔺昉晓,刘显阳,等.鄂尔多斯盆地三叠系延长组沉积演化及其与早印支运动关系的探讨[J].古地理学报,2008,10(2):159～156.
[28] 赵文智,王新民,郭彦如,等.鄂尔多斯盆地西部晚三叠世原型盆地恢复及其改造演化[J].石油勘探与开发,2006,33(1):6～13.
[29]张文正,杨华,傅锁堂,等.鄂尔多斯盆地晚三叠世湖相优质烃源岩发育段中震积岩的发现及其地质意义[J].西北大学学报(自然科学版),2007,(36):31～37.
[30]夏青松.鄂尔多斯盆地南部上三叠统延长组震积岩的发现及地质意义[J].沉积学报,2007,25(2):246～253.
[2] 李云,郑荣才,朱国金,等.沉积物重力流研究进展综述[J].地球科学进展,2011,26( 2) :157～164.
[3]李林,曲永强,孟庆仁,等.重力流沉积:理论研究与野外识别[J].沉积学报,2011,29(4):677～688.
[4] 邹才能,赵文智,张兴阳,等.大型敞流坳陷湖盆浅水三角洲与湖盆中心砂体的形成与分布[J].地质学报,2008,82(6):815～825.
[5]蒲秀刚,周立宏,韩文中,等.岐口凹陷沙一下亚段斜坡区重力流沉积于致密油勘探[J].石油勘探与开发,2014,41(2):138～149.
[6]陈广坡,李娟,吴海波,等.陆相断陷湖盆滑塌型深水重力流沉积特征、识别标志及形成机制——来自海拉尔盆地东明凹陷明D2井全井段连续取心的证据[J].石油学报,2018,39(10):1119～1129.
[7] 李顺明,沈平平,严耀祖.沾化凹陷桩西油田古近系东营组重力流水道的沉积特征及形成条件[J].沉积学报,2010,28(1):83～90.
[8]杨华,李士祥,刘显阳,等.鄂尔多斯盆地致密油、页岩油特征及资源潜力[J].石油学报,2013,34(1):1～11.
[9]付金华,喻建,徐黎明,等.鄂尔多斯盆地致密油勘探开发进展及规模富集可开发主控因素[J].中国石油勘探,2015,20(5):9～19.
[10]杨华,窦伟坦,刘显阳,等.鄂尔多斯盆地三叠系延长组长7沉积相分析[J].沉积学报,2010,28(2):254～263.
[11]杨华,牛小兵,罗顺社,等.鄂尔多斯盆地陇东地区长7段致密砂体重力流沉积模拟实验研究[J].地学前缘,2015,22(3):322～332.
[12]刘芬,朱筱敏,李洋,等.鄂尔多斯盆地西南部延长组重力流沉积特征及相模式[J].石油勘探与开发,2015,42(5):577～588.
[13]李相博,陈启林,刘化清,等.鄂尔多斯盆地延长组3种沉积物重力流及其含油气性[J].岩性油气藏,2010,22(3):16～21.
[14]付金华,罗顺社,牛小兵,等.鄂尔多斯盆地陇东地区长7段沟道型重力流沉积特征研究[J].矿物岩石地球化学通报,2015,34(1):18～24.
[15]廖纪佳,朱筱敏,邓秀芹,等.鄂尔多斯盆地陇东地区延长组重力流沉积特征及其模式[J].地学前缘,2013,20(2):29～39.
[16]李相博,付金华,陈启林,等.砂质碎屑流概念及其在鄂尔多斯盆地延长组深水沉积研究中的应用[J].地球科学进展,2011,26(3):286～294.
[17]邹才能,赵政璋,杨华,等.陆相湖盆深水砂质碎屑流成因机制与分布特征——以鄂尔多斯盆地为例[J].沉积学报,2009,27(6):1065～1075.
[18]庞军刚,李赛,杨友运,等.湖盆深水区细粒沉积成因研究进展——以鄂尔多斯盆地延长组为例[J].石油实验地质,2014,36(6):706～711.
[19]魏斌,魏红红,陈全红,等.鄂尔多斯盆地上三叠统延长组物源分析[J].西北大学学报(自然科学版),2003,33(4):447～450.
[20]何自新.鄂尔多斯盆地演化与油气[M].北京:石油工业出版社,2003:1～153.
[21] 赵俊兴,李凤杰,申晓莉,等.鄂尔多斯盆地南部长6 和长7 油层浊流事件的沉积特征及发育模式[J].石油学报,2008,29(3):389～394.
[22] Rdading H G.Sedimentary Environments:Processes,Fadices and Stratigraphy[M].Oxford :Blackwell Science,1996:407～418.
[23]赵振宇,郭彦如,王艳,等.鄂尔多斯盆地构造演化及古地理特征研究进展[J].特种油气藏,2012,19(5):15～20.
[24]夏义平,徐礼贵,郑良合,等.鄂尔多斯盆地西缘逆冲断裂带构造特征及油气勘探方向[J].石油地质,2005,13(5):13～19.
[25]张天舒,吴因业,郭彬程,等.鄂尔多斯盆地西南缘晚三叠世前陆冲断活动控制的沉积层序特征[J].地学前缘,2012,19(1):40～50.
[27]邓秀芹,蔺昉晓,刘显阳,等.鄂尔多斯盆地三叠系延长组沉积演化及其与早印支运动关系的探讨[J].古地理学报,2008,10(2):159～156.
[28] 赵文智,王新民,郭彦如,等.鄂尔多斯盆地西部晚三叠世原型盆地恢复及其改造演化[J].石油勘探与开发,2006,33(1):6～13.
[29]张文正,杨华,傅锁堂,等.鄂尔多斯盆地晚三叠世湖相优质烃源岩发育段中震积岩的发现及其地质意义[J].西北大学学报(自然科学版),2007,(36):31～37.
[30]夏青松.鄂尔多斯盆地南部上三叠统延长组震积岩的发现及地质意义[J].沉积学报,2007,25(2):246～253.
© 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 |