东海丽水凹陷古新统源-汇系统及控砂模式
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摘要
东海丽水凹陷浅层明月峰组下段和灵峰组上段已发现丽水36-1气田,但对中深层灵峰组勘探尚未获得大的突破,关键原因之一在于中深层砂体变化快、储层预测难度大。根据源-汇系统的研究思路,对物源类型、母岩特征、汇聚体系、聚砂模式等进行了分析。分析结果表明,丽水凹陷发育三大物源(闽浙隆起带、雁荡凸起和灵峰潜山)、3种汇聚通道(侵蚀沟谷、断面、断槽)以及5种控砂模式(陡坡带沟谷式控砂模式、断槽控制轴向源-汇控砂模式;缓坡带沟谷式控砂模式、缓坡带同生断层控砂模式和凸起陡坡带断面控砂模式)。缓坡带沟谷式控砂模式是浅层明月峰组砂体发育的有利模式,陡坡带沟谷式控砂模式、断槽控制轴向源-汇控砂模式、缓坡带同生断层控砂模式是丽水凹陷西次凹中南部深层灵峰组砂体发育的有利模式,凸起陡坡带断面控砂模式是东次凹陡坡带砂体发育的有利模式。
Lishui 36-1 gas field has been found in Lower Mingyuefeng Formation and Upper Lingfeng Formation in Lishui Sag, East China Sea Basin. However, there is no critical breakthrough in mid-deep strata of Lingfeng Formation because quick transformation of sandbodies increasesthe difficulties for reservoir predicting. According to the approach of the source-to-sink system, the source types, source rock characteristics, accumulation pattern and sand-controlling model have been analyzed. The analysis indicates that 3 source types( Minzhe uplift zone, Yandang uplift and Lingfeng buried hills), 3 transporting channels(erosion valleys, fault surface, fault trough) and 5 sand-controlling models(the valley sand-controlling model of steep slope, the trough-control axial source-sink sand-control model, the valley-style sand-control model of gentle slope and the contemporaneous fault sand-control model of gentle slope) are developed in Lishui Sag. The first model is profitable for high-quality reservoir in shallow strata while the next three models are beneficial for Lingfeng lithologic reservoirs. The last model is beneficial for sandbody accumulation in the east steep slope.
Lishui 36-1 gas field has been found in Lower Mingyuefeng Formation and Upper Lingfeng Formation in Lishui Sag, East China Sea Basin. However, there is no critical breakthrough in mid-deep strata of Lingfeng Formation because quick transformation of sandbodies increasesthe difficulties for reservoir predicting. According to the approach of the source-to-sink system, the source types, source rock characteristics, accumulation pattern and sand-controlling model have been analyzed. The analysis indicates that 3 source types( Minzhe uplift zone, Yandang uplift and Lingfeng buried hills), 3 transporting channels(erosion valleys, fault surface, fault trough) and 5 sand-controlling models(the valley sand-controlling model of steep slope, the trough-control axial source-sink sand-control model, the valley-style sand-control model of gentle slope and the contemporaneous fault sand-control model of gentle slope) are developed in Lishui Sag. The first model is profitable for high-quality reservoir in shallow strata while the next three models are beneficial for Lingfeng lithologic reservoirs. The last model is beneficial for sandbody accumulation in the east steep slope.
引文
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[14] 徐长贵.陆相断陷盆地源-汇时空耦合控砂原理: 基本思想、概念体系及控砂模式[J].中国海上油气,2013,25(4):1-11.
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[17] 李超,杨守业,毕磊,等.“从源到汇”的时间尺度:根据U系同位素计算海洋沉积物的搬运时间[J].海洋地质前沿,2015,31(2):26-31.
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[22] 杨守业,毕磊,郭玉龙.东亚大陆边缘两类河流体系的风化与源汇沉积过程[J].吉林大学学报:地球科学版,2015,45(1):1512.
[23] 刘俊海,杨香华,吴志轩,等.东海盆地丽水凹陷古新统锆石示踪作用分析[J].海洋地质与第四纪地质,2004,24(1):85-92.
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[27] 周士科,徐长贵.轴向重力流沉积:一种重要的深水储层:以东海盆地丽水凹陷明月峰组为例[J].地质科技情报,2006,7(4):57-62.
[28] 田兵,庞国印,王琪,等.叠合断陷盆地油气成藏条件分析:以东海丽水-椒江凹陷为例[J].岩性油气藏,2012,24(5):32-37.
[29] 王德滋, 赵广涛, 邱检生.中国东部晚中生代A型花岗岩的构造制约[J].高校地质学报,1995,1(2):13-21.
[30] 邱检生,肖娥,胡键,等.福建北部沿海高分异I型花岗岩的成因: 锆石U-Pb年代学、地球化学和Nd-Hf同位素制约[J].岩石学报,2008,24(11):2468-2484.
[31] 邱检生, 刘亮, 李真.浙江黄岩望海岗石英正长岩的锆石U-Pb年代学与Sr-Nd-Hf同位素地球化学及其对岩石成因的制约[J].岩石学报,2011,27(6):1557-1572.
[32] 李艳军,魏俊浩,姚春亮,等.浙东南石平川花岗岩体LA-ICP-MS锆石U-Pb年代学及构造意义[J].地质论评,2009,55(5):673-684.
[33] 邢光福,陶奎元,杨祝良,等.中国东南沿海中生代火山岩成因研究现状与展望[J].矿物岩石地球化学通报,1999,18(3):189-193.
[34] 叶茂松,解习农,黄灿.陆相坳陷湖盆斜坡带层序格架下沉积模式及隐蔽圈闭勘探:以准噶尔盆地车排子凸起春光油田白垩系为例[J].地质科技情报,2014,33(4):14-158.
[35] 侯国伟,刘金水,周瑞华,等.丽水凹陷低位扇群沉积模式[J].岩性油气藏,2015,27(5):240-244.
[36] Hou Y,He S,Ni J,et al.Tectono-sequence stratigraphic analysis on Paleogene Shahejie Formation in the Banqiao sub-basin,Eastern China[J].Marine and Petroleum Geology,2012,36(1):100-117.
[37] 刘程,周林乾,廖远涛,等.酒泉盆地营尔凹陷下沟组沉积特征及其控制因素[J].地质科技情报,2016,35(3):87-96.
[2] Masona C C,Fildanib A,Gerber T, et al.Climatic and anthropogenic influences on sediment mixing in the Mississippi source-to-sink system using detrital zircons: Late Pleistocene to recent [J].Earth and Planetary Science Letters,2017,458:366-379.
[3] Chorng Shernhorng, Chih Anhuh.Magnetic properties as tracers for source-to-sink dispersal of sediments: A case study in the Taiwan strait short communication[J].Earth and Planetary Science Letters,2011(1/2),309:141-152.
[4] Schattner U,Lazar M.Hierarchy of source-to-sink systems:Example from the Nile distribution across the eastern Mediterranean[J].Sedimentary Geology,2016,343:119-131.
[5] Zhao Yifei, Zou Xinqing, Gao Jianhua,et al.Clay mineralogy and source-to-sink transport processes of Changjiang River sediments in the estuarine and inner shelf areas of the East China Sea[J].Journal of Asian Earth Sciences,2018,152:91-102.
[6] Leithold E L,Blair N E,Wegmann K W.Source-to-sink sedimentary systems and global carbon burial: A river runs through it[J].Earth-Science Reviews,2016,153:30-42.
[7] Li Chao, Yang Shouye, Zhao Jianxin,et al.The time scale of river sediment source-to-sink processes in East Asia[J].Chemical Geology,2016,446:138-146.
[8] Amorosi A.Chromium and nickel as indicators of source-to-sink sediment transfer in a Holocene alluvial and coastal system (Po Plain, Italy)[J].Sedimentary Geology,2012,280:260-269.
[9] Warrick J A.Eel River margin source-to-sink sediment budgets: Revisited[J].Marine Geology,2014,351:25-37.
[10] Alxander C, Walsh J, Orpin A.Modern sediment dispersal and accumulation on the outer poverty continental margin[J].Marine Geology,2010,270(1/4):213-226.
[11] Berryman K,Marden K,Marden M,et al.The postglacial downcutting history in the Waihuka tributary of Waipaoa River,Gisborne district: Implications for tectnonics and landscape evelation in the Hikurangi subduction margion, New Zealand[J].Marine Geology,2010,270(1/4):55-71.
[12] Carter L,Orpin A R,Kuehl S A.From mountain source to ocean sink:The passage of sediment across an active margin, Waipaoa sedimentary system,New Zealand[J].Marine Geology,2010,270(1/4):1-10.
[13] Fuller I C,Marden M.Rapid channel response to variability in sedimentary supply: Cutting and filling of the Tatndale fan,Waipaoa catchment,New Zealand[J].Marine Geology,2010,270(1/4):45-54.
[14] 徐长贵.陆相断陷盆地源-汇时空耦合控砂原理: 基本思想、概念体系及控砂模式[J].中国海上油气,2013,25(4):1-11.
[15] 徐长贵,杜晓峰.陆相断陷盆地源-汇理论工业化应用初探-以渤海海域为例[J].中国海上油气,2017,29(4):9-18.
[16] 林畅松,夏庆龙,施和生,等.地貌演化、源-汇过程与盆地分析[J].地学前缘,2015,22(1):9-20.
[17] 李超,杨守业,毕磊,等.“从源到汇”的时间尺度:根据U系同位素计算海洋沉积物的搬运时间[J].海洋地质前沿,2015,31(2):26-31.
[18] 施和生.油气勘探“源-汇-聚”评价体系及其应用:以珠江口盆地珠一坳陷为例[J].中国海上油气,2015,27(5):1-12.
[19] 祝彦贺,朱伟林,徐强,等.珠江口盆地13.8 Ma陆架边缘三角洲与陆坡深水扇的“源-汇”关系[J].中南大学学报:自然科学版,2011,42(12):3827-3834.
[20] 王珊珊, 曹志敏, 蓝东兆, 等.河口近岸海域源-汇意义分析:以珠江河口海域沉积物中重金属计算分析为例[J].科技通报,2014,30(1):199-202.
[21] 董爱国.黄、东海海域沉积物的源汇效应及其环境意义[D].山东青岛:中国海洋大学,2011.
[22] 杨守业,毕磊,郭玉龙.东亚大陆边缘两类河流体系的风化与源汇沉积过程[J].吉林大学学报:地球科学版,2015,45(1):1512.
[23] 刘俊海,杨香华,吴志轩,等.东海盆地丽水凹陷古新统锆石示踪作用分析[J].海洋地质与第四纪地质,2004,24(1):85-92.
[24] 张妮.沉积盆地的物源综合研究[D].南京:南京大学,2012.
[25] 林孝先.陆源碎屑岩盆地综合物源分析:以鄂尔多斯盆地北部山西组为例[D].成都:成都理工大学,2012.
[26] 樊太亮,吕延仓,丁明华.层序地层体制中的陆相储层发育规律[J].地学前缘,2000,25(5):315-321.
[27] 周士科,徐长贵.轴向重力流沉积:一种重要的深水储层:以东海盆地丽水凹陷明月峰组为例[J].地质科技情报,2006,7(4):57-62.
[28] 田兵,庞国印,王琪,等.叠合断陷盆地油气成藏条件分析:以东海丽水-椒江凹陷为例[J].岩性油气藏,2012,24(5):32-37.
[29] 王德滋, 赵广涛, 邱检生.中国东部晚中生代A型花岗岩的构造制约[J].高校地质学报,1995,1(2):13-21.
[30] 邱检生,肖娥,胡键,等.福建北部沿海高分异I型花岗岩的成因: 锆石U-Pb年代学、地球化学和Nd-Hf同位素制约[J].岩石学报,2008,24(11):2468-2484.
[31] 邱检生, 刘亮, 李真.浙江黄岩望海岗石英正长岩的锆石U-Pb年代学与Sr-Nd-Hf同位素地球化学及其对岩石成因的制约[J].岩石学报,2011,27(6):1557-1572.
[32] 李艳军,魏俊浩,姚春亮,等.浙东南石平川花岗岩体LA-ICP-MS锆石U-Pb年代学及构造意义[J].地质论评,2009,55(5):673-684.
[33] 邢光福,陶奎元,杨祝良,等.中国东南沿海中生代火山岩成因研究现状与展望[J].矿物岩石地球化学通报,1999,18(3):189-193.
[34] 叶茂松,解习农,黄灿.陆相坳陷湖盆斜坡带层序格架下沉积模式及隐蔽圈闭勘探:以准噶尔盆地车排子凸起春光油田白垩系为例[J].地质科技情报,2014,33(4):14-158.
[35] 侯国伟,刘金水,周瑞华,等.丽水凹陷低位扇群沉积模式[J].岩性油气藏,2015,27(5):240-244.
[36] Hou Y,He S,Ni J,et al.Tectono-sequence stratigraphic analysis on Paleogene Shahejie Formation in the Banqiao sub-basin,Eastern China[J].Marine and Petroleum Geology,2012,36(1):100-117.
[37] 刘程,周林乾,廖远涛,等.酒泉盆地营尔凹陷下沟组沉积特征及其控制因素[J].地质科技情报,2016,35(3):87-96.