深部热流体活动对储层成岩作用及孔隙演化的影响:以莺歌海盆地LDX区中新统黄流组为例

doi:10.13745/j.esf.sf.2022.2.57

地学前缘 ›› 2022, Vol. 29 ›› Issue (4): 412-429.DOI: 10.13745/j.esf.sf.2022.2.57

深部热流体活动对储层成岩作用及孔隙演化的影响:以莺歌海盆地LDX区中新统黄流组为例

曹江骏¹(), 罗静兰¹^,^*(), 范彩伟², 李珊珊², 吴仕玖², 符勇¹, 史肖凡¹, 代龙², 侯静娴²

1.西北大学地质学系/大陆动力学国家重点实验室, 陕西西安 710069
2.中海石油(中国)有限公司湛江分公司, 广东湛江 524057

收稿日期:2021-09-02 修回日期:2022-02-25 出版日期:2022-07-25 发布日期:2022-07-28
通讯作者: 罗静兰
作者简介:曹江骏(1993—),男,博士研究生,主要从事沉积学与储层地质学方面的研究工作。E-mail: 282945358@qq.com
基金资助:
国家自然科学基金面上项目(41972129);国家科技重大专项课题(2016ZX05026-003-005);国家科技重大专项课题(2016ZX05024-005);中海油湛江分公司“南海西部高温高压气藏勘探开发技术及勘探新领域研究项目(CNOOC-KJ135ZDXM38ZJ02ZJ)

Deep thermal fluid activity and its influence on the diagenesis and pore evolution of reservoirs: A case study from the Miocene Huangliu Formation reservoir in the LDX area, Yinggehai Basin, northern South China Sea

CAO Jiangjun¹(), LUO Jinglan¹^,^*(), FAN Caiwei², LI Shanshan², WU Shijiu², FU Yong¹, SHI Xiaofan¹, DAI Long², HOU Jingxian²

1. Department of Geology/State Key Laboratory of Continental Dynamics, Northwest University, Xi’an 710069, China
2. Zhanjiang Branch of CNOOC Ltd, Zhanjiang 524057, China

Received:2021-09-02 Revised:2022-02-25 Online:2022-07-25 Published:2022-07-28
Contact: LUO Jinglan

摘要/Abstract

摘要：

为了解莺歌海盆地深部热流体主要类型,研究热流体特征,判断热流体活动范围,分析热流体对储层成岩-孔隙演化的影响,通过铸体薄片、扫描电镜、黏土矿物X射线衍射、物性、电子探针、包裹体均一温度、稳定同位素等分析测试手段,结合前人研究成果,对盆内LDX区中新统黄流组储层进行分析。结果表明,受构造热事件影响及深大断裂控制,在超压驱动下,热流体活动范围主要为3 900 m以下的黄流组中下部,以CO₂热流体为主,H₂S热流体次之。热流体影响下储层具有自生黏土矿物转化速率加快、镜质体反射率突变、地层水矿化度降低、包裹体均一温度大于正常地层最高温度、热液成因矿物发育等特点。将黄流组储层分为超压储层(黄流组中上部)及热超压储层(黄流组中下部)两类。其中,超压储层成岩作用阶段达中成岩A₂亚期,压实及溶蚀作用较弱,胶结作用较强,孔隙演化经历了压实减孔、压实与胶结减孔、胶结减孔与有机酸溶蚀增孔3个过程,孔隙度从38.8%减少到现今的7.6%;热超压储层成岩作用阶段达中成岩B期,压实及溶蚀作用较强,胶结作用较弱,孔隙演化经历了压实减孔、压实与胶结减孔、胶结减孔与有机酸溶蚀增孔、胶结减孔与有机酸及无机酸溶蚀增孔4个过程,孔隙度从38.1%减少到现今的9.2%。有利储层主要发育在黄流组中下部黄二段的热超压储层中。

关键词: 深部热流体, 成岩-孔隙演化, 有利储层, 中新统黄流组, LDX区, 莺歌海盆地

Abstract:

In order to understand the main types of deep-seated thermal fluid in the Yinggehai Basin, We studied the thermal fluid characteristics, determined the range of thermal fluid activity, and analyzed the thermal fluid influence on reservoir diagenesis and pore evolution. Combined with previous research results, we investigated the Miocene Huangliu Formation reservoir in the LDX area by blue epoxy resin-impregnated thin section, scanning electron microscope, clay mineral quantification by XRD, physical property, electron probe, fluid inclusion homogenization temperature, and stable isotope analyses. Results showed that the deep-seated thermal fluid activity—which is affected by tectonic thermal events, controlled by an abyssal fault, driven by overpressure, and dominated by CO₂ thermal fluid and to a lesser extent by H₂S thermal fluid—mainly influenced the middle and lower parts of the Huangliu Formation below 3900 m. The reservoir is characterized by the accelerated transformation of authigenic clay minerals, vitrinite reflectance mutation, reduced formation water salinity, inclusion homogenization temperature above the normal formation maximum temperature, and hydrothermal mineral development under the influence of deep therrmal fluids. The Huangliu Formation involves two types of reservoirs: overpressure reservoir (middle-upper parts of the Huangliu Formation) and thermal overpressure reservoir (lower-middle parts of the Huangliu Formation). The diagenetic stage of the overpressure reservoir reached substage A₂ of mesodiagenesis, with relatively weak compaction, weak dissolution and strong cementation, and experienced pore evolution in three stages: porosity decrease by compaction, porosity decrease by compaction and cementation, and porosity decrease by cementation combined with porosity increase by organic acid dissolution. Overall, porosity decreased from 38.8% to 7.6%. The diagenetic stage in the thermal overpressure reservoir reached stage B of mesodiagenesis, with relatively strong compaction, strong dissolution and weak cementation, and experienced pore evolution in four stages: stages 1-3 are the same as in substage A₂, and stage 4 is similar to stage 3 except the porosity increase is caused by both organic acid and inorganic acid dissolutions. Overall, porosity decreased from 38.1% to 9.2%. Favorable reservoirs mainly develope in the thermal overpressure reservoirs of the second member of the lower-middle parts of the Huangliu Formation.

Key words: deep-seated hot fluid, diagentic-pore evolution, favorable reservoir, Miocene Huangliu Formation, LDX area, Yinggehai Basin

中图分类号:

TE122.3

曹江骏, 罗静兰, 范彩伟, 李珊珊, 吴仕玖, 符勇, 史肖凡, 代龙, 侯静娴. 深部热流体活动对储层成岩作用及孔隙演化的影响:以莺歌海盆地LDX区中新统黄流组为例[J]. 地学前缘, 2022, 29(4): 412-429.

CAO Jiangjun, LUO Jinglan, FAN Caiwei, LI Shanshan, WU Shijiu, FU Yong, SHI Xiaofan, DAI Long, HOU Jingxian. Deep thermal fluid activity and its influence on the diagenesis and pore evolution of reservoirs: A case study from the Miocene Huangliu Formation reservoir in the LDX area, Yinggehai Basin, northern South China Sea[J]. Earth Science Frontiers, 2022, 29(4): 412-429.

图/表 13

图1 莺歌海盆地区域构造划分(a)及地层综合柱状图(b)(据文献[10,20,26]修改)

Fig.1 Regional structure division (a) and comprehensive stratigraphic histogram (b) map of Yinggehai Basin. Modified after [10,20,26].

图2 莺歌海盆地LDX区自生黏土矿物相对含量随深度变化散点图

Fig.2 The scatter diagram of the relative content of authigenic clay minerals varying with depth in the LDX area, Yinggehai Basin

图3 莺歌海盆地LDX区镜质体反射率对数(a)及地层水总矿化度(b)随深度变化散点图

Fig.3 The scatter diagram of logarithm of vitrinite reflectance (a) and total mineralization of strata water (b) varying with depth in the LDX area, Yinggehai Basin

图4 莺歌海盆地LDX区黄流组流体包裹体均一温度及盐度分布特征

Fig.4 Distribution characteristics of the homogenization temperature and salinity of fluid inclusions of the Huangliu Formation in the LDX area, Yinggehai Basin

图5 莺歌海盆地LDX区黄流组及梅山组热液成因矿物镜下照片 a—LDX-6井,4 368.4 m,N1h,成岩晚期鞍状铁白云石胶结,铸体薄片;b—LDX-4井,3 902.7 m,N1h,成岩晚期菱铁矿胶结,铸体薄片;c—LDX-2井,4 178.0 m,N1m,成岩晚期团簇状黄铁矿胶结,铸体薄片;d—LDX-11井,4 167.5 m,N1h,重晶石,电子探针;e—LDX-11井,4 167.5 m,N1h,金红石,电子探针;f—LDX-4井,4 149.0 m,N1m,与黄铁矿伴生的磷灰石,电子探针;g—LDX-4井,4 149.0 m,N1m,重晶石,扫描电镜;h—LDX-4井,4 149.0 m,N1m,硫酸铜,扫描电镜;i—LDX-7井,3 997.8 m,N1h,硫酸铜,扫描电镜。

Fig.5 Microscopic photographs of hydrothermal minerals of the Huangliu and Meishan Formations in the LDX area, Yinggehai Basin

图6 莺歌海盆地LDX区黄流组CO2稳定碳同位素随深度变化及分布特征

Fig.6 CO2 stable carbon isotope of the Huangliu Formation in the LDX area, Yinggehai Basin, varying with depth and its distribution characteristics

图7 莺歌海盆地LDX区黄流组碳酸盐胶结物碳、氧同位素随深度变化征及成因(碳酸盐成因图版引自文献[39])

Fig.7 Carbon and oxygen isotopes of carbonate cements of the Huangliu Formation in LDX area, Yinggehai Basin, varying with depth and their genesis. Carbonate genetic plate adapted from [39].

图8 莺歌海盆地LDX区黄流组黄铁矿铁同位素随铁元素含量变化图

Fig.8 Iron isotope of the Huangliu Formation in LDX area, Yinggehai Basin, varying with iron content of pyrite cements

图9 莺歌海盆地LDX区地震剖面(a)及LDX-7井埋藏热史图(b) T30为黄流组顶部地震反射面;T40为黄流组底部地震反射面。

Fig.9 Seismic section (a) and buried thermal history at well LDX-7 (b) in the LDX area, Yinggehai Basin

图10 莺歌海盆地LDX区黄流组不同类型储层成岩作用及物性差异性对比图

Fig.10 Comparative diagram of diagenesis and physical properties of different types of reservoirs of the Huangliu Formation in the LDX area, Yinggehai Basin

图11 莺歌海盆地LDX区黄流组超压及热超压储层特征图

Fig.11 Overpressure reservoir and thermal overpressure reservoir characteristics of the Huangliu Formation in the LDX area, Yinggehai Basin

图12 莺歌海盆地LDX区黄流组储层成岩阶段主要矿物及孔隙类型镜下特征 a—LDX-7井,4 051.0 m,热超压储层,Ⅱ级石英加大边发育,单偏光;b—LDX-4井,3 762.5 m,超压储层,Ⅱ级石英加大边发育,单偏光;c—LDX-11井,热超压储层,4 168.7 m,丝发状伊利石与书页状高岭石胶结,扫描电镜;d—LDX-1井,3 760.0 m,超压储层,针叶状绿泥石胶结,扫描电镜;e—LDX-6井,4 368.4 m,热超压储层,孔隙类型以粒间溶孔为主,含量较高,单偏光;f—LDX-4井,3 710.4 m,超压储层,孔隙类型以粒间溶孔为主,含量较低,单偏光;g—LDX-4井,3 892.3 m,超压储层,铁方解石胶结,含量较高,单偏光;h—LDX-7井,4 051.0 m,热超压储层,铁方解石与铁白云石胶结,含量较低,单偏光。

Fig.12 Microscopic characteristics of the main minerals and pore types in the diagenetic stage of the Huangliu Formation reservoir in the LDX area, Yinggehai Basin

图13 莺歌海盆地LDX区黄流组不同类型储层成岩-孔隙演化综合模式图(古压力演化据文献[48]修改)

Fig.13 Comprehensive model of diagenetic-pore evolutions of different types of reservoirs of the Huangliu Formation in the LDX area, Yinggehai Basin. Evolution of ancient pressure modified after [48].

参考文献 56

[1]	LIANG H R, XU F H, XU G S, et al. Geochemical characteristics and origins of the diagenetic fluids of the Permian Changxing Formation calcites in the southeastern Sichuan Basin: evidence from petrography, inclusions and Sr, C and O isotopes[J]. Marine and Petroleum Geology, 2019, 103: 564-580.
[2]	陈智远, 孟宪武, 宋晓波, 等. 川西地区雷口坡组成岩流体期次及其来源[J]. 油气地质与采收率, 2021, 28(1): 33-40.
[3]	李明诚. 地壳中热流体活动与油气运移[J]. 地学前缘, 1995, 2(4): 155-162.
[4]	刘建章, 刘伟, 王存武. 沉积盆地活动热流体类型及其石油地质意义[J]. 海洋石油, 2004, 24(3): 8-13.
[5]	杜栩, 郑洪印, 焦秀琼. 异常高压力与油气分布[J]. 地学前缘, 1995, 2(4): 137-148.
[6]	解习农, 成建梅, 孟元林, 等. 沉积盆地流体活动及其成岩响应[J]. 沉积学报, 2009, 27(5): 863-871.
[7]	于志超, 刘立, 孙晓明, 等. 歧口凹陷古近纪热流体活动的证据及其对储层物性的影响[J]. 吉林大学学报(地球科学版), 2012, 42(增刊3): 1-13.
[8]	谢习农, 李思田, 董伟良, 等. 热流体活动示踪标志及其地质意义: 以莺歌海盆地为例[J]. 地球科学: 中国地质大学学报, 1999, 24(2): 184-186.
[9]	王振峰, 何家雄, 解习农. 莺歌海盆地泥-流体底辟带热流体活动对天然气运聚成藏的控制作用[J]. 地球科学: 中国地质大学学报, 2004, 29(2): 203-210.
[10]	王翠丽, 周文, 谢玉洪, 等. 莺歌海盆地泥底辟带高温热事件与储层成岩作用[J]. 地质科技情报, 2015, 34(4): 35-42.
[11]	FU M Y, SONG R C, XIE Y H, et al. Diagenesis and reservoir quality of overpressured deep-water sandstone following inorganic carbon dioxide accumulation: Upper Miocene Huangliu Formation, Yinggehai Basin, South China Sea[J]. Marine and Petroleum Geology, 2016, 77: 954-972.
[12]	HUANG Y H, TARANTOLA A, WANG W J, et al. Charge history of CO₂ in Lishui sag, East China Sea basin: evidence from quantitative Raman analysis of CO₂ -bearing fluid inclusions[J]. Marine and Petroleum Geology, 2018, 98: 50-65.
[13]	高玉巧, 刘立. 海拉尔盆地乌尔逊凹陷无机CO₂与油气充注的时间记录[J]. 沉积学报, 2007, 25(4): 574-582.
[14]	刘娜, 吴克强, 刘立, 等. 莺歌海盆地乐东区片钠铝石特征及其对浅层CO₂充注的指示[J]. 地球科学, 2019, 44(8): 2695-2703.
[15]	ZUO Y H, QIU N S, CHANG J, et al. Geothermal regime and source rock thermal evolution in the Chagan Sag, Inner Mongolia, northern China[J]. Marine and Petroleum Geology, 2015, 59: 245-267.
[16]	杨慧. 西湖凹陷SD构造带深部流体对优质储层的影响[D]. 成都: 成都理工大学, 2016.
[17]	谢玉洪, 李绪深, 童传新, 等. 莺歌海盆地中央底辟带高温高压天然气富集条件、分布规律和成藏模式[J]. 中国海上油气, 2015, 27(4): 1-12.
[18]	黄银涛, 姚光庆, 周锋德. 莺歌海盆地黄流组浅海重力流砂体物源分析及油气地质意义[J]. 地球科学, 2016, 41(9): 1526-1538.
[19]	黄银涛, 文力, 姚光庆, 等. 莺歌海盆地东方区黄流组细粒厚层重力流砂体沉积特征[J]. 石油学报, 2018, 39(3): 290-303. DOI
[20]	范彩伟. 莺歌海大型走滑盆地构造变形特征及其地质意义[J]. 石油勘探与开发, 2018, 45(2): 190-199.
[21]	殷秀兰, 李思田. 莺歌海盆地超压体系的成因及与油气的关系[J]. 地质力学学报, 2000, 6(3): 69-77.
[22]	DUAN W, LI C F, LUO C F, et al. Effect of formation overpressure on the reservoir diagenesis and its petroleum geological significance for the DF11 block of the Yinggehai Basin, the South China Sea[J]. Marine and Petroleum Geology, 2018, 97(11): 49-65.
[23]	张伙兰, 裴健翔, 谢金有, 等. 莺歌海盆地东方区黄流组一段超压储层孔隙结构特征[J]. 中国海上油气, 2014, 26(1): 30-38.
[24]	童传新, 孟元林, 谢玉洪, 等. 莺歌海盆地异常高孔带分布与成因分析[J]. 矿物岩石地球化学通报, 2013, 32(6): 720-728.
[25]	王元, 李贤庆, 王刚, 等. 莺琼盆地中新统海相烃源岩地球化学特征及生烃潜力评价[J]. 现代地质, 2018, 32(3): 500-510.
[26]	童传新, 马剑, 裴健翔, 等. 莺歌海盆地东方区中深层天然气地球化学特征与成因[J]. 新疆石油地质, 2015, 36(3): 258-263.
[27]	李伟, 刘平, 艾能平, 等. 莺歌海盆地乐东地区中深层储层发育特征及成因机理[J]. 岩性油气藏, 2020, 32(1): 19-26.
[28]	SUN M, WANG H, LIAO J H, et al. Sedimentary characteristics and model of gravity flow depositional system for the first member of Upper Miocene Huangliu Formation in Dongfang area, Yinggehai Basin, northwestern South China Sea[J]. Journal of Earth Science, 2014, 25(3): 506-518.
[29]	王华, 陈思, 甘华军, 等. 浅海背景下大型浊积扇研究进展及堆积机制探讨: 以莺歌海盆地黄流组重力流为例[J]. 地学前缘, 2015, 22(1): 21-34. DOI
[30]	谢玉洪, 李绪深, 徐新德, 等. 莺-琼盆地高温高压领域天然气成藏与勘探大突破[J]. 中国石油勘探, 2016, 21(4): 19-29.
[31]	何道清. 碳酸盐岩碳、氧同位素分析激光微取样技术[J]. 西南石油学院学报, 2003, 25(1): 12-15,5.
[32]	魏巍, 朱筱敏, 谈明轩, 等. 查干凹陷早白垩世热流体活动的证据及其对巴音戈壁组碎屑岩储层的影响[J]. 石油与天然气地质, 2017, 38(2): 270-280.
[33]	DOW W G. Kerogen studies and geological interpretations[J]. Journal of Geochemical Exploration, 1977, 7: 79-99.
[34]	解习农, 姜涛, 王华, 等. 莺歌海盆地底辟带热流体突破的地层水化学证据[J]. 岩石学报, 2006, 22(8): 2243-2248.
[35]	HALL D L, STERNER S M, BODNAR R J. Freezing point depression of NaCl-KCl-H₂O solutions[J]. Economic Geology, 1988, 83(1): 197-202.
[36]	胡永亮, 王伟, 周传明. 沉积地层中的黄铁矿形态及同位素特征初探: 以华南埃迪卡拉纪深水相地层为例[J]. 沉积学报, 2020, 38(1): 138-149.
[37]	戴金星. 天然气碳氢同位素特征和各类天然气鉴别[J]. 天然气地球科学, 1993, 4(增刊1): 1-40.
[38]	蔡观强, 郭锋, 刘显太, 等. 东营凹陷沙河街组沉积岩碳氧同位素组成的古环境记录[J]. 地球与环境, 2009, 37(4): 347-354.
[39]	尤丽, 范彩伟, 吴仕玖, 等. 莺歌海盆地乐东区储层碳酸盐胶结物成因机理及与流体活动的关系[J]. 地质学报, 2021, 95(2): 578-587.
[40]	COPLEN T B, KENDALL C, HOPPLE J. Comparison of stable isotope reference samples[J]. Nature, 1983, 302(5905): 236-238.
[41]	郑永飞, 陈江峰. 稳定同位素地球化学[M]. 北京: 科学出版社, 2000: 193-247.
[42]	朱东亚, 孟庆强. 塔里木盆地奥陶系碳酸盐岩中黄铁矿的成因[J]. 岩石矿物学杂志, 2010, 29(5): 516-524.
[43]	坚润堂, 杨帆, 赵献昆. 云南省勐腊县曼洒菱铁矿床Fe同位素特征及其地质意义[J]. 岩石矿物学杂志, 2017, 36(3): 389-401.
[44]	JOHNSON C M, BEARD B L, KLEIN C, et al. Iron isotopes constrain biologic and abiologic processes in banded iron formation genesis[J]. Geochimica et Cosmochimica Acta, 2008, 72(1): 151-169.
[45]	费安国, 朱光有, 张水昌, 等. 全球含硫化氢天然气的分布特征及其形成主控因素[J]. 地学前缘, 2010, 17(1): 350-360.
[46]	杜学斌, 姜涛, 王振峰, 等. 莺歌海盆地CO₂气富集与热流体活动关系[J]. 海洋地质与第四纪地质, 2005, 25(2): 109-114.
[47]	谢玉洪, 李绪深, 童传新, 等. 莺琼盆地高温超压天然气成藏理论与勘探实践[M]. 北京: 石油工业出版社, 2015: 102.
[48]	冯冲, 黄志龙, 童传新, 等. 莺歌海盆地地层压力演化特征及其与天然气运聚成藏的关系[J]. 吉林大学学报(地球科学版), 2013, 43(5): 1341-1350.
[49]	FOLK R L. Petrology of sedimentary rock[M]. Austin: Hemphill Publishing Company, 1968.
[50]	国家经济贸易委员会. 碎屑岩成岩阶段划分: SY/T 5477—2003[S]. 北京: 石油工业出版社, 2003.
[51]	范彩伟, 曹江骏, 罗静兰, 等. 异常高压下海相重力流致密砂岩非均质性特征及其影响因素: 以莺歌海盆地LD10区中新统黄流组储集层为例[J]. 石油勘探与开发, 2021, 48(5): 903-915, 949.
[52]	BEARD D C, WEYL P K. Influence of texture on porosity and permeability of unconsolidated sand[J]. AAPG Bulletin, 1973, 57(2): 349-369.
[53]	任大忠, 孙卫, 屈雪峰, 等. 鄂尔多斯盆地延长组长6储层成岩作用特征及孔隙度致密演化[J]. 中南大学学报(自然科学版), 2016, 47(8): 2706-2714.
[54]	宋子齐, 于小龙, 丁健, 等. 利用灰色理论综合评价成岩储集相的方法[J]. 特种油气藏, 2007, 14(1): 26-29, 105.
[55]	朱东亚, 孟庆强, 金之钧, 等. 富CO₂深部流体对碳酸盐岩的溶蚀-充填作用的热力学分析[J]. 地质科学, 2012, 47(1): 187-201.
[56]	罗静兰, 罗晓容, 白玉彬, 等. 差异性成岩演化过程对储层致密化时序与孔隙演化的影响: 以鄂尔多斯盆地西南部长7致密浊积砂岩储层为例[J]. 地球科学与环境学报, 2016, 38(1): 79-92.

深部热流体活动对储层成岩作用及孔隙演化的影响:以莺歌海盆地LDX区中新统黄流组为例

Deep thermal fluid activity and its influence on the diagenesis and pore evolution of reservoirs: A case study from the Miocene Huangliu Formation reservoir in the LDX area, Yinggehai Basin, northern South China Sea

RichHTML

PDF (PC)

可视化

摘要/Abstract

引用本文

使用本文

图/表 13

参考文献 56

相关文章 4

编辑推荐

Metrics

本文评价

[1]	肖萌，袁选俊，吴松涛，曹正林，唐勇，谢宗瑞，王瑞菊. 准噶尔盆地玛湖凹陷百口泉组砾岩储层特征及其主控因素[J]. 地学前缘, 2019, 26(1): 212-224.
[2]	王策, 梁新权, 周云, 付建刚, 蒋英, 董超阁, 谢玉洪, 童传新, 裴健翔, 刘平. 莺歌海盆地东侧物源年龄标志的建立：来自琼西6条主要河流碎屑锆石LA-ICP-MS U-Pb年龄的研究[J]. 地学前缘, 2015, 22(4): 277-289.
[3]	王华, 陈思, 甘华军, 廖计华, 孙鸣. 浅海背景下大型浊积扇研究进展及堆积机制探讨：以莺歌海盆地黄流组重力流为例[J]. 地学前缘, 2015, 22(1): 21-34.
[4]	徐子英, 孙珍, 张云帆, 周蒂, 姜建群, 樊浩. 南海北部陆缘盆地反转构造研究:以莺歌海盆地临高隆起和珠江口盆地琼海凹陷为例[J]. 地学前缘, 2010, 17(4): 90-98.