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    西湖凹陷平湖斜坡有利相带内储层非均质性成因新认识

    谢晓军 熊连桥 韩雅坤 李鑫 陈莹

    谢晓军, 熊连桥, 韩雅坤, 李鑫, 陈莹, 2024. 西湖凹陷平湖斜坡有利相带内储层非均质性成因新认识. 地球科学, 49(4): 1400-1410. doi: 10.3799/dqkx.2022.246
    引用本文: 谢晓军, 熊连桥, 韩雅坤, 李鑫, 陈莹, 2024. 西湖凹陷平湖斜坡有利相带内储层非均质性成因新认识. 地球科学, 49(4): 1400-1410. doi: 10.3799/dqkx.2022.246
    Xie Xiaojun, Xiong Lianqiao, Han Yakun, Li Xin, Chen Ying, 2024. New Insights into Reservoirs Heterogeneous Genesis of Favorable Facies in Pinghu Formation, Xihu Depression. Earth Science, 49(4): 1400-1410. doi: 10.3799/dqkx.2022.246
    Citation: Xie Xiaojun, Xiong Lianqiao, Han Yakun, Li Xin, Chen Ying, 2024. New Insights into Reservoirs Heterogeneous Genesis of Favorable Facies in Pinghu Formation, Xihu Depression. Earth Science, 49(4): 1400-1410. doi: 10.3799/dqkx.2022.246

    西湖凹陷平湖斜坡有利相带内储层非均质性成因新认识

    doi: 10.3799/dqkx.2022.246
    基金项目: 

    “十三五”国家科技重大专项 2016ZX05024002

    中国博士后科学基金 2021M693543

    详细信息
      作者简介:

      谢晓军(1978-),男,博士,高级工程师,主要从事沉积与储层地质研究工作.ORCID:0000-0001-7768-1586. E-mail:xiexj@cnooc.com.cn

      通讯作者:

      李鑫(1988-),男,博士后,工程师,主要从事沉积与储层地质研究工作.ORCID:0000-0001-6334-0369. E-mail: lixin71@cnooc.com.cn

    • 中图分类号: P618

    New Insights into Reservoirs Heterogeneous Genesis of Favorable Facies in Pinghu Formation, Xihu Depression

    • 摘要: 河流-潮汐双向水流沉积环境中,水体方向、动力、化学属性变化频繁,储层矿物基础、成岩过程复杂多变、物性非均质性强,一直是制约其勘探开发的难点.以中国东海西湖凹陷平湖组为例,针对河流-潮汐背景中潮道和水下分流河道两种高能沉积微相,通过岩心观察、孔渗测试、光镜等方法,从物质基础、物性规律、主控因素3个方面开展研究.结果表明:(1)潮道中上部物性好,孔隙度平均18%、渗透率平均120 mD(1 mD≈10-3 μm2),而潮道底部致密,孔隙度平均4%、渗透率平均0.05 mD;呈现非均质性的主要原因是碳酸盐胶结导致底部致密;(2)水下分流河道上部物性好,孔隙度平均5%、渗透率平均70 mD,而水下分流河道底部致密,孔隙度平均1%、渗透率平均0.01 mD;呈现非均质性的主要原因是高岭石充填导致底部致密.上述研究明确了西湖凹陷平湖组2种优势微相的非均质性成因,对深化河流-潮汐背景下储层非均质性规律及成因机制具有重要的理论指导意义;技术方法、研究成果可应用于东海盆地低渗砂岩储层油气勘探,对于中国近海、国外区块的深层碎屑岩储层油气勘探亦具有重要推广借鉴意义.

       

    • 图  1  西湖凹陷区域位置

      Fig.  1.  Regional location map of Xihu depression

      图  2  西湖凹陷平湖组潮道

      a. 潮道孔隙度与渗透率相关性统计图; b.水下分流河道孔隙度与渗透率相关性统计图.1 mD≈10-3 μm2

      Fig.  2.  Physical properties of Pinghu Formation in Xihu sag

      图  3  潮道微相岩心柱状图及典型沉积构造特征(A1井)

      a. 3 445.57 m,褐色泥质薄层;b. 3 442.40 m,潮束构造;c. 3 443.55 m,羽状交错层理;d. 3 445.27 m,脉状层理;e.3 441.72 m,变形层理、泥砾;f. 3 440.62 m,双黏土层

      Fig.  3.  Core histogram and typical sedimentary structure of tidal channel (Well A1)

      图  4  研究区水下分流河道微相储层岩心柱状图(A3井)

      a. 4 202.75 m,岩性截变面、冲刷面;b. 变形构造;c. 4 207.60 m,泄水构造;d. 4 206.70 m,植物碎片;e. 4 201.70 m,截变接触、低角度交错;f. 4 201.40 m,楔状交错层理

      Fig.  4.  Core histogram of underwater distributary channel (Well A3)

      图  5  研究区潮道微相储层孔渗性随深度的变化规律

      a. A1井,3 439.19~3 447.38 m;b.A2井,潮道底部0.50 m

      Fig.  5.  Variation of porosity and permeability of tidal channel

      图  6  研究区水下分流河道微相储层孔渗性随深度的变化规律

      A3井, 4 191.27~4 202.87 m

      Fig.  6.  Variation of porosity and permeability of underwater distributary channel

      图  7  潮道碳酸盐胶结物与孔隙度相关性统计图(a)和碳酸盐胶结物与渗透率相关性统计图(b)

      Fig.  7.  Correlation between carbonate cement and porosity (a) and correlation between carbonate cement and permeability (b) in tidal channel

      图  8  潮道微相储层矿物组成特征及孔隙类型

      Fig.  8.  Mineral composition characteristics and pore types of tidal channel

      图  9  高岭石与孔隙度(a)和渗透率(b)相关性统计

      高岭石含量据A3井薄片统计

      Fig.  9.  Correlation statistics of kaolinite with porosity (a) and permeability (b)

      图  10  水下分流河道微相孔隙类型及矿物充填特征(A3井)

      a~c.河道上部高孔渗带:长石溶蚀孔,其中b为a局部放大;d~f. 河道底部低孔渗带:高岭石充填;g~i.书页状、手风琴状高岭石形态特征

      Fig.  10.  Pore types and mineral filling characteristics of underwater distributary channel (Well A3)

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    • 收稿日期:  2022-02-12
    • 网络出版日期:  2024-04-30
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