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四川盆地复兴地区凉高山组陆相页岩有机质孔隙发育特征及主控因素

王鹏威 申宝剑 刘忠宝 李敏 李倩文 戎佳 王倩茹

王鹏威, 申宝剑, 刘忠宝, 李敏, 李倩文, 戎佳, 王倩茹. 四川盆地复兴地区凉高山组陆相页岩有机质孔隙发育特征及主控因素[J]. 石油实验地质, 2024, 46(3): 499-509. doi: 10.11781/sysydz202403499
引用本文: 王鹏威, 申宝剑, 刘忠宝, 李敏, 李倩文, 戎佳, 王倩茹. 四川盆地复兴地区凉高山组陆相页岩有机质孔隙发育特征及主控因素[J]. 石油实验地质, 2024, 46(3): 499-509. doi: 10.11781/sysydz202403499
WANG Pengwei, SHEN Baojian, LIU Zhongbao, LI Min, LI Qianwen, RONG Jia, WANG Qianru. Characteristics and main controlling factors of organic pore development in continental shales of the Lianggaoshan Formation in the Fuxing area, Sichuan Basin[J]. PETROLEUM GEOLOGY & EXPERIMENT, 2024, 46(3): 499-509. doi: 10.11781/sysydz202403499
Citation: WANG Pengwei, SHEN Baojian, LIU Zhongbao, LI Min, LI Qianwen, RONG Jia, WANG Qianru. Characteristics and main controlling factors of organic pore development in continental shales of the Lianggaoshan Formation in the Fuxing area, Sichuan Basin[J]. PETROLEUM GEOLOGY & EXPERIMENT, 2024, 46(3): 499-509. doi: 10.11781/sysydz202403499

四川盆地复兴地区凉高山组陆相页岩有机质孔隙发育特征及主控因素

doi: 10.11781/sysydz202403499
基金项目: 

国家自然科学基金面上项目 42272143

中国石化科技攻关项目 P22137

详细信息
    作者简介:

    王鹏威(1986—),男,博士、副研究员,从事非常规油气地质研究。E-mail: wangpw.syky@sinopec.com

  • 中图分类号: TE122.23

Characteristics and main controlling factors of organic pore development in continental shales of the Lianggaoshan Formation in the Fuxing area, Sichuan Basin

  • 摘要: 四川盆地复兴地区侏罗系凉高山组发育一套典型的中高成熟度陆相页岩凝析油藏。针对处于凝析油阶段的页岩储层中有机孔发育特征及发育规律的研究比较薄弱,采用全岩光片有机显微组分鉴定、氩离子抛光—扫描电镜观察和能谱测量等实验方法,分析了复兴地区凉高山组页岩有机质孔隙发育特征及主控因素。研究结果表明,在高成熟演化阶段(Ro=1.30%),凉高山组陆相页岩的原始有机质和固体沥青内部发育有机质孔隙,有机质孔以纳米级孔隙为主,形状不规则,以蜂窝状聚集,局部连通形成微米级孔隙或微裂缝。有机显微组分类型是凉高山组页岩有机质孔发育的基础,相对高的有机质丰度及热演化程度是凉高山组页岩有机质孔隙发育多少的关键因素,无机矿物格架及成岩—生烃演化过程是有机质孔保存的最终保障。

     

  • 图  1  四川盆地复兴地区构造位置(a)和Z1井凉高山组地层柱状(b)

    Figure  1.  Structural location of Fuxing area in Sichuan Basin (a) and stratigraphic histogram of Lianggaoshan Formation in well Z1 (b)

    图  2  四川盆地复兴地区Z1井凉高山组页岩原生有机质内有机质孔隙镜下特征

    a-b.2 535.62 m, 原生有机质顺层分布,局部弯曲,有机质内发育孔隙,图b为图a红框部分的放大照片;c-d.2 531.65 m,原生有机质呈三角形,内部发育孔隙,图d为图c红框部分的放大照片;e.2 530.13 m,局部有机孔连通形成大孔隙;f.2 557.18 m,有机质和黏土絮状混杂在一起,有机质内可见有机孔。

    Figure  2.  Microscopic characteristics of organic pores in primary organic matter of shale at Lianggaoshan Formation in well Z1, Fuxing area, Sichuan Basin

    图  3  四川盆地复兴地区Z1井凉高山组页岩固体沥青内有机质孔镜下特征

    a.2 533.92 m, 顺层连续和断续分布的固体沥青,有机质孔发育;b.2 515.42 m,顺层连续和断续分布的固体沥青,局部发生变形,有机质孔发育;c.2 540.08 m,顺层连续和断续分布的固体沥青,有机质孔发育;d-e.2 554.18 m,块状固体沥青,有机质孔发育;f.2 552.42 m, 黄铁矿颗粒间充填沥青,有机质孔发育。

    Figure  3.  Microscopic characteristics of organic pores in bitumen in shale of Lianggaoshan Formation in well Z1, Fuxing area, Sichuan Basin

    图  4  四川盆地复兴地区Z1井凉高山组页岩干酪根碳同位素纵向变化规律

    Figure  4.  Longitudinal variation rule of kerogen carbon isotope in shale of Lianggaoshan Formation in well Z1, Fuxing area, Sichuan Basin

    图  5  四川盆地复兴地区Z1井凉高山组页岩样品光学显微镜和扫描电镜下有机显微组分特征

    a-b.2 562.52 m,黄铁矿晶间固体沥青内发育有机质孔,其他位置镜质体内部分无有机质发育,图b为图a红框部分的SEM照片;c-d.2 513.08 m,镜质体结构紧密,局部富氢组分见有机质孔隙,图d为图c红框部分的SEM照片;e-f.2 558.77 m,有机质结构紧密,局部见有机质孔隙,图f为图e红框部分的SEM照片。

    Figure  5.  Characteristics of organic macerals under optical microscope and scanning electron microscope of shale samples from Lianggaoshan Formation, well Z1, Fuxing area, Sichuan Basin

    图  6  四川盆地复兴地区Z1井凉高山组不同有机显微组分的扫描电镜照片及能量色散光谱

    a-b. 2 563.52 m,21-24代表能谱点;c-d. 2 568.76 m,8和9分别代表能谱点。

    Figure  6.  SEM photos and energy dispersion spectra of different organic macerals of Lianggaoshan Formation in well Z1, Fuxing area, Sichuan Basin

    图  7  四川盆地复兴地区Z1井凉高山组不同有机显微组分的碳元素原子含量百分比

    Figure  7.  Percentage of carbon content from different organic macerals of Lianggaoshan Formation in well Z1, Fuxing area, Sichuan Basin

    图  8  四川盆地复兴地区Z1井凉高山组页岩样品TOC与孔隙度相关关系

    Figure  8.  Correlation between TOC content and porosity of shale samples from Lianggaoshan Formation, well Z1, Fuxing area, Sichuan Basin

    图  9  四川盆地侏罗系陆相页岩与志留系海相页岩矿物含量平均值对比

    Figure  9.  Comparison of average mineral content of Jurassic continental shale and Silurian marine shale in Sichuan Basin

    图  10  不同矿物格架下有机孔发育特征

    a.Z1井,凉高山组,2 560.52 m,石英含量为44.2%,黏土矿物含量为50.2%,长石含量为4.4%,×4 000;b.Z1井,凉高山组,2 532.83 m,石英含量为38.7%,黏土矿物含量为48.8%,长石含量为10.9%,×4 000;c. Z1井,凉高山组,2 535.62 m,石英含量为34.0%,黏土矿物含量为59.0%,长石含量为6.8%,×30 000;d.XL101井,东岳庙段,2 268.9 m,石英含量为20.1%,黏土矿物含量为67.4 %,方解石含量为7.2%,×30 000。Q为石英,CL为黏土矿物,Py为黄铁矿,C为方解石,F为长石。

    Figure  10.  Organic pore development characteristics under different mineral frameworks

    图  11  四川盆地复兴地区中侏罗统凉高山组页岩成岩—生烃演化模式据参考文献[33-34]修改。

    Figure  11.  Evolution model of shale diagenesis and hydrocarbon generation in Middle Jurassic Lianggaoshan Formation in Fuxing area, Sichuan Basin

    表  1  实测四川盆地复兴地区Z1井凉高山组黏土矿物组成

    Table  1.   Measured clay mineral composition of Lianggaoshan Formation in well Z1, Fuxing area, Sichuan Basin

    样品编号 黏土矿物总量/% 伊/蒙间层(I/S) /% 伊利石(I)/ % 绿泥石(C)/ %
    1 72.6 42 28 30
    2 14.1 45 25 30
    3 65.0 48 30 22
    4 63.6 41 28 31
    5 62.6 43 31 26
    6 65.1 39 27 34
    7 64.3 39 28 33
    8 65.7 42 34 24
    9 65.2 45 29 26
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  • 收稿日期:  2023-06-25
  • 修回日期:  2024-04-02
  • 刊出日期:  2024-05-28

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