Quantitative simulation of the densification process of sandstone reservoir in the Xu 3 Member of Xujiahe Formation in western Sichuan Depression, Sichuan Basin
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摘要:
为了明确川西坳陷须三段砂岩储层致密化过程, 定量恢复致密砂岩储层孔隙度演化, 综合利用常规薄片、铸体薄片、扫描电镜和包裹体等资料, 对须三段成岩作用进行了系统分析, 探讨了成岩作用与孔隙度演化之间的关系。在此基础上, 结合地层埋藏史和热演化史研究, 基于效应模拟原则, 即不对具体成岩作用进行模拟, 而是通过地质参数来模拟各种成岩作用的综合叠加结果, 从而建立须三段砂岩孔隙度演化数学模型, 明确砂岩储层致密化过程。研究结果表明: 须三段主要发育岩屑石英砂岩和岩屑砂岩; 砂岩经历压实、胶结、溶蚀等成岩作用, 其中压实作用和胶结作用是主要的破坏性成岩作用, 且一直存在于砂岩储层演化过程中; 溶蚀作用是主要的建设性成岩作用, 且只出现在特定的60~120℃温度窗口。基于对现今砂岩孔隙度与深度关系的观察, 明确砂岩先后经历了压实、胶结作用和溶蚀作用, 以及溶蚀后的压实、胶结作用。因此, 可将孔隙度演化划分为正常压实与胶结阶段、溶蚀增孔阶段和溶蚀后正常压实与胶结3个阶段。此外, 将孔隙度演化分解为孔隙度减小模型和孔隙度增大模型, 这2种模型在孔隙度演化的3个阶段分别叠加, 可得到模拟孔隙度演化的三段式分段函数模型, 进而实现砂岩储层孔隙度演化过程模拟。通过应用该模型对典型砂岩储层孔隙度演化过程的模拟表明, 川西坳陷须三段因压实作用和早期胶结作用影响, 具有早期致密的特点。
Abstract:In order to clarify the densification process and quantitatively restore the porosity evolution of the Xu 3 Member sandstone reservoir in western Sichuan Depression, the diagenesis of the Xu 3 Member was system atically analyzed using thin sections, scanning electron microscope and fluid inclusion analysis. Meanwhile, the relationship between diagenesis and porosity evolution was discussed.Based on the study of formation burial history and thermal evolution history, a mathematical model of porosity evolution for the Xu 3 Member sandstone was established to clarify the densification process of sandstone reservoir using the principle of effect simulation, that is, the specific diagenesis was not simulated, but the comprehensive superposition results of various diagenesis were simulated through geological parameters.It found that lithic quartz sandstone and lithic sandstone were mainly developed in the Xu 3 Member, and sand stone underwent compaction, cementation, dissolution and others. Among them, compaction and cementation are the main destructive diagenesis and occur in the whole evolution process, while dissolution is the main constructive diagenesis and only occurs in a specific evolution stage with window characteristics.Based on the current observation of the relationship between porosity and depth of sandstone, the sandstone had undergone compaction and cementation, corrosion, and compaction and cementation after corrosion.As a result, the porosity evolution could be divided into three stages: normal compaction stage, pore increasing stage during corrosion andnormal compaction after corrosion.Furthermore, the porosity evolution could be divided into porosity decreasing model and porosity increasing model.These two models were superimposed on the three stages of porosity evolution, and a three-stage piecewise function characterized the porosity evolution was proposed.Using this function, the total porosity evolution simulation of sandstone reservoir could be realized.Simulation results found that the Xu 3 Member in western Sichuan Depression was dominated by early densification due to compaction and early cementation using the proposed quantitative model.
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图 1 川西坳陷主要井位分布、构造单元划及须家河组地层剖面图
Figure 1. Main well location distribution, structural unit division and stratigraphic profile of Xujiahe Formation in western Sichuan Depression
图 2 川西坳陷须三段储层岩性三角图
Figure 2. Lithology triangle map of Xu 3 Member reservoir in western Sichuan Depression
图 3 川西坳陷须家河组须三段砂岩储层压实特征
a.线-凹凸接触，大邑6井，5 562.44 m，(+)，铸体薄片；b.长石颗粒变形，大邑6井，5 532.94 m，(+)，普通薄片；c.长石颗粒破裂，大邑4井，5 005.6 m，(+)，普通薄片；d.早期方解石胶结充填粒间孔，大邑101井，4 611.67 m，(-)，铸体薄片
Figure 3. Compaction characteristics of sandstone reservoirs in Xu 3 Member in western Sichuan Depression
图 4 川西坳陷须家河组须三段胶结作用特征(蓝色为铸体薄片孔隙)
a.2期石英次生加大，大邑1井，4 637.19 m，(+)，铸体薄片；b.粒间溶孔充填自生石英晶体，新856井，4 217.1 m，(-)，铸体薄片；c.次生石英晶体充填于粒间孔，鸭3井，3 427.6 m，扫描电镜；d.白云石充填粒间孔和粒内溶孔，大邑2井，4 605.5 m，(-)，普通薄片；e.方解石胶结物充填粒内溶孔，大邑103井，4 693 m，(-)，铸体薄片；f.铁方解石充填粒间孔和粒内溶孔，鸭3井，3 427.6 m，(-)，普通薄片；g.铁白云石中充填粒间孔和粒内溶孔，新856井，4 001.77 m，(-)，铸体薄片；h.铁方解石交代充填长石粒内溶孔的白云石，大邑1井，4 645.87 m，(-)，普通薄片；i.方解石胶结物充填裂缝，大邑2井，4 605.02 m，(-)，铸体薄片; j.粒间、粒内早期碳酸盐发亮红光，粒间、粒内中期铁方解石和铁白云石发暗红光-不发光，大邑2井，4 604.9 m，阴极发光; k.粒间、粒内早期碳酸盐发亮红光，粒间、粒内中期铁方解石和铁白云石发暗红光-不发光，大邑102井，4 590.68 m，阴极发光; l.晚期充填裂缝方解石发红光，大邑102井，4 599.06 m，阴极发光
Figure 4. Quartz and carbonate cementation characteristics of the Xu 3 Member in western Sichuan Depression
图 5 四川盆地川西坳陷须三段砂岩储层胶结物盐水包裹体均一温度直方图
Figure 5. Histogram of brine inclusion homogenization temperature of authigenic cements in Xu 3 Member sandstone reservoir in western Sichuan Depression, Sichuan Basin
图 6 川西坳陷须家河组须三段胶结作用和溶蚀作用特征(蓝色为铸体薄片孔隙)
a.高岭石胶结物充填粒内溶孔，鸭3井，3 427.6 m，(-)，铸体薄片；b.伊利石胶结物充填粒间孔，川绵39井，5 119.41 m，扫描电镜；c.颗粒表面绿泥石，大邑2井，4 616.76 m，扫描电镜；d.黏土矿物交代石英次生加大边, 大邑102井，4 592.91 m，(+)，普通薄片；e.长石胶结物交代石英次生加大边，大邑102井，4 584.76 m，正交光；f.高岭石胶结物充填粒内溶孔，且形成于铁方解石胶结之前，大邑1井，4 638.45 m，单偏光；g.长石次生加大，大邑102井，4 585.68 m，(+)，普通薄片；h.长石粒内溶蚀，大邑2井，4 617.81 m，(-)，铸体薄片；i.岩屑粒内溶蚀，川绵39井，5 119.41 m，(-)，铸体薄片
Figure 6. Clay mineral and feldspar cementation and dissolution characteristics of Xu 3 Member in western Sichuan Depression
图 7 川西坳陷须家河组须三段储集层镜下包裹体特征
a.粒间碳酸盐胶结物包裹体均一温度，新856井，3 996.04 m；b.粒间碳酸盐胶结物包裹体均一温度，大邑2井，4 605.02 m；c.粒间碳酸盐胶结物包裹体均一温度，大邑2井，4 605.02 m；d.石英次生加大边包裹体均一温度，川孝568井，4 080.73 m；e.石英次生加大边包裹体均一温度，大邑102井，4 601.12 m；f.石英次生加大边包裹体均一温度，大邑2井，4 605.02 m；g.裂缝中方解石包裹体均一温度，大邑102井，4 599.16 m；h.裂缝中方解石包裹体均一温度，大邑2井，4 605.02 m；i.裂缝中方解石包裹体均一温度，大邑2井，4 605.02 m
Figure 7. Microscopic inclusion characteristics of the Xu 3 Member of the Xujiahe Formation in western Sichuan Depression
图 8 四川盆地川西坳陷须三段砂岩储层成岩序列
T.三叠纪; J.侏罗纪; K.白垩纪; E.古近纪; N.新近纪; Q.第四纪; J3p.蓬莱镇组; J3sn.遂宁组; J2s.上沙溪庙组; J2x.下沙溪庙组; J2q.千佛崖组; J1b.白田坝组; T3x5.须五段; T3x4.须四段; T3x3.须三段
Figure 8. Diagenetic sequence of Xu 3 Member sandstone in western Sichuan Depression, Sichuan Basin
图 9 四川盆地川西坳陷须家河组砂岩孔隙度现今剖面特征
Figure 9. Relationship between porosity and burial depth of Xu 3 Member sandstone, western Sichuan Depression, Sichuan Basin
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