鄂尔多斯盆地石盒子组-山西组致密储层形成主控因素与发育模式：以彬长地区为例

李松; 马立元; 王濡岳; 邓杰; 李昱东; 全晓园; 蒋融

doi:10.19509/j.cnki.dzkq.tb20220468

鄂尔多斯盆地石盒子组-山西组致密储层形成主控因素与发育模式：以彬长地区为例

doi: 10.19509/j.cnki.dzkq.tb20220468

李松^1,,
马立元¹,
王濡岳^1, ,,
邓杰²,
李昱东³,
全晓园²,
蒋融²

1.
中国石油化工股份有限公司石油勘探开发研究院, 北京 102206
2.
中国石油化工股份有限公司华北油气分公司勘探开发研究院, 郑州 450006
3.
中国石油玉门油田分公司勘探开发研究院, 甘肃酒泉 735008

基金项目:

中国石化科技部项目"鄂尔多斯盆地中石化探区上古生界致密气富集规律与目标优选" P21088-3

详细信息

作者简介:
李松, E-mail: 106155219@qq.com

通讯作者:
王濡岳, E-mail: wry1990@vip.qq.com

中图分类号: P618.130.2⁺1
计量
- 文章访问数: 43
- PDF下载量: 17
- 被引次数: 0
出版历程
- 收稿日期: 2022-08-28
- 录用日期: 2023-03-03
- 修回日期: 2023-02-21

Main controlling factors and development model of tight reservoirs in the Shihezi Formation-Shanxi Formation in the Ordos Basin: Taking the Binchang area as an example

1.
Research Institute of Petroleum Exploration and Production, SINOPEC, Beijing 102206, China
2.
Exploration and Development Research Institute of North China Branch Company, SINOPEC, Zhengzhou 450006, China
3.
Research Institute of Petroleum Exploration & Development, Yumen Oilfield, PetroChina, Jiuquan Gansu 735008, China

More Information

Author Bio:
LI Song, E-mail: 106155219@qq.com

Corresponding author: WANG Ruyue, E-mail: wry1990@vip.qq.com

摘要

摘要:
明确致密储层"甜点"的分布是致密储层油气勘探的重点。通过岩心观察、薄片鉴定、X射线衍射、包裹体均一温度测定、常规物性分析等手段, 对鄂尔多斯盆地南部彬长地区上古生界致密砂岩沉积特征、储层特征、成岩作用进行了详细研究, 明确了储层形成的主要控制因素并建立了优质储层的发育模式。结果表明: 沉积相是储层形成的基础, 辫状河三角洲平原分流河道心滩微相岩石粒度粗, 孔隙结构为小孔-中细喉型, 储层物性相对较好; 曲流河三角洲前缘水下分流河道及河口坝微相岩石粒度细, 孔喉结构为微孔-微喉型, 储层物性相对较差。成岩作用对优质储层的发育与分布具有重要控制作用。间歇性火山凝灰质在酸性地层蚀变为高岭石, 而在碱性地层蚀变为绿泥石套膜, 抑制了石英次生加大和方解石胶结, 保护了储集空间。石英次生加大主要为泥岩转化形成的SiO₂渗滤到砂岩中形成的, 中晚期方解石充填长石、岩屑溶孔为方解石顶底板胶结的主要原因。晚期构造改造形成的微裂缝无方解石胶结, 改善了储层物性, 对气藏起调整作用。彬长地区在3 750 m和3 900 m埋深段附近为2个溶蚀孔发育带。最优储层为溶蚀孔发育带内火山凝灰质转化形成的富含绿泥石套膜的中-粗砂岩; 次优储层主要分布在溶蚀孔发育带内单砂体厚度较大、有旋回且无泥岩隔档的砂体的中下部, 主要为缺少绿泥石套膜的中-粗砂岩, 方解石胶结与石英次生加大作用最低。研究成果进一步深化了鄂尔多斯盆地南部地区上古生界致密砂岩优质储层发育的成因, 对该地区天然气勘探开发具有重要指导意义。
- 沉积相 /
- 成岩作用 /
- 致密储层 /
- 主控因素 /
- 储层发育模式 /
- 上古生界 /
- 鄂尔多斯盆地
Abstract: Objective
Defining the distribution of sweet spots in tight reservoirs is the focus of tight oil and gas exploration.
Methods
Using core observation, thin section identification, X-ray diffraction, homogenization temperature measurements of inclusions, and conventional physical property analysis, the sedimentary characteristics, reservoir characteristics, and diagenesis of Upper Palaeozoic tight sandstones in the Binchang area, southern Ordos Basin were studied in detail.The main controlling factors of reservoir formation were identified and the development model of high-quality reservoirs was established.
Results
The results show that sedimentary facies are the basis of reservoir formation, and the core beach microfacies of the braided river delta plain have coarse grain sizes, small pore-medium-fine throat pore structures, and relatively good reservoir physical properties. The underwater distributary channel and estuary bar in front of the meandering river delta have fine grain sizes and pore throat structures of micropore-microat throat pore structure, and the reservoir's physical properties are relatively poor. Diagenesis plays an important role in controlling the development and distribution of high-quality reservoirs. Intermittent volcanic tuff is transformed into kaolinite in acidic strata and altered into chlorite sheaths in alkaline strata, which inhibits quartz overgrowth and calcite cementation and protects the reservoir space. The secondary enlargement of quartz is mainly caused by the leaching of SiO₂ from mudstone to sandstone.The main reasons for the cementation of calcite roof and floor are the filling of feldspar and the dissolution of cuttings in the middle and late stages of calcite. The microfractures formed by late tectonic transformation have no calcite cementation, which improves the physical properties of the reservoir and plays an adjusting role in the gas reservoir. There are two solution pore development zones near burial depths of 3 750 m and 3 900 m in the Binchang area. The optimal reservoir is the medium-coarse-grained sandstone rich in chlorite mantle formed by the transformation of volcanic tuffaceous matter in the dissolution pore development zone. The sub-optimal reservoir is mainly distributed in the middle and lower parts of the sand body with a greater single-body thickness, cyclicity and no mudstone interval in the dissolution pore development zone.This zone is composed mainly of medium-coarse-grained sandstone lacking chlorite film, calcite cementation and secondary enlargement of quartz are the lowest.
Conclusion
These research results further increase the understanding of the genesis of the development of high-quality tight sandstone reservoirs in the Upper Palaeozoic, providing important guidance for natural gas exploration and development in this area.
- sedimentary facie /
- diagenesis /
- tight reservoir /
- dominant factor /
- reservoir development model /
- Upper Paleozoic /
- Ordos Basin
注释:

所有作者声明不存在利益冲突。

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图 1 鄂尔多斯盆地构造分区(a)及彬长地区上古生界综合柱状图(b)

Figure 1. Tectonic division of the Ordos Basin(a) and the comprehensive columnar map of the Upper Palaeozoic strata in the Binchang area(b)

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图 2 彬长地区不同沉积微相孔渗图

Figure 2. Pore permeability diagram of the different sedimentary microfacies in the Binchang area

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图 3 彬3-长探1井沉积相及粒度概率图

Figure 3. Probability diagram of sedimentary facies and grain size in the Bin 3-Changtan 1 wells

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图 4 长探1井盒1段孔渗-孔喉半径综合分布图

①②③代表不同粒度压汞-孔喉半径与相应的孔渗关系匹配；φ为孔隙度；k为渗透率

Figure 4. Comprehensive diagram of the pore permeability-pore throat radius of the He 1 Member in the Changtan 1 well

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图 5 彬长地区储层成岩阶段及孔隙度演化图

K₁Z.下白垩统志丹群；J.侏罗系；T₃y.上三叠统延长组；T₂Z.中三叠统纸坊组；T₂h.中三叠统和尚沟组；T₁l.下三叠统刘家沟组；P₂sh.中二叠统石千峰组；P₂s.中二叠统上石盒子组；P₁x.下二叠统下石盒子组；P₁s.下二叠统山西组；C₃t.上石炭统太原组

Figure 5. Diagenetic stage and porosity evolution map of reservoirins in the Binchang area

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图 6 彬长地区石盒子组-山西组典型成岩作用微观特征

a.彬1井，3 703.96 m，山1段，黑云母压实变形；b.彬1井，3 704.33 m，山1段，石英次生加大；c.长探1井，3 924.11 m，盒1段，凝灰岩蚀变高岭石；d.彬1井，3 715.02 m，山1段，黏土矿物鳞片状伊利石化；e.彬1井，3 705.03 m，山1段，丝状伊利石充填粒内见晶间孔；f.长探1井，3 767.39 m，盒7段，片状高岭石与丝状伊利石充填孔隙；g.长探1井，3 921.23 m，盒1段，中期方解石交代长石，茜素红红色；h.长探1井，3 919.66 m，山1段，铁方解石交代方解石，茜素红紫色；i.长探1井，3 763.84 m，盒7段，凝灰岩蚀变绿泥石套膜；j.长探1井，3 916.5 m，盒1段，长石溶蚀；k.长探1井，3 763.83 m，盒7段，钠长石次生加大；l.彬1井，3 708.45 m，山1段，石英溶蚀

Figure 6. Microscopic characteristics of typical diagenesis of the Shihezi Formation-Shanxi Formation in the Binchang area

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图 7 长探1井石英次生加大包裹体均一温度

Figure 7. Homogenization temperature diagram of secondary enlargement of quartz in the Changtan 1 well

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图 8 彬1井石英次生加大与自生黏土矿物关系

Figure 8. Relationship between secondary enlargement of quartz and authigenic clay in the Bin 1 well

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图 9 彬1井石英次生加大与深度关系

Figure 9. Relationship between secondary enlargement of quartz and depth in the Bin 1 well

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图 10 方解石包裹体均一温度分布

Figure 10. Homogeneous temperature distribution of calcite inclusions

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图 11 Ca²⁺质量浓度与岩心孔隙度关系

Figure 11. Relationship between Ca²⁺ concentration and core porosity

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图 12 方解石体积分数及Ca²⁺质量浓度距顶底板厚度占比

Figure 12. Ratio of the calcite content and Ca²⁺ concentration to the thickness between the roof and floor

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图 13 长探1井绿泥石体积分数-方解石体积分数-孔渗综合图

Figure 13. Comprehensive map of chlorite content-calcite content-porosity and permeability in the Changtan 1 well

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图 14 彬长地区构造微裂缝未充填方解石

a.彬1井, 3 715.52 m，山1段，裂缝未充填方解石；b.彬4井，3 913.39 m，盒1段，裂缝未充填方解石；c.长探1井，3 916.5 m，盒1段，裂缝未充填方解石；d.长探1井，3 958.63 m，山1段，裂缝未充填方解石

Figure 14. Structural microfractures are not filled with calcite in the Binchang area

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图 15 致密储层发育模式综合图

Figure 15. Comprehensive map of the tight reservoir development model

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表 1 彬长地区孔隙结构类型

Table 1. Pore structure types of the Binchang area

层段	类型	岩性	排驱压力/MPa		中值压力/MPa		中值喉道半径/μm		孔喉组合
层段	类型	岩性	区间值	平均值	区间值	平均值	区间值	平均值	孔喉组合
盒1	1	(含砾)粗砂岩	0.35~0.42	0.38	1.15~2.16	1.66	0.769~0.986	0.825	小孔-中细喉
	2	中-细砂岩	0.80~2.61	1.47	20.02~35.15	27.58	0.04~0.70	0.26	小孔-细喉
	3	细砂岩	0.30~1.62	0.80	62.12~63.84	62.98	0.02~0.05	0.03	微孔-微喉
盒7	1	(含砾)粗砂岩	0.82~1.02	0.87	4.12~6.43	5.21	0.096~0.162	0.128	小孔-细喉
盒7	2	细-中砂岩	1.54~2.03	1.63	9.47~20.16	13.42	0.038~0.085	0.062	小孔-细微喉

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表 2 彬长地区石盒子组-山西组储层沉积微相与物性关系

Table 2. Relationship between reservoir sedimentary microfacies and physical properties of the Shihezi Formation-Shanxi Formation reservoir in the Binchang area

沉积亚相	沉积微相	岩性	沉积构造	平均孔隙度/%	平均渗透率/10^-3 μm²
辫状河三角洲平原	心滩	含砾粗砂岩	冲刷面	4.75	0.394
		粗砂岩	槽状、板状交错层理、块状层理	3.68	0.204
		中砂岩	槽状、板状交错层理、块状层理	4.05	0.110
曲流河三角洲前缘	水下分流河道	中砂岩	槽状、板状交错层理、沙纹层理、块状层理	2.20	0.100
	水下分流河道	细砂岩	槽状、板状交错层理、沙纹层理、块状层理	1.30	0.056
	河口坝	中砂岩	板状交错层理，块状层理	2.44	0.015
	河口坝	细砂岩	板状交错层理，块状层理	2.34	0.110

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