东海丽水凹陷L气田富CO<sub>2</sub>流体来源及对储层的影响

肖晓光; 李帅; 张武; 姜雪; 马文睿

doi:10.19509/j.cnki.dzkq.tb20240288

东海丽水凹陷L气田富CO₂流体来源及对储层的影响

doi: 10.19509/j.cnki.dzkq.tb20240288

中海石油（中国）有限公司上海分公司，上海 200335

基金项目: “十四五”重大科技项目“近海重点潜在富烃洼陷评价技术”（KJGG2022-0301）

详细信息

通讯作者:
E-mail：xiaoxg@cnooc.com.cn

中图分类号: P618.13
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- 文章访问数: 48
- PDF下载量: 8
- 被引次数: 0
出版历程
- 收稿日期: 2024-05-30
- 录用日期: 2024-09-23
- 修回日期: 2024-09-09
- 网络出版日期: 2025-04-27

Source of CO₂-rich fluid and its impact on reservoir quality of L gas field in Lishui Sag, East China Sea Basin

Shanghai Branch of CNOOC Ltd., Shanghai 200335, China

More Information

Corresponding author: E-mail：xiaoxg@cnooc.com.cn

摘要

摘要:
富CO₂流体−砂岩相互作用是砂岩储层次生孔隙主要形成机制之一。L气田作为丽水凹陷已发现的商业性气田，其主要产层不仅CO₂气体含量高，而且片钠铝石富集。为了揭示CO₂来源、形成时间、充注强度，及其对储层的影响，对L气田的岩矿、物性、碳氧同位素和相关地球化学特征展开了系统分析。研究区储层中自生碳酸盐矿物主要为铁白云石、片钠铝石和铁方解石，其次为白云石、菱铁矿和方解石，片钠铝石纵向上集中分布于明下段的中下部（CO₂高含量段）。CO₂主要为无机来源，幔源与壳源成因各半，其充注有2期，第一期CO₂充注时间为晚古新世，约57 Ma；第二期CO₂充注时间为早中新世，约18 Ma，以第一期为主。CO₂充注的时间、强度是决定其对储层影响是否有利的关键因素，L气田储层刚性颗粒含量不高，容易被压实致密，溶蚀也不强烈，加上地温梯度高有机酸生成的窗口窄，有机酸对储层的改善有限，而早期CO₂的充注不仅会生成碳酸产生溶蚀孔，而且会增强砂体的抗压实能力，能够保存一定量的原生孔，从而有利优质储层的发育。研究成果可为气田发育盆地的油气勘探提供借鉴。
- 丽水凹陷 /
- 片钠铝石 /
- CO₂充注 /
- 碳氧同位素 /
- 优质储层
Abstract: Objective
The interaction between CO₂-rich fluids and sandstone is one of the main mechanisms of secondary pore generation in sandstone reservoirs. The L gas field, located in Lishui Sag, is not only characterized by high CO₂ content but also by the enrichment of ammonium dawsonite in its main production layers.
Methods
This study systematically analyzes the rock and mineral composition, physical properties, carbon and oxygen isotopes, and related geochemistry to reveal the source, formation time, filling intensity of CO₂, and its influence on the reservoir in the L gas field.
Results
The results are as follows: (1) In the reservoir of the study area, authigenic carbonate minerals are primarily iron dolomite, sodium aluminate, and iron calcite, followed by dolomite, siderite, and calcite. (2) Ammonium dawsonite is vertically concentrated in middle and lower parts of the Lower Member of Mingyuefeng Formation, where the CO₂ content is high. (3) CO₂ is mainly of inorganic origin, with contributions from both mantle and crust sources. (4) There were two phases of CO₂ charging. The first filling event occurred around 57 Ma during the Late Paleocene and was the major charging period. The second filling event occurred during the Early Miocene, about 18 Ma. (5) The timing and intensity of CO₂ charging are key factors determining its impact on the reservoir. Due to the low content of rigid particles in the L gas field, the reservoir is prone to compaction, and the dissolution is not strong. Additionally, the geothermal gradient is high, and the organic acid window is narrow, limiting the reservoir improvement by organic acids. Early CO₂ filling not only generates carbonate dissolution pores but also enhances the anti-compaction ability of the sand bodies, preserving a certain amount of primary porosity. This process is beneficial for the development of high-quality reservoirs.
Conclusion
The research results can provide reference for oil and gas exploration in the sedimentary basin of the gas field.
- Lishui Sag /
- dawsonite /
- CO₂ charging /
- carbon and oxygen stable isotopes /
- high-quality reservoir

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图 1 丽水凹陷构造位置及构造单元划分（据文献[24]修改）

Figure 1. Tectonic location and division of structural units of Lishui Sag

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图 2 丽水凹陷明下段和灵上段岩性分类三角图

Figure 2. Rock type classification triangular plot in Lower Member of Mingyuefeng Formation and Upper Member of Lingfeng Formation in Lishui Sag

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图 3 L气田明月峰组和灵峰组（目的层）储层物性分布直方图

Figure 3. Histogram of reservoir property distribution of Mingyuefeng Formation and Lingfeng Formation of L gas field

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图 4 L气田储层镜下微观特征

a. L2井，2235.82 m，明下段，片钠铝石交代长石，（+）；b. L2井，2247.24 m，明下段，片钠铝石交代长石，（+）；c. L2井，2293.63 m，明下段，片钠铝石交代石英及岩屑，（+）；d. L2井，明下段，2235.82 m，放射束片钠铝石围绕铁白云石生长，（+）；e. L2井，2235.30 m，明下段，纤维状片钠铝石，集合体呈放射状、花束状部分占据长石溶解孔隙，（−）；f. L2井，2235.30 m，明下段，纤维状片钠铝石，集合体呈放射状、花束状部分占据长石溶解孔隙，（−）；g. L2井，2293.63 m，明下段，片钠铝石、自形粉晶白云石，（+）；h. L2井，2235.82 m，明下段，菱铁矿、白云石，（+）；i. L1井，2575.83 m，明下段，方解石充填孔隙，（−）；j. L1井，2583.97 m，明下段，方解石围绕片钠铝石生长，（+）；k. L1井，2575.73 m，明下段，石英主要发蓝紫色光，粒间铁方解石胶结物主要发橙红−暗橙红色光，普遍交代碎屑颗粒边缘，粒间少量自生高岭石胶结物发靛蓝色光，阴极发光；l. L2井，2246.62 m，明下段，颗粒间充填书页状自生高岭石、自生石英等，扫描电镜

Figure 4. Microscopic characteristics of reservoir of L gas field

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图 5 L1和L2井片钠铝石纵向分布特征（虚线表示地层段界面）

Figure 5. Vertical evolution of the dawsonite content of the Well L1 and Well L2

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图 6 丽水凹陷L气田CO₂有机与无机成因判别（据文献[30]修改）

Figure 6. Identification of organic or inorganic origin of CO₂ of L gas field in Lishui Sag

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图 7 L气田气样中⁴⁰Ar−⁴He^[34-35](a)和R/Ra−⁴⁰Ar/³⁶Ar(b)关系图

Figure 7. Relationship between ⁴⁰Ar and ⁴He (a) and R/Ra and ⁴⁰Ar/³⁶Ar (b) of gas samples in L gas field

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图 8 L气田$\delta^{13}{\mathrm{C}}_{{\mathrm{CO}}_2-{\mathrm{PDB}}} $−R/Ra关系图（据文献[36]修改）

Figure 8. Relationship between $\delta^{13}{\mathrm{C}}_{{\mathrm{CO}}_2\text{-}{\mathrm{PDB}}} $ and R/Ra in L gas field

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图 9 L气田油气包裹体镜下微观特征

a. L2井，2246.10 m，纯CO₂包裹体，透射光，（−）；b. L2井，2246.10 m，纯CO₂包裹体，透射光，（−）；c. A3井，2741.18 m，纯CO₂包裹体，透射光，（−）；d. A3井，2741.18 m，纯CO₂包裹体，透射光，（−）；e. L2井，2293.20 m，混合气包裹体，透射光，（−）；f. L2井，2293.20 m，混合气包裹体，荧光

Figure 9. Microscopic characteristics of oil and gas inclusions in L gas field

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图 10 明月峰组纯CO₂气包裹体拉曼谱图

Figure 10. Laser Raman spectrogram of CO₂ inclusions of Mingyuefeng Formation

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图 11 富CO₂包裹体与盐水包裹体等容P−T相图

Figure 11. P-T diagram of CO₂-rich inclusion and brine inclusion

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图 12 L气田油气、二氧化碳充注期次与埋藏史关系图

Figure 12. Relationship between oil and gas filling, CO₂ filling, and burial history in L gas field

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图 13 L气田碳酸盐胶结物$ \delta^{13}{\mathrm{C}}_{{\mathrm{CO}}_{2}\text{-}{\mathrm{PDB}}} $和δ¹⁸O_SMOW相关图版（据文献[29]修改）

Figure 13. Correlogram of $ \delta^{13}{\mathrm{C}}_{{\mathrm{CO}}_{2}\text{-}{\mathrm{PDB}}} $ and δ¹⁸O_SMOW of carbonate cements in L gas field

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图 14 原生孔(a)和次生孔(b)与片钠铝石含量关系图

Figure 14. Relationship between primary pore (a) and secondary pore (b) and dawsonite content

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图 15 孔隙度(a)和渗透率(b)与片钠铝石含量关系图

Figure 15. Relationship between porosity (a) and permeability (b) and dawsonite content

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表 1 L气田CO₂及稀有气体组分含量和同位素组成分析结果

Table 1. Analysis results of CO₂ and rare gas component content and isotopic composition in L gas field

井位	深度/m	$\delta^{13}{\mathrm{C}}_{{\mathrm{CO}}_2-{\mathrm{PDB}}} $/‰	⁴⁰Ar/%	⁴He/%	R/Ra	³He/⁴He	⁴⁰Ar/³⁶Ar	X/%	H_me/%
A1	3628	−5.9	3.27×10⁻⁴	2.64×10⁻⁴	3.60	5.041×10⁻⁶	3906.85	72.9	45.70
L1	2250～2265							85.3
L1	2265～2283							90.4
L2	2315～2336	−9.2			4.24	5.93×10⁻⁶		25.7	53.80
L2	2238～2260	−4.6			4.26	5.97×10⁻⁶		91.4	54.16
A2	3456	−5.7	3.16×10⁻⁴	2.55×10⁻⁴	3.64	5.1×10⁻⁶	3760.05	75.7	46.21
A3	2870	−5.7	3.41×10⁻⁴	2.90×10⁻⁴	3.58	5.012×10⁻⁶	4024.29	75.7	45.44
A5	3403	−5.9	3.72×10⁻⁴	2.71×10⁻⁴	3.60	5.041×10⁻⁶	3969.36	72.9	45.70
注：R/Ra. 样品氦R和大气氦Ra的同位素比值；X. 混合气体中无机CO₂的体积分数；H_me. 气藏中幔源氦的比例

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表 2 L气田含二氧化碳气包裹体分析结果

Table 2. Analysis results of CO₂-bearing inclusions in L gas field

井号	深度/m	组名	测井解释	岩性	包裹体类型	包裹体总密度/(g·cm⁻³)	共生盐水包裹体均一温度/℃
A3	2741.18	灵下段	干层	细−中粒岩屑砂岩	纯二氧化碳气相	0.550	100～105
A3	2747.80	灵下段	干层	细−中粒岩屑砂岩	混合气	0.530	90～110
A3	2786.00	灵下段	气层	中粒岩屑砂岩	纯二氧化碳气相	0.460	100～110
L2	2246.10	明下段	气层	中粒岩屑砂岩	纯二氧化碳气相	0.167	113.2
L2	2291.00	明下段	气层	中粒岩屑砂岩	混合气	0.159	124
L2	2293.00	明下段	气层	细粒岩屑砂岩	油气	0.156	130～140

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