四川盆地不同地区二叠系茅口组缝洞粗晶方解石碳氧同位素差异及其古岩溶环境意义

高兆龙; 淡永; 张玺华; 曹华; 邓敏; 陈聪; 胡罗嘉

doi:10.11932/karst20240309

四川盆地不同地区二叠系茅口组缝洞粗晶方解石碳氧同位素差异及其古岩溶环境意义

doi: 10.11932/karst20240309

高兆龙¹,
淡永^{2, 3, ,},
张玺华¹,
曹华¹,
邓敏^{2, 3},
陈聪¹,
胡罗嘉¹

1.
中国石油西南油气田分公司勘探开发研究院, 四川成都 610041
2.
中国地质调查局成都地质调查中心(西南地质科技创新中心), 四川成都 610081
3.
自然资源部沉积盆地与油气资源重点实验室, 四川成都 610081

基金项目: 中国石油天然气股份有限公司攻关性应用性科技专项《海相碳酸盐岩油气规模增储上产与勘探开发技术研究》（2023ZZ16）子课题《碳酸盐岩油气富集规律及有利区带研究》，中国石油西南油气田公司科学研究与技术开发项目《四川盆地二叠系规模增储关键问题攻关研究》子课题《四川盆地下二叠统资源潜力与成藏条件研究》（20220301-03），自然资源部深时地理环境重建与应用重点实验室开放基金资助项目（DGERA20231108）共同资助

详细信息

作者简介:
高兆龙（1990－），男，硕士，工程师，主要从事油气田勘探工作

通讯作者:
淡永（1986－），男，博士，副研究员，主要从事沉积地质及古岩溶油气储层地质研究工作。E-mail：dy920@qq.com。

中图分类号: P618.13
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出版历程
- 收稿日期: 2023-11-22
- 网络出版日期: 2024-08-15
- 刊出日期: 2024-06-25

Differences of carbon and oxygen isotopes in coarse-grained calcite from the Permian Maokou Formation in different regions of Sichuan Basin and their significance in paleokarst environment

GAO Zhaolong¹,
DAN Yong^{2, 3
, ,},
ZHANG Xihua¹,
CAO Hua¹,
DENG Min^{2, 3},
CHEN Cong¹,
HU Luojia¹

1.
Research Institute of Petroleum Exploration and Development, Southwest Oil and Gas Field Company, PetroChina, Chengdu, Sichuan 610041, China
2.
Chengdu Center, China Geological Survey, Chengdu, Sichuan 610081, China
3.
Key Laboratory of Sedimentary Basin and Oil and Gas Resources, Ministry of Natural Resources, Chengdu, Sichuan 610081, China

摘要

摘要: 茅口组缝洞型储层是四川盆地重要的天然气产层。为认识这些缝洞的形成环境以及在盆地不同地区的差异, 通过测试和收集缝洞方解石碳氧同位素数据，发现茅口组方解石碳氧同位素可分为4类，分别指示4种不同流体性质的古岩溶环境：第Ⅰ类缝洞方解石氧同位素值与茅口组灰岩或中二叠海水值基本一致，δ¹³C为1.8‰~3.83‰，δ¹⁸O为−8.95‰~−4.11‰，指示准同生岩溶环境；第Ⅱ类缝洞方解石具有较高负偏的δ¹³C和δ¹⁸O值，δ¹³C＜0‰，δ¹⁸O为−12‰~−9‰，指示大气淡水岩溶环境；第Ⅲ类缝洞方解石具有较低的δ¹⁸O值，比基岩明显负偏，而δ¹³Ｃ值与基岩值基本一致，δ¹³Ｃ为0‰~3.83‰，δ¹⁸O为−12‰~−8.5‰，主要指示埋藏岩溶环境；第Ⅳ类缝洞方解石δ¹⁸O值明显偏负（＜−12‰），指示高温热液环境。区域对比发现川中、川南较川北氧同位素更负偏，而川北、川中碳同位素较川南更负偏，认为川南地区以埋藏岩溶为主、大气淡水岩溶和准同生岩溶次之，形成以裂缝型为主的储层；川中地区除准同生岩溶、大气淡水岩溶外，还发育有高温热液岩溶，热液岩溶对川中茅口组白云岩中孔洞发育具有贡献；川北地区以准同生岩溶、大气淡水岩溶为主，形成了川北以溶蚀孔洞为主的储层。
- 四川盆地茅口组 /
- 碳氧同位素 /
- 古岩溶作用 /
- 岩溶储层 /
- 热液岩溶
Abstract: Oil and gas fields in karst carbonate reservoirs are widely distributed in China. A number of karst fracture-vuggy reservoirs have been found in the Tarim Basin, the Ordos Basin and the Sichuan Basin. Therefore, research of reservoirs in karst fractured caves has become one of the focuses in recent years, which indicates a promising future and huge potential for exploring karst carbonate reservoirs in China. Reservoirs in fractured caves of the Maokou Formation have always been one of the key areas for oil and gas exploration in the Sichuan Basin. Since the last century when reservoirs in fractured caves in the southern Sichuan region were discovered, breakthroughs have been made in this field in the Yuanba area of northern Sichuan, Yunjin area of southern Sichuan, and the Penglaiba area of central Sichuan, demonstrating good exploration prospects. However, there has always been controversy over the origin of fractured caves. One view suggests that the exposure of the Maokou Formation caused by the Dongwu Movement and the occurrence of freshwater karst are the main reasons for the development of fractured caves in the Maokou Formation, while another view suggests that fractured caves in the Maokou Formation are related to the tectonic fluid activity during the burial period. these two views are mostly based on research in the southern Sichuan region, and further consideration of the entire Sichuan Basin is needed to search for relevant evidence from geological phenomena to geochemistry.To understand the causes and differences of these fractured caves, we systematically sampled calcite for data of carbon and oxygen isotopes from outcrop profiles or from drilling fractured caves in different areas of the Sichuan Basin, in order to determine the paleokarst environment in which fractured caves were developed. Study results show that fractured caves of the Maokou Formation in this basin are mainly composed of small-and-medium-sized dissolution pores, fractures, and dissolution fractures. The carbon and oxygen isotopes of calcite in the Maokou Formation can be divided into four types, indicating four types of paleokarst environment with different fluid properties. Type I is the quasi syngenetic karst environment in which the oxygen isotope values of calcite in fractured caves are basically consistent with the values of limestone or of Middle Permian seawater in the Maokou Formation, with δ¹³C ranging from 1.80‰ to 3.83‰ and δ¹⁸O ranging from −8.95‰ to −4.11‰. Type II is the freshwater karst environment in which high negative δ¹³C and δ¹⁸O values are present in calcite of fractured caves, with δ¹³C<0‰ and δ¹⁸O ranging from −12.00‰ to −9.00‰. Type III is the buried karst environment in which lower δ¹⁸O values are significantly negative compared to the values of bedrock. However, δ¹³C values are basically consistent with those of bedrock, with δ¹³C ranging from 0‰ to 3.83‰ and δ¹⁸O ranging from −12.00‰ to −8.50‰. Type IV is the high-temperature hydrothermal environment in which δ¹⁸O values are significantly negative (<−12.00‰).Regional comparison shows that the oxygen isotopes in central and southern Sichuan are more negative than those in northern Sichuan, while the carbon isotopes in northern and central Sichuan are more negative than those in southern Sichuan. Research suggests that buried karst is the main type in southern Sichuan, followed by freshwater karst and quasi syngenetic karst, all together forming reservoirs dominated by fractures. In addition to quasi syngenetic karst and freshwater karst, high-temperature hydrothermal karst is also developed in central Sichuan. The high-temperature hydrothermal karst has formed dissolution pore reservoirs related to dolomite. The northern Sichuan is mainly characterized by quasi syngenetic karst and freshwater karst, forming reservoirs mainly composed of dissolution pores.
- the Maokou Formation in Sichuan Basin /
- carbon and oxygen isotopes /
- paleokarst /
- karst reservoir /
- hydrothermal karst

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图 1 四川盆地构造分区及二叠系茅口组取样井分布（据^[26]有修改）

Figure 1. Structural zoning and distribution of sampling wells in the Permian Maokou Formation of the Sichuan Basin

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图 2 四川盆地茅口组粗晶方解石发育特征

a. 溶缝中方解石和沥青充填，茅四段 3 949.06~3 949.16 m，高石1；b. 构造网裂缝极发育，泥质和方解石充填，茅三段 1 683.06~1 683.18 m，威阳17井；c. 构造高角度缝充填方解石，茅二b ，隆40；d. 扩溶缝，方解石全充填，茅二b，3 652.16~3 652.44 m，包20；e. 扩溶缝，方解石晶体充填，茅二b，3 630.56~3 630.73 m，包20；f. 溶蚀孔洞，方解石晶体半充填，茅三，元坝8；g.溶蚀孔洞，方解石半充填，茅二a，1 722.75~1 723.09 m，威阳17井；h. 溶洞，方解石半充填，茅二b 3 652.75~3 652.84 m，包20；i.不整合面下发育溶洞，方解石充填，茅三，兴文古宋；j.亮晶砂屑灰岩中发育溶蚀孔洞，方解石全充填，茅二a，古蔺河沟头；k. 白云岩内密集发育孔洞，5~8 个·m⁻¹，方解石充填，茅二b，重庆石柱回龙场

Figure 2. Development characteristics of coarse-grained calcite in the Maokou Formation of the Sichuan Basin

a. dissolution joints filled with calcite and bitumen, Mao Section 4, 3949.06–3949.16 m, Gaoshi 1; b. extensive development of structural network fractures filled with mudstone and calcite, Mao Section 3, 1,683.06–1,683.18 m, Weiyang Well 17; c. high-angle structural joints filled with calcite, Mao Section 2b, uplift 40; d. widened dissolution joints fully filled with calcite, Mao Section 2b, 3,652.16–3,652.44 m, Bao 20; e. widened dissolution joints partially filled with calcite crystals, Mao Section 2b, 3,630.56–3,630.73 m, Bao 20; f. dissolution pores semi-filled with calcite crystals, Mao Section 3, Yuanba 8; g. dissolution pores semi-filled with calcite, Mao Section 2a, 1,722.75–1,723.09 m, Weiyang Well 17; h. a doline semi-filled with calcite, Mao Section 2b, 3,652.75–3,652.84 m, Bao 20; i. dissolution caves developed below unconformity surfaces, filled with calcite, Mao Section 3, Xingwengusong; j. dissolution pores developed in lustrous sand-grain limestone, fully filled with calcite, Mao Section 2a, Gulinhegoutou; k. calcite-filled pores densely developed in dolomite, 5–8 per m−1, Mao Section 2b, Shizhuhuilongchang of Chongqing

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图 3 四川盆地不同地区茅口组缝洞方解石碳氧同位素交汇图

Figure 3. Intersection of carbon and oxygen isotopes of calcite from the Maokou Formation in different regions of the Sichuan Basin

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图 4 四川盆地茅口组不同产出状态方解石碳氧同位素交汇图

Figure 4. Intersection of carbon and oxygen isotopes of calcite from different fractured caves in the Maokou Formation of the Sichuan Basin

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表 1 四川盆地不同地区茅口组缝洞方解石碳氧同位素测试结果统计

Table 1. Test results of carbon and oxygen isotopes of calcite from the Maokou Formation in different regions of the Sichuan Basin

样品类型	δ¹³C_（V-PDB）‰			δ¹⁸O_（V-PDB）‰			样品数量
样品类型	最小	最大	平均	最小	最大	平均	样品数量
川北缝洞方解石	−2.10	4.71	1.41	−9.61	−4.39	−7.08	21
川中缝洞方解石	−2.30	3.00	0.87	−13.91	−6.80	−9.97	10
川南缝洞方解石	−1.21	4.90	2.96	−11.83	−5.84	−9.41	71
茅口组灰岩基岩	1.50	4.80	3.82	−11.40	−4.70	−7.28	27
中二叠世海水^[30]	2.50	5.50	/	−10.00	0	/	/

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表 2 四川盆地不同产出状态方解石碳氧同位素测试结果统计

Table 2. Test results of carbon and oxygen isotopes of calcite from different fractured caves of the Sichuan Basin

样品产出状态	δ¹³C_（V-PDB）‰			δ¹⁸O_（V-PDB）‰			样品数量
样品产出状态	最小	最大	平均	最小	最大	平均	样品数量
构造裂缝方解石	−0.11	4.70	3.07	−11.28	−5.84	−9.25	56
溶缝方解石	−2.30	4.13	2.03	−11.83	−7.93	−9.97	12
溶蚀孔洞方解石	−2.13	4.71	1.54	−13.91	−4.39	−8.23	34
茅口组灰岩基岩	1.50	4.80	3.82	−11.40	−4.70	−7.28	27
中二叠世海水^[30]	2.50	5.50	/	−10.00	0	/	/

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表 3 四川盆地茅口组缝洞方解石同位素特征判别形成环境

Table 3. Environment identified by calcite isotope characteristics in the Maokou Formation of the Sichuan Basin

发育期次	形成环境	同位素特征
发育期次	形成环境	δ¹³C(PDB)‰	δ¹⁸O(PDB)‰
Ⅰ	准同生期岩溶环境	1.80~3.83	−8.95~−4.11
Ⅱ	表生期大气淡水岩溶环境	＜0	−12.00~−9.00
Ⅲ	埋藏期岩溶环境	0~3.83	−12.00~−8.50
Ⅳ	高温热液岩溶环境	/	＜12.00

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