塔里木盆地顺南地区深层碳酸盐岩热液溶蚀及其油气勘探意义——以顺南蓬1井为例

韩俊; 董少峰; 尤东华; 张胜; 肖重阳; 王英明

doi:10.11781/sysydz202304770

塔里木盆地顺南地区深层碳酸盐岩热液溶蚀及其油气勘探意义——以顺南蓬1井为例

doi: 10.11781/sysydz202304770

1.
中国石化西北油田分公司, 乌鲁木齐 830011
2.
西南石油大学地球科学与技术学院, 成都 610500
3.
中国石化石油勘探开发研究院无锡石油地质研究所, 江苏无锡 214126
4.
中地同创能源科技有限公司, 武汉 430000

基金项目:

国家自然科学基金企业创新发展联合基金项目 U21B2063

中国石化科技部项目 P21033-1

详细信息

作者简介:
韩俊(1983—)，男，博士，副研究员，从事碳酸盐岩油气地质与勘探综合研究。E-mail: hanj.xbsj@sinopec.com

中图分类号: TE122.2
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出版历程
- 收稿日期: 2023-05-09
- 修回日期: 2023-06-21
- 刊出日期: 2023-07-28

Hydrothermal dissolution of deep-buried carbonate rocks and its significance for hydrocarbon exploration in Shunnan area, the Tarim Basin: taking well Peng-1 in Shunnan area as a case

1.
SINOPEC Northwest Oil Field Company, Urumqi, Xinjiang 830011, China
2.
School of Geosciences and Technology, Southwest Petroleum University, Chengdu, Sichuan 610500, China
3.
Wuxi Research Institute of Petroleum Geology, SINOPEC, Wuxi, Jiangsu 214126, China
4.
China Geology Alliance (Wuhan) Energy Technology Co., Ltd., Wuhan, Hubei 430000, China

摘要

摘要: 为揭示深层碳酸盐岩储层的成因机理，对塔里木盆地顺南地区蓬1井进行了研究。顺南蓬1井取心段揭示，在埋深超过7 500 m的碳酸盐岩中发育有大量的裂缝和溶蚀孔洞，基于详细的岩心观察和描述发现这些溶蚀孔洞主要分布在取心段下部上寒武统白云岩中，而在取心段上部下奥陶统碳酸盐岩中很少。溶蚀孔洞的直径随埋藏深度的增加逐渐增大，表明这些孔洞是由来源于深部的热流体而非大气淡水下渗溶蚀形成的。各成岩矿物(白云岩、方解石)与宿主围岩具有相似的碳同位素值和⁸⁷Sr/⁸⁶Sr比值，说明成岩流体与原始碳酸盐岩发生了强烈的水—岩反应，主要继承了原始封存的孔隙水的地球化学特征。但是，明显偏负的氧同位素值(平均-13.26‰)表明它们形成于较高温度的成岩流体中，这一推论也得到了流体包裹体显微测温的证实，表明白云岩的重结晶和随后方解石的沉淀都与断裂相关的深部热流体密切相关。此外，全直径CT扫描揭示，裂缝可以明显改善热液白云石化作用形成的白云岩的储集性能，尤其是渗透率，至少提高一个数量级，即从0.02×10^-3 μm²提高至0.39×10^-3 μm²。鉴于塔深1井及古城地区具有相似的情况，塔里木盆地深层—超深层碳酸盐岩可能广泛发育热液相关的白云岩储层。因此，在塔里木盆地及其他地区未来的油气勘探中，热液改造型相关的白云岩储层值得重点关注。
- 热液溶蚀 /
- 深层白云岩储层 /
- 油气勘探 /
- 顺南地区 /
- 塔里木盆地
Abstract: In order to reveal the genetic mechanism of deep-buried carbonate reservoirs, a study was made based on well Peng-1 in Shunnan area of the Tarim Basin. The core section of well Peng-1 revealed that a large number of fractures and dissolution pores were developed in the carbonate rocks with buried depth of over 7 500 m. Based on detailed core observation and description, it was found that the dissolution pores were mainly distributed in the Upper Cambrian dolomites in the lower part of the core section and few in the Lower Ordovician carbonates in the upper part of the core section. The diameter of pores increases gradually with the increase of burial depth, which indicated that the pores were formed by infiltration of deep-seated hydrothermal fluids rather than meteoric water. The similar δ¹³C values and ⁸⁷Sr/⁸⁶Sr ratios of different types of minerals (including dolomite and calcite) with host rocks indicated that the diagenetic fluids inherited the geochemical characteristics of original sequestered pore water through intense water-rock action with the original carbonate rocks. However, the significantly negative δ¹⁸O values (with an average of -13.26 ‰) suggested that they were precipitated from fluids with high temperatures. This inference was verified by the results of fluid inclusion microthermometry, which confirmed that dolomite recrystallization and subsequent calcite precipitation were closely associated with fault-related deep-seated hydrothermal fluids. In addition, whole diameter CT scanning revealed that fractures can significantly improve the reservoir property and permeability of the dolomite formed by hydrothermal dolomitization. The permeability can be improved by at least one order of magnitude, i.e. from 0.02×10^-3 μm² to 0.39×10^-3 μm². Hydrothermal-related dolomite reservoirs may be extensively developed in the deep/ultra-deep buried carbonates in the Tarim Basin in view of the occurrence of such phenomenon in the well TS1 and Gucheng area. Thus, in the future hydrocarbon exploration in the Tarim Basin and elsewhere, hydrothermal-altered dolomite reservoirs deserve more attention.
- hydrothermal dissolution /
- deep-buried dolomite reservoir /
- hydrocarbon exploration /
- Shunnan area /
- Tarim Basin
注释:

1) 所有作者声明不存在利益冲突。

1) 利益冲突声明/Conflict of Interests

2) 作者贡献/Authors’ Contributions

2) 韩俊参与岩心观察；韩俊完成实验设计；尤东华完成实验操作；董少峰和韩俊参与实验数据分析；肖重阳完成岩石薄片观察和图件绘制；韩俊、张胜、王英明参与论文写作和修改。所有作者均阅读并同意最终稿件的提交。

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图 1 塔里木盆地顺南地区构造位置(a)及地层综合柱状图(b)

据李宗杰等^[16]，略有修改。

Figure 1. Simplified geological map (a) and composite stratigraphic column (b) of Shunnan area, the Tarim Basin

下载: 全尺寸图片幻灯片

图 2 塔里木盆地顺南地区蓬1井上寒武统—下奥陶统岩心宏观特征

a.粉细晶白云岩，发育高角度构造裂缝被方解石完全充填，蓬莱坝组，7 327.17~7 327.37 m；b.纹层状粉细晶白云岩，蓬莱坝组，7 332.94~7 333.14 m；c.浅灰色细晶白云岩，针孔状溶孔发育，下丘里塔格组，7 556.99~7 557.11 m；d.灰白色细—中晶白云岩，溶孔发育，形态不规则，下丘里塔格组，7 561.35~7 561.51m；e.深灰色细—中晶白云岩，蜂窝状溶孔发育，被鞍形白云石和方解石完全充填—半充填，下丘里塔格组，7 626.79~7 626.94 m。

Figure 2. Marcoscopic characteristics of the Upper Cambrian-Lower Ordovician cores from well Peng-1 in Shunnan area, the Tarim Basin

下载: 全尺寸图片幻灯片

图 3 塔里木盆地顺南地区蓬1井上寒武统—下奥陶统岩心微观特征

a.粉细晶白云岩，蓬莱坝组，7 326.69 m，单偏光；b.残留的原始粪球粒，蓬莱坝组，7 330.92m，单偏光；c.粉细晶白云岩，裂缝被方解石充填，蓬莱坝组，7 326.52~7 326.62 m，阴极发光；d.细—中晶白云岩，镶嵌状接触，下丘里塔格组，7 559.9 m，单偏光；e-f.中粗晶白云岩，鞍形白云石和方解石充填溶蚀孔洞，下丘里塔格组，7 626.79~7 626.94 m，e为单偏光，f为阴极发光。

Figure 3. Microscopic characteristics of the Upper Cambrian-Lower Ordovician cores from well Peng-1 in Shunnan area, the Tarim Basin

下载: 全尺寸图片幻灯片

图 4 塔里木盆地顺南地区蓬1井不同类型碳酸盐矿物碳—氧同位素(a)、氧—锶同位素(b)交会图

Figure 4. Cross-plots of δ¹³C and δ¹⁸O values (a), δ¹⁸O values and ⁸⁷Sr/⁸⁶Sr ratios (b) of different types of carbonate minerals of well Peng-1 in Shunnan area, the Tarim Basin

下载: 全尺寸图片幻灯片

图 5 塔里木盆地顺南地区蓬1井各成岩矿物均一温度和盐度交会图

Figure 5. Cross-plots of homogenization temperature and salinity of different types of minerals of well Peng-1 in Shunnan area, the Tarim Basin

下载: 全尺寸图片幻灯片

图 6 塔里木盆地顺南地区蓬1井寒武系各类型白云岩储层全直径CT扫描储集空间发育特征

a-c为寒武系不同位置岩心CT扫描照片，不同颜色代表不同孔径。

Figure 6. Characteristics of reservoir spaces of different types of Cambrian dolomite reservoirs of well Peng-1 in Shunnan area of the Tarim Basin revealed by whole diameter CT scanning

下载: 全尺寸图片幻灯片

表 1 塔里木盆地顺南地区蓬1井各成岩矿物碳、氧、锶同位素测试分析结果

Table 1. Isotopic data (δ¹³C, δ¹⁸O and ⁸⁷Sr/⁸⁶Sr ratios) of different types of minerals of well Peng-1 in Shunnan area, the Tarim Basin

样品编号	深度/m	岩性	δ¹³C/‰	δ¹⁸O/‰	⁸⁶Sr/⁸⁷Sr	±2σ
SHNP1-01	7 326.52~7 326.62	深灰色泥晶白云岩	-1.24	-8.27	0.709 375	0.000 017
		裂缝方解石	-2.35	-13.12	0.709 112	0.000 013
		裂缝方解石	-2.19	-13.31
SHNP1-02	7 327.37~7 327.56	浅灰色颗粒泥晶灰岩	-1.44	-12.58	0.709 080	0.000 018
		裂缝方解石	-2.25	-13.32	0.709 224	0.000 013
		裂缝方解石	-2.42	-13.31
SHNP1-03	7 626.79~7 626.94	灰色细晶白云岩	-1.12	-10.00	0.709 141	0.000 015
SHNP1-03	7 626.79~7 626.94	孔洞方解石	-2.53	-14.03	0.709 165	0.000 012
SHNP1-04	7 627.42~7 627.51	灰色细晶白云岩	-1.30	-10.55	0.708 956	0.000 016
SHNP1-04	7 627.42~7 627.51	鞍形白云石	-2.16	-12.40	0.709 516	0.000 009

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表 2 塔里木盆地顺南地区蓬1井各成岩矿物流体包裹体显微测温结果

Table 2. Results of fluid inclusion microthermometry of different types of minerals of well Peng-1 in Shunnan area, the Tarim Basin

样号	矿物	个数	均一温度(T_h)/℃			冰点温度(T_m)/℃			盐度/%
样号	矿物	个数	最小值	最大值	平均值	最小值	最大值	平均值	最小值	最大值	平均值
SHNP1-1	方解石	3	170.3	173.5	171.7	-28.9	-21.5	-24.9	23.4	28	25.5
		2	160.9	160.9	160.9	-23.6	-23.2	-23.4	24.5	24.7	24.6
		2	162.3	166.6	164.5	-23.1	-20.4	-21.8	22.6	24.4	23.5
		5	173.1	176.3	174.5	-23.8	-21.9	-23.1	23.6	24.8	24.4
		1	178.7	178.7	178.7	-22.9	-22.9	-22.9	24.3	24.3	24.3
		3	168.5	179.8	175.0	-26.5	-23.4	-25.3	24.6	26.5	25.7
SHNP1-2	方解石	1	192.5	192.5	192.5	-24.6	-24.6	-24.6	25.3	25.3	25.3
		2	185.6	193.5	189.6	-25.0	-25.0	-25.0	25.6	25.6	25.6
		3	178.1	189.8	182.0	-24.8	-22.0	-23.7	24.0	25.5	24.8
		5	172.5	187.3	179.8	-25.6	-18.3	-23.5	21.2	25.9	24.6
		3	162.5	173.7	167.9	-24.3	-19.2	-21.8	21.8	25.1	23.5
		4	158.8	164.4	162.4	-23.8	-22.5	-23.0	24.2	24.8	24.5
SHNP1-3	鞍形白云石	3	172.5	184.5	179.1	-20.7	-20.7	-20.7	22.8	22.8	22.8
	鞍形白云石	4	186.1	197.8	191.1	-22.8	-19.9	-21.7	22.3	24.2	23.5
	方解石	1	215.2	215.2	215.2	-21.2	-21.2	-21.2	23.2	23.2	23.2
	方解石	2	206.1	210.1	208.1	-21.8	-21.8	-21.8	23.6	23.6	23.6
SHNP1-4	鞍形白云石	3	160.8	172.5	166.1	-20.2	-10.0	-16.4	13.9	22.5	19.4
		1	178.5	178.5	178.5	-21.4	-21.4	-21.4	23.3	23.3	23.3
		1	184.5	184.5	184.5	-27.9	-27.9	-27.9	27.4	27.4	27.4
	石英	3	170.6	188.2	178.7	-14.4	-13.2	-13.8	17.1	18.1	17.6
	石英	5	188.2	188.5	188.3	-16.7	-12.9	-14.6	16.8	20.0	18.2

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表 3 塔里木盆地顺南地区蓬1井寒武系下丘里塔格组储层特征测井解释

Table 3. Reservoir characteristics of Cambrian Lower Qiulitage Formation of well Peng-1 in Shunnan area of the Tarim Basin revealed by logging interpretation

地层	深度/m	GR/API	RT/(Ω·m)	AC/(μs/ft)	SH/%	孔隙度/%	渗透率/10^-3 μm²	解释结论储层级别
₃ql	7 579~7 606	29.2~19	920~562	49.2~46.1	1.6	2.8	0.02	Ⅲ类
	7 606~7 611.5	14.7~21.9	199~168	56.3~52.4	3.5	6.6	0.12~0.26	Ⅱ类
	7 611.5~7 618	18.9~11.8	319~1 066	49.9~46.2	2.4	2.6~3.7	0.04~0.12	Ⅲ类
	7 618~7 621	21.9~16.5	44.3~52.7	56.1~53.7	5.7	8.6	0.39	Ⅱ类
	7 625~7 629.5	11.5~16.1	1 217~623	43.7~47.2	2.8	3.6	0.02	Ⅲ类

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