塔里木盆地塔中地区下奥陶统白云岩的成岩流体演化:来自团簇同位素的证据

doi:10.11743/ogg20200107

石油与天然气地质 ›› 2020, Vol. 41 ›› Issue (1): 68-82.doi: 10.11743/ogg20200107

塔里木盆地塔中地区下奥陶统白云岩的成岩流体演化:来自团簇同位素的证据

刘嘉庆^1,²(), 李忠^1,^2,*(), 颜梦珂^1,², PeterK.Swart³, 杨柳⁴, 卢朝进^3,⁵

1. 中国科学院地质与地球物理研究所岩石圈演化国家重点实验室, 北京 100029
2. 中国科学院大学, 北京 100049
3. 迈阿密大学罗森斯蒂尔海洋与大气科学学院, 佛罗里达州迈阿密 33149
4. 中国石油杭州地质研究院, 浙江杭州 310023
5. 中国石油大学(北京), 北京 102249

收稿日期:2019-07-31 出版日期:2020-02-01 发布日期:2020-01-19
通讯作者: 李忠 E-mail:liujiaqing@mail.iggcas.ac.cn;lizhong@mail.iggcas.ac.cn
作者简介:刘嘉庆(1984-),女,博士研究生、高级工程师,沉积学。E-mail:liujiaqing@mail.iggcas.ac.cn
基金资助:
国家科技重大专项(2017ZX05008-003)

Diagenetic fluid evolution of dolomite from the Lower Ordovician in Tazhong area, Tarim Basin: Clumped isotopic evidence

Jiaqing Liu^1,²(), Zhong Li^1,^2,*(), Mengke Yan^1,², K.Swart Peter³, Liu Yang⁴, Chaojin Lu^3,⁵

1. State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China
2. University of Chinese Academy of Sciences, Beijing 100049, China
3. Department of Marine Geosciences, Rosenstiel School of Marine and Atmospheric Sciences, University of Miami, Miami, FL 33149, USA
4. Hangzhou Research Institute of Geology, PetroChina, Hangzhou, Zhejiang 310023, China
5. China University of Petroleum(Beijing), Beijing 102249, China

Received:2019-07-31 Online:2020-02-01 Published:2020-01-19
Contact: Zhong Li E-mail:liujiaqing@mail.iggcas.ac.cn;lizhong@mail.iggcas.ac.cn
Supported by:
国家科技重大专项(2017ZX05008-003)

摘要/Abstract

摘要：

基于碳酸根中¹³C-¹⁸O键的相对丰度与温度的关系，碳酸盐团簇同位素（Δ₄₇）具有独特的温度指示特征，而且不受碳酸盐沉淀时流体的化学和同位素组成的影响，是成岩流体研究中很好的温度指标。应用该指标可以更好地解决与温度相关的成岩流体来源及演化的问题。论文主要针对塔里木盆地塔中地区下奥陶统鹰山组白云岩样品，在详细的岩矿观察基础上，选取了基质（孔隙发育处）、孔洞内充填物和裂缝内充填物进行了团簇同位素测试分析，解析了深层-超深层碳酸盐岩储层的流体性质、演化与其对储层发育的影响。测试结果表明，塔中地区下奥陶统鹰山组白云岩主要经历了3期成岩流体改造：第一期流体为浅-中埋藏，为粉晶-细晶结构，团簇同位素形成温度T（Δ₄₇）分布范围为69~94℃，流体氧同位素值（δ¹⁸O_w，SMOW）分布范围为+1.81‰~+5.19‰，为奥陶系改造海水；第二期流体为晚期深埋藏卤水，多表现为细晶与中-粗晶结构，T（Δ₄₇）为111~113℃，δ¹⁸O_w（SMOW）值为+8.46‰~+8.95‰，指示进一步增加的水-岩相互作用；第三期为热流体，T（Δ₄₇）为130~147℃，δ¹⁸O_w（SMOW）值为+7.93‰~+9.42‰，矿物氧同位素较第二期明显偏负，且鞍状白云石发育。孔洞和裂缝内充填碳酸盐岩的碳、氧同位素分布范围较宽，δ¹⁸O_carb（VPDB）值为-17.38 ‰~-5.84‰，δ¹³C_carb（VPDB）值为-3.57‰~-1.33‰，也揭示了多期次流体活动的叠加改造。岩心和显微观测结果显示，白云岩具有很好的储集空间，埋藏溶蚀作用和断裂带附近的热流体活动叠加是鹰山组白云岩储层发育的主要建设性成岩作用。

关键词: 团簇同位素, 碳酸盐, 成岩流体, 储层, 白云岩, 下奥陶统, 塔中地区, 塔里木盆地

Abstract:

Based on the relationship between the relative abundance of ¹³C and ¹⁸O bonds and temperature, carbonate clumped isotope (Δ₄₇) has the special characteristic of indicating temperature even in the absence of knowledge about the chemical and isotopic composition of the fluid from which the carbonates precipitated.This property hence makes the technique an excellent temperature proxy in the study of diagenetic fluids.As such, this study employs clumped isotopes to examine the origin of diagenetic fluids in deep and ultra-deep subsurface settings and we assess their impact on the development of reservoir quality.This study considers both the matrix and associated cements.Three episodes of diagenesis are revealed. In the first stage, the fluids formed in a shallow-to-medium burial environment and the matrix was altered to have a powder-crystal to finely-crystalline texture.The range of Δ₄₇ derived temperatures ranges from 69 to 94℃, and the δ¹⁸O_w values are from +1.81‰ to +5.19‰ SMOW.These data suggest that the fluid is modified seawater.The second diagenetic episode was influence by a brine after the sequence was deeply-bured.Here, the matrix was altered to a me-dium-crystalline texture and the Δ₄₇ derived temperatures range from 111 to 113℃, and the δ¹⁸O_w values range from +8.46‰ to +8.95‰ SMOW, indicating that a substantial water-rock interaction occurred.The third diagenetic episode was induced by hydrothermal fluids, likely travelling along faults and fractures, which yielded abundant saddle dolomite.Here, Δ₄₇ derived temperatures varies from 130 to 147℃ and the δ¹⁸O_w values from +7.93‰ to +9.42‰ SMOW.The vug-and vein-filling carbonates have a wide range of δ¹⁸O_carb and δ¹³C_carb values.The δ¹⁸O_carb values span -17.38‰ to -5.84‰ VPDB, and the δ¹³C_carb values from 3.57‰ to -1.33‰ VPDB, indicating multiple stages of fluid modification.Both the cores and photomicrographs demonstrate excellent reservoir quality for the Lower Ordovician Tazhong dolomites.

Key words: clumped isotope, carbonate, diagenetic fluid, reservoir, dolomite, Lower Ordovician, Tazhong area, Tarim Basin

中图分类号:

TE135

刘嘉庆,李忠,颜梦珂,等. 塔里木盆地塔中地区下奥陶统白云岩的成岩流体演化:来自团簇同位素的证据[J]. 石油与天然气地质, 2020, 41(1): 68-82. doi: 10.11743/ogg20200107 Jiaqing Liu,Zhong Li,Mengke Yan,et al. Diagenetic fluid evolution of dolomite from the Lower Ordovician in Tazhong area, Tarim Basin: Clumped isotopic evidence[J]. Oil & Gas Geology, 2020, 41(1): 68-82. doi: 10.11743/ogg20200107

图/表 10

图1

图2

图3

图4

图5

图6

表1

表2

塔中地区下奥陶统鹰山组白云岩碳、氧同位素测试结果"

井号	深度/m	岩石类型	产状	δ¹³C(VPDB)/%	δ¹⁸O(VPDB)/%
ZG442H	5 555.86	粉-细晶云岩	孔洞内充填方解石	-2.19	-6.12
TZ12	5 299.00	细晶白云岩	基质白云石(孔隙发育)	-0.91	-5.55
TZ12	5 299.00	泥-粉晶云岩	基质白云石(致密)	-1.74	-3.50
TZ12	5 248.02	泥-粉晶云岩	基质白云石(致密)	-1.42	-4.74
TZ12	5 248.02	粉晶白云岩	孔洞内充填方解石	-1.51	-11.13
TZ12	5 241.65	细晶白云岩	基质白云石(孔隙发育)	-1.00	-8.37
TZ12	5 237.40	粗晶白云岩	孔洞内充填白云石	-1.33	-17.38
TZ12	5 232.20	粉晶白云岩	孔洞内充填方解石	-1.78	-14.21
TZ3	3 770.03	白云岩	裂缝内充填方解石	-2.62	-9.55
TZ3	3 761.97	白云岩	裂缝内充填方解石	-3.35	-6.62
TZ3	3 761.97	白云岩	裂缝内充填方解石	-1.46	-6.54
TZ3	3 761.74	白云岩	孔洞内充填方解石	-2.77	-10.98
TZ3	3 761.74	白云岩	孔洞内充填方解石	-2.60	-11.38
TZ3	4 222.08	白云岩	裂缝内充填方解石	-2.93	-11.89
TZ3	4 222.08	白云岩	裂缝内充填方解石	-2.08	-13.07
TZ3	4 205.65	白云岩	裂缝内充填方解石	-2.93	-8.77
TZ3	4 200.00	白云岩	裂缝内充填方解石	-2.42	-7.56
TZ3	4 192.92	白云岩	裂缝内充填方解石	-2.18	-11.36
TZ3	4 069.40	细晶白云岩	基质白云石(孔隙发育)	-2.04	-4.51
TZ3	4 069.40	泥晶白云岩	泥晶白云石	-1.93	-3.86
TZ3	4 066.40	白云岩	裂缝内充填方解石	-3.14	-9.75
TZ3	4 021.70	白云岩	孔洞内充填方解石	-3.01	-8.26
TZ3	3 966.33	白云岩	裂缝内充填方解石	-2.24	-6.14
TZ3	3 966.33	白云岩	裂缝内充填方解石	-3.18	-12.05
ZG46-3H	5 584.50	粉-细晶白云岩	孔洞内充填方解石	-3.57	-5.84
ZG46-3H	5 589.27	球粒白云岩	孔洞内充填方解石	-2.87	-11.06
ZG46-3H	5 582.53	粉-细晶白云岩	基质白云石(孔隙发育)	-1.83	-7.22
ZG9	6 267.90	中-细晶白云岩	基质白云石(孔隙发育)	0.40	-6.10
ZG9	6 267.90	中-细晶白云岩	基质白云石(致密)	0.89	-5.80

表2

图7

图8

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井号	样品号	深度/m	岩石类型	产状	δ¹³C(VPDB)/‰	δ¹⁸O(VPDB)/‰	Δ₄₇/‰	δ¹⁸O_w(SMOW)/‰	T/℃
ZG9	ZG9-2	6 261.62	中-粗晶白云岩	基质白云石(孔隙发育)	0.88	-5.39	0.542	5.19	94
					0.77	-5.59	0.581	1.81	71
					0.83	-5.49	0.562	3.50	83
ZG512	ZG512-5	5 587.94	粉晶中-细晶云岩	基质白云石(孔隙发育)	-2.10	-3.73	0.516	8.95	111
ZG512	ZG512-5	5 587.94	粉晶中-细晶云岩	裂缝内充填方解石	-3.20	-9.10	0.488	9.42	133
ZG512	ZG512-6	5 588.51	中-粗晶云岩	基质白云石(孔隙发育)	-1.39	-9.28	0.527	2.39	104
ZG512	ZG512-6	5 588.51	中-粗晶云岩	孔洞内充填方解石	-2.31	-12.01	0.472	7.93	147
ZG512	ZG512-7	5 589.66	粉-细晶云岩	孔洞内充填白云石	-1.69	-3.93	0.515	8.80	112
ZG512	ZG512-8	5 589.77	粉-细晶云岩	基质白云石(孔隙发育)	-1.07	-4.44	0.513	8.46	113
ZG512	ZG512-8	5 589.77	粉-细晶云岩	孔洞内充填白云石	-1.91	-3.32	0.573	4.79	75
ZG503	ZG503-1	6 060.40	灰质云岩	裂缝内充填方解石	-2.04	-9.03	0.492	9.13	130
TZ12	TZ12-3	5 297.90	粉晶白云岩	裂缝内充填方解石	-1.35	-3.13	0.585	4.04	69

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塔里木盆地塔中地区下奥陶统白云岩的成岩流体演化:来自团簇同位素的证据

Diagenetic fluid evolution of dolomite from the Lower Ordovician in Tazhong area, Tarim Basin: Clumped isotopic evidence

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