塔里木盆地下寒武统肖尔布拉克组储层成因

魏天媛; 蔡春芳; 扈永杰; 刘大卫; 蒋子文

doi:10.14027/j.issn.1000-0550.2021.116

塔里木盆地下寒武统肖尔布拉克组储层成因

doi: 10.14027/j.issn.1000-0550.2021.116

魏天媛^{1, 2, 3,},
蔡春芳^{1, 2, 3, ,},
扈永杰⁴,
刘大卫⁵,
蒋子文^{1, 2, 3}

1.
中国科学院地质与地球物理研究所, 中国科学院新生代地质与环境重点实验室, 北京 100029
2.
中国科学院地球科学研究院, 北京 100029
3.
中国科学院大学地球与行星科学学院, 北京 100049
4.
中国石化集团国际石油勘探开发有限公司, 北京 100029
5.
中国石化石油勘探开发研究院, 北京 102206

基金项目:

国家科技重大专项 2017ZX0508-003-040

详细信息

作者简介:
魏天媛,女,1996年出生,博士研究生,储层沉积学,E-mail: weity@mail.iggcas.ac.cn

通讯作者:
蔡春芳,男,研究员,E-mail: cai_cf@mail.iggcas.ac.cn

中图分类号: P618.13

计量

文章访问数: 295
HTML全文浏览量: 54
PDF下载量: 76
被引次数: 0

Origin of Reservoirs in the Lower Cambrian Xiaoerbulak Formation, Tarim Basin

WEI TianYuan^{1, 2, 3
,},
CAI ChunFang^{1, 2, 3
, ,},
HU YongJie⁴,
LIU DaWei⁵,
JIANG ZiWen^{1, 2, 3}

1.
Key Laboratory of Cenozoic Geology and Environment, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China
2.
Institutions of Earth Science, Chinese Academy of Sciences, Beijing 100029, China
3.
College of Earth and Planetary Sciences, University of Chinese Academy of Sciences, Beijing 100049, China
4.
SINOPEC International Exploration and Production Corporation, Beijing 100029, China
5.
Petroleum Exploration and Production Research Institute, SINOPEC, Beijing 102206, China

Funds:

National Science and Technology Major Project 2017ZX0508-003-040

摘要

摘要: 在深层—超深层碳酸盐储层仍有大量油气出现,但优质储层成因尚不明确。通过对塔里木盆地寒武系肖尔布拉克组典型井和露头样品进行岩石学观察,总结出主要发育四类岩石类型：微生物岩、颗粒云岩、晶粒云岩和泥晶灰岩。根据阴极发光、流体包裹体测试、碳酸盐矿物碳氧同位素测试,认为上述白云岩基质形成于弱氧化海水；近地表—浅埋藏环境下则主要形成细晶白云石胶结物；深埋藏条件发育中粗晶白云石胶结物和鞍形白云石。随着埋深增大,白云石δ¹⁸O呈现降低的趋势,反映形成温度升高,但都具有较正的δ¹³C。方解石由于烃类并入,具有负偏的δ¹³C（-4.07‰±0.92‰）,为热化学硫酸盐还原（TSR）成因。原位微量稀土测试显示成岩流体从早期到晚期：从具有海水特征的配分曲线逐步演化为中稀土富集,最终变为轻稀土富集的模式,反映了从海水为主的孔隙水演化为热流体为主的孔隙水的过程。定量统计表明热液溶蚀可提高储层3%的面孔率,最大孔隙度达10%。根据沉积—成岩改造类型,划分出三类优质储层：热液/大气水改造的凝块石储层、热液/TSR改造的浅滩相颗粒云岩储层、TSR改造的膏盐相关白云岩储层。该研究为塔里木盆地寒武系碳酸盐岩油气勘探提供了有利的指导,有助于理解深层—超深层优质白云岩储层成因。
- 塔里木盆地 /
- 肖尔布拉克组 /
- 白云岩储层 /
- 成岩流体 /
- 热液 /
- TSR
Abstract: Well-developed deep-time and deep-burial dolostone reservoirs are currently sedimentlogical research topics in petroleum exploration, for example in the Sichuan and Tarim Basins in China, and the South Oman Salt Basin. Due to the influence of sedimentary environments and constructive diageneses, ancient deep and ultra-deep dolostone （>4 500 m） have demonstrated high-quality reservoir properties in some case studies. The porosity of some intervals is up to 10%⁃20%, producing oil and gas of industrial standard, and are of great importance in hydrocarbon exploration. However, our understanding of the genesis of the pore structures of deeply buried dolostone reservoirs is still limited： are they generated from later diagenesis, or are they preserved sediments retaining early diagenetic pores? Distinguishing between these two types of pores and explaining their formation mechanisms is a controversial and much-debated topic in sedimentology. The Cambrian Xiaoerbulak Formation underwent long periods of deep burial settings, to a maximum burial depth of 6 000 m. This formation is characterized by the complexity of the diagenesis of dolostone and the heterogeneity of the reservoirs. In addition, they are associated with many different microbialite types.Overall, this suggested that the Xiaoerbulak Formation is a suitable case for solving the debated issue of late microbialitic dissolution. For this reason, the Cambrian Xiaoerbulak Formation in the Tarim Basin was selected as the research object, and the rocks from typical wells and field profiles were carefully selected and used in a variety of advanced experiments, comprising multi-scale geological and geochemical methods included microscopic observation of rocks and minerals, stable δ¹³C and δ¹⁸O isotope analysis, and in-situ trace element and rare earth element analyses. Combined with basic data from previous sedimentological studies, this paper attaches importance to the analysis of fluid⁃rock interactions and solves deep and ultra-deep issues such as the evolution of diagenetic fluids and dissolution transformation of dolomite reservoirs. Firstly, based on comprehensive and detailed petrological observations, it is concluded that there are four main types of rocks developed in the Xiaoerbulak Formation： microbialites （thrombolite dolostone, foam spongy dolostone, oncolite dolostone, stromatolite dolostone, bonded sandy dolostone, and algal framework dolostone）, dolo-grainstone, crystalline dolomite （dolo-micrite and fine crystalline dolomite） and micritic limestone. The analyses of porosity and permeability suggest that dolo-grainstone and thrombolites contain the best reservoir properties. In contrast, stromatolite dolostone and fine crystalline dolostone have lower porosities and permeabilities. Cathodoluminescence studies, fluid inclusion data and carbon and oxygen isotope testing suggest that matrix dolomite and fine-crystalline dolomite were formed in sedimentary oxidized seawater with δ¹⁸O values of -6.16‰ ± 0.72‰. Subsequently, fine-crystalline dolomite cements （δ¹⁸O = -7.47‰ ± 1.2‰） were mainly formed in near-surface to shallow burial environments. In deep burial conditions, coarse-crystalline dolomite cements （δ¹⁸O =-11.35‰ ± 1.41‰） and saddle dolomites （δ¹⁸O = -10.44‰ ± 0.6‰） were developed. With gradually increasing depth, oxygen isotope values of carbonate minerals show a decreasing trend, indicating a rising formation temperature. However, these dolomites have relatively positive carbon isotopes, and there is no significant change among them. By comparison, due to the oxidation of hydrocarbons and their incorporation into calcite, the calcite has negative δ¹³C values （-4.07‰ ± 0.92‰）, suggesting that it is typical of thermochemical sulfate reduction （TSR）.The presence of hydrothermal minerals, including saddle dolomite and authigenic quartz, is evidence of homogenization temperatures above that of the formation. In-situ trace element and rare earth tests show that diagenetic fluids evolved from early to late stages： distribution curves indicate enriched heavy rare earth elements （HREE）, to enrichment of medium rare earth elements （MREE）, and finally to a mode of enrichment of light rare earth elements （LREE）. In consequence, the following evolutionary sequence of diagenetic fluids was comprehensively considered： from seawater-dominated pore water, shallow-buried iron-rich pore water, medium-deep buried manganese-rich pore water, to lately crust-derived hydrothermal fluid-dominated pore water, and finally evolved into acidic fluids related to TSR dissolution. It is noteworthy that the properties of the fluids gradually evolved from low-temperature and low-salinity to high-temperature and high-salinity. Quantitative statistics show that hydrothermal dissolution increased the porosity of the reservoir by 3%； the maximum porosity is close to 10%.Thus it is concluded that the late dissolution re-formation of those formed in early high-energy mound-shoal facies contributed most to the development of high-quality reservoirs. Depending on the type of sedimentation- diagenetic re-formation, three categories of high-quality reservoirs are classified in the Xiaoerbulak Formation as follows：（i） hydrothermal/meteoric water-altered thrombolitic reservoir of high-energy reef and shoal facies；（ii） hydrothermal/TSR-altered shoal facies dolo-grainstone reservoirs； and （iii） TSR-altered gypsum-related dolostone reservoirs. This list provides favorable exploration directions for Xiaoerbulak Formation carbonate oil and gas exploration in the Tarim Basin, and also helps to better understand the genesis of deep and ultra-deep high-quality dolomite reservoirs.
- Tarim Basin /
- Xiaoerbulak Formation /
- dolomite reservoir /
- diagenetic fluid /
- hydrothermal /
- TSR

HTML全文

图 1 塔里木盆地肖尔布拉克组沉积时期岩相古地理图及采样井、露头分布（修改自文献[61]）

Figure 1. Lithofacies paleogeographic map with locations of sampled wells and the Xiaoerbulak Formation outcrops in the Tarim Basin (modified from reference [61])

Fig.1

下载: 全尺寸图片幻灯片

图 2 塔里木盆地肖尔布拉克组埋藏史图（修改自文献[62]）

Figure 2. Burial histories of the Xiaoerbulak Formation, Tarim Basin (modified from reference [62])

Fig.2

下载: 全尺寸图片幻灯片

图 3 各类矿物充填/胶结作用及其阴极发光特征

（a）泡沫绵层石白云岩中纤状白云石早于细晶白云石充填,什艾日克剖面；（b）与图a同一视域的阴极发光特征；（c）肖下段凝块石丘中凝块石白云岩的准同生溶蚀孔洞,肖尔布拉克东沟剖面；（d）与图c同一视域的阴极发光特征；（e）泡沫绵层石白云岩中中粗晶白云石,什艾日克剖面；（f）与图e同一视域的阴极发光特征；（g）粉细晶云岩中细晶白云石早于中粗晶白云石早于鞍形白云石早于热液方解石充填,肖尔布拉克东沟剖面,单偏光；（h）黏结砂屑云岩中热液溶蚀孔洞边缘见鞍形白云石溶蚀边,肖尔布拉克西沟剖面,正交光；（i）细晶云岩中热液石英充填鞍形白云石晶间孔,舒探1井,2 000.0 m,正交光；（j）白云石在长柱状硬石膏边缘胶结,舒探1井,1 992.4 m,正交光；（k）砂屑云岩中沥青和铸模孔伴生,舒探1井,1 886.5 m,肖尔布拉克组,单偏光；（l）砂屑云岩中TSR造成的硬石膏溶蚀孔,楚探1井,7 775.3 m,肖尔布拉克组,正交光

Figure 3. Thin⁃section and cathodoluminesence photomicroraphs of different kinds of minerals filled/cemented

Fig.3

下载: 全尺寸图片幻灯片

图 4 塔里木盆地柯坪露头微生物岩分布图

Figure 4. Section of microbial rocks in Keping outcrop, Tarim Basin

Fig.4

下载: 全尺寸图片幻灯片

图 5 柯坪地区肖尔布拉克组微生物岩沉积相模式（修改自文献[43]）

Figure 5. Sedimentary facies model of microbial rocks from the Keping area of the Xiaoerbulake Formation (modified from reference [43])

Fig.5

下载: 全尺寸图片幻灯片

图 6 塔里木盆地下寒武统肖尔布拉克组岩石类型及储层特征

（a）凝块石云岩,具球粒状凝块结构,藻纹层结构不发育,球粒弥散呈斑状构成凝块,发育凝块间溶孔,肖尔布拉克西沟剖面,单偏光；（b）泡沫绵层云岩,泥晶化程度较弱,藻迹模糊,什艾日克剖面,单偏光；（c）核形石云岩,核形石颗粒大小不一,散乱分布,肖尔布拉克东3沟剖面,单偏光；（d）叠层石云岩,顺纹层充填鞍形白云石,舒探1井,1 883.5 m,单偏光；（e）黏结砂屑云岩,发育包覆状微生物溶孔,方1井,4 570.0 m,单偏光；（f）藻格架云岩,原生格架孔发育,舒探1井,1 910.5 m,单偏光；（g）颗粒云岩充填柱状硬石膏,致密,康2井,5 500.0 m,正交光；（h）藻砂屑云岩,粒间充填亮晶白云石胶结物,舒探1井,1 886.5 m,单偏光；（i）荧光显微镜下砂屑白云岩具荧光显示,肖尔布拉克组,肖尔布拉克剖面；（j）泥粉晶云岩,可见鞍形白云石,舒探1井,1 990.4 m,正交光；（k）粉细晶云岩,晶间溶孔发育,舒探1井,1 915.3 m,单偏光；（l）泥晶灰岩,致密,偶见三叶虫碎片,新河1井,7 600.0 m,单偏光

Figure 6. Rock types and reservoir properties in Lower Cambrian Xiaoerbulake Formation, Tarim Basin

Fig.6

下载: 全尺寸图片幻灯片

图 7 塔里木盆地肖尔布拉克组成岩作用序列

Figure 7. Paragenetic sequence of the Xiaoerbulake Formation, Tarim Basin

Fig.7

下载: 全尺寸图片幻灯片

图 8 各期充填/胶结物碳氧同位素组成

Figure 8. Carbon and oxygen isotope compositions of fillings and cements at different times

Fig.8

下载: 全尺寸图片幻灯片

图 9 各类充填物流体包裹体数据

（a）温度；（b）盐度

Figure 9. Fluid inclusion data of different diagenetic minerals

(a) homogenization temperatures; (b) salinity

下载: 全尺寸图片幻灯片

图 10 塔里木盆地肖尔布拉克组各类充填物铁锰含量

Figure 10. Fe and Mn contents of different kinds of filling in the Xiaoerbulak Formation, Tarim Basin

Fig.10

下载: 全尺寸图片幻灯片

图 11 各类充填物稀土配分曲线

Figure 11. Average rare earth element and yttrium profiles for different kinds of filling

Fig.11

下载: 全尺寸图片幻灯片

图 12 各类白云岩孔隙度—渗透率柱状图

Figure 12. Porosity⁃permeability histogram for different kinds of dolostone

Fig.12

下载: 全尺寸图片幻灯片

图 13 舒探1井岩心柱状图

Figure 13. Imaging logging characteristics of rock core in well Shutan1

Fig.13

下载: 全尺寸图片幻灯片

表 1 各期次流体性质、产物与关系

沉积/成岩流体	均一温度与盐度	稀土配分模式	微量元素含量	性质	产物
沉积海水	40 ℃,3.5 wt%^[48]	LREE亏损 HREE富集	中—高Fe 低Mn	弱氧化性	粉细晶白云石基质
接近海水的孔隙水	小于50 ℃^[48]	LREE亏损 HREE富集	中—高Fe 低Mn	低盐度	氧同位素接近基质的细晶白云石胶结物
浅埋藏条件孔隙水	70 ℃~100 ℃^[44],6~14wt.%^[48]	MREE富集	极高Fe 高Mn	稍高温,还原性	氧同位素偏负的细晶白云石胶结物
中深埋藏条件孔隙水	94 ℃~121 ℃,10~29 wt.%	MREE富集	高Fe 高Mn	高温高盐度	中粗晶白云石胶结物
壳源热流体	136 ℃~182 ℃,13~25 wt.%	MREE富集	极高Fe 极高Mn	高温高盐度还原酸性	鞍形白云石,石英
TSR相关流体	128 ℃~152 ℃,18~23 wt.%	LREE富集	低Fe 低Mn	高温高盐度酸性	方解石

下载: 导出CSV

参考文献(94)

[1]	Sun S Q. 白云岩的孔隙演化与储层特性[J]. 项光,译.国外油气勘探,1995,7（5）：551-563. Sun S Q. Pore evolution and reservoir characteristics of dolostone[J]. Xiang Guang, trans. Equipment for Geophysical Prospecting, 1995, 7（5）： 551-563.
[2]	张静,胡见义,罗平,等. 深埋优质白云岩储集层发育的主控因素与勘探意义[J]. 石油勘探与开发,2010,37（2）：203-210. Zhang Jing, Hu Jianyi, Luo Ping, et al. Master control factors of deep high-quality dolomite reservoirs and the exploration significance[J]. Petroleum Exploration and Development, 2010, 37（2）： 203-210.
[3]	Ohm S E, Karlsen D A, Austin T J F. Geochemically driven exploration models in uplifted areas： Examples from the Norwegian Barents Sea[J]. AAPG Bulletin, 2008, 92（9）： 1191-1223.
[4]	白莹,罗平,王石,等. 台缘微生物礁结构特点及储集层主控因素：以塔里木盆地阿克苏地区下寒武统肖尔布拉克组为例[J]. 石油勘探与开发,2017,44（3）：349-358. Bai Ying, Luo Ping, Wang Shi, et al. Structure characteristics and major controlling factors of platform margin microbial reef reservoirs： A case study of Xiaoerbulak Formation, Lower Cambrian, Aksu area, Tarim Basin, NW China[J]. Petroleum Exploration and Development, 2017, 44（3）： 349-358.
[5]	Ma Y S, Guo T L, Zhao X F, et al. The formation mechanism of high-quality dolomite reservoir in the deep of Puguang gas field[J]. Science China （Seri. D）： Earth Sciences, 2008, 51（1）： 53-64.
[6]	Jiang L, Worden R H, Cai C F. Thermochemical sulfate reduction and fluid evolution of the Lower Triassic Feixianguan Formation sour gas reservoirs, northeast Sichuan Basin, China[J]. AAPG Bulletin, 2014, 98（5）： 947-973.
[7]	Jiang L, Worden R H, Cai C F, et al. Dolomitization of gas reservoirs： The Upper Permian Changxing and Lower Triassic Feixianguan Formations, northeast Sichuan Basin, China[J]. Journal of Sedimentary Research, 2014, 84（10）： 792-815.
[8]	Peyravi M, Rahimpour-Bonab H, Nader F H, et al. Dolomitization and burial history of Lower Triassic carbonate reservoir-rocks in the Persian Gulf （Salman offshore field）[J]. Carbonates and Evaporites, 2015, 30（1）： 25-43.
[9]	Wilson A O. Depositional and diagenetic facies in the Jurassic Arab-C and-D reservoirs, Qatif field, Saudi Arabia[M]//Roehl P O, Choquette P W. Carbonate petroleum reservoirs. New York： Springer, 1985： 319-340.
[10]	朱光有,陈斐然,陈志勇,等. 塔里木盆地寒武系玉尔吐斯组优质烃源岩的发现及其基本特征[J]. 天然气地球科学,2016,27（1）：8-21. Zhu Guangyou, Chen Feiran, Chen Zhiyong, et al. Discovery and basic characteristics of the high-quality source rocks of the Cambrian Yuertusi Formation in Tarim Basin[J]. Natural Gas Geoscience, 2016, 27（1）： 8-21.
[11]	王招明,谢会文,陈永权,等. 塔里木盆地中深1井寒武系盐下白云岩原生油气藏的发现与勘探意义[J]. 中国石油勘探,2014,19（2）：1-13. Wang Zhaoming, Xie Huiwen, Chen Yongquan, et al. Discovery and exploration of Cambrian subsalt dolomite original hydrocarbon reservoir at Zhongshen-1 well in Tarim Basin[J]. China Petroleum Exploration, 2014, 19（2）： 1-13.
[12]	杨海军,陈永权,田军,等. 塔里木盆地轮探1井超深层油气勘探重大发现与意义[J]. 中国石油勘探,2020,25（2）：62-72. Yang Haijun, Chen Yongquan, Tian Jun, et al. Great discovery and its significance of ultra-deep oil and gas exploration in well Luntan-1 of the Tarim Basin[J]. China Petroleum Exploration, 2020, 25（2）： 62-72.
[13]	Beavington-Penney S J, Nadin P, Wright V P, et al. Reservoir quality variation on an Eocene carbonate ramp, El Garia Formation, offshore Tunisia： Structural control of burial corrosion and dolomitisation[J]. Sedimentary Geology, 2008, 209（1/2/3/4）： 42-57.
[14]	Vandeginste V, Swennen R, Reed M H, et al. Host rock dolomitization and secondary porosity development in the Upper Devonian Cairn Formation of the Fairholme carbonate complex （South-west Alberta, Canadian Rockies）： Diagenesis and geochemical modelling[J]. Sedimentology, 2009, 56（7）： 2044-2060.
[15]	Bourdet J, Pironon J, Levresse G, et al. Petroleum accumulation and leakage in a deeply buried carbonate reservoir, Níspero field （Mexico）[J]. Marine and Petroleum Geology, 2010, 27（1）： 126-142.
[16]	Li K K, Cai C F, Jia L Q, et al. The role of thermochemical sulfate reduction in the genesis of high-quality deep marine reservoirs within the central Tarim Basin, western China[J]. Arabian Journal of Geosciences, 2015, 8（7）： 4443-4456.
[17]	Cai C F, Worden R H, Bottrell S H, et al. Thermochemical sulphate reduction and the generation of hydrogen sulphide and thiols （mercaptans） in Triassic carbonate reservoirs from the Sichuan Basin, China[J]. Chemical Geology, 2003, 202（1/2）： 39-57.
[18]	Cai C F, Xie Z Y, Worden R H, et al. Methane-dominated thermochemical sulphate reduction in the Triassic Feixianguan Formation east Sichuan Basin, China： Towards prediction of fatal H2S concentrations[J]. Marine and Petroleum Geology, 2004, 21（10）： 1265-1279.
[19]	Cai C F, He W X, Jiang L, et al. Petrological and geochemical constraints on porosity difference between Lower Triassic sour- and sweet-gas carbonate reservoirs in the Sichuan Basin[J]. Marine and Petroleum Geology, 2014, 56： 34-50.
[20]	Jiang L, Worden R H, Cai C F. Generation of isotopically and compositionally distinct water during thermochemical sulfate reduction （TSR） in carbonate reservoirs： Triassic Feixianguan Formation, Sichuan Basin, China[J]. Geochimica et Cosmochimica Acta, 2015, 165： 249-262.
[21]	Jiang L, Pan W Q, Cai C F, et al. Fluid mixing induced by hydrothermal activity in the Ordovician carbonates in Tarim Basin, China[J]. Geofluids, 2015, 15（3）： 483-498.
[22]	Giles M R, de Boer R B. Secondary porosity： Creation of enhanced porosities in the subsurface from the dissolution of carbonate cements as a result of cooling formation waters[J]. Marine and Petroleum Geology, 1989, 6（3）： 261-269.
[23]	Huang S J, Huang K K, Tong H P, et al. Origin of CO2 in natural gas from the Triassic Feixianguan Formation of northeast Sichuan Basin[J]. Science China Earth Sciences, 2010, 53（5）： 642-648.
[24]	Surdam R C, Boese S W, Crossey L J. The chemistry of secondary porosity： Part 2. Aspects of porosity modification[M]//McDonald D A, Surdam R C. Clastic diagenesis. Tulsa, Okla, American： AAPG Bulletin, 1984： 127-149.
[25]	Schmidt T V, McDonald D A. The role of secondary porosity in the course of sandstone diagenesis[M]//Scholle P A, Schluger P R. Aspects of Diagenesis. Tulsa, Okla, American： SEPM Special Publication, 1979： 1-207.
[26]	Taylor T R, Giles M R, Hathon L A, et al. Sandstone diagenesis and reservoir quality prediction： Models, myths, and reality[J]. AAPG Bulletin, 2010, 94（8）： 1093-1132.
[27]	Al-Aasm I. Origin and characterization of hydrothermal dolomite in the western Canada sedimentary basin[J]. Journal of Geochemical Exploration, 2003, 78-79： 9-15.
[28]	Davies G R, Smith L B, Jr. Structurally controlled hydrothermal dolomite reservoir facies： An overview[J]. AAPG Bulletin, 2006, 90（11）： 1641-1690.
[29]	Lavoie D, Chi G, Urbatsch M, et al. Massive dolomitization of a pinnacle reef in the Lower Devonian West Point Formation （Gaspé Peninsula, Quebec）： An extreme case of hydrothermal dolomitization through fault-focused circulation of magmatic fluids[J]. AAPG Bulletin, 2010, 94（4）： 513-531.
[30]	Krouse H R, Viau C A, Eliuk L S, et al. Chemical and isotopic evidence of thermochemical sulphate reduction by light hydrocarbon gases in deep carbonate reservoirs[J]. Nature, 1988, 333（6172）： 415-419.
[31]	朱光有,张水昌,梁英波,等. 四川盆地深部海相优质储集层的形成机理及其分布预测[J]. 石油勘探与开发,2006,33（2）：161-166. Zhu Guangyou, Zhang Shuichang, Liang Yingbo, et al. Formation mechanism and distribution prediction of high-quality marine reservoir in deeper Sichuan Basin[J]. Petroleum Exploration and Development, 2006, 33（2）： 161-166.
[32]	Ma Y S, Guo X S, Guo T L, et al. The Puguang gas field： New giant discovery in the mature Sichuan Basin, southwest China[J]. AAPG Bulletin, 2007, 91（5）： 627-643.
[33]	王一刚,文应初,洪海涛,等. 四川盆地三叠系飞仙关组气藏储层成岩作用研究拾零[J]. 沉积学报,2007,25（6）：831-839. Wang Yigang, Wen Yingchu, Hong Haitao, et al. Diagenesis of Triassic Feixianguan Formation in Sichuan Basin, Southwest China[J]. Acta Sedimentologica Sinica, 2007, 25（6）： 831-839.
[34]	Ehrenberg S N, Walderhaug O, Bjørlykke K. Carbonate porosity creation bymesogenetic dissolution： Reality or illusion[J]. AAPG Bulletin, 2012, 96（2）： 217-233.
[35]	Bjørlykke K, Jahren J. Open or closed geochemical systems during diagenesis in sedimentary basins： Constraints on mass transfer during diagenesis and the prediction of porosity in sandstone and carbonate reservoirs[J]. AAPG Bulletin, 2012, 96（12）： 2193-2214.
[36]	Machel H G, Buschkuehle B E. Diagenesis of the Devonian Southesk-Cairn Carbonate Complex, Alberta, Canada： Marine cementation, burial dolomitization, thermochemical sulfate reduction, anhydritization, and squeegee fluid flow[J]. Journal of Sedimentary Research, 2008, 78（5）： 366-389.
[37]	Hao F, Zhang X F, Wang C W, et al. The fate of CO2 derived from thermochemical sulfate reduction （TSR） and effect of TSR on carbonate porosity and permeability, Sichuan Basin, China[J]. Earth-Science Reviews, 2015, 141： 154-177.
[38]	邵龙义,何宏,彭苏萍,等. 塔里木盆地巴楚隆起寒武系及奥陶系白云岩类型及形成机理[J]. 古地理学报,2002,4（2）：19-30. Shao Longyi, He Hong, Peng Suping, et al. Types and origin of dolostones of the Cambrian and Ordovician of Bachu uplift area in Tarim Basin[J]. Journal of Palaeogeography, 2002, 4（2）： 19-30.
[39]	邵龙义,韩俊,马锋,等. 塔里木盆地东部寒武系白云岩储层及相控特征[J]. 沉积学报,2010,28（5）：953-961. Shao Longyi, Han Jun, Ma Feng, et al. Characteristics of the Cambrian dolomite reservoirs and their facies-controlling in eastern Tarim Basin[J]. Acta Sedimentologica Sinica, 2010, 28（5）： 953-961.
[40]	黄擎宇,刘迪,叶宁,等. 塔里木盆地寒武系白云岩储层特征及成岩作用[J]. 东北石油大学学报,2013,37（6）：63-74. Huang Qingyu, Liu Di, Ye Ning, et al. Reservoir characteristics and diagenesis of the Cambrian dolomite in Tarim Basin[J]. Journal of Northeast Petroleum University, 2013, 37（6）： 63-74.
[41]	沈安江,郑剑锋,陈永权,等. 塔里木盆地中下寒武统白云岩储集层特征、成因及分布[J]. 石油勘探与开发,2016,43（3）：340-349. Shen Anjiang, Zheng Jianfeng, Chen Yongquan, et al. Characteristics, origin and distribution of dolomite reservoirs in Lower-Middle Cambrian, Tarim Basin, NW China[J]. Petroleum Exploration and Development, 2016, 43（3）： 340-349.
[42]	郑剑锋,黄理力,袁文芳,等. 塔里木盆地柯坪地区下寒武统肖尔布拉克组地球化学特征及其沉积和成岩环境意义[J]. 天然气地球科学,2020,31（5）：698-709. Zheng Jianfeng, Huang Lili, Yuan Wenfang, et al. Geochemical features and its significance of sedimentary and diagenetic environment in the Lower Cambrian Xiaoerblak Formation of Keping area, Tarim Basin[J]. Natural Gas Geoscience, 2020, 31（5）： 698-709.
[43]	严威,郑剑锋,陈永权,等. 塔里木盆地下寒武统肖尔布拉克组白云岩储层特征及成因[J]. 海相油气地质,2017,22（4）：35-43. Yan Wei, Zheng Jianfeng, Chen Yongquan, et al. Characteristics and genesis of dolomite reservoir in the Lower Cambrian Xiaoerblak Formation, Tarim Basin[J]. Marine Origin Petroleum Geology, 2017, 22（4）： 35-43.
[44]	程丽娟,李忠,刘嘉庆,等. 塔里木盆地巴楚—塔中地区寒武系盐下白云岩储层成岩作用及物性特征[J]. 石油与天然气地质,2020,41（2）：316-327. Cheng Lijuan, Li Zhong, Liu Jiaqing, et al. Diagenesis and physical properties of subsalt dolomite reservoirs of the Cambrian, Bachu-Tazhong areas, Tarim Basin[J]. Oil & Gas Geology, 2020, 41（2）： 316-327.
[45]	金振奎,余宽宏. 白云岩储集层埋藏溶蚀作用特征及意义：以塔里木盆地东部下古生界为例[J]. 石油勘探与开发,2011,38（4）：428-434. Jin Zhenkui, Yu Kuanhong. Characteristics and significance of the burial dissolution of dolomite reservoirs： Taking the Lower Palaeozoic in eastern Tarim Basin as an example[J]. Petroleum Exploration and Development, 2011, 38（4）： 428-434.
[46]	赵文智,沈安江,胡素云,等. 中国碳酸盐岩储集层大型化发育的地质条件与分布特征[J]. 石油勘探与开发,2012,39（1）：1-12. Zhao Wenzhi, Shen Anjiang, Hu Suyun, et al. Geological conditions and distributional features of large-scale carbonate reservoirs onshore China[J]. Petroleum Exploration and Development, 2012, 39（1）： 1-12.
[47]	赵文智,沈安江,胡素云,等. 塔里木盆地寒武—奥陶系白云岩储层类型与分布特征[J]. 岩石学报,2012,28（3）：758-768. Zhao Wenzhi, Shen Anjiang, Hu Suyun, et al. Types and distributional features of Cambrian-Ordovician dolostone reservoirs in Tarim Basin, northwestern China[J]. Acta Petrologica Sinica, 2012, 28（3）： 758-768.
[48]	Jiang L, Cai C F, Worden R H, et al. Multiphase dolomitization of deeply buried Cambrian petroleum reservoirs, Tarim Basin, north-west China[J]. Sedimentology, 2016, 63（7）： 2130-2157.
[49]	余浩元,蔡春芳,郑剑锋,等. 微生物结构对微生物白云岩孔隙特征的影响：以塔里木盆地柯坪地区肖尔布拉克组为例[J]. 石油实验地质,2018,40（2）：233-243. Yu Haoyuan, Cai Chunfang, Zheng Jianfeng, et al. Influence of microbial textures on pore characteristics of microbial dolomites： A case study of Lower Cambrian Xiaoerbulake Formation in Keping area, Tarim Basin[J]. Petroleum Geology & Experiment, 2018, 40（2）： 233-243.
[50]	Jiang L, Worden R H, Cai C F, et al. Diagenesis of an evaporite-related carbonate reservoir in deeply buried Cambrian strata, Tarim Basin, northwest China[J]. AAPG Bulletin, 2018, 102（1）： 77-102.
[51]	Jia L Q, Cai C F, Zhang J G, et al. Effect of thermochemical sulfate reduction on carbonate reservoir quality： Cambrian and Ordovician oilfield, Tazhong area, Tarim Basin, China[J]. Marine and Petroleum Geology, 2021, 123： 104745.
[52]	Cai C F, Hu W S, Worden R H. Thermochemical sulphate reduction in Cambro-Ordovician carbonates in Central Tarim[J]. Marine and Petroleum Geology, 2001, 18（6）： 729-741.
[53]	贾承造,魏国齐,姚慧君,等. 盆地构造演化与区域构造地质[M]. 北京：石油工业出版社,1995：1-42. Jia Chengzao, Wei Guoqi, Yao Huijun, et al. Basin tectonic evolution and regional tectonic geology[M]. Beijing： Petroleum Industry Press, 1995： 1-42.
[54]	Cai C F, Zhang C M, Cai L L, et al. Origins of Palaeozoic oils in the Tarim Basin： Evidence from sulfur isotopes and biomarkers[J]. Chemical Geology, 2009, 268（3/4）： 197-210.
[55]	Cai C F, Zhang C M, Worden R H, et al. Application of sulfur and carbon isotopes to oil⁃source rock correlation： A case study from the Tazhong area, Tarim Basin, China[J]. Organic Geochemistry, 2015, 83-84： 140-152.
[56]	潘文庆,陈永权,熊益学,等. 塔里木盆地下寒武统烃源岩沉积相研究及其油气勘探指导意义[J]. 天然气地球科学,2015,26（7）：1224-1232. Pan Wenqing, Chen Yongquan, Xiong Yixue, et al. Sedimentary facies research and implications to advantaged exploration regions on Lower Cambrian source rocks, Tarim Basin[J]. Natural Gas Geoscience, 2015, 26（7）： 1224-1232.
[57]	陈永权,周新源,杨海军. 塔里木盆地塔中地区上寒武统三种截面特征白云岩的岩石地球化学特征与成因研究[J]. 沉积学报,2010,28（2）：209-218. Chen Yongquan, Zhou Xinyuan, Yang Haijun. Geochemical research and genesis of dolostones with different crystal characteristics occurring in the Upper Cambrian, centeral area of Tarim Basin[J]. Acta Sedimentologica Sinica, 2010, 28（2）： 209-218.
[58]	白莹,罗平,刘伟,等. 微生物碳酸盐岩储层特征及主控因素：以塔里木盆地阿克苏地区下寒武统肖尔布拉克组上段为例[J]．中国石油勘探,2018,23（4）：95-106. Bai Ying, Luo Ping, Liu Wei, et al. Characteristics and main controlling factors of microbial carbonate reservoir： A case study of Upper member of Lower Cambrian Xiaoerbulake Formation in Akesu area, Tarim Basin[J]. China Petroleum Exploration, 2018, 23（4）： 95-106.
[59]	Qiu N S, Chang J, Zuo Y H, et al. Thermal evolution and maturation of Lower Paleozoic source rocks in the Tarim Basin, northwest China[J]. AAPG Bulletin, 2012, 96（5）： 789-821.
[60]	Wang T G, He F Q, Wang C J, et al. Oil filling history of the Ordovician oil reservoir in the major part of the Tahe oilfield, Tarim Basin, NW China[J]. Organic Geochemistry, 2008, 39（11）： 1637-1646.
[61]	胡明毅,孙春燕,高达. 塔里木盆地下寒武统肖尔布拉克组构造—岩相古地理特征[J]. 石油与天然气地质,2019,40（1）：12-23. Hu Mingyi, Sun Chunyan, Gao Da. Characteristics of tectonic-lithofacies paleogeography in the Lower Cambrian Xiaoerbulake Formation, Tarim Basin[J]. Oil & Gas Geology, 2019, 40（1）： 12-23.
[62]	高孝巧. 塔里木盆地巴楚—塔中地区肖尔布拉克组沉积特征及控储机理[D]. 北京：中国地质大学（北京）,2018. Gao Xiaoqiao. Sedimentary characteristics and its control mechanisms on reservoirs of the Xiaoerbulak Formation in Bachu-Tazhong region, Tarim Basin, NW China[D]. Beijing： China University of Geosciences （Beijing）, 2018.
[63]	贾承造. 中国塔里木盆地构造特征与油气[M]. 北京：石油工业出版社,1997：1-438. Jia Chengzao. Tectonic characteristics and petroleum Tarim Basin China[M]. Beijing： Petroleum Industry Press, 1997： 1-438.
[64]	Bau M, Dulski P. Distribution of yttrium and rare-earth elements in the Penge and Kuruman iron-formations, Transvaal Supergroup, South Africa[J]. Precambrian Research, 1996, 79（1/2）： 37-55.
[65]	Sheppard S M F, Schwarcz H P. Fractionation of Carbon and Oxygen isotopes and magnesium between coexisting metamorphic calcite and dolomite[J]. Contributions to Mineralogy and Petrology, 1970, 26（3）： 161-198.
[66]	Haley B A, Klinkhammer G P, Mcmanus J. Rare earth elements in pore waters of marine sediments[J]. Geochimica et Cosmochimica Acta, 2004, 68（6）： 1265-1279.
[67]	Jacobs L, Emerson S, Huested S S. Trace metal geochemistry in the Cariaco Trench[J]. Deep Sea Research Part A. Oceanographic Research Papers, 1987, 34（5/6）： 965-981.
[68]	Canfield D E, Thamdrup B. Towards a consistent classification scheme for geochemical environments, or, why we wish the term ‘suboxic’ would go away[J]. Geobiology, 2009, 7（4）： 385-392.
[69]	Dong S F, Chen D Z, Qing H, et al. Hydrothermal alteration of dolostones in the Lower Ordovician, Tarim Basin, NW China： Multiple constraints from petrology, isotope geochemistry and fluid inclusion microthermometry[J]. Marine and Petroleum Geology, 2013, 46： 270-286.
[70]	李慧莉,邱楠生,金之钧,等. 塔里木盆地的热史[J]. 石油与天然气地质,2005,26（5）：613-617. Li Huili, Qiu Nansheng, Jin Zhijun, et al. Geothermal history of Tarim Basin[J]. Oil & Gas Geology, 2005, 26（5）： 613-617.
[71]	Li K K, Cai C F, He H, et al. Origin of palaeo-waters in the Ordovician carbonates in Tahe oil-field, Tarim Basin： Constraints from fluid inclusions and Sr, C and O isotopes[J]. Geofluids, 2011, 11（1）： 71-86.
[72]	Zhang C L, Xu Y G, Li Z X, et al. Diverse Permian magmatism in the Tarim Block, NW China： Genetically linked to the Permian Tarim mantle plume?[J]. Lithos, 2010, 119（3/4）： 537-552.
[73]	McLennan S M. Rare earth elements in sedimentary rocks； Influence of provenance and sedimentary processes[J]. Reviews in Mineralogy and Geochemistry, 1989, 21（1）： 169-200.
[74]	Kučera J, Cempírek J, Dolníček Z, et al. Rare earth elements and yttrium geochemistry of dolomite from post-Variscan vein-type mineralization of the Nízký Jeseník and Upper Silesian Basins, Czech Republic[J]. Journal of Geochemical Exploration, 2009, 103（2/3）： 69-79.
[75]	Hecht L, Freiberger R, Gilg H A, et al. Rare earth element and isotope （C, O, Sr） characteristics of hydrothermal carbonates： Genetic implications for dolomite-hosted talc mineralization at Göpfersgrün （Fichtelgebirge, Germany）[J]. Chemical Geology, 1999, 155（1/2）： 115-130.
[76]	Frimmel H E. Trace element distribution in Neoproterozoic carbonates as palaeoenvironmental indicator[J]. Chemical Geology, 2009, 258（3/4）： 338-353.
[77]	Azomani E, Azmy K, Blamey N, et al. Origin of Lower Ordovician dolomites in eastern Laurentia： Controls on porosity and implications from geochemistry[J]. Marine and Petroleum Geology, 2013, 40： 99-114.
[78]	Canfield D E, Raiswell R, Bottrell S H. The reactivity of sedimentary iron minerals toward sulfide[J]. American Journal of Science, 1992, 292（9）： 659-683.
[79]	Fu Y J, van Berk W, Schulz H M. Hydrogen sulfide Formation, fate, and behavior in anhydrite-sealed carbonate gas reservoirs： A three-dimensional reactive mass transport modeling approach[J]. AAPG Bulletin, 2016, 100（5）： 843-865.
[80]	Cai C F, Li K K, Li H T, et al. Evidence for cross formational hot brine flow from integrated 87Sr/86Sr, REE and fluid inclusions of the Ordovician veins in Central Tarim, China[J]. Applied Geochemistry, 2008, 23（8）： 2226-2235.
[81]	Tian W, Campbell I H, Allen C M, et al. The Tarim picrite⁃basalt⁃rhyolite suite, a Permian flood basalt from northwest China with contrasting rhyolites produced by fractional crystallization and anatexis[J]. Contributions to Mineralogy and Petrology, 2010, 160（3）： 407-425.
[82]	Tonietto S, Pope M C. Diagenetic evolution and its ifluence on petrophysical properties of the Jurassic Smackover Formation thrombolite and grainstone units of Little Cedar Creek Field, Alabama[J]. GCAGS Journal, 2013, 2： 68-84.
[83]	宋金民,罗平,杨式升,等. 塔里木盆地苏盖特布拉克地区下寒武统肖尔布拉克组碳酸盐岩微生物建造特征[J]. 古地理学报,2012,14（3）：341-354. Song Jinmin, Luo Ping, Yang Shisheng, et al. Carbonate rock microbial construction of the Lower Cambrian Xiaoerblak Formation in Sugaitblak area, Tarim Basin[J]. Journal of Palaeogeography, 2012, 14（3）： 341-354.
[84]	宋金民,罗平,杨式升,等. 塔里木盆地下寒武统微生物碳酸盐岩储集层特征[J]. 石油勘探与开发,2014,41（4）：404-413,437. Song Jinmin, Luo Ping, Yang Shisheng, et al. Reservoirs of Lower Cambrian microbial carbonates, Tarim Basin, NW China[J]. Petroleum Exploration and Development, 2014, 41（4）： 404-413, 437.
[85]	李朋威,罗平,陈敏,等. 塔里木盆地西北缘上震旦统微生物碳酸盐岩储层特征与成因[J]. 石油与天然气地质,2015,36（3）：416-428. Li Pengwei, Luo Ping, Chen Min, et al. Characteristics and origin of the Upper Sinian microbial carbonate reservoirs at the northwestern margin of Tarim Basin[J]. Oil & Gas Geology, 2015, 36（3）： 416-428.
[86]	李朋威,罗平,宋金民,等. 微生物碳酸盐岩储层特征与主控因素：以塔里木盆地西北缘上震旦统—下寒武统为例[J]. 石油学报,2015,36（9）：1074-1089. Li Pengwei, Luo Ping, Song Jinmin, et al. Characteristics and main controlling factors of microbial carbonate reservoirs： A case study of Upper Sinian- Lower Cambrian in the northwestern margin of Tarim Basin[J]. Acta Petrolei Sinica, 2015, 36（9）： 1074-1089.
[87]	邓世彪,关平,庞磊,等. 塔里木盆地柯坪地区肖尔布拉克组优质微生物碳酸盐岩储层成因[J]. 沉积学报,2018,36（6）：1218-1232. Deng Shibiao, Guan Ping, Pang Lei, et al. Genesis of excellent Xiaoerbulak microbial carbonate reservoir in Kalpin area of Tarim Basin, NW China[J]. Acta Sedimentologica Sinica, 2018, 36（6）： 1218-1232.
[88]	Tarasewicz J P T, Woodcock N H, Dickson J A D. Carbonate dilation breccias： Examples from the damage zone to the Dent Fault, northwest England[J]. GSA Bulletin, 2005, 117（5/6）： 736-745.
[89]	Wang X L, Chou I M, Hu W X, et al. In situ observations of liquid⁃liquid phase separation in aqueous MgSO4 solutions： Geological and geochemical implications[J]. Geochimica et Cosmochimica Acta, 2013, 103： 1-10.
[90]	潘文庆,刘永福, Dickson J A D,等. 塔里木盆地下古生界碳酸盐岩热液岩溶的特征及地质模型[J]. 沉积学报,2009,27（5）：983-994. Pan Wenqing, Liu Yongfu, Dickson J A D, et al. The geological model of hydrothermal activity in outcrop and the characteristics of carbonate hydrothermal karst of Lower Paleozoic in Tarim Basin[J]. Acta Sedimentologica Sinica, 2009, 27（5）： 983-994.
[91]	Qing H R, Mountjoy E W. Origin of dissolution vugs, caverns, and breccias in the Middle Devonian Presqu’ile barrier, host of Pine Point mississippi valley-type deposits[J]. Economic Geology, 1994, 89（4）： 858-876.
[92]	Jiang L, Worden R H, Yang C B. Thermochemical sulphate reduction can improve carbonate petroleum reservoir quality[J]. Geochimica et Cosmochimica Acta, 2018, 223： 127-140.
[93]	Hutcheon I, Krouse H R, Abercrombie H J. Controls on the origin and distribution of elemental sulfur, H2S, and CO2 in Paleozoic hydrocarbon reservoirs in western Canada[M]//Vairavamurthy M A, Schoonen M A A, Eglinton T I, et al. Geochemical transformations of sedimentary sulfur. Washington, DC, American： ACS, 1995： 426-438.
[94]	Moore C H, Druckman Y. Burial Diagenesis and porosity evolution, Upper Jurassic Smackover, Arkansas and Louisiana[J]. AAPG Bulletin, 1981, 65（4）： 597-628.

[1]	杨朝屹, 夏青松, 杨鹏, 何成其, 刘芳兰, 卿山. 川西—川北地区中二叠统白云岩成岩流体特征分析及复合成岩环境重建 . 沉积学报, 2024, (): -. doi: 10.14027/j.issn.1000-0550.2024.021
[2]	王剑, 周路, 刘金, 马聪, 卞保力, 李啸, 张宝真. 湖相热液白云岩成因机理 . 沉积学报, 2024, 42(1): 130-141. doi: 10.14027/j.issn.1000-0550.2022.037
[3]	王振宇, 宁科科, 屈海洲, 胡安平, 张云峰, 陈薇, 罗新生, 张兴宇. 阿克苏地区寒武系肖尔布拉克组不同白云岩的孔隙特征、成因及演化 . 沉积学报, 2023, 41(1): 256-269. doi: 10.14027/j.issn.1000-0550.2021.157
[4]	宋亚芳, 陈代钊, 郭川, 周锡强. 塔里木盆地肖尔布拉克剖面肖尔布拉克组下段微生物碳酸盐岩沉积特征 . 沉积学报, 2020, 38(1): 55-63. doi: 10.14027/j.issn.1000-0550.2019.024
[5]	郑剑锋, 陈永权, 黄理力, 严威, 倪新锋, 李保华, 郭晓燕. 苏盖特布拉克剖面肖尔布拉克组储层建模研究及其勘探意义 . 沉积学报, 2019, 37(3): 601-609. doi: 10.14027/j.issn.1000-0550.2018.142
[6]	朱永进, 倪新锋, 刘玲利, 乔占峰, 陈永权, 郑剑锋. 裂后沉降期碳酸盐岩缓坡沉积响应及成储特征——以塔里木盆地下寒武统肖尔布拉克组为例 . 沉积学报, 2019, 37(5): 1044-1057. doi: 10.14027/j.issn.1000-0550.2019.006
[7]	袁静, 俞国鼎, 钟剑辉, 董志芳, 谢君, 单康. 构造成岩作用研究现状及展望 . 沉积学报, 2018, 36(6): 1177-1189. doi: 10.14027/j.issn.1000-0550.2018.120
[8]	尤东华, 韩俊, 胡文瑄, 陈强路, 曹自成, 席斌斌, 鲁子野. 塔里木盆地顺南501井鹰山组白云岩储层特征与成因 . 沉积学报, 2018, 36(6): 1206-1217. doi: 10.14027/j.issn.1000-0550.2018.092
[9]	邓世彪, 关平, 庞磊, 刘沛显, 金亦秋, 张艳秋. 塔里木盆地柯坪地区肖尔布拉克组优质微生物碳酸盐岩储层成因 . 沉积学报, 2018, 36(6): 1218-1232. doi: 10.14027/j.issn.1000-0550.2018.084
[10]	陈安清, 侯明才, 陈洪德, 徐胜林, 钟怡江, 刘文均. 中国海相碳酸盐岩勘探领域拓展历程及沉积学的基本驱动作用 . 沉积学报, 2017, 35(5): 1054-1062. doi: 10.14027/j.cnki.cjxb.2017.05.016
[11]	高达, 林畅松, 胡明毅, 黄理力. 利用自然伽马能谱测井识别碳酸盐岩高频层序——以塔里木盆地塔中地区T1井良里塔格组为例 . 沉积学报, 2016, 34(4): 707-715. doi: 10.14027/j.cnki.cjxb.2016.04.011
[12]	杨程宇, 李美俊, 倪智勇, 杨福林, 陈昊卫. 塔里木盆地西北缘玉尔吐斯组硅质岩成因及石油地质意义 . 沉积学报, 2016, 34(4): 653-661. doi: 10.14027/j.cnki.cjxb.2016.04.005
[13]	熊益学, 陈永权, 关宝珠, 邓力萍, 倪新锋, 熊冉. 塔里木盆地下寒武统肖尔布拉克组北部台缘带展布及其油气勘探意义 . 沉积学报, 2015, 33(2): 408-415. doi: 10.14027/j.cnki.cjxb.2015.02.020
[14]	. 碳酸盐岩中地开石的分布特征及其成因 . 沉积学报, 2012, 30(2): 310-317.
[15]	倪新锋. 塔里木盆地英买力—哈拉哈塘地区奥陶系碳酸盐岩岩溶型储层特征及成因 . 沉积学报, 2011, 29(3): 465-474.
[16]	张荣虎. 塔里木盆地白垩系巴什基奇克组陆相砂岩中碳酸盐岩碎屑特征及其地质意义 . 沉积学报, 2009, 27(3): 410-418.
[17]	陈景山. 塔里木盆地奥陶系碳酸盐岩古岩溶作用与储层分布 . 沉积学报, 2007, 25(6): 858-868.
[18]	于炳松, 陈建强, 李兴武, 林畅松. 塔里木盆地肖尔布拉克剖面下寒武统底部硅质岩微量元素和稀土元素地球化学及其沉积背景 . 沉积学报, 2004, 22(1): 59-66.
[19]	蒲仁海, 卿海若, Mark Anthony Urban. Midale油田奥陶系白云岩储层格架与油藏特征 . 沉积学报, 2004, 22(2): 234-243.
[20]	方国庆, 刘德良. 塔里木盆地西北缘中奥陶统其浪组风暴岩中遗迹化石及其环境意义 . 沉积学报, 2000, 18(1): 68-72.

施引文献

资源附件(0)

访问统计

点击查看大图

图(13) / 表 (1)

计量

文章访问数: 295
HTML全文浏览量: 54
PDF下载量: 76
被引次数: 0

全文HTML

0. 引言

白云岩富含大量的油气资源。资料表明80%以上的北美碳酸盐岩油气藏赋存于白云岩^[1]。早于志留纪的46个碳酸盐岩油气田中,90%以上是以白云岩为储集层^[2]。深层—超深层（>4 500 m）白云岩储层成因是近年来石油勘探领域的研究热点^[3]。典型实例包括：塔里木盆地寒武系^[4]、四川盆地上二叠统—下三叠统白云岩储层^[5⁃7]、波斯湾下三叠统白云岩储层^[8]和侏罗纪白云岩储层^[9]。其中,塔里木盆地寒武系盐下勘探面积达150 000 km²,占全盆地面积四分之一。目前已发现塔里木盆地30多个碳酸盐岩规模油气田,探明石油地质储量超过21×10⁸ t,探明天然气地质储量超过5 000×10⁸ m^3[10]。位于塔中隆起的ZS1井和ZS1C 井在中寒武统盐上（ZS1井6 426~6 487 m）和盐下（中深1井6 597~6 785 m,ZS1C井6 861~6 944 m）获得工业油气流^[11],塔北地区轮探1井则在寒武系吾松格尔组8 203~8 260 m白云岩储层中获日产油134 m³、天然气4.59×10⁴ m^3[12],指示塔里木盆地盐下碳酸盐岩储层勘探潜力巨大。

海相碳酸盐岩储层物性受控于沉积环境和成岩改造。深层储层由于受上覆沉积物的重压,经历强烈的压实胶结作用,原始孔隙被消耗殆尽,早期岩溶形成的孔洞也较难保存,但相关研究表明埋深大于5 000 m的白云岩储层仍发育大型溶蚀孔洞^[13⁃21]。孔隙的成因机制包括：地层水的冷却作用^[22⁃23],有机质热成熟产生的有机酸和CO₂^[24⁃26],热液溶蚀^[27⁃29]和热化学硫酸盐还原作用（TSR）^{[6,16⁃20,30⁃33]}。然而,考虑到埋藏条件下低的水岩比、饱和孔隙水、限制的孔隙水流动等特点,埋藏溶蚀对储层的改善作用存在一定的争议^[34⁃35]。对于热化学硫酸盐还原作用（TSR）而言,TSR产生的酸性流体对白云石和硬石膏进行溶解,但也会造成方解石的沉淀^[36⁃37],其对储层的作用有待进一步研究。

针对国内勘探向深层进军的趋势,寻找深层规模储层成为重点和难点,而其成因研究成为指导油气勘探的理论基础。然而,塔里木盆地肖尔布拉克组白云岩经历多期构造运动、油气充注和复杂的成岩作用,储层形成是沉积环境、成岩作用和构造作用综合作用的结果,这种复杂性导致其有利的控制因素仍不明确。目前,普遍达成的共识是肖尔布拉克组储层具有明显的相控性,丘滩体系沉积为储层发育的基础（内缓坡浅滩^[38⁃39]、中缓坡丘滩及颗粒滩^[40⁃43]）。前人已在研究层位识别出大气水^[43⁃44]、有机酸和埋藏白云石化^[45⁃47]、热液活动^[44,48⁃49]和热化学硫酸盐还原作用^[50⁃52]等多期溶蚀证据,证实了肖尔布拉克组经历多期次流体改造。但是关于各类溶蚀类型对储层的贡献,则尚未达成一致。比如,沈安江等^[41]、郑剑锋等^[42]、严威等^[43]认为在此丘滩相基础上受高频海平面波动控制的准同生期溶蚀才是储层发育的关键性因素,热液活动对储层改造规模有限,仅在一定程度上起到了补充作用。赵文智等^[46⁃47]则认为相对于古岩溶作用,塔北地区构造—热液白云石化和热液溶蚀对储层贡献最大。程丽娟等^[44]更支持准同生淡水溶蚀型和构造—热流体改造型储集体。黄擎宇等^[40]、Jiang et al.^[48]则认为相对于准同生期溶蚀,后期岩溶及热液溶蚀控制了储层的发育。Jiang et al.^[50]、Cai et al.^[52]更倾向于认为膏盐相关的热化学硫酸盐作用对储层形成贡献了主要力量。肖尔布拉克组不仅储层赋存机制和成因存在争议,而且在不同期次流体的性质和来源方面,缺乏深入探讨,各类溶蚀对储层的贡献也缺乏定量化的统计,制约深层碳酸盐岩的油气勘探。基于以上问题,对塔里木盆地肖尔布拉克组储层的形成机理做系统地研究。本文采取塔里木盆地典型露头及井下岩石样品,结合岩石学观察,并采用全岩地球化学以及原位分析实验方法,确立成岩序列,恢复成岩流体,定量估算成岩事件对储层的改造作用,并依据沉积—成岩类别划分储层。本研究不仅对油气勘探具有一定的指导意义,而且对深层优质碳酸盐岩储层成因具有理论意义。

4. 流体演化特征

根据成岩序列,结合多种地球化学测试,得出研究区如下的流体演化特征：沉积流体为海水,表现在基质δ¹³C值在1.02‰±1.21‰（n=10）,δ¹⁸O值-6.16‰±0.72‰（n=10）,落在早期海源灰岩白云石化范围内（寒武纪同时期海水δ¹³C介于2.5‰~0.5‰,δ¹⁸O介于9‰~-4‰^[65]）,反映海源流体成因。基质粉细晶白云石具有的与现代海水特征相近的LREE亏损、HREE富集特征,记录了海水信号。基质粉细晶白云石的总REE低,轻微Ce负异常（Ce_SN/Ce_SN^*=0.71±0.25）,高Fe（502.5±160.3 μg/g）,低Mn（168.39±52.12 μg/g）含量记录了弱氧化的海水性质^[65]。

随着沉积物逐渐埋藏至半脱离地表水体范围,进入半封闭的流体环境,流体逐渐演化为接近海水的孔隙水,反映在碳氧同位素值（δ¹³C集中在0.78‰±0.24‰、δ¹⁸O值-6.4‰±0.57‰）与基质相近的细晶白云石胶结物,且未观察到流体包裹体,阴极发光为暗红色,说明孔隙水仍然继承早成岩海水特点,为准同生期流体产物。此外,与基质相似的稀土配分特征进一步支持其继承了以古海水为主的孔隙水信号。

随着埋藏加深进入浅埋藏成岩流体环境,沉积物脱离海水而逐渐演化为还原性孔隙水环境,与基质有显著差异。反映在δ¹⁸O值（-8.54‰±0.1‰,n=5）稍微负偏的细晶白云石胶结物,说明受到埋藏重结晶和地温升高影响。具有高Fe（1 468.27±1 630.13 μg/g,n=18）、高Mn（279.74±134.06 μg/g,n=18）含量和MREE富集特征。现今形成于铁化环境下的碳酸盐胶结物常具有典型的MREE富集特征^[66]。此外,现今孔隙水研究表明锰化带和铁化带分别具有最高的Mn和Fe含量^[67⁃68]。这是因为在这两个还原带中,锰（氧）化物和铁（氧）化物的还原程度最大。因此主微量和稀土特征共同指示了在还原条件下孔隙水中铁锰氧化物被还原。

中深埋藏阶段,孔隙水具有高温高盐度特征。中粗晶白云石胶结物流体包裹体具有高的均一温度（94.3 ℃~121.2 ℃）,与进一步负偏δ¹⁸O值（-11.35‰±1.41‰）一致,均指示了较高的沉淀温度。铁锰氧化物进一步被还原,白云石具有更高的锰含量和MREE富集模式。

埋藏期热液流体充注,具有高温高盐度特征,热液矿物鞍形白云石、石英流体包裹体均一温度峰值分别为140 ℃~160 ℃、130 ℃~150 ℃。鞍形白云石被限定在早二叠世热液白云石化生成^[69],流体包裹体温度高于肖尔布拉克组在早二叠世古地温100 ℃^[70⁃72]。且鞍形白云石氧同位素进一步负偏,分布在-10.44‰±0.6‰,为典型高温热液特征,这支持上述成岩矿物代表热液沉淀^[28]。Eu正异常,被认为是热液流体和塔里木盆地富含Eu的前寒武纪斜长岩基底水岩相互作用的结果^[73],且酸性和高温环境下均有利于流体Eu以正二价还原态存在,导致Eu正异常^[74⁃75],因此推测成岩流体为还原酸性热液^[76]。鞍形白云石MREE富集可能指示其从酸性壳源流体中沉淀^[75],结合高Mn含量（623.15±219.58 μg/g,n=4）,较高Fe（1 165.91±285.39 μg/g,n=4）,无Ce负异常,支持铁锰氧化物被还原^[66,77]。

方解石稀土配分曲线与基质白云石相差很大,且稀土总量高达55.06 μg/g,远高于其他充填物,结合盐度特征,共同指示了最高盐度流体。此外,最低的Fe（109.49±92.72 μg/g,n=9）、Mn（7.68±8.20 μg/g,n=9）含量可能说明铁参与了TSR反应并生成黄铁矿^[78]（图3j）,该过程会释放H⁺,产生酸性流体。虽然TSR作用会生成低盐度的水^[79],但是方解石仍具有高盐度特征,被认为是产生的低盐度水加入下寒武统地层水,而非方解石^[48]。LREE富集可能是流体和富含LREE的火成岩基底反应的结果,轻微Eu正异常（1.43±0.1）,被认为是高温还原流体^[74,80]。结合塔里木盆地火山岩浆活动在二叠纪很活跃,且广泛发育酸性碱性岩浆喷发和辉绿岩侵入体^[72,81],认为酸性还原热流体可能来自二叠纪岩浆热流体。

综上,流体依次演化为：沉积弱氧化海水、接近海水的孔隙水、浅埋藏富铁孔隙水、中深埋藏高温高盐度孔隙水、埋藏期高盐度还原酸性壳源热流体、晚期最高盐度高温TSR流体（表1）。

表 1 各期次流体性质、产物与关系

沉积/成岩流体	均一温度与盐度	稀土配分模式	微量元素含量	性质	产物
沉积海水	40 ℃,3.5 wt%^[48]	LREE亏损 HREE富集	中—高Fe 低Mn	弱氧化性	粉细晶白云石基质
接近海水的孔隙水	小于50 ℃^[48]	LREE亏损 HREE富集	中—高Fe 低Mn	低盐度	氧同位素接近基质的细晶白云石胶结物
浅埋藏条件孔隙水	70 ℃~100 ℃^[44],6~14wt.%^[48]	MREE富集	极高Fe 高Mn	稍高温,还原性	氧同位素偏负的细晶白云石胶结物
中深埋藏条件孔隙水	94 ℃~121 ℃,10~29 wt.%	MREE富集	高Fe 高Mn	高温高盐度	中粗晶白云石胶结物
壳源热流体	136 ℃~182 ℃,13~25 wt.%	MREE富集	极高Fe 极高Mn	高温高盐度还原酸性	鞍形白云石,石英
TSR相关流体	128 ℃~152 ℃,18~23 wt.%	LREE富集	低Fe 低Mn	高温高盐度酸性	方解石

6. 结论

（1）塔里木盆地下寒武统肖尔布拉克组主要发育四类岩石类型,分别为颗粒云岩、微生物岩（凝块石、泡沫棉层白云石、核形石、叠层石、黏结砂屑云岩、藻格架云岩）、晶粒云岩（泥粉晶和粉细晶云岩）和泥晶灰岩。其中颗粒云岩和凝块石云岩物性最好。

（2）原位微量稀土、碳氧同位素以及流体包裹体温度数据指示的流体演化过程依次为沉积弱氧化海水、准同生期接近海水的孔隙水、浅埋藏富铁孔隙水、中深埋藏高温高盐度孔隙水、埋藏期较高盐度还原酸性壳源热流体、晚期极高盐度高温TSR热流体。

（3）划分出肖尔布拉克组三类优质储层类型,分别为微生物礁滩相大气水/热液改造凝块石白云岩、浅滩相热液/TSR溶蚀颗粒白云岩以及TSR有关的膏盐白云岩储层,为今后的塔里木盆地盐下肖尔布拉克碳酸盐岩油气勘探提供了有利的证据。

参考文献 (94)

姓名
邮箱
手机号码
标题
留言内容
验证码

留言板

塔里木盆地下寒武统肖尔布拉克组储层成因

doi: 10.14027/j.issn.1000-0550.2021.116

作者简介:
魏天媛,女,1996年出生,博士研究生,储层沉积学,E-mail: weity@mail.iggcas.ac.cn

通讯作者:
蔡春芳,男,研究员,E-mail: cai_cf@mail.iggcas.ac.cn

计量

Origin of Reservoirs in the Lower Cambrian Xiaoerbulak Formation, Tarim Basin

计量

目录

塔里木盆地下寒武统肖尔布拉克组储层成因

doi: 10.14027/j.issn.1000-0550.2021.116

作者简介:
魏天媛,女,1996年出生,博士研究生,储层沉积学,E-mail: weity@mail.iggcas.ac.cn

通讯作者: 蔡春芳,男,研究员,E-mail: cai_cf@mail.iggcas.ac.cn

English Abstract

Origin of Reservoirs in the Lower Cambrian Xiaoerbulak Formation, Tarim Basin

全文HTML

2.1. 成岩矿物

2.2. 岩石类型

2.3. 成岩序列

3.1. 碳氧同位素

3.2. 流体包裹体均一温度

3.3. 主微量及稀土元素测试

5.1. 微生物丘滩相大气水/热液改造凝块石白云岩

5.2. 浅滩相热液/TSR溶蚀颗粒白云岩

5.3. 与TSR有关膏盐白云岩储层

目录

友情链接

期刊在线

联系我们

留言板

塔里木盆地下寒武统肖尔布拉克组储层成因

doi: 10.14027/j.issn.1000-0550.2021.116

作者简介: 魏天媛,女,1996年出生,博士研究生,储层沉积学,E-mail: weity@mail.iggcas.ac.cn

通讯作者: 蔡春芳,男,研究员,E-mail: cai_cf@mail.iggcas.ac.cn

计量

出版历程

Origin of Reservoirs in the Lower Cambrian Xiaoerbulak Formation, Tarim Basin

计量

出版历程

目录

塔里木盆地下寒武统肖尔布拉克组储层成因

doi: 10.14027/j.issn.1000-0550.2021.116

作者简介: 魏天媛,女,1996年出生,博士研究生,储层沉积学,E-mail: weity@mail.iggcas.ac.cn

通讯作者: 蔡春芳,男,研究员,E-mail: cai_cf@mail.iggcas.ac.cn

English Abstract

Origin of Reservoirs in the Lower Cambrian Xiaoerbulak Formation, Tarim Basin

全文HTML

2.1. 成岩矿物

2.2. 岩石类型

2.3. 成岩序列

3.1. 碳氧同位素

3.2. 流体包裹体均一温度

3.3. 主微量及稀土元素测试

5.1. 微生物丘滩相大气水/热液改造凝块石白云岩

5.2. 浅滩相热液/TSR溶蚀颗粒白云岩

5.3. 与TSR有关膏盐白云岩储层

目录

友情链接

期刊在线

联系我们

作者简介:
魏天媛,女,1996年出生,博士研究生,储层沉积学,E-mail: weity@mail.iggcas.ac.cn

通讯作者:
蔡春芳,男,研究员,E-mail: cai_cf@mail.iggcas.ac.cn

作者简介:
魏天媛,女,1996年出生,博士研究生,储层沉积学,E-mail: weity@mail.iggcas.ac.cn