塔北、塔中地区寒武系—奥陶系白云岩多成因模式

王丹

doi:10.14027/j.issn.1000-0550.2023.128

塔北、塔中地区寒武系—奥陶系白云岩多成因模式

doi: 10.14027/j.issn.1000-0550.2023.128

王丹

1.
中国海洋石油国际有限公司,北京 100010

基金项目:

国家自然科学基金项目 U1663209

详细信息

作者简介:
王丹,男,1978年出生,博士,高级工程师,碳酸盐岩储层地质学,E-mail: 279388044@qq.com

http://www.cjxb.ac.cn/cn/article/doi/10.14027/j.issn.1000⁃0550.2023.128.
http://www.cjxb.ac.cn/cn/article/doi/10.14027/j.issn.1000⁃0550.2023.128.
中图分类号: P534.4

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Geochemical Characteristics and Origins of the Cambrian-Ordovician Dolomites in Northern and Central Tarim Basin

WANG Dan

1.
CNOOC International Limited, Beijing 100010, China

Funds:

National Natural Science Foundation of China U1663209

摘要

摘要: 目的塔里木盆地下古生界厚层白云岩具有良好的油气勘探前景,但目前其成因尚未达成统一的认识。通过对这些白云岩的成因研究,可为塔里木盆地下古生界厚层白云岩的油气勘探提供一定的理论支撑。方法基于国际学术界通用的白云石分类方案,对塔北、塔中地区寒武系—奥陶系白云岩开展了详细的岩相学和地球化学（微量—稀土元素、δ¹³C和δ¹⁸O及⁸⁷Sr/⁸⁶Sr比值）研究。 结果和结论 基质白云石可识别出6种类型：（1）泥粉晶白云石（Md1）；（2）残余拟晶白云石（Md2）；（3）粉—细晶、直面、自形—半自形、漂浮状白云石（Md3）；（4）细晶、直面、自形—半自形白云石（Md4）；（5）细—粗晶、他形、曲面白云石（Md5）；（6）粗晶、曲面、鞍形白云石（Md6）。Md1和Md2的成岩流体为不同程度蒸发浓缩的同期海水,形成于相对局限沉积环境的同生—准同生白云石化作用；Md3和Md4的成岩流体为地层中残留的海源孔隙水,形成于浅—中埋藏白云石化作用；Md5的成岩流体为海源流体,形成于深埋藏白云石化作用或早期白云石的重结晶作用；Md6的形成流体为与宿主白云岩发生强烈水岩反应的深部热液,主要形成于深部热液及围岩之间相互调节、再平衡过程中的“热液调节白云石化作用”对宿主白云岩的改造作用。
- 岩相学 /
- 地球化学特征 /
- 白云石化作用 /
- 下古生界 /
- 塔里木盆地
Abstract: Objective The genesis of dolomites is still controversy, and dolomite reservoirs play an important role in carbonate oil and gas exploration, whose reservoir properties （porosity and permeability） are largely influenced by the genesis types and texture characteristics of dolomites. In recent years, many large oil and gas fields have also been found in domestic dolomite reservoirs, such as Tarim Basin, Sulige gas field in Ordos Basin, Puguang and Yuanba gas field in Sichuan Basin and Anyue large or super large gas field. Therefore, systematic researches on the texture types and genetic mechanisms of dolomites yield profound theoretical significance, and also will promote greater advance in carbonate oil and gas exploration in China. The Tarim Basin shares large volume of oil and gas reserves, the exploration target horizons within which has gradually shifted from medium shallow- to medium-buried layers to ultra-deep layers. Especially, industrial oil and gas flows were encountered in the deeply-buried dolomites of the Lower Paleozoic in the Tarim Basin, making the formation, evolution and reservoir characteristics of deep dolomite reservoirs in this basin become the focus of scholars' research. However, the formation mechanism of the Cambrian-Ordovician dolomites in the Tarim Basin has not yet reached a consensus due to deep burial depth, complex genesis and difficult exploration of these dolomites. This study increases the understanding of their origin and provides theoretical support for oil and gas exploration in the region. Methods Detailed petrographic and geochemical （trace-rare earth elements, stable carbon and oxygen isotopes and ⁸⁷Sr/⁸⁶Sr ratios） studies of these dolomites were conducted on the Cambrian-Ordovician dolomites of northern and central Tarim Basin based on the international classification scheme of dolomite. Results and Conclusions According to the occurrence of dolomites, the Cambrian-Ordovician dolomites were divided into matrix and cement dolomites. Based on grain sizes, contact relationship between crystal planes （plane or curved surface）, and crystal shape （euhedral, subhedral or anhedral）, six types of dolomite structures were further identified for the matrix dolomite：（1） very fine to fine crystalline dolomite （Md1）；（2） relict mimetic dolomite （Md2）；（3） very fine to fine crystalline, planar-e（s） floating dolomite （Md3）；（4） fine crystalline, planar-e（s） dolomite （Md4）；（5） fine to coarse crystalline, nonplanar-a dolomite （Md5）； and （6） coarse crystalline, nonplanar saddle dolomite （Md6）. The distribution patterns of rare earth elements （REE）（slight enrichment or depletion of light REE, weak Eu negative or positive anomalies, and weak Ce negative or positive anomalies）, δ¹³C values （-2.83‰ -1.72‰； average -1.64‰） and ⁸⁷Sr/⁸⁶Sr values （0.708 7~0.711 6； average 0.709 5） in the six matrices are similar to Cambrian-Ordovician micritic limestone and contemporaneous seawater. The diagenetic fluids of Md1 and Md2 are coeval seawater with varying degrees of evaporation and concentration, and were formed by （pene）contemporaneous dolomitization （including sabkha and reflux infiltration dolomitization） in relatively restricted depositional environments. The parent fluids of Md3 and Md4 are residual seawater, created by shallow-to medium-burial dolomitization. The diagenetic fluids of Md5 are variants of contemporaneous water, formed by deep-burial dolomitization or recrystallization of earlier dolomites. Deep hydrothermal fluids were responsible for the Md6 formation as a result of strong water-rock interactions with the host dolomites, influenced by mutual regulation and re-equilibration between the deep hydrothermal fluids and surrounding rocks.
- lithofacies /
- geochemical characteristics /
- dolomitization /
- Lower Paleozoic /
- Tarim Basin
注释:
1) 脚注:
1) http://www.cjxb.ac.cn/cn/article/doi/10.14027/j.issn.1000⁃0550.2023.128.
2) 脚注:
2) http://www.cjxb.ac.cn/cn/article/doi/10.14027/j.issn.1000⁃0550.2023.128.

HTML全文

图 1 塔里木盆地构造格局和主要构造单元^[19⁃20]

Figure 1. Structural configuration and major structural units of the Tarim Basin^[19⁃20]

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图 2 塔里木盆地南北向地层切面（据文献[18]修改）

Figure 2. North⁃south stratigraphic profile of the Tarim Basin (modified from reference [18])

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图 3 塔里木盆地寒武系—下奥陶系综合地层图（据文献[18,21⁃22]修改）

Figure 3. Integrated stratigraphy of Cambrian to Lower Ordovician successions in the Tarim Basin (modified from references [18,21⁃22])

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图 4 泥—粉晶白云石（Md1）岩石学特征

(a) interbedded very fine crystalline dolomites and anhydrite, well HT1, 6 430.80 m; (b) fibrous anhydrite with pebbles of very fine crystalline dolomite (yellow arrows), plane⁃polarized light (PPL), well HT1, 6 430.82 m, Cambrian (Є); (c) isometric granular and/or elliptical gypsum crystals containing very fine intracrystalline dolomites, PPL, well HT1, 6 430.82 m, Є; (d) isometric granular and/or elliptical gypsum crystals with intracrystalline prismatic anhydrite crystals (yellow arrows), cross⁃polarized light(XPL), well HT1, 6 430.82 m, Є; (e) meter⁃scale, shallowing⁃upward cyclic deposition of lower dolo⁃thrombolite and upper dolo⁃laminites with dissolution porosity, Penglaiba section, Lower Qiulitage subgroup of the Upper Cambrian; (f) layers of very fine crystalline dolomite and mud⁃rich material, PPL, TS1, 7 874.30 m, Є

Figure 4. Petrology of very fine to fine crystalline dolomite (Md1)

Fig.4

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图 5 残余拟晶基质白云石（Md2）岩石学特征

(a) algal aggregate replacement by very fine dolomite crystals, with pores cemented by dolomites, PPL, well TS1, 7 461.30 m, Є; (b) dark⁃gray algal aggregates with intragrain pores cemented by dolomites, PPL, Penglaiba section, Є; (c) dark⁃red luminescent algal aggregates and bright⁃red luminescent intragrain dolomite cements, cathodoluminescence (CL), Penglaiba section, Є

Figure 5. Petrology of relict mimetic dolomite (Md2)

Fig.5

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图 6 细晶、直面、自形—半自形、漂浮状基质白云石（Md3）和中晶、直面、自形—半自形基质白云石（Md4）岩石学特征

(a) partially dolomitized limestone ^[26], with mottled dolomites along stylolites, northern Tarim Basin, Ordovician (scale bar = 3 cm); (b) planar euhedral to subhedral dolomite crystals (Md2) clustered along the stylolite, with some in the micrite matrix ^[26], northern Tarim Basin, Ordovician; (c) Md2 in siliceous cement matrix, with parts showing gulf outlines, XPL, well DG1, 6 261.88 m, Є; (d) Md2 in siliceous cements, scanning electron microscope (SEM), well T1, 3 179.89 m, Є; (e) energy dispersive scanning (EDS) of siliceous cements, orange spot in (d); (f) EDS of matrix dolomite, yellow spots in (d); (g) fine crystalline, planar⁃e(s) dolomites (Md4), PPL, well S88, 6 409.10 m, Penglaiba Formation; (h) fine crystalline dolomite with petal nuclease and slightly curved surfaces^[26], PPL, well GL1, 6 456.10 m, Ordovician

Figure 6. Petrology of very fine to fine crystalline, planar⁃e(s) floating dolomite (Md3) and fine crystalline, planar⁃e(s) dolomite (Md4)

Fig.6

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图 7 细—粗晶、曲面、他形基质白云石（Md5）和粗晶、曲面、鞍形基质白云石（Md6）岩石学特征

(a) fine crystalline, nonplanar anhedral matrix dolomites (Md5) in the lower right, and coarse crystalline saddle dolomite cements (Sd⁃c) in upper⁃left⁃hand sections of the photomicrograph, PPL, well S15, 5 389.10 m, Є; (b) Md5 with mottled dull red luminescence, and Sd⁃c with dull red to nonluminescence, CL, well S15, 5 389.10 m, Є; (c) coarse crystalline, nonplanar saddle matrix dolomite, PPL, well Z4, 5 811.90 m, Є; (d) coarse crystalline, nonplanar saddle matrix dolomite ^[26], PPL, well T1, 3 172.93 m, Є; (e) extremely coarse saddle dolomite crystals with intercrystalline porosity and abundant microfaults, PPL, well Z4, 5 816.00 m, Є; (f) extremely coarse crystalline saddle dolomites showing sweeping extinction, XPL, well Z4, 5 816.00 m, Є

Figure 7. Petrology of fine to coarse crystalline, nonplanar⁃a dolomite (Md5) and coarse crystalline, nonplanar saddle dolomite (Md6)

Fig.7

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图 8 塔北、塔中地区寒武系—奥陶系碳酸盐岩中共生矿物成岩序列

Figure 8. Paragenetic sequence of coexisting minerals of Cambrian⁃Lower Ordovician carbonates in northern and central Tarim Basin

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图 9 塔北、塔中地区各类型白云石及泥晶灰岩稀土分配模式图

(a) micritic and dolomitic limestones, data from references [32⁃33]; (b) very fine to fine crystalline dolomite (Md1); (c) relict mimetic dolomite (Md2); (d) fine crystalline, planar⁃e(s) dolomite (Md4); (e) fine to coarse crystalline, nonplanar⁃a dolomite (Md5); (f) coarse crystalline, nonplanar saddle dolomite (Md6); (g) silty to fine crystalline dolomite, data from reference [34]; (h) medium to coarse crystalline dolomite, data from reference [34]

Figure 9. REE patterns for different types of dolomites and micritic limestone in northern and central Tarim Basin

Fig.9

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图 10 塔北地区（a）和塔中地区（b）寒武系—奥陶系泥晶灰岩与白云岩δ¹³C⁃δ¹⁸O交会图

estimated δ¹³C and δ¹⁸O data for Cambrian to Lower Ordovician seawater from references [35⁃37]

Figure 10. Cross⁃plot of δ¹³C and δ¹⁸O values for limestone and different types of matrix dolomites in (a) northern Tarim Basin; and (b) central Tarim Basin

Fig.10

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图 11 塔北地区（a）和塔中地区（b）寒武—奥陶系泥晶灰岩与白云岩Sr⁸⁷/Sr⁸⁶⁃δ¹⁸O交汇图

estimated ⁸⁷Sr/⁸⁶Sr and δ¹⁸O data for Cambrian to Lower Ordovician seawater from references [35⁃37]

Figure 11. Cross⁃plot of ⁸⁷Sr/⁸⁶Sr and δ¹⁸O data for limestone and different types of matrix dolomites in (a) northern Tarim Basin; and (b) central Tarim Basin

Fig.11

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图 12 塔北、塔中地区寒武系—奥陶系白云岩元素数据有效性判别图

(a) Zr vs. ∑REE; (b) Sc vs. ∑REE; (c) Dy_N/Sm_N ratios vs. δCe; (d) Dy_N/Sm_N ratios vs. ∑REE

Figure 12. Evaluatorys of elemental geochemical data of the Cambrian⁃Ordovician dolomites in northern and central Tarim Basin

Fig.12

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图 13 塔北、塔中地区同生—准同生白云石化作用模式图

Figure 13. (Pene)contemporaneous dolomitization model of northern and central Tarim Basin

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图 14 塔北、塔中地区寒武系—奥陶系碳酸盐岩地层埋藏史

(a) S17 and S15^[61⁃62]; (b) outcrops in the Keping^[63]; (c) TZ1 and ZS5^[64]

Figure 14. Burial history of the Cambrian⁃Lower Ordovician carbonate successions in northern and central Tarim Basin

Fig.14

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图 15 塔北、塔中地区寒武系—奥陶系碳酸盐岩构造—热液调节白云石化作用模式图（地层厚度不按比例）

Figure 15. Structural⁃hydrothermal cannibalized dolomitization model of the Cambrian⁃Ordovician carbonates in northern and central Tarim Basin (the stratal thickness is not scaled)

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0. 引言

白云岩的成因仍然存在很大争议^[1⁃3],同时白云岩作为储层在碳酸盐岩油气勘探中具有非常重要的地位,其储集性能很大程度上受白云岩成因类型和结构特征影响^[4]。近年来,国内白云岩储层中发现了多个大型（油）气田,如塔里木盆地、鄂尔多斯盆地苏里格气田、四川盆地普光—元坝及安岳大型或超大型气田等^[5⁃6]。因此,对白云岩的结构类型及成因机理进行深入研究,不仅具有较大的理论意义,而且也将促进我国碳酸盐岩油气勘探取得更大的进展。

塔里木盆地作为重要的含油气盆地,勘探目标层位逐渐由中浅层转移到深层—超深层^[5,7]。特别是下古生界深层白云岩中不断钻取工业油气流,使得该地区深层白云岩储层的形成、演化及储集特征等一系列问题成为研究的热点^[8⁃16]。但由于这些白云岩的埋藏深、成因复杂、勘探难度大等特点^[17⁃18],导致目前塔里木盆地寒武系—奥陶系白云岩的形成机制尚未达成统一的认识。因此,深入研究塔北、塔中及周边区域寒武系—奥陶系白云岩的结构类型和形成机理,探讨其成因联系,以期对塔里木盆地下古生界白云岩的油气勘探突破提供一定的理论支持。

2. 实验材料与实验方法

白云岩样品取自塔北地区（钻井：DG2、DG3、DG7、S13、S15和S888）和塔中地区（钻井：Z1、Z4、Z13、T1、GL1和HT1）。在对研究区内白云石的精细分类基础之上,为了保证地球化学分析的准确性,利用微钻（最小直径1 mm）对各种类型白云石和灰岩进行精细取样。选定19个样品开展微量—稀土元素测试,65个样品开展碳、氧同位素测试,31个样品进行锶同位素比值测试。

微量—稀土元素测试在中国科学院地质与地球物理研究所微量元素地球化学分析实验室完成,称取40 mg粉末样品,采用HNO₃+HF进行溶解,分析仪器为Finnigan MAT 公司 ELEMENT 型高分辨率等离子质谱仪。选用后太古宙澳大利亚页岩（Post Archean Australian Shale,PAAS）^[23]对测试结果进行了标准化。δCe和δEu的计算公式分别为：δCe=Ce_N/ (La_N×Pr_N)^1/2,δEu=Eu_N/（Sm_N×Gd_N）^1/2,式中的下角标N代表标准化值。碳、氧同位素测试在中国科学院地质与地球物理研究所稳定同位素实验室完成,采用磷酸法制备CO₂,分析仪器为MAT253质谱仪,测试结果采用VPDB标准,测试精度高于0.1‰。锶同位素测试在中国科学院地质与地球物理研究所固体同位素实验室完成,测试仪器为MAT262型质谱仪,测试结果误差（2σ）低于0.000 015。

7. 结论

（1）基于国际学术界通用的白云石分类方法,将塔北、塔中地区寒武系—奥陶系基质白云岩划分为6种类型：①泥—粉晶基质白云石（Md1）；②残余拟晶基质白云石（Md2）；③粉—细晶、直面、自形—半自形、漂浮状基质白云石（Md3）；④细晶、直面、自形—半自形基质白云石（Md4）；⑤细—粗晶、曲面、他形基质白云石（Md5）；⑥粗晶、曲面、鞍形基质白云石（Md6）。

（2） Md1~Md5的稀土配分模式、δ¹³C和⁸⁷Sr/⁸⁶Sr与寒武系—奥陶系泥微晶灰岩及同时期海水具有类似的特征,表明它们的成岩流体均为海源流体。与断裂系统密切相关的关系和与其他类型基质白云石类似的地球化学特征,指示Md6可能形成于与宿主白云岩发生强烈水岩反应的深部热液。

（3）研究区寒武系—奥陶系白云岩主要形成于同生—准同生白云石化作用（包括萨布哈白云石化作用和回流渗透白云石化模式）、埋藏白云石化作用（包括浅—中埋藏白云石化作用和深埋藏白云石化作用）、构造—热液调节白云石化作用。

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塔北、塔中地区寒武系—奥陶系白云岩多成因模式

doi: 10.14027/j.issn.1000-0550.2023.128

作者简介:
王丹,男,1978年出生,博士,高级工程师,碳酸盐岩储层地质学,E-mail: 279388044@qq.com

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Geochemical Characteristics and Origins of the Cambrian-Ordovician Dolomites in Northern and Central Tarim Basin

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塔北、塔中地区寒武系—奥陶系白云岩多成因模式

doi: 10.14027/j.issn.1000-0550.2023.128

1. 中国海洋石油国际有限公司,北京 100010

作者简介:
王丹,男,1978年出生,博士,高级工程师,碳酸盐岩储层地质学,E-mail: 279388044@qq.com

English Abstract

Geochemical Characteristics and Origins of the Cambrian-Ordovician Dolomites in Northern and Central Tarim Basin

1. CNOOC International Limited, Beijing 100010, China

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3.1. 泥—粉晶白云石（Md1）

3.2. 残余拟晶基质白云石（Md2）

3.3. 粉—细晶、直面、自形—半自形、漂浮状基质白云石（Md3）

3.4. 细—中晶、直面、自形—半自形基质白云石（Md4）

3.5. 细—粗晶、曲面、他形基质白云石（Md5）

3.6. 粗晶、曲面、鞍形基质白云石（Md6）

5.1. 微量—稀土元素

5.2. 碳氧同位素（δ¹³C和δ¹⁸O）

5.3. 锶同位素比值（⁸⁷Sr/⁸⁶Sr）

6.1. 数据有效性评价

6.2. 白云岩的形成机制

6.2.1. Md1的形成机制

6.2.2. Md2的形成机制

6.2.3. Md3和Md4的形成机制

6.2.4. Md5的形成机制

6.2.5. Md6的形成机制

目录

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塔北、塔中地区寒武系—奥陶系白云岩多成因模式

doi: 10.14027/j.issn.1000-0550.2023.128

作者简介: 王丹,男,1978年出生,博士,高级工程师,碳酸盐岩储层地质学,E-mail: 279388044@qq.com

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出版历程

Geochemical Characteristics and Origins of the Cambrian-Ordovician Dolomites in Northern and Central Tarim Basin

计量

出版历程

目录

塔北、塔中地区寒武系—奥陶系白云岩多成因模式

doi: 10.14027/j.issn.1000-0550.2023.128

1. 中国海洋石油国际有限公司,北京 100010

作者简介: 王丹,男,1978年出生,博士,高级工程师,碳酸盐岩储层地质学,E-mail: 279388044@qq.com

English Abstract

Geochemical Characteristics and Origins of the Cambrian-Ordovician Dolomites in Northern and Central Tarim Basin

1. CNOOC International Limited, Beijing 100010, China

全文HTML

3.1. 泥—粉晶白云石（Md1）

3.2. 残余拟晶基质白云石（Md2）

3.3. 粉—细晶、直面、自形—半自形、漂浮状基质白云石（Md3）

3.4. 细—中晶、直面、自形—半自形基质白云石（Md4）

3.5. 细—粗晶、曲面、他形基质白云石（Md5）

3.6. 粗晶、曲面、鞍形基质白云石（Md6）

5.1. 微量—稀土元素

5.2. 碳氧同位素（δ13C和δ18O）

5.3. 锶同位素比值（87Sr/86Sr）

6.1. 数据有效性评价

6.2. 白云岩的形成机制

6.2.1. Md1的形成机制

6.2.2. Md2的形成机制

6.2.3. Md3和Md4的形成机制

6.2.4. Md5的形成机制

6.2.5. Md6的形成机制

目录

友情链接

期刊在线

联系我们

作者简介:
王丹,男,1978年出生,博士,高级工程师,碳酸盐岩储层地质学,E-mail: 279388044@qq.com

作者简介:
王丹,男,1978年出生,博士,高级工程师,碳酸盐岩储层地质学,E-mail: 279388044@qq.com

5.2. 碳氧同位素（δ¹³C和δ¹⁸O）

5.3. 锶同位素比值（⁸⁷Sr/⁸⁶Sr）