准噶尔盆地玛湖凹陷风城组黄铁矿硫同位素地球化学特征及其指示意义

江程舟; 王贵文; 王松; 张益粼; 黄玉越

doi:10.11781/sysydz2025051106

准噶尔盆地玛湖凹陷风城组黄铁矿硫同位素地球化学特征及其指示意义

doi: 10.11781/sysydz2025051106

江程舟^{1, 2, 3,},
王贵文^{2, 3, ,},
王松^{2, 3},
张益粼⁴,
黄玉越^{2, 3}

1.
中国石油勘探开发研究院，北京 100083
2.
中国石油大学(北京) 地球科学学院，北京 102249
3.
中国石油大学(北京) 油气资源与探测国家重点实验室，北京 102249
4.
中国石化勘探分公司物探研究院，成都 610041

基金项目:

国家自然科学基金 41872133

中国石油—中国石油大学(北京)战略合作协议 ZLZX2020-01-05-03

详细信息

作者简介:
江程舟(1997—)，男，博士，从事硫同位素地球化学研究。E-mail: jcz_cup@163.com

通讯作者:
王贵文(1966—)，男，博士，教授，从事页岩油储层地质学研究。E-mail: wanggw@cup.edu.cn

中图分类号: TE122.2
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- 被引次数: 0
出版历程
- 收稿日期: 2024-12-10
- 修回日期: 2025-08-22
- 刊出日期: 2025-09-28

Geochemical characteristics and implications of pyrite sulfur isotope in Fengcheng Formation of Mahu Sag, Junggar Basin

JIANG Chengzhou^{1, 2, 3
,},
WANG Guiwen^{2, 3
, ,},
WANG Song^{2, 3},
ZHANG Yilin⁴,
HUANG Yuyue^{2, 3}

1.
Research Institute of Petroleum Exploration and Development, PetroChina, Beijing 100083, China
2.
College of Geosciences, China University of Petroleum (Beijing), Beijing 102249, China
3.
State Key Laboratory of Petroleum Resources and Prospecting, China University of Petroleum (Beijing), Beijing 102249, China
4.
Geophysical Research Institute, SINOPEC Exploration Company, Chengdu, Sichuan 610041, China

摘要

摘要: 准噶尔盆地玛湖凹陷风城组跨越石炭系—二叠系界线，是一套典型的海陆过渡环境下形成的页岩油储层。扫描电镜(SEM)观察和铬还原法的对比研究表明，该区不但总硫含量明显高于鄂尔多斯盆地三叠系延长组长7段、松辽盆地白垩系嫩江组及柴达木盆地古近系下干柴沟组泥岩，且黄铁矿类型多样(包括自形黄铁矿和草莓状黄铁矿)。目前针对该层段黄铁矿成因的相关研究仍处于起步阶段，结合主量元素分析及前人研究成果认为，剧烈的火山活动和古亚洲洋水体中的硫酸盐是风城组黄铁矿的主要硫来源，含硫热液为次要硫来源，而河流输入的风化物质影响较小。同时，基于黄铁矿硫同位素组成(δ³⁴S)特征，风城组可划分为2个阶段：阶段1是风一段顶部到风二段中部，受海洋与湖盆连通性控制的硫酸盐含量变化会导致δ³⁴S值出现明显的正偏和负偏；阶段2是风二段上部到风三段，δ³⁴S值的波动主要受沉积速率的影响。此外，剧烈的火山作用也可引起δ³⁴S值的负偏。对风城组黄铁矿硫同位素分馏的影响因素研究，有利于进一步解析硫循环以及重建成岩及沉积模式。最后，综合TOC含量与硫同位素揭示的水体环境变化指出，湖盆开放性的增加、强烈蒸发作用导致的高盐度水体分层以及剧烈的火山活动是风城组有机质富集和保存的关键因素。
- 黄铁矿 /
- 硫来源 /
- 硫同位素 /
- 有机质富集 /
- 风城组 /
- 玛湖凹陷 /
- 准噶尔盆地
Abstract: The Fengcheng Formation in the Mahu Sag of the Junggar Basin spans the Carboniferous and Permian boundary and represents a typical shale oil reservoir deposited in a marine to continental transitional environment. Comparative studies using scanning electron microscopy (SEM) and the chromium reduction method have revealed that the total sulfur content in this formation is significantly higher than that of the mudstones in the seventh member of the Triassic Yanchang Formation in the Ordos Basin, the Cretaceous Nenjiang Formation in the Songliao Basin, and the Paleogene Lower Ganchaigou Formation in the Qaidam Basin. In addition, pyrite of diverse morphologies develops, including euhedral and framboidal pyrite. However, relevant research on pyrite genesis in this formation is still at an early stage. Based on major element analysis and previous studies, the study concluded that intense volcanic activities and sulfates from the Paleo-Asian Ocean were the main sulfur sources of pyrite in the Fengcheng Formation, and the sulfur-bearing hydrothermal fluids were the secondary source. Riverine input of weathered materials had a relatively minor influence. Meanwhile, based on the characteristics of pyrite sulfur isotope composition (δ³⁴S), the evolution of the Fengcheng Formation was divided into two stages: Stage 1 extended from the top of the first member (C₂f₁) to the middle of the second member (C₂-P₁f₂) of the Fengcheng Formation. The variations in sulfate concentrations controlled by the connectivity between the ocean and the lake basin led to significant positive and negative deviations in δ³⁴S values. Stage 2 extended from the upper part of C₂-P₁f₂ to the third member (P₁f₃). The fluctuations in δ³⁴S values were mainly influenced by sedimentation rate. In addition, intense volcanic activities also caused negative deviations in δ³⁴S values. Studies on factors affecting sulfur isotope fractionation in pyrite of the Fengcheng Formation is beneficial for further understanding the sulfur cycle and reconstructing diagenetic and sedimentary models. Finally, based on the total organic carbon (TOC) content and water environment variations indicated by sulfur isotopes, it is concluded that increased lake basin openness, stratification of high-salinity water caused by strong evaporation, and intense volcanic activities are the key factors influencing the enrichment and preservation of organic matter in the Fengcheng Formation.
- pyrite /
- sulfur source /
- sulfur isotope /
- organic matter enrichment /
- Fengcheng Formation /
- Mahu Sag /
- Junggar Basin
注释:

利益冲突声明/Conflict of Interests

所有作者声明不存在利益冲突。

All authors declare no relevant conflict of interests.

作者贡献/Authors’Contributions

江程舟完成论文的撰写和修改；王贵文、江程舟负责稿件的总体构思和数据分析；江程舟负责实验设计；江程舟、王松、黄玉越、张益粼参与图件绘制。所有作者均阅读并同意最终稿件的提交。

The manuscript was drafted and revised by JIANG Chengzhou. WANG Guiwen and JIANG Chengzhou were responsible for the overall conceptualization and data analysis of the manuscript. The experiment was designed by JIANG Chengzhou. JIANG Chengzhou, WANG Song, HUANG Yuyue, and ZHANG Yilin participated in figure drawing. All authors have read the final version of the paper and consented to its submission.

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图 1 准噶尔盆地玛湖凹陷位置及地层综合柱状图

a.晚石炭世—早二叠世西准噶尔地区沉积相，修改自文献[24]；b.玛湖凹陷构造位置; c.风城组地层柱状图，修改自文献[19]。

Figure 1. Location and comprehensive stratigraphic column of Mahu Sag, Junggar Basin

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图 2 准噶尔盆地玛湖凹陷玛页1井风城组黄铁矿形态

a.自形黄铁矿，4 685.5 m，新鲜断块样品；b.不规则状黄铁矿集合体，4 813.8 m，氩离子抛光样品；c.充填型草莓状黄铁矿，4 759.4 m，氩离子抛光样品；d.聚集型草莓状黄铁矿，4 740.4 m，氩离子抛光样品。

Figure 2. Pyrite morphologies in Fengcheng Formation in well Maye 1 of Mahu Sag, Junggar Basin

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图 3 准噶尔盆地玛湖凹陷玛页1井风城组地球化学综合柱状图

Figure 3. Comprehensive geochemical columns of Fengcheng Formation in well MY1, Mahu Sag, Junggar Basin

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图 4 准噶尔盆地玛湖凹陷风城组硫来源示意图

Figure 4. Sulfur sources in Fengcheng Formation of Mahu Sag, Junggar Basin

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图 5 准噶尔盆地玛湖凹陷风城组硫同位素分馏因素示意图

Figure 5. Factors affecting sulfur isotope fractionation in Fengcheng Formation of Mahu Sag, Junggar Basin

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表 1 准噶尔盆地玛湖凹陷玛页1井风城组主量元素统计

Table 1. Statistics of major elements in Fengcheng Formation of well MY1, Mahu Sag, Junggar Basin

深度/m	Na₂O/%	MgO/%	Al₂O₃/%	SiO₂/%	P₂O₅/%	K₂O/%	CaO/%	TiO₂/%	MnO/%	Fe₂O₃/%	LOI/%	CaO^*/%	CIA/%
4 716.34	3.6	8.8	7.8	45.2	0.0	3.2	10.3	0.3	0.1	3.2	17.0	10.3	31.4
4 720.15	3.9	6.7	3.5	60.1	0.0	1.3	8.4	0.1	0.0	1.5	13.9	8.3	20.6
4 720.29	4.0	6.8	3.5	60.5	0.0	1.3	8.6	0.1	0.0	1.6	14.5	8.6	20.2
4 721.06	3.2	8.8	7.0	51.2	0.0	3.2	8.6	0.2	0.0	2.7	14.7	8.6	31.9
4 738.73	2.2	9.9	8.2	48.9	0.0	4.3	7.7	0.4	0.1	3.7	14.7	7.6	36.6
4 740.43	2.7	8.9	8.5	48.4	0.0	3.6	9.0	0.3	0.1	3.5	15.6	8.9	36.1
4 744.90	4.1	3.4	10.9	58.0	0.1	3.7	5.6	0.3	0.0	4.0	8.8	5.4	45.3
4 751.36	1.9	12.9	6.2	44.5	0.0	3.8	9.9	0.3	0.0	2.7	18.2	9.9	28.5
4 759.42	1.6	10.9	5.1	43.1	0.0	2.2	13.6	0.2	0.0	2.3	21.5	13.5	22.7
4 766.56	1.1	6.2	4.8	63.2	0.0	2.6	7.7	0.1	0.0	1.8	13.1	7.6	29.9
4 773.86	2.1	9.6	8.0	49.2	0.0	4.2	7.4	0.4	0.1	3.6	14.6	7.4	36.8
4 773.99	5.5	0.8	14.7	62.5	0.1	4.9	2.1	0.3	0.0	4.0	4.6	1.7	54.9
4 775.86	5.2	2.0	14.0	56.6	0.1	4.9	5.8	0.0	0.0	2.7	7.8	5.6	47.1
4 790.94	3.6	4.6	10.0	57.1	0.1	3.7	5.8	0.2	0.1	3.8	10.2	5.6	43.6
4 794.99	2.1	2.5	8.1	59.4	0.1	4.1	9.3	0.2	0.0	3.1	10.9	9.1	34.6
4 799.67	1.0	8.1	6.6	49.2	0.0	4.7	9.9	0.3	0.1	3.2	16.5	9.8	29.7
4 800.45	0.7	9.3	3.8	52.3	0.0	2.4	11.2	0.1	0.1	1.7	18.5	11.1	21.1
4 800.98	2.7	5.1	10.9	52.5	0.1	5.6	6.6	0.4	0.1	4.3	11.8	6.4	42.5
4 802.20	1.4	5.8	7.0	53.5	0.0	4.2	9.7	0.2	0.1	3.0	15.0	9.6	31.5
4 804.95	4.3	1.4	13.9	61.5	0.1	5.9	2.1	0.5	0.0	4.4	5.5	1.8	53.6
4 813.65	0.6	4.5	6.7	48.6	0.0	5.4	15.3	0.2	0.0	2.7	16.8	15.2	24.1
4 813.75	0.2	1.0	15.6	58.9	0.0	14.2	2.6	0.0	0.0	2.1	4.7	2.5	48.0
4 816.79	1.1	3.9	4.1	51.7	0.0	1.9	16.9	0.1	0.0	1.9	18.0	16.8	17.2
4 830.31	2.5	7.9	9.5	46.8	0.1	5.0	9.3	0.2	0.1	2.8	15.3	9.1	36.5
4 835.28	1.5	9.1	8.5	49.6	0.0	5.8	7.7	0.3	0.0	2.9	14.1	7.6	36.4
4 840.37	1.5	6.6	11.3	54.3	0.1	8.3	5.0	0.3	0.0	3.9	9.6	4.8	43.7
4 842.99	0.8	7.5	5.1	53.9	0.0	3.7	10.8	0.2	0.0	1.8	16.2	10.7	25.1
4 845.61	1.2	5.8	11.7	56.1	0.1	9.8	4.3	0.4	0.0	4.2	7.1	4.0	43.8
4 848.23	0.8	3.2	7.0	57.6	0.0	5.4	10.3	0.3	0.0	3.3	11.0	10.2	30.0
4 850.43	1.1	2.5	11.5	60.6	0.1	9.2	4.7	0.3	0.0	4.0	6.4	4.5	44.0
4 851.11	0.7	2.3	5.3	73.7	0.0	3.8	4.9	0.2	0.0	2.4	5.7	4.9	36.1
4 853.35	0.9	9.9	7.0	47.9	0.0	5.6	9.1	0.3	0.0	2.7	15.8	8.9	31.2
注：LOI为烧失量，CaO^*是硅酸盐中的CaO，CIA是化学蚀变指数。

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表 2 准噶尔盆地玛湖凹陷风城组岩性、黄铁矿硫含量、硫同位素及TOC含量统计

Table 2. Statistics of lithology, pyrite sulfur content, sulfur isotope, and TOC content in Fengcheng Formation of Mahu Sag, Junggar Basin

编号	深度/m	地层	阶段	岩性	ω(TOC)/%	ω(CRS)/%	δ³⁴S/‰
1 2	4 608.7 4 627.8	P₁f₃	(火山作用) 阶段2	富有机质页岩含云粉细砂岩	1.20 0.65	2.71 1.12	-14.17 1.12
3 4 5 6 7 8	4 633.2 4 643.0 4 650.0 4 658.9 4 668.8 4 682.8	C₂-P₁f₂	(火山作用) 阶段2	含云粉细砂岩富有机质页岩含云粉细砂岩富有机质页岩含云粉细砂岩富有机质页岩	0.14 0.59 0.25 0.64 0.54 0.69	0.10 0.87 0.35 0.54 0.62 1.10	-3.95 0.81 8.46 -7.70 2.41 -0.85
9 10 11 12 13 14 15 16 17 18	4 705.6 4 711.6 4 722.3 4 734.0 4 755.2 4 770.3 4 780.2 4 793.6 4 800.2 4 811.5	C₂-P₁f₂	阶段1	含碱性矿物页岩含碱性矿物页岩富有机质页岩富有机质页岩富有机质页岩富有机质页岩含碱性矿物页岩富有机质页岩富有机质页岩含碱性矿物页岩	0.80 0.76 0.73 0.63 0.71 0.94 0.70 0.51 0.75 0.58	1.34 1.05 0.62 0.99 0.91 1.67 0.69 0.37 0.68 0.43	6.08 3.39 -0.97 -14.31 -9.92 -7.32 6.33 -4.16 -3.31 9.05
19 20	4 841.1 4 850.0	C₂f₁	阶段1	富有机质页岩富有机质页岩	0.68 1.18	1.21	-11.21 -9.72

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表 3 中国不同陆相盆地硫含量及TOC含量统计

Table 3. Statistics of sulfur and TOC contents of different continental basins in China

陆相盆地	地层	湖泊类型	样品数	总S含量/%		ω(CRS)/%		ω(TOC)/%		δ³⁴S/‰
陆相盆地	地层	湖泊类型	样品数	范围	平均值	范围	平均值	范围	平均值	范围	分馏
准噶尔盆地	风城组	碳酸盐型碱湖	20			0.10~2.17	0.94	0.1~1.2	0.7	-14.31~9.05	23.36
鄂尔多斯盆地	长7段	淡水—微咸水湖	36	0.11~3.45	0.83			1.4~9.5	5.0	3.0~9.8	6.8
松辽盆地	嫩江组	淡水—微咸水湖	65	0.05~2.96	0.67			0.1~8.7	2.2	-4.93~26.89	31.82
柴达木盆地	下干柴沟组	硫酸盐型盐湖	23	0.12~0.88	0.53			0.1-1.5	0.7
注：据参考文献[31-33]修改。

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