鄂西黄陵背斜周缘震旦系灯影组白云岩成因分析

doi:10.11720/wtyht.2025.1346

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摘要鄂西克拉通内裂陷东部黄陵背斜震旦系灯影组发育一套以白云岩为主的碳酸盐岩储层,开展白云岩形成环境和成因机制研究对该地区碳酸盐岩储层发育机制和常规油气勘探具有重要作用。本文利用铸体薄片、阴极发光薄片、场发射扫描电镜、碳酸盐岩碳氧同位素分析、主微量元素分析、全岩矿物分析和白云岩有序度测定等方法,分析了黄陵背斜周缘灯影组白云岩化学元素组成和岩石矿物学特征,进而对白云岩的形成环境、发育机制和改造过程进行了研究。结果表明,灯影组白云岩的CaO和MgO分子数比例为1∶1,Sr含量较低,符合准同生白云岩特征;微量元素、碳氧同位素分析结果证明其形成于Fe、Mn含量较低的海水环境,古海水盐度(Z)平均值为128.41,平均温度21.32 ℃,平均成岩温度为49.36 ℃,具备形成准同生白云岩的环境条件。同时,灯影组白云石氧同位素δ¹⁸O显著低于灯影期海水,白云石有序度为0.61~0.99,频率峰值分布于0.8~0.9之间,证明其经历过逐步加深的深埋藏改造作用;全岩矿物分析结果证明白云石含量与有序度呈正相关,反映了在埋藏改造过程中白云石化程度越高,白云石有序度也越高。由此认为本地区灯影组白云岩原始成因为早期准同生白云石,后经长期埋藏改造,低有序度的泥晶白云石发生重结晶作用, 逐渐向粉晶、细晶白云石转化,同时白云石有序度升高,最终形成准同生——埋藏改造成因白云岩。

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	李浩涵
	张聪
	李文正
	张春贺
	张远
	王梓
	陈维堃
	方镕慧

关键词 ：黄陵背斜, 灯影组, 白云石成因, 白云石有序度, 成岩环境

Abstract：

A suite of dolomite-dominated carbonate reservoirs is developed in the Sinian Dengying Formation in the Huangling anticline in the eastern part of the intracratonic rift, western Hubei Province. Investigating the formation environment and genetic mechanism of dolomites is crucial for determining the developmental mechanism of carbonate reservoirs and facilitating conventional oil and gas exploration in the study area. This study employed various analytical techniques, including cast thin sections, cathodoluminescence thin sections, field emission scanning electron microscopy, carbon and oxygen isotope analyses of carbonate rocks, major and trace element analyses, whole-rock mineral analyses, and determination of the degree of order of dolomite. Using these techniques, this study analyzed the chemical composition and mineralogical characteristics of dolomites from the Dengying Formation on the periphery of the Huangling anticline. Furthermore, this study explored the formation environment, developmental mechanism, and modification process of dolomites. The results indicate that the dolomites from the Dengying Formation contained the same proportions of CaO and MgO molecules and low Sr content, aligning with the characteristics of penecontemporaneous dolomites. The analytical results of trace elements and carbon and oxygen isotopes confirm that the dolomites formed in a marine environment with low Fe and Mn contents. The average paleoseawater salinity (Z) of 128.41, average temperature of 21.32 ℃, and average diagenetic temperature of 49.36 ℃ created the favorable environmental conditions for forming penecontemporaneous dolomites. Additionally, the dolomite from the Dengying Formation exhibited significantly lower δ¹⁸O compared to the Dengyingian seawater, degrees of order ranging from 0.61 to 0.99, and a peak frequency distribution between 0.8 and 0.9, indicating that the dolomite experienced a progressively deepening burial modification process. The whole-rock mineral analyses reveal that the content of dolomite was positively correlated with its degree of order, suggesting that a high degree of dolomitization corresponded to a higher degree of order during burial modification. Therefore, this study holds that dolomites in the Dengying Formation were originally formed by penecontemporaneous dolomite. Through prolonged burial modification, micritic dolomite with a low degree of order experienced recrystallization, gradually transitioning into very finely crystalline/finely crystalline dolomite, accompanied by an elevated degree of order. Ultimately, dolomites of a penecontemporaneous-burial modification origin formed in the study area.

Key words： Huangling anticline Dengying Formation dolomite origin degree of order of dolomite diagenetic environment

收稿日期: 2024-08-16 修回日期: 2025-02-19 出版日期: 2025-08-20

ZTFLH:

P632

基金资助:国家自然科学基金青年基金项目(42302177);国家自然科学基金项目(U2244208);中国地质调查局地质调查项目(DD20240050)

通讯作者: 张聪(1986-),女,博士,教授级高工,从事非常规油气分析测试研究工作。Email:zh_cong520@qq.com

作者简介: 李浩涵(1986-),男,硕士,高级工程师,从事非常规油气调查研究工作。Email:akazan@126.com

引用本文:

李浩涵, 张聪, 李文正, 张春贺, 张远, 王梓, 陈维堃, 方镕慧. 鄂西黄陵背斜周缘震旦系灯影组白云岩成因分析[J]. 物探与化探, 2025, 49(4): 790-801.
LI Hao-Han, ZHANG Cong, LI Wen-Zheng, ZHANG Chun-He, ZHANG Yuan, WANG Zi, CHEN Wei-Kun, FANG Rong-Hui. Genetic analysis of dolomites in the Sinian Dengying Formation on the periphery of the Huangling anticline, western Hubei Province. Geophysical and Geochemical Exploration, 2025, 49(4): 790-801.

链接本文:

https://www.wutanyuhuatan.com/CN/10.11720/wtyht.2025.1346 或 https://www.wutanyuhuatan.com/CN/Y2025/V49/I4/790

Fig.1 研究区灯影期沉积相及灯影组地层柱状图(据李文正等^[14]修改)

Fig.2 灯影组白云岩岩相类型薄片特征
a—QLK-23号样品单偏光镜下照片;b—QLK-23号样品正交光镜下照片;c—QLK-23号样品阴极光镜下照片;d—QLK-11号样品单偏光镜下照片;e—QLK11号样品正交光镜下照片;f—QLK-11号样品阴极光镜下照片

Fig.3 灯影组白云岩场发射扫描电镜照片
a—QLK-23号样品全貌,白云石晶体以自形为主,晶间孔发育(×500);b—照片a局部放大,白云石以自形的菱面体为主,晶体间发育晶间孔(×1000);c—照片b局部放大,白云石晶间孔发育(×2000);d—QLK-11号样品全貌,白云石晶体以自形为主,晶间孔发育 (×500);e—照片d局部放大,白云石以自形的菱面体为主,晶体间发育晶间孔(×1000);f—照片e局部放大,白云石晶间孔发育(×2000)

序号	样品编号	岩性	微量元素含量/10^-6						主量元素含量/%				碳氧同位素
序号	样品编号	岩性	Sr 光谱	Sr 质谱	Mn	Fe	w(Fe)/ w(Mn)	w(Mn)/ w(Sr)	SiO₂	Al₂O₃	CaO	MgO	δC¹³/ PDB,‰	δO¹⁸/ PDB,‰	古盐度指标(Z)	古海水温度T/℃	成岩温度T/℃
1	QLK-01	粉—泥晶白云岩	61.94	86.6	97.70	357.78	3.66	1.13	0.50	0.18	32.37	23.08	-2.29	-6.55	119.35	17.96	45.57
2	QLK-02	纹层状泥质泥晶白云岩	149.91	99.5	94.20	5374.44	57.05	0.95	6.82	1.81	27.51	20.80	1.89	-7.45	127.46	21.9	50.19
3	QLK-03	粉—泥晶硅质灰岩	479.53	43	190.10	62.22	0.33	4.42	13.29	0.06	26.33	20.03	3.54	-5.45	131.84	13.42	40
4	QLK-04	粒屑粉—泥晶灰岩	2683.77	1361	34.20	/	0.00	0.03	1.52	0.05	53.66	1.48	2.65	-6.3	129.59	16.9	44.29
5	QLK-05	泥—粉晶白云岩	2462.38	77.1	169.90	147.78	0.87	2.20	0.68	0.10	32.57	23.07	3.83	-6.65	131.83	18.39	46.08
6	QLK-06	细晶含灰白云岩	1994.75	67.1	216.80	132.22	0.61	3.23	0.72	0.09	32.64	22.74	5.03	-5.39	134.92	13.19	39.7
7	QLK-07	泥—粉晶白云岩	1090.57	90.5	166.90	482.22	2.89	1.84	0.30	0.11	32.68	20.55	3.89	-6.56	132	18	45.62
8	QLK-08	粉—细晶白云岩	2573.67	63.2	144.10	4106.67	28.50	2.28	5.58	1.58	27.91	18.56	3.81	-5.99	132.12	15.61	42.72
9	QLK-09	粉—细晶白云岩	1620.55	1528.4	/	38.89	/	/	0.45	0.08	54.03	1.38	3.77	-5.27	132.4	12.71	39.1
10	QLK-10	泥—粉晶云质灰岩	984.39	397.6	2.50	15.56	6.22	0.01	3.77	0.15	50.88	1.63	1.61	-8.22	126.5	25.44	54.2
11	QLK-11	粉—细晶灰质白云岩	1463.82	1149.4	19.40	/	0.00	0.02	2.23	0.08	54.13	0.63	3.68	-6.07	131.81	15.94	43.12
12	QLK-12	粉—细晶灰质白云岩	664.52	73.9	139.80	70.00	0.50	1.89	4.43	0.16	30.83	22.19	2.82	-7.95	129.12	24.18	52.79
13	QLK-13	粉—细晶白云质灰岩	1192.04	117.3	116.80	2107.78	18.05	1.00	1.28	0.34	32.33	19.40	3.07	-7.08	130.06	20.26	48.28
14	QLK-14	泥—粉晶白云岩	1308.22	684.5	337.10	124.44	0.37	0.49	2.51	0.21	39.91	14.44	1.03	-9.78	124.54	33.09	62.47
15	QLK-15	粉—细晶云质灰岩	861.54	2027.9	10.70	7.78	0.73	0.01	17.43	0.16	40.02	1.73	1.31	-9.7	125.15	32.68	62.04
16	QLK-16	粉晶含灰白云岩	1702.04	36.6	68.40	31.11	0.45	1.87	0.16	0.05	32.54	23.31	2.93	-6.95	129.84	19.68	47.61
17	QLK-17	粉—细晶白云岩	2327.16	2073.7	12.70	140.00	11.02	0.01	1.79	0.14	51.02	3.33	3.53	-6.08	131.5	15.98	43.18
18	QLK-18	粉晶白云岩	1841.99	64.3	87.50	248.89	2.84	1.36	0.13	0.06	32.92	22.77	2.95	-6.81	129.95	19.08	46.89
19	QLK-19	粉—泥晶白云岩	62.49	1687.1	19.50	7.78	0.40	0.01	14.35	0.11	41.48	2.47	2.48	-7.81	128.49	23.54	52.06
20	QLK-20	粉—泥晶白云岩	57.44	95.8	99.90	132.22	1.32	1.04	0.31	0.16	33.45	22.37	1.23	-8.04	125.82	24.6	53.26
21	QLK-21	泥—粉晶白云岩	63.87	857.5	204.50	4876.67	23.85	0.24	16.56	2.99	32.59	4.55	2.16	-7.86	127.81	23.77	52.32
22	QLK-22	泥—粉晶白云岩	81.86	1029.4	106.40	1796.67	16.89	0.10	6.73	1.03	45.38	2.38	2.35	-7.8	128.23	23.49	52.01
23	QLK-23	泥—粉晶白云岩	60.23	173.1	154.50	248.89	1.61	0.89	1.23	0.21	32.77	22.10	0.87	-7.57	125.31	22.44	50.81
24	QLK-24	泥—粉晶白云岩	102.88	73.9	101.40	256.67	2.53	1.37	0.27	0.12	32.74	23.12	1.18	-7.04	126.21	20.08	48.08
25	YX-01	泥—粉晶白云岩	54.88	100.1	207.80	7.78	0.04	2.08	0.75	0.06	32.89	22.87	3.35	-6.25	131.05	16.69	44.04
26	YX-02	泥—粉晶白云岩	42.51	936.3	24.50	116.67	4.76	0.03	2.41	0.14	52.39	1.25	1.97	-6.85	127.92	19.25	47.1
27	YX-03	泥—粉晶白云岩	87.58	283.7	7.10	/	0.00	0.03	1.24	0.05	54.06	1.28	1.55	-4.17	128.4	8.54	33.64
28	YX-04	粉—泥晶白云岩	82.75	92.1	76.70	132.22	1.72	0.83	0.67	0.10	32.61	23.06	1.95	-8.34	127.14	26.01	54.83
29	YX-05	粉—泥晶白云岩	64.72	46.4	178.70	85.56	0.48	3.85	25.64	0.06	20.82	17.36	-1.28	-8.6	120.4	27.25	56.2
30	YX-06	粉—泥晶白云岩	57.01	39.1	140.90	225.56	1.60	3.60	0.29	0.06	32.36	23.23	1.96	-8.06	127.3	24.69	53.36
31	YX-07	粉—泥晶含硅白云岩	37.75	49.2	256.60	70.00	0.27	5.22	0.63	0.05	32.56	22.62	/	/	/	/	/
32	YX-08	粉—泥晶白云岩	36.41	82.8	73.10	342.22	4.68	0.88	29.55	0.12	19.56	16.47	3	-8.83	129.05	28.36	57.41
33	YX-09	粉—泥晶白云岩	43.43	79.2	154.20	85.56	0.55	1.95	1.09	0.05	32.08	22.28	2.65	-8.41	128.54	26.34	55.2
34	YX-10	泥—粉晶白云岩	61.82	1128.6	12.20	303.33	24.86	0.01	24.17	0.24	31.96	4.81	3.38	-7.98	130.25	24.32	52.95
35	YX-11	粉—泥晶白云岩	67.23	76.2	201.30	70.00	0.35	2.64	8.10	0.08	28.51	21.23	1.74	-8.1	126.83	24.88	53.57
36	YX-12	粒屑粉—泥晶白云岩	71.48	1354.8	0.80	85.56	106.94	0.00	6.29	0.12	46.72	3.24	2.29	-7.72	128.15	23.13	51.59
37	YX-13	含粒屑粉—泥晶白云岩	32.58	787.3	55.90	93.33	1.67	0.07	0.95	0.11	54.04	1.37	0.73	-7.31	125.15	21.27	49.47
38	YX-14	粉—细晶白云岩	79.11	9.5	9.50	202.22	21.29	1.00	3.76	0.21	50.34	1.78	2.91	-8.27	129.14	25.68	54.46

Table 1 鄂西地区佑溪、青林口剖面主量元素、微量元素和碳氧同位素数据

Table 2 矿物含量与白云石有序度数据

Fig.4 CaO和MgO含量关系

Fig.5 Sr元素含量分布直方图

Fig.6 白云石有序度分布直方图(n=28)

Fig.7 白云石含量与白云石有序度关系

Fig.8 黄陵背斜周缘震旦系灯影组白云岩成因模式
a—震旦纪末期灯影组强烈蒸发条件下的高盐海水环境下,白云石迅速结晶生成低有序度的泥晶白云石;b—侏罗纪末期灯影组埋深达到最大,白云石经过深埋改造、重结晶作用形成高有序度的粉晶白云岩;c—抬升过程中灯影组出露地表,接受改造作用

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