松辽盆地晚白垩世湖相白云岩碳氧同位素特征及其古环境意义

doi:10.19657/j.geoscience.1000-8527.2023.023

摘要/Abstract

摘要：

松辽盆地上白垩统青山口组和嫩江组是重要的烃源岩层位,以暗色泥岩为主,夹有数层白云岩层和白云岩结核层。湖泊碳酸盐岩是分布范围最广泛的一类陆相碳酸盐岩,是陆相盆地在特殊环境下的产物,其形成与盆地气候-环境演化密切相关,是深时古地理、古气候、古环境等信息的良好记录载体。另外,白云岩是碳酸盐岩层系中最主要的油气储渗体,因此开展重要含油层系白云岩研究有助于了解陆地古环境演化及烃源岩储层特征。本文对松辽盆地东南缘鸟河剖面青山口组一段和李家坨子剖面嫩江组一段湖泊白云岩开展碳、氧同位素特征分析,探讨其古环境意义。结果表明,松辽盆地晚白垩世白云岩具有重碳(δ¹³C_鸟河=5.89‰~0.78‰,δ¹³C_李家坨子=-8.36‰~6.70‰)、轻氧(δ¹⁸O_鸟河=-10.03‰~-7.84‰,δ¹⁸O_李家坨子=-11.30‰~-3.82‰)特征,且δ¹³C-δ¹⁸O相关性较高(R²>0.7),表明松辽盆地晚白垩世白云岩是湖水滞留时间较长的封闭型咸水-半咸水湖泊体系的产物。根据经验判别式Z=2.048×(δ¹³C+50)+1.498×(δ¹⁸O+50)计算,青山口组、嫩江组白云岩Z平均值分别为124和126.5,表明白云岩形成过程中可能受到海水入侵作用影响。进一步通过海水与淡水氧同位素混合模型,估算了海侵作用的规模,综合认为松辽盆地晚白垩世湖相白云岩沉积于海侵背景下、湖水长期滞留的封闭型咸水-半咸水湖泊。

关键词: 松辽盆地, 白垩纪, 白云岩, 碳氧稳定同位素, 古环境

Abstract:

The Late Cretaceous Qingshankou and Nenjiang Formations in the Songliao Basin, extensively deposited with dark mudstone, and interspersed with layers of dolomite and dolomite nodules, are regarded as important source rock strata.Studying important oil-bearing dolomite can help to understand the terrestrial paleoenvironment evolution and source rock reservoir characteristics.In this study, carbon and oxygen isotopes of dolomites from the Qingshankou Formation (the first member) in Niaohe section and the Nenjiang Formation (the first member) in Lijiatuozi section in the southeastern margin of Songliao Basin are analyzed to explore paleoenvironmental significance.The results show that δ¹³C values of dolomites in both sections are relatively high (δ¹³C_Niaohe=-5.89‰~0.78‰, δ¹³C_Lijiatuozi=-8.36‰~6.70‰), while δ¹⁸O values are relatively low (δ¹⁸O_Niaohe=-10.03‰~-7.84‰, δ¹⁸O_Lijiatuozi=-11.30‰~-3.82‰), and the correlation between δ¹³C and δ¹⁸O is high (R²>0.7). This demonstrates that the late Cretaceous dolomites in the Songliao Basin were the product of closed (semi-)brackish lacustrine system with a long retention time.According to the empirical equation Z=2.048×(δ¹³C+50)+1.498×(δ¹⁸O+50), the average values of dolomites in Qingshankou and Nenjiang Formations are 124 and 126.5, respectively, indicating that the dolomites may be affected by seawater intrusion during the formation process.Furthermore, we estimated the scale of transgression using a mixing model of seawater and freshwater oxygen isotopes.In conclusion, we consider that the Late Cretaceous lacustrine dolomite in the Songliao Basin was deposited in closed (semi-)brackish lacustrine system with a long retention time, under a transgressive background.

Key words: Songliao Basin, Cretaceous, dolomite, carbon and oxygen isotope, paleoenvironment

中图分类号:

P534.53

张一范, 高远, 陈积权, 黄帅, 海伦, 毋正轩, 杨柳, 董甜. 松辽盆地晚白垩世湖相白云岩碳氧同位素特征及其古环境意义[J]. 现代地质, 2023, 37(05): 1243-1253.

ZHANG Yifan, GAO Yuan, CHEN Jiquan, HUANG Shuai, HAI Lun, WU Zhengxuan, YANG Liu, DONG Tian. Carbon and Oxygen Isotope Characteristics of Late Cretaceous Lacustrine Dolomite in the Songliao Basin and their Paleoenvironmental Implications[J]. Geoscience, 2023, 37(05): 1243-1253.

图/表 5

图1 松辽盆地构造分区与研究区剖面位置(a)和松辽盆地综合柱状图(b)(改自Feng 等[26])

Fig.1 Tectonic division of Songliao Basin and location of sections (a) and generalized stratigraphic column of the Songliao Basin (b)(modified from Feng et al.[26])

图2 野外露头剖面白云岩特征 (a)李家坨子剖面局部露头;(b)鸟河剖面白云岩结核;(c)李家坨子剖面白云岩结核

Fig.2 Characteristics of dolomite outcrops

图3 松辽盆地白云岩碳、氧同位素特征 (a)(c)分别为李家坨子剖面和鸟河剖面白云岩碳、氧同位素特征;(b)为松科1井白云岩碳、氧同位素特征(数据来自Gao等[23])

Fig.3 Carbon and oxygen isotope compositions of dolomites in the Songliao Basin

图4 松辽盆地白云岩δ13C、δ18O交会图 (a)松辽盆地晚白垩世白云岩δ13C、δ18O交会图;(b)(c)(d)分别为李家坨子剖面、鸟河剖面、松科1井白云岩δ13C-δ18O交会图

Fig.4 Crosspolts of δ13C and δ18O of dolomites in the Songliao Basin

表1 松辽盆地白云岩碳氧同位素结果

Table 1 C-O isotope compositions of dolomites in the SongliaoBasin

样品号	剖面	δ¹³C_VPDB (‰)	δ¹⁸O_VPDB (‰)	δ¹⁸O _VSMOW (‰)	δ¹⁸O_water (‰)	Z
LT03	李家坨子剖面	7.05	-7.71	22.96	0-8.75	138
LT05		-3.30	-11.30	19.26	-12.33	115
LT12		-8.36	-3.82	26.97	-4.87	108
LT16		-4.06	-11.21	19.36	-12.24	113
LT20		-3.09	-11.09	19.48	-12.12	115
LT23		6.70	-7.15	23.54	-8.20	137
LT25		6.21	-7.51	23.17	-8.55	136
LT27		4.49	-8.55	22.10	-9.59	132
LT29		4.72	-7.79	22.88	-9.83	133
LT32		2.16	-8.77	21.87	-9.81	127
LT34		0.99	-9.23	21.39	-10.27	125
LT38		2.84	-8.13	22.53	-9.17	129
LT86		-2.20	-10.58	20.00	-11.62	118
LT89		1.20	-9.54	21.07	-10.58	125
NH02C	鸟河剖面	0.65	-7.85	22.82	-10.41	125
NH03C		0.72	-7.84	22.83	-10.40	125
NH4		-0.01	-8.60	22.04	-11.16	123
NH04C		-0.17	-8.57	22.08	-11.13	123
NH05C		0.78	-7.97	22.70	-10.53	125
NH07C		0.02	-8.88	21.75	-11.44	123
NH10		0.65	-8.18	22.48	-10.73	125
NH42		-4.74	-10.03	20.57	-12.58	113
NH43		-5.89	-9.42	21.19	-11.98	111

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