塔里木盆地鹰山组白云岩成因与Mg同位素证据

doi:10.13745/j.esf.sf.2022.10.43

摘要/Abstract

摘要：

中-下奥陶统鹰山组作为塔里木盆地中央隆起区潜在的重要勘探接替层系,其白云岩成因认识仍不清楚,因此制约了对该区域的进一步勘探。鹰山组由下至上依次发育白云岩、白云质灰岩和灰岩,表明发生了灰岩向白云岩的交代转化过程。交代白云岩的形成需要足够的含镁流体和长期的镁泵输送机制,而新兴的Mg同位素技术在示踪白云石化流体来源和迁移路径方面已经取得良好效果。因此,本研究通过系统采集鹰山组白云岩、白云质灰岩和灰岩,开展岩石学、微量元素、碳氧同位素和Mg同位素测试。实验结果显示,鹰山组发育6类岩石,分别是泥晶-微晶白云岩(D1)、粉晶-细晶白云岩(D2)、颗粒白云岩(D3)、中晶-粗晶白云岩(D4)、白云质灰岩(DL)和灰岩(L)。鹰山组碳酸盐岩的δ¹³C_V-PDB值为-2.10‰~-0.37‰(平均值-1.37‰),δ¹⁸O_V-PDB值为-7.51‰~-3.54‰(平均值-5.41‰),δ²⁶Mg值为-4.03‰~-1.28‰(平均值-2.55‰)。 δ²⁶Mg、Na含量、Sr/Ba、Mn/Fe、δ¹³C_V-PDB、δ¹⁸O_V-PDB、古盐度(Z)和古温度(T)在垂向上显示出一定的联动性和系统性。通过综合分析与讨论得出以下几点认识:(1)鹰山组δ²⁶Mg值垂向变化趋势与沉积旋回具有密切联系,沉积旋回的顶部为富镁流体源区,旋回界面为流体迁移通道; (2)识别出4种Mg同位素变化趋势与白云石化流体迁移规律,即云灰互层结构(L→DL→D)、准同生白云岩结构(D1→D2)、渗透回流白云岩结构(D1→D2→D3→D4→L)和埋藏白云岩结构(D4→DL/D); (3)鹰山组白云岩形成主要与海平面周期性波动有关,海平面下降时,蒸发作用促使局限水体中富集Mg²⁺,并且富镁流体会沿着下伏高孔高渗的颗粒灰岩垂向迁移至下伏地层,有利于白云石化作用的持续进行,当富镁流体遇到孔隙度不发育的泥晶灰岩时,富镁流体无法进入矿物晶格中,白云石化作用停止。海平面上升时,局限水体转变为开阔水体,海水与富镁流体源区相互混合,降低了流体的白云石化驱动力,致使白云石化作用逐渐减弱,从而发育灰质白云岩和灰岩;(4)除受海平面控制外,深埋藏阶段经历的多期交代、重结晶或热液作用也有利于鹰山组白云岩的形成;(5)白云石化作用对鹰山组沉积储层具有建设性意义,早期白云石化作用有利于孔隙的继承和保存,而晚埋藏和热液白云石化对储层起破坏作用。

关键词: Mg同位素, 白云岩成因, 奥陶系鹰山组, 塔里木盆地, 中央隆起

Abstract:

The Yingshan Formation of the Middle-Lower Ordovician is a potential exploration replacement series in the Central Uplift of the Tarim Basin, however, the genesis of dolostone is still unclear, which hinders dolomite exploration in the basin. The ongoing dolomatization in the Yingshan Formation, as evidenced by the sequential, bottom-to-top developments of dolostone, dolomitic limestone and limestone, makes it feasible to study the dolostone reservoirs by Mg isotope analysis that has shown good results in tracing the source and migration pathway of dolomitic fluid. In this study, we systematically collected dolostone, dolomitic limestone and limestone from the Yingshan Formation and carried out comprehensive petrological, trace elemental and isotope (C, O, Mg) analyses. Six types of dolostone were identified in the Yingshan Formation: dolomicrite/micro-crystalline dolostone (D1), powder/fine-crystalline dolostone (D2), granular dolostone (D3), medium/coarse-crystalline dolostone (D4), dolomitic limestone (DL) and limestone (L). The δ¹³C_V-PDB value of carbonate rock ranged between -2.10‰ to -0.37‰ (average -1.37‰), δ¹⁸O_V-PDB value between -7.51‰ to -3.54‰ (average -5.41‰), and δ²⁶Mg value between -4.03‰ to -1.28‰ (average -2.55‰), and certain degree of correlation in the vertical direction was observed between δ²⁶Mg, Na, Sr/Ba, Mn/Fe, δ¹³C_V-PDB, δ¹⁸O_V-PDB, paleosalinity (Z) and plaeotemperature (T). Results on dolomite genesis revealed (1) the δ²⁶Mg variation trend in the vertical direction was closely related to sedimentary cycles, where the top layer was identified as the source area of Mg-rich fluid and the layer interface as the migration channel. (2) There were four migration pathways of dolomitic fluid identified based on the Mg isotopic variation trends: L→DL→D, D1→D2, D2→D3→D4→L and D4→L/DL. (3) The formation of dolostone was mainly related to the periodic fluctuation of sea-level: with decreasing sea level, Mg-rich fluid formed in the confined water via evaporation migrated vertically downward along the high-porosity, high-permeability granular limestone to promote continuous dolomitazation, or it encountered low-porosity argillaceous limestone and failed to enter the rock lattice, thus terminating dolomitization; whereas rising sea-level destroyed the source area of Mg-rich fluid, thus weakening or interrupting dolomitization to form calcareous dolostone and limestone. (4) Multi-stage metasomatism, recrystallization and hydrothermal processes in the deep-burial stage were also conducive to the formation of dolostone. (5) Dolomitization had significant impact on the sedimentary reservoirs, where early dolomitization was conducive to the inheritance and preservation of pores while late-burial and hydrothermal dolomitization destroyed the reservoirs.

Key words: Mg isotope, dolostone origin, Ordovician Yingshan Formation, Tarim Basin, Central Uplift

中图分类号:

P581
P534.42

李茜, 朱光有, 李婷婷, 艾依飞, 张岩, 王珊, 陈志勇, 田连杰. 塔里木盆地鹰山组白云岩成因与Mg同位素证据[J]. 地学前缘, 2023, 30(4): 352-375.

LI Xi, ZHU Guangyou, LI Tingting, AI Yifei, ZHANG Yan, WANG Shan, CHEN Zhiyong, TIAN Lianjie. Genesis of dolostone of the Yingshan Formation in Tarim Basin and Mg isotope evidence[J]. Earth Science Frontiers, 2023, 30(4): 352-375.

图/表 11

图1 塔里木盆地中央隆起构造区划图与奥陶系综合地层柱状图 (据文献[59]修改) a-塔里木盆地中央隆起地理位置; b-中央隆起构造区和取样钻井(ZG9和GC17)分布; c-塔里木盆地中央隆起奥陶系综合地层柱状图。

Fig.1 Tectonic zoning map of the Central Uplift (a, b) and composite stratigraphic column of Ordovician strata in Tarim Basin (c). Modified after [59].

图2 塔里木盆地中央隆起构造区中-下奥陶统鹰山组D1、D2和D3岩石学特征 a-D1,岩心呈深灰色,鹰2段下部,ZG9井,深度6 253.54 m; b- D1,白云石晶粒极小,晶粒之间排列紧密,鹰2段下部,ZG9井,深度6 254.22 m,正交光; c-D1,镜下水平纹层和窗格构造发育,鹰2段下部,ZG9井,深度6 251.60 m,正交光; d-D1,晶间孔被方解石或黏土矿物充填,孔隙发育差,鹰2段下部,ZG9井,深度6 251.00 m,单偏光; e-D2,岩心呈灰色,具有斑状或团块状结构,鹰3段上部,GC17井,深度6 284.60 m; f-D2,粉晶白云石和细晶白云石共同发育,白云石晶体呈自形-半自形,晶体之间呈镶嵌状接触,具有雾心亮边结构,鹰3段上部,GC17井,深度6 287.69 m,正交光; g-D2,具有残余颗粒结构,晶间溶孔较发育,鹰3段上部,GC17井,深度6 281.98 m,单偏光; h-D2,裂缝和缝合线发育,孔隙或裂缝中被沥青充填,鹰3段上部,GC17井,深度6 287.88 m,正交光; i-D3,岩心呈深灰色,鹰3段中部,GC17井,深度6 291.39 m; j-D3,具有原始碳酸盐岩(如灰岩)颗粒残余结构,鹰3段中部,GC17井,深度6 291.39 m,正交光; k-D3,白云石以细晶白云石为主,晶体呈镶嵌状接触,晶面浑浊,可见残余颗粒幻影,鹰3段中部,GC17井,深度6 289.60 m,单偏光; l-D3,残余砂屑结构显著,砂屑呈次圆状-圆状,鹰3段中部,GC17井,深度6 289.36 m,单偏光。

Fig.2 Petrological characteristics of rock types D1, D2 and D3

图3 塔里木盆地中央隆起构造区中-下奥陶统鹰山组D4、DL和L岩石学特征 a-D4,岩心呈浅灰色,断面颗粒较粗,鹰3段下部,GC17井,深度6 297.23 m; b-D4,晶粒直径大,晶体以半自形-他形为主,晶粒间呈紧密镶嵌分布,鹰3段下部,GC17井,深度6 298.40 m,单偏光; c-D4,白云石晶体具有微弱的波状消光,鹰3段下部,GC17井,深度6 292.37 m,正交光; d-DL,岩心呈深灰色和浅灰色不一的斑块状、条带状,鹰2段中部,ZG9井,深度6 249.95 m; e-DL,白云石和方解石共同发育,鹰2段中部,ZG9井,深度6 248.30 m,正交光; f-L,岩心呈深灰色-灰褐色,鹰2段上部,ZG9井,深度6 286.41 m; g-砂屑灰岩(L),砂屑颗粒大小不一,粒间孔缝发育,鹰2段上部,ZG9井,深度6 247.60 m,正交光; h-生物颗粒灰岩(L),主要由亮晶方解石和生物碎屑组成,鹰2段上部,ZG9井,深度6 241.80 m,单偏光/正交光; i-泥晶灰岩(L),镜下为黑色,由泥晶方解石组成,孔隙不发育,鹰2段上部,ZG9井,深度6 243.60 m。

Fig.3 Petrological characteristics of rock types D4, DL and L

表1 塔里木盆地中央隆起中一下奥陶统鹰山组碳酸盐岩微量元素、碳氧同位素及镁同位素含量测试数据及相关地球化学表征参数计算结果表

Table 1 Data of trace elemental and stable isotopic compositions on carbonate rock samples from the Yingshan Formation and related geochemical parameters by calculation

图4 塔里木盆地中央隆起中-下奥陶统鹰山组碳酸盐岩微量元素组成图

Fig.4 Trace element discrimination diagrams for petrological interpretation of carbonate rocks from the Yingshan Formation

图5 塔里木盆地中央隆起中-下奥陶统鹰山组碳酸盐岩碳、氧同位素交互图 (奥陶纪海水的δ13CV-PDB和δ18OV-PDB数据引自文献[83])

Fig.5 Isotopic discrimination diagrams for carbonate genesis in the Yingshan Formation. Seawater Δ13CVPDB and δ18OVPDB values adapted from [83].

图6 塔里木盆地中央隆起中-下奥陶统鹰山组碳酸盐岩镁同位素特征

Fig.6 Dual-isotope plots for sample quality assessment (a, b) and isotopic characteristics of carbonate rocks from the Yingshan Formation (c-f)

图7 塔里木盆地中央隆起构造区中-下奥陶统鹰山组高频沉积旋回划分图 D2-1-粉晶白云岩; D2-2-细晶白云岩; D4-1-中晶白云岩; D4-2-粗晶白云岩。

Fig.7 Composite chart showing correlation in the vertical direction between high-frequency sedimentary cycles and isotopic/geochemical proxies in the Yingshan Formation

图8 塔里木盆地中央隆起构造区中-下奥陶统鹰山组碳酸盐岩Mg同位素变化趋势与白云石流体迁移规律 a-云灰互层结构(L→DL→D); b-准同生白云岩结构(D1→D2); c-渗透回流白云岩结构(D1→D2→D3→D4→L); d-埋藏白云岩结构(D4→DL/D)。D2-1-粉晶白云岩; D2-2-细晶白云岩; D4-1-中晶白云岩; D4-2-粗晶白云岩。

Fig.8 Composite chart showing Mg isotope variation trends correlating with migration pathways of dolomitic fluid in the Yingshan Formation. (a) L→DL→D; (b) D1→D2; (c) D1→D2→D3→D4→L; (d) D4→DL/D).

图9 灰岩、白云岩与海水 Mg 同位素组成对比图 (据文献[35]修改)

Fig.9 Comparison of Mg isotopic compositions of limestone (blue), dolostone (yellow) and seawater (red). Modified after [35].

图10 塔里木盆地中央隆起构造区中-下奥陶统鹰山组白云岩形成演化模型 a-鹰山组鹰3段上部,海平面逐渐降低,强烈的蒸发作用促使在沉积旋回顶部形成富镁流体源区,随后富镁流体在密度差作用下垂向迁移至下伏地层,使得下伏灰岩地层逐层发生云化; b-鹰山组鹰3段下部,随着埋藏深度的增加,鹰山组鹰3段下部进入深埋藏阶段的孔隙流体和热液流体也有利于白云石化作用的持续进行; c-鹰山组鹰2段,海平面持续上升,海水混入富镁流体源区,导致流体Mg/Ca降低,白云石化作用逐渐降低,白云岩自下而上发育减少。

Fig.10 Models for the formation and evolution of dolostone in the upper 3rd (a), lower 3rd (b) and 2nd (c) members of the Yingshan Formation

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