Origination of Limestone-Marl Alternations from Qixia Formation of South China
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摘要: 华南中二叠统栖霞组沉积了一套特殊的碳酸盐岩地层, 该套地层富含有机质和硅质结核, 是中国南方四套区域性海相烃源岩之一.在野外露头上, 灰岩-泥灰岩韵律层因为其抗风化能力不同而受到广泛关注, 其在整个华南栖霞组分布广泛.其中, 灰岩层富含各种生物碎屑, 主要包括钙藻、有孔虫和腹足, 其次还有腕足, 棘皮类和介形虫, 偶尔见苔藓虫和三叶虫.灰岩层中较好的保存了易碎的钙质藻类, 说明灰岩的胶结作用发生在成岩早期, 没有明显压实作用的痕迹.泥灰岩以粒泥生物碎屑灰岩和黑色钙质泥岩为主, 主要的生物碎屑以腕足和介形虫为主.生物碎屑都非常破碎, 壳体大都平行层面, 颗粒之间发育大量压溶缝, 说明泥灰岩层经历过强烈的成岩压实作用.基于对灰岩-泥灰岩韵律层的生屑类型和成岩现象的分析, 提出差异成岩作用来解释该套地层的形成过程: 泥灰岩层中不稳定的文石在早期成岩过程中溶蚀, 然后迁移到灰岩层中形成方解石胶结灰岩层; 随后机械压实作用和化学压实作用主要发生在泥灰岩层中; 最终灰岩-泥灰岩层由于差异成岩作用导致其抗风化能力不同而形成不同的露头特征.其中文石溶蚀发生在海水埋藏环境, 有机质的分解为其提供了动力来源, 这与栖霞期较高的原始生产力相符合.Abstract: The Middle Permian of South China is a unique carbonate succession, which is rich in organic matter and chert nodule, and is one set of the most important marine source rocks. Limestone-marl alternations are widely distributed in this area. The limestones are rich in skeletal detritus, dominated by algae, foraminifera, and mollusks with subordinate amounts of brachiopods, echinoderms, and ostracods, and minor bryozoans and trilobites. Fragile skeletons such as calcareous algae were well preserved, indicating that cementation took place during early diagenesis with little diagenetic compaction. Marls are bioclastic wackestone or dark mudstone. Bioclasts are diverse, including remnants of brachiopods, ostracods and rare trilobites. Bioclastic flakes are oriented parallel to bedding planes, and thin-shelled fragments, e.g., ostracods, are broken due to compaction of the unlithified sediment. Between the particles are micrite and a large number of dissolution seams. As to the particular features of the limestone-marl alternations, it is inferred that differential diagenesis occurred between limestones and marls. Aragonite in marl layers was dissolved to cement limestone, which took place in shallow-burial realm. Mechanical compaction and then pressure dissolution were concentrated in the less cemented strata. The dissolution of aragonite in the shallow marine burial realm is thought to have been initiated by modification of the pore-water chemistry by bacterial oxidation of organic matter.
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Key words:
- limestone-marl alternations /
- aragonite /
- calcite /
- sedimentary rocks /
- Qixia Formation /
- South China
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图 1 华南栖霞期古地理和灰岩-泥灰岩韵律层分布
Fig. 1. The paleogeography of South China in Qixia stage and the distribution of limestone-marl alternations
图 2 四川广元上寺剖面栖霞组沉积环境
Fig. 2. The sedimentary environment of Qixia Formation at Shangsi section, Guangyuan, Sichuan
图 3 广元上寺剖面灰岩-泥灰岩韵律层特征
a.泥灰岩为主的韵律层；b.灰岩为主的韵律层；c.泥灰岩的压实现象；d.灰岩和泥灰岩互层；e.灰岩和泥灰岩互层；f.天青石(菊花石)
Fig. 3. Characteristics of limestone-marl alternations (LMA) from Shangsi section, Guangyuan, Sichuan
图 4 灰岩-泥灰岩韵律层的微相特征
a.灰岩，生屑很好的保存，52层；b.灰岩，易碎的米齐藻保存完好，54层；c.灰岩，生屑方向任意，54层；d.泥灰岩，注意生物碎屑的定向性，52层；e.泥灰岩，生屑破碎，有机质富集，54层；f.泥灰岩，壳体内充填会内而没有被压扁，54层
Fig. 4. Sedimentary microfacies of limestone-marl alterations
图 5 灰岩-泥灰岩韵律层的形成过程(据Westphal et al., 2000)
Fig. 5. The formation process of limestone-marl alternations
表 1 广元上寺剖面灰岩-泥灰岩韵律层生屑颗粒含量
Table 1. The content of bioclastic grains of limestone-marl alternations from Shangsi section
标本号 岩性 低镁方解石 文石 高镁方解石 介形虫 腕足 有孔虫 软体动物 钙藻(%) 棘皮动物 Pgy-R-51-1′ L 10 3 0 0 0 0 Pgy-R-51-1 M 50 20 0 0 5 0 Pgy-R-54-1 L 15 6 0 5 35 5 Pgy-R-54-1′ M 150 30 10 0 3 0 Pgy-R-54-2 L 35 10 50 10 3 0 Pgy-R-54-2′ M 100 50 15 0 3 0 Pgy-R-54-3′ L 80 15 30 0 3 0 Pgy-R-54-3 M 250 20 15 5 1 3 Pgy-R-55-3 L 35 5 40 10 7 3 Pgy-R-55-3′ M 100 20 10 0 7 5 Pgy-R-60-2 L 30 20 3 0 0 0 Pgy-R-60-2′ M 125 40 11 0 0 0 Pgy-R-61-1 L 50 23 8 0 3 0 Pgy-R-61-1′ M 100 30 90 0 0 0 Pgy-R-62-2 L 10 15 0 0 1 0 Pgy-R-62-2′ M 100 40 28 0 0 0 Pgy-R-65-1 L 25 40 0 0 1 1 Pgy-R-65-1′ M 60 35 0 0 0 0 Pgy-R-70-1 L 20 5 12 0 0 0 Pgy-R-70-1′ M 15 15 6 0 0 0 Pgy-R-70-3 L 60 30 3 0 0 0 Pgy-R-70-3′ M 20 15 0 0 0 0 注：L代表灰岩；M代表泥灰岩. 
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表 2 二叠纪海水主要离子浓度(mol/kg H2O)
Table 2. The main ion concentration of Permian seawater
年龄(Ma) Na+ K+ Ca2+ Mg2+ Cl- SO42- Mg2+/Ca2+ 0 485 11 11 55 565 29 5.2 258~251 469 10 14 52 565 23 3.7 283~274 439 10 17 60 565 19 3.5 296~283 461 10 15 52 565 20 3.5 245 478 13 14 47 565 25 3.5 255 477 15 15 43 565 23 2.8 265 477 15 15 43 565 23 2.8 275 481 12 12 52 565 27 4.3 285 476 16 17 40 565 21 2.4 296~251 460 11 20 54 550 20~45 2.7 注：据Hardie, 1996; Horita et al., 1991 ;Lowenstein et al., 2005 .
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