Characteristics and Environmental Interpretation of Cone-in-Cone Structure, Early Cretaceous Bayingebi Formation, Celaomiao Depression
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摘要: 为了全面了解测老庙坳陷早白垩世叠锥构造的沉积特征，并探讨其成因及形成环境等问题，运用野外露头实测、光薄片观察、X射线衍射分析、阴极发光照相、扫描电镜照相等方法，发现叠锥构造发育于钙质结核外侧，覆盖所有方向，呈放射状，直圆锥锥顶指向结核中心；叠锥矿物成分主要为纤维状低镁方解石，纤维状方解石呈锥形套叠，具波状消光；阴极发光显微镜下呈均一的棕红色，不具微量元素分异和析出的成岩色带；叠锥结核的发育规模明显受制于原生沉积环境.结果表明叠锥结核的发育具有明显的阶段性；其发育的原生沉积环境应为水深在5~30 m、水体能量较高的滨浅湖沉积环境.推测叠锥构造的形成可能是同沉积期生物沉积作用和胶结作用，以及后期上覆岩层静压力共同作用的结果.Abstract: To better understand the sedimentary characteristics of the cone-in-cone structure in the outcrop areas, and to explore the causes of the formation and the environmental issues of the cone-in-cone structure, we employ methods such as outcrop measure, polished thin section observation, X-ray diffraction analysis, cathode-ray luminescence, electronic scanning in this study. It is discovered that cone-in-cone structure develops radially around the calcareous concretions, with conical apex pointing straight to the concretion center; the major mineral composition of cone-in-cone structure is fibrous low magnesium calcite, with fibrous calcite crystals being cone-shaped nest, with wavy extinction which appears uniform red-brown under cathodoluminescence microscopy without diagenetic ribbon with trace element fractionation and precipitation. The developing scale of cone-in-cone concretions is in the control of primary sedimentary environment obviously. It is considered that the growth of cone-in-cone concretions has distinct stages; the original sedimentary environment should be shallow lake sedimentary environment with about 5-30 m depth and relatively higher energy. It is concluded that the formation of cone-in-cone structure is a result of synsedimentary biological deposition, cementation and later overburden static pressure.
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Key words:
- cone-in-cone /
- Bayingebi Formation /
- Celaomiao depression /
- sedimentology /
- environmental geology
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图 1 国内外典型叠锥样品
a.国外学者所展示的典型叠锥样品，取样位置不明，据Selles-Martinez(1994)；b.硅质叠锥样品，摩洛哥Erfoud东南部Hamada地区，Lower Visean Merdani Formation，据Lugli et al.(2005)；c.发育于湖泊滨岸带泥岩中的叠锥，伊犁盆地三工河组(取样点坐标：44°00′35.23″ N；81°03′ 38.52″E)
Fig. 1. Typical cone-in-cone samples in the domestic and overseas
图 2 内蒙古测老庙地区地质构造简图及研究区位置
图a中：1.上白垩统乌兰苏海组；2.下白垩统苏红图组；3.下白垩统巴音戈壁组；4.下元古界宝音图群；5.中元古界渣尔泰山群；6.燕山期黑云母花岗岩；7.燕山期二长花岗岩；8.印支期伟晶状白云母花岗岩；9.华力西期黑云母花岗岩；10.花岗闪长岩；11.华力西期黑云母花岗岩；12.华力西期花岗闪长岩；13.华力西期石英闪长岩；14.华力西期角闪辉长岩；15.加里东期伟晶状白云母花岗岩；16.黑云母斜长变粒岩；17.不整合地质界线；18.蚀变断裂破碎带；图b中：浅蓝色线为1 700 m等高线，向北东方向高程降低；红色曲线为岩体与下白垩统地层之间的不整合界线；深蓝色线为野外实测路线；黄色虚线为叠锥结核统计路线；中国地图据中华人民共和国地图(1∶5 900 000)，中国地图出版社，2012年第1版
Fig. 2. Geological structure sketch of Celaomiao area, Inner Mongolia and the position of the study area
图 3 叠锥赋存地层各岩相特征
a.红色泥岩(受滨浅湖改造后的风化壳)覆盖在灰白色花岗岩体上，黄色虚线中为发育叠锥构造的钙质结核；b.红色泥岩，结构破碎，无可视节理表现，断口呈贝壳状，含有少量有机质，见植物根迹组构；c.灰绿色泥岩，厚度较薄，结构破碎，与红色泥岩呈相变接触；d.深灰色粉砂质泥岩，成层性较好，具波状层理，含有大量植物碎屑，见Skolithos linearis生物遗迹构造；e.灰黑色薄层油页岩，有机质含量高
Fig. 3. Lithofacies characteristics of the cone-in-cone bearing strata
图 4 发育于受滨浅湖改造后的风化壳的叠锥结核，巴音戈壁组中段，下白垩统
a.研究区出露最大的结核，叠锥构造呈放射状发育于结核外侧，锥顶指向结核中心；b.直圆锥锥顶指向结核中心；c.叠锥构造细部特征，同轴套叠的圆锥顶角基本一致，锥的内侧面有肋骨形的棱和沟槽；d.白色虚线中为被包裹在叠锥结核中的花岗岩风化壳碎块
Fig. 4. The cone-in-cone concretions which appear in the granite weathering crust modified by shallow lake, K1by2
图 5 叠锥构造的显微镜下特征
a.纤维状低镁方解石，纤维直径为5~10 μm，扫描电镜；b.叠锥纵切面，纤维状方解石呈“V”字形套叠，多个锥体套叠使得锥底边缘在纵剖面上呈锯齿状(白色虚线)，见少量石英、长石颗粒被方解石包裹其中(红色圆圈中)，正交偏光；c.锥体的顶端，纤维状方解石呈放射状散开，正交偏光；d.纤维状方解石将大块岩屑包裹在其中，正交偏光
Fig. 5. The microscopic characteristics of cone-in-cone structure
图 6 叠锥结核C1的整体形态及其各期次内部特征
Fig. 6. The entire morphologies and the internal characteristics of each issue of cone-in-cone concretion C1
图 7 叠锥结核及其所赋存的地层各项特征变化趋势
a.叠锥结核C1的整体形态；a'.叠锥结核C1各期次的划分；b.第Ⅰ期次泥晶灰岩，结构均一致密，方解石含量高，正交偏光；b'.第Ⅰ期次泥晶灰岩矿物组成；c.第Ⅱ期次叠锥灰岩，方解石呈纤维状且出现明显定向性，可见“V”字形套叠纹层，有碎屑颗粒被包裹在纹层中，正交偏光；c'.第Ⅱ期次叠锥灰岩矿物组成；d.第Ⅲ期次叠锥灰岩，方解石呈纤维状，内部结构不均一，羽状形态与“V”字形纹层形态交替出现，正交偏光；d'.第Ⅲ期次叠锥灰岩矿物组成；e.第Ⅳ期次叠锥灰岩，纤维状方解石定向性极好，呈“V”字形套叠，锯齿状裂隙等间距出现，正交偏光；e'.第Ⅳ期次叠锥灰岩矿物组成
Fig. 7. The characteristics of cone-in-cone concretions and their bearing strata
图 8 测老庙坳陷西部露头区叠锥结核形成环境演化模式
Fig. 8. The patterns of cone-in-cone concretions formation environment, western Celaomiao depression
图 9 鄂尔多斯盆地东北部叠锥构造(a)及同层暗色泥岩(b)
Fig. 9. The cone-in-cone structure (a) and the mudstone symbiosed (b) in the northeast of Ordos basin
表 1 叠锥赋存地层各岩相矿物成分
Table 1. The mineral composition of each lithofacies of the cone-in-cone bearing strata
岩相 石英(%) 长石(%) 蒙脱石(%) 绿泥石(%) 伊利石(%) 高岭石(%) 方解石(%) 白云石(%) 红色泥岩 51 7 0 15 15 10 2 0 灰绿色泥岩 44 6 15 10 15 10 0 0 深灰色粉砂质泥岩 37 17 20 5 10 5 3 3 油页岩 39 8 25 10 10 0 5 3 
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表 2 不同岩性、不同沉积构造与相应水深对应关系
Table 2. The correspondences between different lithology, sedimentary structure and corresponding depth
岩性 水深(m) 沉积构造 水深(m) 蒸发岩 0~5 大型交错层理 0.5~5.0 砾岩、砂岩 1~10 大型交错层理 0.5~5.0 鲕粒灰岩 1~15 波状层理、平行层理 5~20 泥质粉砂岩 5~20 波状层理、平行层理 5~20 礁灰岩 5~25 水平层理 ＞17 暗色泥岩 ＞20 鲍马序列、槽模、丘状交错层理 ＞30 油页岩 ＞50 鲍马序列、槽模、丘状交错层理 ＞30 注：据张才利等(2011).
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