新疆阿合奇地区志留系砂岩地球化学特征及大地构造背景<sup>*</sup>

陈小双, 吕奥, 宋贺民, 刘磊, 杨宝忠, 侯红星. (2018)新疆阿合奇地区志留系砂岩地球化学特征及大地构造背景^* [J]. 古地理学报, 20(2): 271-284
Chen Xiao-Shuang, Lü Ao, Song He-Min, Liu Lei, Yang Bao-Zhong, Hou Hong-Xing. (2018)Geochemical characteristics and tectonic history of the Silurian sandstones in Akeqi area,Xinjiang[J]. Journal Of Palaeogeography, 20(2): 271-284. 复制到剪切板

Doi: 10.7605/gdlxb.2018.02.020
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新疆阿合奇地区志留系砂岩地球化学特征及大地构造背景^*

陈小双¹, 吕奥¹, 宋贺民², 刘磊¹, 杨宝忠^1,², 侯红星³

1 中国地质大学(武汉)地球科学学院,湖北武汉 430074

2 中国人民武装警察部队黄金第七支队,山东烟台 264004

3 中国人民武装警察部队黄金第二总队, 河北廊坊 065000

第一作者简介陈小双,男,1992年生,硕士研究生,构造地质学专业。E-mail: 823376471@qq.com。

通讯作者简介杨宝忠,男,1969年生,中国地质大学(武汉)地球科学学院副教授,主要从事沉积地质学的教学及研究。E-mail: Bzyang@cug.edu.cn。

收稿日期:2017-05-12

基金资助:*中国地质调查局地调协作项目“新疆柯坪地区晚古生代地层综合研究”(编号: 2015010038)资助

摘要

塔里木板块西北缘沉积地层的研究,对于恢复南天山洋的演化过程有重要意义。文中利用岩石地球化学的手段,对新疆阿合奇地区志留系砂岩进行物源和构造背景分析。研究表明,阿合奇地区志留系砂岩样品的 SiO₂含量范围变化较大,为 61.97%~93.91%,平均含量为 76.76%;稀土元素球粒陨石标准化配分型式为右倾型,( La/Yb) _N值较高,δ Eu值较低, Ce异常不明显。中—顶志留统塔塔埃尔塔格组砂岩的成熟度高于下志留统柯坪塔格组。地球化学物源分析图解和大地构造背景判别表明: 研究区沉积物源区逐渐由活动型向稳定型转换,下志留统部分沉积物来自于火成岩物源区,具有主动大陆边缘和大陆岛弧性质;中—顶志留统沉积物全部来自于成熟大陆的石英岩沉积物源区。结合广泛分布的奥陶系—志留系平行不整合,认为晚奥陶世研究区为活动大陆边缘,南天山洋盆向南俯冲到塔里木板块之下;早志留世,向南俯冲结束,研究区大地构造背景开始由活动大陆边缘向稳定的被动大陆边缘转换,来自活动型物源区的沉积物逐渐减少,稳定型物源区的碎屑物质逐渐增多;中—末志留世,研究区构造背景完全转变为被动大陆边缘,碎屑物质全部来自于稳定型物源区。上述成果表明,南天山洋的演化过程中确实存在双向俯冲。

关键词: 新疆; 阿合奇地区; 志留系; 南天山洋; 双向俯冲; 活动大陆边缘

中图分类号:P542,P597 文献标志码:A 文章编号:1671-1505(2018)02-0271-14

Geochemical characteristics and tectonic history of the Silurian sandstones in Akeqi area,Xinjiang

Chen Xiao-Shuang¹, Lü Ao¹, Song He-Min², Liu Lei¹, Yang Bao-Zhong^1,², Hou Hong-Xing³

1 School of Earth Sciences,China University of Geosciences(Wuhan),Wuhan 430074,Hubei

2 The 7th Gold Detachment of Chinese Armed Police Force,Yantai 264004,Shandong

3 The 2nd Gold Crop of Chinese Armed Police Force, Langfang 065000, Hebei;

About the first author Chen Xiao-Shuang,born in 1992,is a master degree candidate at the School of Earth Sciences,China University of Geosciences(Wuhan). He is mainly engaged in the research of tectonic geology. E-mail: 823376471@qq.com.

About the corresponding author Yang Bao-Zhong,born in 1969,is an associate professor at the School of Earth Sciences,China University of Geosciences(Wuhan). He is currently engaged in the research of sedimentary geology. E-mail: Bzyang@cug.edu.cn.

Fund:[Financially supported by the Geological Survey Collaboration Projects of China Geological Survey Bureau “Comprehensive Research of Late Paleozoic Strata in Kalpin Region,Xinjiang”(No.2015010038)]

Abstract

The South Tianshan Orogenic Belt is located between the Tarim Plate and Yili-Central Tianshan Plate. The tectonic evolution of the South Tianshan Ocean in the Paleozoic has long been debated. Litho-geochemical features of the major and trace elements of the Silurian sandstones from Akeqi area, northwestern margin of the Tarim Plate of Xinjiang,show that Chondrite-normalized REE distribution patterns of the samples are all right skewed, with high(La/Yb)_N value, low δEu value, and negative Ce anomaly. The maturity of the sandstones from the Middle to Top Silurian Tataertage Formation is higher than the samples from the Lower Silurian Kepingtage Formation. The provenance and tectonic setting of the sandstones were evaluated using ternary diagrams that highlight their geochemical characteristics. The results suggest that the provenance of the Akeqi area gradually transformed from active provenance to stable provenance. Some sediments from the Kepingtage Formation are sourced from active continental margin and continental island arc, indicating felsic igneous provenance; Sediments from the Tataertage Formation were sourced from quartzite sediment provenance of mature continent. Combined with widely distributed parallel unconformities between the Ordovician and the Lower Silurian, it can be inferred that the Akeqi area was located in an active continental margin, the South Tianshan Ocean subducted southward beneath the Tarim Plate shortly during the Late Ordovician, which provided the active provenance for the study area. From the Early Silurian, as southwards subduction ended, the tectonic setting of Akeqi area transformed from active continental margin to stable passive continental margin. Sediments from active and stable provenances gradually decreased and increased, respectively. During the deposition of Middle to Top Silurian succession, tectonic setting of the Akeqi area completely transformed to stable passive continental margin, so that sediments were exclusively sourced from stable provenances. In conclusion, this study proposes that bidirectional subduction was developed during the evolution of the South Tianshan Ocean within the Paleozoic.

Key words: Xinjiang; Akeqi area; Silurian; South Tianshan Ocean; bidirectional subduction; active continental margin

文章图片

天山造山带位于中国新疆地区, 是中亚造山带的重要组成部分, 也是国内研究的热点地区。天山造山带北邻准噶尔板块, 南部为塔里木板块, 在地质上根据南北2条缝合带从北向南依次划分为北天山、中天山及南天山造山带。南天山造山带的构造演化过程是国内外争议的焦点, 其中最关键的地质问题是南天山洋的俯冲方式及最终闭合、碰撞造山的时间。对于这一问题, 国内外许多学者从岩相学、锆石年代学、地球化学等方面进行了深入研究, 并提出了不同的观点(高俊等, 1995a; 李曰俊等, 2009; Charvet et al., 2011; Han et al., 2011; 蔡东升和卢华复, 2012; Ma et al., 2013; Xiao et al., 2013)。对于南天山洋盆的俯冲方式, 多数学者认为南天山洋盆晚寒武世— 奥陶纪开始向北俯冲至中天山— 伊犁板块之下, 古生代塔里木板块北缘一直为被动大陆边缘(高俊等, 1995b; Han et al., 2011; 高晓芬等, 2014; Xia et al., 2014); 另有部分学者通过对南天山造山带南缘及塔里木板块北缘出露的岩浆岩研究发现, 南天山洋在构造演化过程中存在双向俯冲, 在向北俯冲的同时, 向南短暂地俯冲到塔里木板块之下, 塔里木板块北缘在早古生代存在活动大陆边缘(Ma et al., 2013; 郭瑞清等, 2013a, 2013b; 张英利等, 2014)。所以塔里木板块西北缘在早古生代是否存在活动大陆边缘的构造背景, 是解决问题的关键。但是由于造山带的隆升和剥蚀导致地质记录保存不完整, 使得来自造山带岩浆岩和变质岩岩石学以及构造地质学的研究受到了制约; 而与造山带耦合的塔里木盆地内部的沉积地层保存较完好, 较完整地保留了南天山洋盆演化的地质信息(王松, 2014), 因此对塔里木板块西北缘沉积地层的研究, 对于恢复南天山洋盆的演化过程有重要意义。文中利用岩石地球化学的手段, 对新疆阿合奇地区志留系砂岩进行物源和构造背景分析, 以便进一步对南天山洋盆的构造演化及俯冲方式进行讨论。

1 区域地质概况

研究区位于新疆阿克苏市以西约200, km的阿合奇地区, 处于托什干河以南(图 1)、塔里木盆地的西北缘, 北部毗邻南天山造山带, 位于南天山造山带和塔里木板块的交汇处, 地质演化受到了二者的共同影响(图 2)。以托什干河为界, 阿合奇地区北部地层属阔克沙勒岭地层小区, 南部地层属柯坪地层小区。研究区位于柯坪地层小区, 广泛发育古生代地层, 奥陶系— 二叠系均有发育, 保留了大量盆地及周边构造单元演化的地质信息, 是研究南天山洋构造演化的理想区域, 但是一直以来由于受到自然地理条件的限制, 研究程度较低。

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	图 1 新疆阿合奇地区志留系剖面位置Fig.1 Location of the Silurian section in Akeqi area, Xinjiang

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	图 2 新疆阿合奇地区大地构造位置及古生界地层划分(修改自李曰俊等, 2009)Fig.2 Tectonic location and stratigraphic column of Akeqi area, Xinjiang(modified from Li et al., 2009)

研究区内志留系分布广泛, 根据野外地质调查及前人资料可划分为下志留统柯坪塔格组(S₁k)和中— 顶志留统塔塔埃尔塔格组(S_2-4t), 2个组之间为整合接触。柯坪塔格组(S₁k)在测区内发育不完整, 与柯坪县大湾剖面对比, 下部缺失部分地层, 与下伏奥陶系为平行不整合接触, 局部呈断层接触(图 3-a)。王庆同等(2014)在研究区柯坪塔格组底部发现了笔石化石, 确定柯坪塔格组形成时代为早志留世兰多维列期。本次工作在研究区西北部库尔喀克库勒测制了下志留统柯坪塔格组(S₁k)剖面(图 4-a), 将该组划分为2个岩性段: 柯坪塔格组一段为灰黑色细粒岩屑砂岩夹粉砂岩、粉砂质泥岩, 组成粉砂岩— 细砂岩— 粉砂岩— 细砂岩沉积旋回, 偶夹2或3层灰白色中厚层中粒岩屑砂岩或岩屑石英砂岩, 不整合覆盖于上奥陶统印干组(O₃y)灰白色白云岩、白云质灰岩之上, 为陆棚沉积; 柯坪塔格组二段岩性为灰绿色中粒岩屑砂岩, 夹灰白色中粒岩屑砂岩或岩屑石英砂岩, 偶夹粉砂岩, 组成多个向上变薄的沉积旋回, 砂岩中见交错层理(图 3-b), 为近滨沉积。在研究区东南部阿尔帕确依契克测制了中— 顶志留统塔塔埃尔塔格组(S_2-4t)剖面(图 4-b), 下部岩性为中粒岩屑石英砂岩或石英砂岩夹细砂岩、粉砂岩, 上部岩性为紫红色细砂岩、粉砂岩夹灰绿色、灰白色中粒岩屑石英砂岩, 整体为向上变细的沉积序列, 为临滨— 前滨沉积, 向上与中下泥盆统依木干他乌组(D_1-2y)紫红色中— 细粒石英砂岩夹紫红色粉砂岩、泥岩整合接触(图 3-c)。志留系垂向演化序列上沉积相的变化, 说明整体上为一个海进— 海退序列, 以塔塔埃尔塔格组紫红色砂岩的出现作为转折, 砂岩整体颜色由灰绿色转变为紫红色, 说明气候由温暖湿润向干旱炎热转化(刘景彦, 2012)。

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图 3 新疆阿合奇地区志留系沉积学和岩石学特征
a— 柯坪塔格组(S₁k)与印干组(O₃y)呈平行不整合接触; b— 柯坪塔格组(S₁k)砂岩中的交错层理; c— 依木干他乌组(D_1-2y)与塔塔埃尔塔格组(S_2-4t)呈整合接触; d— 柯坪塔格组(S₁k)岩屑砂岩, 正交光; e— 柯坪塔格组(S₁k)岩屑砂岩, 正交光; f— 塔塔埃尔塔格组(S_2-4t)石英砂岩, 正交光Fig.3 Field and microscope photos showing sedimentary and petrological characteristics of the Silurian in Akeqi area, Xinjiang

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	图 4 新疆阿合奇地区志留系实测剖面 a— 库尔喀克库勒下志留统柯坪塔格组(S₁k)实测剖面图(PM44); b— 阿尔帕确依契克中— 顶志留统塔塔埃尔塔格组(S_2-4t)实测剖面图(PM51)Fig.4 Measured stratigraphic sections of the Silurian in Akeqi area, Xinjiang

笔者对志留系砂岩进行了薄片鉴定: 砂岩由碎屑物质和填隙物组成, 碎屑主要由石英、岩屑和少量长石组成, 含有微量的云母、电气石、锆石等, 磨圆差, 次棱角状— 棱角状, 分选较好, 填隙物以泥质胶结物为主, 其次为硅质、钙质胶结物等, 含量为12%~25%。柯坪塔格组一段碎屑物质以单晶石英为主, 含量为60%~75%; 长石含量为1%~3%, 其中斜长石含量高于钾长石含量; 岩屑含量为20%~40%, 主要由泥岩、碳酸盐岩等沉积岩屑组成, 含有少量的变质岩屑及酸性喷出岩屑。柯坪塔格组二段相较于一段, 长石含量相同, 石英及岩屑含量略高, 填隙物减少。与柯坪塔格组相比, 塔塔埃尔塔格组砂岩石英含量较高, 达90%~96%, 且分布较为集中; 岩屑含量明显减少, 仅3%~5%, 变质岩屑及酸性喷出岩屑几乎消失, 说明中— 顶志留统砂岩成熟度高于下志留统。

2 地球化学特征

2.1 测试方法

为研究志留系砂岩物源特征, 对下志留统柯坪塔格组及中— 顶志留统塔塔埃尔塔格组实测剖面进行了逐层采样(采样位置见图 4), 样品岩性主要为灰黑色、灰绿色细砂岩、中砂岩, 共采集地球化学样品33件。岩石全岩测定由核工业北京地质研究院分析测试研究中心完成。主量元素测试采用X射线荧光光谱法(XRF), 测试仪器为飞利浦PW2404X射线荧光光谱仪, 依据GB/T14506.3-2010硅酸盐岩石化学分析方法测定, 相对偏差小于5%。微量元素依据DZ/T0223-2001电感耦合等离子体质谱(ICP-MS)方法通则测定, 在Finnigan MAT的HR-ICP-MS(Element Ⅰ )上进行, 分析精度优于3%。

2.2 主量元素特征

砂岩主量元素数据如表 1。志留系砂岩的SiO₂含量范围变化较大, 为61.97%~93.91%, 平均含量为76.76%; 柯坪塔格组砂岩SiO₂平均含量为72.98%, 塔塔埃尔塔格组平均含量为84.32%, 说明中— 顶志留统砂岩中石英或者富含SiO₂的矿物含量明显增大。志留系砂岩中Al₂O₃含量为3.08%~15.11%, 平均含量为10.32%, 质量分数高, 说明其与长石、云母、黏土矿物等富铝的矿物有关; 塔塔埃尔塔格组Al₂O₃平均含量为6.42%, 明显低于柯坪塔格组的平均含量12.12%, 说明富铝的矿物含量减少。志留系砂岩中Fe₂O₃平均含量为3.72%, MgO平均含量为1.36%, CaO平均含量为0.89%, Na₂O平均含量为1.30%, K₂O平均含量为2.34%, MnO平均含量为0.09%, TiO₂平均含量为0.51%, FeO平均含量为2.49%, P₂O₅平均含量为0.13%, Fe₂O₃平均含量为6.48%; 塔塔埃尔塔格组砂岩Fe₂O₃、MgO、Na₂O、K₂O含量明显低于柯坪塔格组, 说明中— 顶志留统砂岩成熟度较高。Al₂O₃/SiO₂值可以作为碎屑沉积物成熟度的指标(Roser and Korsch, 1988), 样品Al₂O₃/SiO₂值在0.02~0.29之间, 整体上为负相关性, 柯坪塔格组样品Al₂O₃/SiO₂均值为0.17, 位于长石砂岩(0.11)和杂砂岩(0.20~0.23)之间; 塔塔埃尔塔格组样品Al₂O₃/SiO₂均值为0.08, 位于石英砂岩(0.01~0.04)和长石砂岩(0.11)之间, 说明砂岩成熟度增加(Condie et al., 1992)。样品中Na₂O、K₂O含量较低, K₂O/Na₂O值除1个样品为8.85外, 其余在0.44~4.29之间, 平均为2.07。柯坪塔格组CIA值为36.78~70.36、平均值为61.87, 塔塔埃尔塔格组CIA值为50.63~74.89、平均值为65.25, 志留系均值为63.00, 说明源区经受了低— 中等程度的化学风化。

表 1 新疆阿合奇地区志留系砂岩主量元素地球化学数据(%) Table1 Geochemical data of major elements of sandstones from the Silurian in Akeqi area, Xinjiang(%)

样品号	SiO₂	Al₂O₃	Fe₂O₃	MgO	CaO	Na₂O	K₂O	MnO	TiO₂	P₂O₅	FeO	烧失量
b875	73.33	11.84	4.14	1.51	1.150	1.89	2.62	0.073	0.572	0.132	3.25	2.60
b877	72.24	12.16	4.32	1.57	1.310	1.91	2.70	0.058	0.578	0.128	3.30	2.88
b880	78.83	9.40	3.73	1.25	0.631	1.48	2.02	0.048	0.439	0.122	2.80	1.99
b882	73.77	12.35	4.40	1.66	0.418	1.83	2.71	0.050	0.547	0.137	3.20	2.09
b884	79.03	7.81	2.87	1.01	2.530	1.54	1.49	0.185	0.398	0.117	1.80	2.97
b887	71.14	13.82	4.45	1.77	0.387	1.93	3.27	0.059	0.629	0.131	3.05	2.36
b889	71.18	13.69	4.65	1.80	0.413	1.83	3.21	0.070	0.655	0.141	3.10	2.31
b890	71.66	13.65	4.46	1.69	0.298	1.69	3.38	0.048	0.631	0.144	2.95	2.31
b891	74.17	11.92	4.27	1.63	0.577	1.77	2.64	0.056	0.602	0.147	3.00	2.18
b893	87.40	5.29	2.56	0.77	0.490	0.92	0.97	0.038	0.281	0.106	1.65	1.16
b896	61.97	17.76	7.13	2.31	0.616	1.01	4.33	0.209	0.741	0.253	4.90	3.62
b897	77.87	10.29	3.56	1.28	0.508	1.37	2.31	0.047	0.523	0.138	2.40	2.08
b898	66.70	15.17	5.52	2.13	0.706	1.90	3.57	0.069	0.709	0.158	3.55	3.21
b900	65.18	15.08	5.26	2.56	1.140	1.77	3.46	0.081	0.686	0.127	3.85	4.34
b902	69.54	14.12	4.88	1.89	0.450	1.71	3.33	0.062	0.641	0.134	3.60	3.02
b904	67.52	15.10	5.03	2.09	0.482	1.89	3.52	0.062	0.713	0.158	3.65	3.37
b906	85.91	6.24	1.96	0.66	0.653	1.20	1.28	0.033	0.346	0.122	1.50	1.56
b908	66.46	14.77	5.25	2.11	1.300	1.47	3.54	0.082	0.714	0.151	3.95	4.01
b910	67.81	14.53	5.03	2.03	1.060	1.56	3.43	0.080	0.694	0.151	3.75	3.50
b913	69.01	14.09	5.03	2.01	0.576	1.94	3.20	0.078	0.677	0.154	3.90	3.13
b916	81.92	5.48	1.72	0.95	3.480	1.32	0.84	0.156	0.345	0.151	1.40	3.41
b920	72.97	12.11	4.21	1.57	1.020	1.90	2.70	0.066	0.574	0.124	3.30	2.63
GP1602	77.58	10.13	4.98	1.04	0.228	0.82	2.53	0.036	0.625	0.065	1.65	1.96
GP1603	81.57	8.71	3.18	0.99	0.138	0.82	2.04	0.084	0.632	0.065	1.05	1.69
GP1604	73.74	12.75	4.25	1.37	0.145	1.16	3.11	0.074	0.696	0.051	1.25	2.64
GP1605	91.11	3.71	1.20	0.40	0.516	0.36	0.90	0.173	0.239	0.026	0.45	1.37
GP1606	82.88	8.58	2.23	0.84	0.169	1.02	1.90	0.046	0.451	0.075	1.45	1.69
GP1607	91.52	3.77	1.87	0.57	0.101	0.10	0.85	0.054	0.258	0.032	1.15	0.78
GP1608	86.09	6.03	2.48	0.78	0.331	0.56	1.22	0.069	0.282	0.042	1.85	2.09
GP1609	84.98	3.08	1.13	0.48	4.290	0.69	0.43	0.301	0.150	0.433	0.75	3.95
GP1610	93.91	1.85	0.72	0.34	1.150	0.48	0.21	0.075	0.078	0.065	0.45	1.11
GP1611	75.39	11.25	4.73	1.43	0.489	0.70	2.70	0.088	0.589	0.146	3.45	2.48
GP1612	88.72	4.10	1.44	0.49	1.460	0.45	0.93	0.151	0.263	0.052	0.80	1.86

表 1 新疆阿合奇地区志留系砂岩主量元素地球化学数据(%) Table1 Geochemical data of major elements of sandstones from the Silurian in Akeqi area, Xinjiang(%)

2.3 微量元素和稀土元素特征

砂岩微量元素数据如表 2所示。志留系微量元素分布特征与上地壳组成相似, 但是高场强元素Nb、Ta含量明显偏低, 大离子亲石元素Sr强烈亏损, Cr元素强烈富集。

表 2 新疆阿合奇地区志留系砂岩微量元素和稀土元素地球化学数据表(μ g/g) Table2 Geochemical data of trace elements and rare elements of sandstones from the Silurian in Akeqi area, Xinjiang(μ g/g)

地层	样品号	Sc	V	Cr	Co	Ni	Rb	Sr	Th	Nb	Hf	Ta	Pb	U	Zr		La	Ce		Pr	Nd
	b875	8.25	60.4	43.0	10.50	21.7	109.0	88.9	14.2	16.30	10.30	1.240	25.7	2.97	338		49.6	98.1		11.7	42.3
	b877	8.52	70.4	48.4	11.00	24.4	109.0	70.6	13.0	15.1	9.68	1.150	16.4	3.02	336		51.0	90.9		10.5	42.9
	b880	6.45	45.4	36.5	6.37	16.4	76.8	53.9	11.5	11.90	7.31	0.864	20.5	2.48	281		44.9	90.0		10.2	39.1
	b882	9.03	78.3	62.0	10.30	21.6	109.0	59.0	12.7	14.80	9.22	1.010	7.4	2.38	339		49.2	96.6		11.0	41.0
	b884	7.74	53.5	35.8	7.96	18.7	61.8	76.8	12.4	11.10	11.40	0.756	61.1	2.16	421		44.4	88.5		10.3	39.2
	b887	10.30	79.0	54.6	12.20	22.9	130.0	66.7	13.8	17.00	9.83	1.230	14.0	2.50	383		47.9	94.5		11.2	39.0
	b889	11.00	88.6	57.3	12.30	24.5	135.0	62.4	15.6	16.80	11.20	1.090	23.4	2.74	429		52.8	106.0		12.2	45.5
	b890	10.40	82.1	53.4	10.70	23.3	137.0	61.4	14.4	16.40	9.86	1.140	8.4	2.23	407		53.1	106.0		11.8	44.4
	b891	9.92	70.8	52.2	8.89	22.1	110.0	67.1	13.8	15.50	10.90	1.130	16.4	2.30	398		47.0	91.0		10.9	40.7
	b893	4.59	40.4	37.8	4.35	11.3	37.9	40.7	8.3	8.34	7.42	0.520	20.6	1.42	287		29.9	60.4		7.2	27.3
	b896	16.10	136.0	93.5	19.70	38.3	196.0	84.3	19.8	21.50	12.00	1.520	31.1	3.21	427		72.8	131.0		15.5	60.3
	b897	9.61	67.8	64.1	8.33	19.5	101.0	63.5	14.8	14.10	13.30	0.903	27.7	2.32	499		43.1	83.1		9.6	37.8
	b898	11.40	85.9	71.2	12.90	28.2	143.0	75.4	14.1	16.80	10.40	1.030	16.6	2.22	367		50.9	93.7		10.7	41.7
	b900	11.40	88.2	56.1	14.50	28.9	160.0	69.0	14.5	17.60	10.30	0.983	21.3	2.53	356		54.4	100.0		11.8	44.6
	b902	10.30	86.3	61.1	13.60	27.7	149.0	65.8	14.4	17.50	9.85	1.310	11.7	2.05	361		54.0	105.0		11.9	44.2
	b904	11.40	118.0	69.2	15.10	28.7	154.0	78.4	14.8	18.30	10.00	1.250	5.4	2.45	385		56.5	106.0		12.1	42.7
	b906	4.49	36.6	26.1	4.86	11.0	53.8	44.2	9.1	9.33	5.91	0.579	18.2	1.25	225		37.6	76.5		8.4	28.3
	b908	10.80	122.0	54.5	14.20	26.8	138.0	52.8	16.1	16.00	11.80	1.180	36.8	3.24	401		52.2	95.7		11.4	44.9
	b910	11.10	108.0	56.9	14.10	26.4	148.0	59.4	16.7	18.20	10.90	1.130	16.5	2.97	398		58.0	103.0		12.5	46.1
	b913	10.10	102.0	53.0	11.50	27.3	134.0	61.5	14.0	17.40	10.90	1.240	35.0	2.96	317		54.1	100.0		11.7	46.2
	b916	5.73	35.7	31.5	5.45	13.2	32.7	55.4	9.5	8.48	10.20	0.657	40.0	2.34	332		30.7	52.5		6.7	27.9
	b920	8.57	88.2	46.1	10.20	23.6	114.0	93.9	14.1	15.40	9.71	1.140	19.5	2.80	342		55.3	102.0		12.2	44.7
	GP1602	7.47	66.4	40.6	8.38	16.5	97.0	69.3	12.1	12.70	10.10	0.987	8.4	3.24	424		43.1	84.0		10.2	36.0
	GP1603	7.75	60.6	45.2	7.97	14.6	77.9	93.7	11.9	13.10	10.70	0.997	9.7	2.73	442		48.6	92.0		11.0	41.7
	GP1604	10.20	80.8	48.9	11.60	20.7	130.0	99.3	14.9	17.40	8.15	1.270	13.5	3.25	360		54.1	104.0		13.6	45.4
	GP1605	2.68	26.5	12.6	3.08	7.4	32.4	42.7	5.1	5.16	3.69	0.442	3.8	1.19	166		14.9	29.1		3.5	13.7
	GP1606	6.06	39.0	28.9	3.94	11.2	62.8	56.6	10.9	10.60	6.12	0.798	60.4	2.31	252		38.4	73.8		8.3	32.7
	GP1607	3.27	37.8	19.7	5.75	8.4	33.1	15.0	6.4	6.19	4.51	0.380	36.3	1.55	200		18.4	35.5		4.3	15.0
	GP1608	4.35	36.3	23.2	4.76	11.6	48.4	33.2	6.8	7.71	3.63	0.553	18.9	1.48	155		31.4	58.7		7.0	24.6
	GP1609	2.09	25.6	11.4	4.07	16.3	17.4	84.3	4.6	3.88	2.64	0.255	20.7	1.40	104		18.4	51.6		7.8	33.2
	GP1610	1.14	15.3	8.2	1.62	4.9	7.0	23.0	2.8	1.69	2.92	0.138	18.5	0.70	120		9.4	20.9		2.5	9.8
	GP1611	8.60	69.4	41.1	10.00	16.8	107.0	44.9	12.3	13.90	8.62	0.886	35.5	2.64	344		40.2	83.2		9.2	35.0
	GP1612	3.79	31.2	19.4	4.24	9.8	35.2	39.4	8.3	6.16	7.14	0.363	64.8	1.87	301		27.8	55.2		6.8	28.4
地层	样品号	Sm	Eu	Gd	Tb	Dy	Ho	Er	Tm		Yb	Lu	Y	Σ REE		LREE/ HREE	LaN/ YbN		δ Eu		δ Ce
	b875	8.00	1.47	6.25	0.99	5.85	0.99	3.44	0.50		2.93	0.57	29.6	232.70		9.81	12.14		0.61		0.96
	b877	7.23	1.30	5.85	0.97	5.33	1.01	2.84	0.51		2.86	0.49	27.8	223.70		10.26	12.79		0.59		0.91
	b880	7.53	1.18	5.70	0.91	4.50	0.75	2.47	0.36		2.35	0.40	22.3	210.35		11.06	13.71		0.53		0.99
	b882	7.15	1.50	6.56	1.06	5.39	0.90	2.85	0.48		2.98	0.45	27.5	227.12		9.99	11.84		0.66		0.98
	b884	6.82	1.55	6.16	1.03	5.03	0.98	2.79	0.50		2.82	0.45	29.2	210.53		9.65	11.29		0.72		0.98
	b887	6.98	1.67	6.21	1.01	5.44	0.91	2.93	0.50		2.99	0.48	26.4	221.71		9.84	11.49		0.76		0.97
	b889	7.38	1.85	7.12	1.05	5.38	1.02	2.81	0.47		3.29	0.51	29.8	247.38		10.42	11.51		0.77		0.99
	b890	7.33	1.75	6.49	1.01	4.87	0.83	2.75	0.50		2.94	0.47	27.0	244.24		11.30	12.96		0.76		0.99
	b891	7.07	1.53	6.42	0.95	4.74	0.83	2.62	0.43		2.74	0.44	24.2	217.36		10.34	12.30		0.68		0.95
	b893	4.75	1.02	3.91	0.57	3.26	0.56	1.51	0.28		1.53	0.24	15.6	142.38		11.01	14.02		0.70		0.98
	b896	11.20	1.92	8.28	1.43	7.08	1.41	4.01	0.60		3.98	0.66	39.6	320.18		10.66	13.12		0.58		0.91
	b897	6.65	1.26	5.53	0.90	4.40	0.87	2.53	0.43		2.78	0.44	26.8	199.43		10.15	11.12		0.62		0.96
	b898	7.30	1.65	6.32	1.01	5.04	0.98	2.50	0.47		2.80	0.51	26.9	225.58		10.49	13.04		0.73		0.94
	b900	8.07	2.02	6.48	1.04	5.30	1.01	3.02	0.51		3.45	0.47	28.7	242.17		10.38	11.31		0.83		0.92
	b902	8.90	1.81	6.88	0.97	5.10	1.02	3.07	0.55		3.40	0.51	30.0	247.31		10.50	11.39		0.68		0.97
	b904	8.99	1.83	6.82	1.00	4.63	0.95	2.73	0.53		3.11	0.54	29.9	248.43		11.23	13.03		0.69		0.95
	b906	6.51	1.00	4.66	0.64	2.97	0.45	1.42	0.21		1.47	0.20	14.3	170.32		13.17	18.35		0.53		1.01
	b908	6.82	1.43	5.77	0.96	5.52	1.02	3.25	0.54		3.18	0.52	29.3	233.20		10.24	11.77		0.68		0.92
	b910	7.99	1.44	6.51	1.13	5.76	1.07	3.43	0.48		3.11	0.57	31.8	251.09		10.38	13.38		0.59		0.89
	b913	6.84	1.60	5.91	1.07	5.68	1.05	3.29	0.46		3.22	0.57	28.6	241.69		10.38	12.05		0.75		0.93
	b916	5.33	0.84	4.44	0.77	3.56	0.60	1.94	0.28		1.99	0.32	20.2	137.87		8.92	11.07		0.51		0.86
	b920	7.51	1.42	6.33	1.02	6.11	1.10	3.39	0.49		3.73	0.58	32.5	245.88		9.81	10.63		0.61		0.92
	GP1602	6.21	1.89	6.17	1.22	5.71	0.99	3.16	0.49		3.49	0.49	30.5	203.12		8.35	8.86		0.92		0.95
	GP1603	6.88	1.31	6.20	1.09	5.94	1.02	2.91	0.42		3.28	0.46	27.4	222.81		9.45	10.63		0.60		0.94
	GP1604	8.41	1.84	7.68	1.18	5.33	1.03	3.06	0.50		3.82	0.52	27.7	250.47		9.84	10.16		0.69		0.92
	GP1605	2.54	0.41	2.06	0.34	1.70	0.30	0.99	0.16		1.21	0.15	8.6	71.06		9.28	8.83		0.52		0.95
	GP1606	6.10	1.66	5.55	0.78	3.79	0.71	2.02	0.35		2.43	0.32	17.6	176.87		10.09	11.34		0.86		0.97
	GP1607	2.60	0.62	2.28	0.46	2.46	0.42	1.33	0.22		1.26	0.22	12.1	85.04		8.83	10.47		0.76		0.95
	GP1608	3.79	0.86	4.32	0.69	3.26	0.69	1.90	0.29		1.90	0.27	17.9	139.66		9.49	11.85		0.64		0.93
	GP1609	7.40	2.23	7.55	1.17	6.00	0.97	2.56	0.32		2.12	0.27	27.6	141.55		5.75	6.23		0.90		1.06
	GP1610	1.73	0.41	1.99	0.33	1.35	0.21	0.59	0.10		0.71	0.10	6.6	50.08		8.33	9.56		0.67		1.04
	GP1611	6.17	1.31	6.55	1.09	5.82	1.14	3.21	0.49		3.38	0.53	28.2	197.28		7.88	8.53		0.63		1.02
	GP1612	6.02	1.21	5.18	0.92	4.20	0.74	2.09	0.29		2.09	0.30	18.4	141.23		7.94	9.54		0.65		0.96

柯坪塔格组砂岩∑ REE含量变化较大, 为137.87~320.18 μ g/g、平均为224.57 μ g/g, 塔塔埃尔塔格组砂岩稀土元素总量明显低于柯坪塔格组含量, ∑ REE为50.08~250.5 μ g/g、平均为152.65 μ g/g; ∑ REE与SiO₂含量具有良好的负相关性。总体上轻、重稀土分异较明显, LREE/HREE为5.75~13.17, 平均为9.86; La/Yb值为8.68~25.58, 平均为16.07; (La/Yb)_N值为6.23~18.35, 平均为11.53; 说明轻稀土相对富集, 重稀土相对亏损。δ Eu为0.51~0.92, 平均为0.68, 具有明显的Eu负异常; δ Ce为0.86~1.06, 平均为0.96, 具有微弱或无Ce负异常; δ Ce和δ Eu没有明显的相关性。在样品的稀土元素球粒陨石标准化配分模式图(图 5-a)上, 配分型式基本一致, 为右倾式, 轻稀土富集, 重稀土亏损, 具有中度Eu负异常特征。样品稀土元素上地壳标准化模式图(图 5-b)较平坦, (La/Yb)_UCC平均值为1.18, δ Eu平均为1.06, 说明样品稀土配分型式与上地壳相似。

	Figure Option View Download New Window
	图 5 新疆阿合奇地区志留系砂岩稀土元素标准化配分模式图 a— 稀土元素球粒陨石标准化配分模式图(标准化数据引自Sun and Mclennan, 1989); b— 稀土元素上地壳标准化配分模式图(标准化数据引自Taylor and Mclennan, 1985)Fig.5 Normalized REE distribution patterns of sandstones from the Silurian in Akeqi area, Xinjiang

3 讨论

3.1 物源分析

沉积物的地球化学组成取决于主要源区的成分或者不同物源区成分的混合比例, 排除气候、地形、成岩作用等因素之后, 砂岩组分主要受到物源区母岩性质和构造背景的影响。REE和Zr、Th、Sc、Y等一些微量元素在风化、搬运和成岩过程中相对不易迁移, 能提供物源区成分的信息, 并且包括物源区地质体成分随时间变化的信息(毛光周和刘池洋, 2011; 熊小辉和肖加飞, 2011; 周科, 2014)。虽然研究区经受了低— 中等程度的化学风化, 但是砂岩的REE配分特征基本一致, 说明仍能反映源区的基本特征, 所以可以利用碎屑岩的地球化学特征来判断沉积物母岩性质, 分析研究区志留纪大地构造背景等。

铕的异常系数(δ Eu)可以灵敏地反映体系内的地球化学状态, 并可作为鉴别物质来源的重要参数(张鑫等, 2007)。在样品的球粒陨石标准化配分模式图(图 5-a)上, Eu表现为负异常, δ Eu平均值为0.68, 说明物源区岩石以花岗岩为主(花岗岩的δ Eu< 0.9, 张鑫等, 2007)。柯坪塔格组δ Eu平均值为0.66, 塔塔埃尔塔格组δ Eu平均值为0.71、最高可达0.92, 鉴于δ Eu值相对升高, 说明来自以花岗岩为主的物源区的碎屑物质减少。

La/Sc值对于平均物源区成分的判别比较敏感, 可作为区分基性— 超基性与酸性物质成分的指标(Taylor and Mclennan, 1985; Gu et al., 2002)。在Co/Th-La/Sc图解中(图 6-a), 志留系由底部到顶部La/Sc值逐渐升高, Co/Th值逐渐降低, 化学成熟度增加。样品投点落在显生宙克拉通砂岩物源区, 并且塔塔埃尔塔格组样品物源区相对于柯坪塔格组更加趋向于稳定构造型碎屑物源区, 说明中— 末志留世研究区物源已经逐渐稳定。

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	图 6 新疆阿合奇地区志留系砂岩物源判别图解 a— 砂岩Co/Th-La/Sc图解(底图来自于Gu et al., 2002); b— 砂岩La/Yb-∑ REE判别图解(底图来自于Allè gre和Minster, 1978)Fig.6 Provenance discrimination diagrams of sandstones from the Silurian in Akeqi area, Xinjiang

Allè gre和Minster(1978)提出的La/Yb-∑ REE源岩属性判别图解, 可用于判断岩石大类成因及物源区特征。在判别图解(图 6-b)中, 柯坪塔格组样品投点落入沉积岩区与花岗岩区, 反映早志留世物源区岩石主要为花岗岩及古老沉积岩; 塔塔埃尔塔格组样品投点主要落入沉积岩区, 少数落入花岗岩区, 说明自早志留世至末志留世, 来自于花岗岩物源区的碎屑物质逐渐减少, 来自于古老沉积岩物源区的碎屑物质逐渐增多。La/Yb-∑ REE判别图(图6-b)分析结果与Co/Th-La/Sc图解(图6-a)相似, 说明自早志留世以来研究区碎屑物质源区由活动构造型物源区逐渐向稳定构造型物源区转变, 至中— 末志留世研究区已经逐步转变为稳定构造型物源区。

砂— 泥岩物源区性质函数判别图解是Roser和Korsch(1988)建立的, 它是以砂— 泥岩中几种氧化物含量为变量, 并根据各自在反映物源特征中的地位, 建立了区分砂— 泥岩物源区的2个判别函数。将志留系样品的主量元素分析数据, 根据判别函数进行计算并投图(图 7), 发现除1个样品点落入镁铁质物源区外, 柯坪塔格组样品投点多数落入长英质物源区与石英岩沉积物源区的交汇处, 少数落入石英岩沉积物源区, 表明早志留世研究区碎屑物质可能同时来自于沉积物源区和火成岩物源区; 塔塔埃尔塔格组数据投点全部落入成熟大陆的石英岩沉积物源区, 来自于火成岩物源区的碎屑物质消失, 表明中— 末志留世研究区碎屑物质更可能来源于相对稳定的陆源区或继承性的、更老的沉积岩再旋回堆积的产物(Roser and Korsch, 1988), 研究结果与东部乌什南索格当他乌剖面志留系的沉积物源分析结果一致(周新源等, 2002)。从判别图上(图 7)可以看出, 早志留世研究区碎屑物质来自于沉积物源区和火成岩物源区, 后期火成岩物源区物质逐渐减少, 说明研究区逐渐由活动型物源区向稳定型转变, 至中— 末志留世, 火成岩物源区碎屑物质消失, 研究区沉积物全部来源于石英岩沉积物源区, 说明研究区碎屑物质来源已经转变为稳定型物源区。

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	图 7 新疆阿合奇地区志留系砂岩源区性质函数判别图解(底图来自于Roser 和Korsch, 1988)Fig.7 Provenance signatures discriminant function diagram of sandstones from the Silurian in Akeqi area, Xinjiang (Base map after Roser and Korsch, 1988)

3.2 构造背景分析

不同构造环境形成的沉积岩的碎屑物质组成和地球化学成分不同, 可据此判定沉积物源区的构造背景。Bhatia和Crook(1986)通过对砂岩和泥岩地球化学特征的研究, 认为一些不活泼微量元素如La、Th、Y、Zr、Ti、Co、Ni等及其比值如La/Y、Ti/Zr等比较稳定, 能够判别物源区构造环境, 并归纳出多种判别图解。通过微量元素判别图解, 将构造背景分为大洋岛弧、大陆岛弧、主动大陆边缘和被动大陆边缘4种类型。在杂砂岩的La-Th-Sc判别图解(图 8-a)中, 样品投点全部落入主动大陆边缘和被动大陆边缘中。由于主动大陆边缘和被动大陆边缘分布区出现了重叠, 利用Th-Sc-Zr/10图解(图 8-b)进一步区分, 样品落入大陆岛弧与被动大陆边缘区域。柯坪塔格组样品投点大部分落入大陆岛弧区, 少数样品点落入被动大陆边缘区域。塔塔埃尔塔格组样品投点主要落入被动大陆边缘, 3个样品点落入大陆岛弧区域。在Bhatia(1983)提出的La/Y-Sc/Cr判别图解中(图 9-a), 柯坪塔格组样品投点几乎全部落入被动大陆边缘区域之上, 塔塔埃尔塔格组样品点大部分落入被动大陆边缘区域之中, 其余样品点落入被动大陆边缘区域之上。结合La-Th-Sc及Th-Sc-Zr/10判别图解, 说明至少在中— 末志留世研究区已转化为被动大陆边缘。

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图 8 新疆阿合奇地区志留系砂岩La-Th-Sc(a)和Th-Sc-Zr/10(b)构造背景判别图解(底图来自于Bhatia和Crook, 1986)
OIA— 大洋岛弧; CIA— 大陆岛弧; ACM— 活动大陆边缘; PM— 被动大陆边缘Fig.8 Tectonic setting discrimination diagrams of La-Th-Sc(a)and Th-Sc-Zr/10(b) of sandstones from the Silurian in Akeqi area, Xinjiang(Base map after Bhatia and Crook, 1986)

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图 9 新疆阿合奇地区志留系砂岩La/Y-Sc/Cr(a)和K₂O/Na₂O-SiO₂(b)构造背景判别图解(底图a来自于Bhatia, 1983; 底图b来自于Roser and Korsch, 1986)
OIA— 大洋岛弧; CIA— 大陆岛弧; ACM— 活动大陆边缘; PM— 被动大陆边缘Fig.9 Tectonic setting discrimination diagrams of La/Y-Sc/Cr(a)and K₂O/Na₂O-SiO₂(b) of sandstones from the Silurian in Akeqi area, Xinjiang(Base map a after Bhatia, 1983 and Base map b after Roser and Korsch, 1986)

Roser和Korsch(1986)利用砂泥岩中K₂O/Na₂O值与SiO₂含量的变化规律, 提出了K₂O/Na₂O-SiO₂构造环境判别图解。柯坪塔格组样品多数落在活动大陆边缘与被动大陆边缘的交界处(图 9-b), 投点更接近活动大陆边缘区域, 塔塔埃尔塔格组样品点则全部落入被动大陆边缘区, 说明在早志留世, 研究区正处于主动大陆边缘向被动大陆边缘转换的构造背景, 因此同时具有主动大陆边缘和被动大陆边缘的性质; 中— 晚志留世, 研究区大地构造背景已经完全转变为被动大陆边缘。

南天山洋盆是否存在向南俯冲, 解决这一问题的关键在于理清塔里木板块北缘的大陆边缘性质。近年来, 随着塔里木板块北缘研究成果的逐渐增多, 对于该问题的认识也逐渐清晰。塔里木北缘发育有一系列近东西向断续出露的中酸性侵入岩, 西起老虎台, 向东延伸至库尔勒一带(姜常义等, 2001; 郭瑞清等, 2013a; 张斌等, 2014)。这些岩石均形成于早古生代, 岩体年龄集中在426.3— 404.8, Ma, 均具有大陆弧花岗岩的性质, 说明至少在志留纪塔里木北缘已转化为主动大陆边缘, 南天山洋盆向南俯冲到塔里木板块之下(王超等, 2009; 张斌等, 2014)。郭瑞清等(2013b)报道了库鲁克塔格西段地区板块汇聚边缘火山弧性质的奥陶纪花岗岩, 认为南天山洋盆向南俯冲至少在晚奥陶世已经开始。在前人(邬光辉等, 2009, 2010; 常健等, 2012; 刘景彦等, 2012; 牛露等, 2013; 郭春涛等, 2015)对塔里木北缘碎屑锆石的研究过程中, 在志留系、泥盆系、石炭系中均检测到了年龄峰为~450, Ma的年龄数据, 且塔里木北缘东侧奥陶纪锆石含量远多于西侧; 邬光辉等(2009, 2010)认为东侧锆石来自于阿尔金造山带, 但刘景彦等(2012)在对塔北隆起中部碎屑锆石(461— 414, Ma)研究后认为, 晚奥陶世— 早志留世, 阿尔金造山带与塔北隆起之间距离较远, 隔着满加尔凹陷, 物源体系来自于阿尔金的可能性不大, 南天山洋的存在也使物源不可能来自于中天山地区, 而应该与南天山洋盆的早古生代俯冲事件有关。李路路等(2017)在柯坪地区发现少量锆石年龄为435— 437, Ma, 认为其与塔里木北缘出露的侵入岩相对应, 与南天山的俯冲作用有关。张斌等(2014)认为南天山洋盆向南的俯冲作用并不强烈, 可能为短期地局部俯冲, 持续时间并不长。塔里木东北缘南天山洋向南的俯冲持续到中泥盆世结束, 而研究区持续到早志留世已经结束, 这也可以用来解释研究区岩浆岩锆石数量相对于塔里木东侧保存较少的原因。

研究区下志留统柯坪塔格组与下伏上奥陶统之间为平行不整合接触, 发育有风化壳, 前人在相邻区域内也有大量的报道(林畅松等, 2011; 张宇航等, 2012; 何碧竹等, 2013; 刘晓煌等, 2013)。不整合面的存在, 说明晚奥陶世— 早志留世研究区存在一次洋陆的转换事件, 结合前人资料及文中分析结果, 表明晚奥陶世, 塔里木板块北缘为活动大陆边缘, 受加里东运动的影响, 南天山洋盆向南俯冲到塔里木板块之下, 形成岛弧性质的花岗岩等; 由于南天山洋盆的持续俯冲, 塔里木板块遭到强烈挤压和隆升, 研究区上升为陆, 上奥陶统遭受强烈剥蚀, 成为研究区志留系部分活动大陆边缘和大陆岛弧性质碎屑物质的来源, 这也与志留系— 上奥陶统平行不整合相吻合。早志留世, 研究区重新开始接受沉积, 构造背景由活动大陆边缘开始向被动大陆边缘转化, 说明南天山洋盆向南俯冲已经基本结束。南天山洋盆向南俯冲过程中形成的大量碎屑物质再次进入研究区接受沉积, 因此下志留统柯坪塔格组部分碎屑物质源区具活动大陆边缘或岛弧性质, 随着活动大陆边缘向被动大陆边缘构造属性的转换, 研究区构造活动逐渐减弱, 由地层底部到顶部活动大陆边缘或岛弧性质的碎屑物质含量逐渐减少。至中— 末志留世, 研究区完全转变为被动大陆边缘的构造背景, 碎屑物质全部来自于稳定物源区。

4 结论

1)志留系砂岩的地球化学特征显示, 新疆阿合奇地区早志留世部分碎屑物质来自于活动型物源区, 后期逐渐减少, 至中— 末志留世完全消失, 此时沉积物全部来自于成熟大陆的石英岩沉积物源区, 表明研究区物源由活动型物源逐渐转变为稳定型物源。

2)南天山洋盆构造演化过程中存在双向俯冲: 晚奥陶世, 南天山洋盆向南俯冲到塔里木板块之下, 使得阿合奇地区上升为陆, 形成奥陶系— 志留系不整合。早志留世以后, 南天山洋盆向南俯冲结束, 阿合奇地区构造活动逐渐减弱, 构造背景由活动大陆边缘向被动大陆边缘转化, 因此部分碎屑物质具有活动大陆边缘及岛弧特征; 中— 末志留世, 阿合奇地区已完全转化为被动大陆边缘, 碎屑物质来自于成熟大陆的石英岩物源区。

(责任编辑张西娟; 英文审校吴晨亮)

作者声明没有竞争性利益冲突.

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2012

0.0

蔡东升, 卢华复. 2012. 南天山古生代板块构造演化. 地质论评, 41(5): 432-443.

[Cai D

, Lu H

. 2012. Paleozoic plate tectonic evolution of southern Tianshan. Geological Review, 41(5): 432-443]

The synthetic analyses based on paleontologic stratigraphy, paleomagnetics, petrogeo-chemistry, and isotopic ages show that a paleo-ocean should have existed in Southern Tianshan during the Ordovician-Permian. The earliest rifting was marked by the continental rift eruption of the Sinian Beiyixi Formation (Z1b). From the Sinian to Ordovician, the evolution from a rift to a passive continental-margin ocean-basin was completed in the Silurian and Devonian, the oceanic crust of southern Tianshan began to be subducted beneath the Kasakstan plate. In the terminal Devonian to the Early Carboniferous, the oceanic crust was consumed at all, so the continent-continent collision occurred between the Tarim and Kasakstan plates. In the Carboniferous-Early Permian a sea basin opening to the west still existed in Southern Tianshan and it was closed finally in the Permian.

据南天山古生物地层、古地磁、岩石地球化学和同位素年龄等资料的综合分析结果；认为该区在奥陶纪－二叠纪曾为古大洋。最初裂开为大洋是以震旦纪贝义西组大陆裂谷火山喷发为标志，从晨旦纪－奥陶纪完成了从裂谷到被动大陆边缘海盆的演化；志留纪－泥盆纪南天山洋壳向哈萨克斯坦板块之下俯冲，泥盆纪末至石炭纪早期，塔里木板块与哈萨克斯坦板块发生陆－陆碰撞。石炭纪－早二叠纪在南天山仍存在一个向西开口的前陆残余海盆。它最终关

... 蔡东升和卢华复,2012 ...

2012

0.0

常健, 邱楠生, 李佳蔚. 2012. 塔里木柯坪地区下志留统碎屑锆石U-Pb年代学特征及其地质意义. 地球科学与环境学报, 34(3): 32-43.

[Chang

, Qiu N

, Li J

. 2012. U-Pb dating of detrital zircon from Lower Silurian in Keping area of Tarim Basin and its geological implication. Journal of Earth Sciences and Environment, 34(3): 32-43]

柯坪地区物源及演化与塔里木盆地的古地理位置密切相关.通过对下志留统碎屑锆石的形态特征和UPb年龄分布特征进行分析,系统研究了柯坪地区下志留统的物源及其演化.结果表明:柯坪地区下志留统锆石均为岩浆锆石,锆石UPb年龄反映的是成岩年龄或结晶年龄,可有效指示物源区;下志留统柯坪塔格组的物源区主要为沙雅隆起西部、塔中隆起及塔西南前缘隆起,之后受海侵的影响,塔中隆起被海水淹没,下志留统塔塔埃尔塔格组的物源区演变为沙雅隆起西部、塔西南前缘隆起及塔中隆起的南部于田、康西瓦地区;满加尔凹陷的存在使得柯坪地区与塔中、塔东地区的物源具有很大的差异;900~700 Ma的锆石年龄谱表明,塔里木地块与冈瓦纳大陆具有一定的亲缘关系.

... 常健等,2012 ...

1995

0.0

高俊, 汤耀庆, 赵民, 王军. 1995 a. 新疆南天山蛇绿岩的地质地球化学特征及形成环境初探. 岩石学报, 11(S1): 85-97.

[Gao

, Tang Y

, Zhao

, Wang

. 1995a. The preliminary studies on tectonic environment of formation and geological and geochemical characters of ophiolites, south Tianshan Mountains, Xinjiang. Acta Petrologica Sinica, 11(S1): 85-97]

... 对于这一问题,国内外许多学者从岩相学、锆石年代学、地球化学等方面进行了深入研究,并提出了不同的观点(高俊等,1995a ...

1995

0.0

高俊, 肖序常, 汤耀庆, 赵民, 王军. 1995 b. 西南天山构造地层学初步研究. 地层学杂志, 19(2): 122-128.

[Gao

, Xiao X

, Tang Y

, Zhao

, Wang

. 1995. Preliminary research on the tectonostratigraphy in the southwestern Tianshan Mountains. Journal of Stratigraphy, 19(2): 122-128]

... 伊犁板块之下,古生代塔里木板块北缘一直为被动大陆边缘(高俊等,1995b ...

2014

0.0

... 高晓芬等,2014 ...

2015

0.0

郭春涛, 李忠, 高剑, 董顺利. 2015. 塔里木盆地西北缘乌什地区石炭系沉积与碎屑锆石年代学记录及其反映的构造演化. 岩石学报, 31(9): 2679-2695.

[Guo C

, Li

, Gao

, Dong S

. 2015. Depositional and detrital zircon geochronological records of Carboniferous System in Wushi, northwest Tarim Basin: Implications for tectonic evolution. Acta Petrologica Sinica, 31(9): 2679-2695]

The Visean to Bashkirian profile is well exposed in the Wushi area, the northwestern margin of the Tarim Basin, Northwest China. Numerous sandstone samples were chosen to carry out U-Pb and Lu-Hf isotope test by LA-ICP-MS method. Based on detailed analysis of geochronology, heavy minerals, sandstone skeleton component, this research further explores sedimentary evolution and its geodynamic mechanism about the Tarim Basin and the periphery orogen in Carboniferous. Sandstone skeleton component analysis shows that sandstone grains are dominated by quartz, and volcanic-metavolcanic is lithic fragments. Its main provenance is the recycled orogen, and has the trend to migrate to the inner craton from the bottom to top. The main proportions of heavy mineral assemblages are stable heavy minerals, such as zircon, tourmaline, TiO 2 minerals. Heavy mineral analysis reflects the distant source and relatively stable tectonic setting are possible. The geochronological results show that the four samples have approximately similar U-Pb age patterns and Hf isotopic compositions, mainly reflecting multiphase tectono-thermal events with age groups of 392~496Ma, 708~868Ma, 893~1044, with ε Hf ( t ) ranged from -15 to 13. In addition, there are also a small amount of 1713~1917Ma, 2376~2606Ma age. The geochronological information and provenance system are very similar to Silurian to Devonian strata underlying the unconformity. Comparing with the main potential source areas, the main provenance is the northern Tarim palaeohigh. The redeposition of pre-Carboniferous strata in Tarim Basin, associated with the erosion source in the Kunlun-Altun orogen, may also have some contribution, and became the mainly provenance of detrital zircon of 893~1044Ma before Early Visean; while the two facts, detrital composition maturity increased and the abundance of 893~1044Ma decreased rapidly, suggested that the material from the latter source diminished, and the mature material from the palaeohigh raised after Late Visean. In other words, although the radiolarian information shows that the South Tianshan Ocean had closed after Early Visean, the provenance system didn't change greatly until Bashkirian, and the information about collision, orogenic events and their effects of the South Tianshan and the Tarim hadn't been recorded.

针对塔里木西北缘乌什地区石炭纪维宪期(Visean)至巴什基尔期(Bashkirian)连续较好的露头剖面,在沉积序列、砂岩组分及重矿物组合分析基础上,重点通过LA-ICP-MS分析砂岩样品碎屑锆石的原位U-Pb和Lu-Hf同位素,解析其年代学、物源特征及构造属性等信息。研究显示,石炭系砂岩碎屑颗粒以石英为主,火山岩屑和变质火山岩屑极少,物源构造属性主要指示再旋回造山带,且向上有向克拉通迁移的趋势;重矿物组合以锆石、电气石和TiO 2 矿物等稳定重矿物为主,反映远源和相对稳定的构造背景。4个砂岩样品总体具有类似的碎屑锆石U-Pb年龄组成,主要反映三期年龄:392~496Ma、708~868Ma和893~1044Ma,其 ε Hf ( t )大多介于-15~13之间;此外也少量存在1713~1917Ma、2376~2606Ma年龄,与该区石炭系不整合下伏地层(至少志留-泥盆系)物源构成类似。对比研究显示,上述碎屑物源以塔里木基底古隆起为主,与昆仑-阿尔金造山带剥蚀物源相关的塔里木前石炭纪沉积也可能提供部分再旋回物源,并成为西北缘早石炭世维宪期前沉积的893~1044Ma年龄碎屑锆石的主要来源;而维宪期后碎屑成分成熟度的增大和893~1044Ma年龄碎屑锆石丰度的锐减可能说明与昆仑-阿尔金造山带相关物源的减少,塔里木大陆内部(隆起)成熟物源的增加。换句话说,尽管放射虫资料说明早石炭世早维宪期后南天山洋已经关闭,但直到晚石炭世巴什基尔期塔里木西北仍然延续了前石炭纪的沉积物源格局,并未记录到南天山造山事件的沉积学效应。

... 郭春涛等,2015)对塔里木北缘碎屑锆石的研究过程中,在志留系、泥盆系、石炭系中均检测到了年龄峰为~450,Ma的年龄数据,且塔里木北缘东侧奥陶纪锆石含量远多于西侧 ...

2013

0.0

郭瑞清, 尼加提·阿布都逊, 秦切, 贾晓亮, 朱志新, 王克卓, 李亚萍. 2013 a. 新疆塔里木北缘志留纪花岗岩类侵入岩的地质特征及构造意义. 地质通报, 32(2/3): 220-238.

[Guo R

, Nijiati

, Qin

, Jia X

, Zhu Z

, Wang K

, Li Y

. 2013a. Geological characteristics and tectonic significance of Silurian granitic intrusions in the northern Tarim craton, Xinjiang. Geological Bulletin of China, 32(2/3): 220-238]

塔里木北缘在古生代是否是主动大陆边缘对于了解南天山洋的俯冲方式及中亚造山带西南缘的增生历史具有重要意义。塔里木北缘断续出露一条侵入岩带,西起老虎台,经黑英山—密勒洞—野云沟-库尔勒一带,再往东与库鲁克塔格地块的侵入岩连在一起。选取志留纪欧西达坂岩体、铁门关岩体、铁门关东南岩体和博斯腾湖乡岩体作为典型岩体进行定年、岩石学和地球化学的研究。获得铁门关东南岩体的锆石U-Pb年龄为419.2Ma±3.1Ma,博斯腾乡岩体的锆石U-Pb年龄为418Ma±2.7Ma。地球化学特征显示,志留纪侵入岩为钙碱性—高钾钙碱性I型花岗岩,微量元素富集Rb、K、U等大离子亲石元素(LILE)、亏损Nb、Ta、Ti、P等高场强元素(HFSE),具有板块汇聚边缘火山弧花岗岩的地球化学特征。综合区域地质资料及前人成果,推测在早古生代南天山洋存在双向俯冲,并从志留纪已经开始向南俯冲-消减,一直延续到早石炭世,到晚石炭世闭合。

... 郭瑞清等,2013a,2013b ...

... 郭瑞清等,2013a ...

2013

0.0

郭瑞清, 秦切, 木合塔尔·扎日, 赵亮亮, 孙敏佳, 魏震. 2013 b. 新疆库鲁克塔格西段奥陶纪花岗岩体地质特征及构造意义. 地学前缘, 20(4): 251-263.

[Guo R

, Qin

, Muhetaer

, Zhao L

, Sun M

, Wei

. 2013b. Geological characteristics and tectonic significance of Ordovician granite intrusions in the western segment of Quruqtagh, Xinjiang. Earth Science Frontiers, 20(4): 251-263]

摘　要：塔里木盆地北缘是塔里木克拉通与南天山造山带结合部位,发育近东西展布的古生代花岗质侵入岩带,该侵入岩带对探究塔里木北缘构造背景及属性乃至南天山洋演化至关重要。文中研究岩体位于库鲁克塔格西段的博斯腾湖南岸,主要岩性为二长花岗岩,LA-ICP-MS U-Pb锆石年龄分别为（458±3）Ma和（454.6±4.6）Ma,代表花岗岩结晶年龄。地球化学特征显示,花岗岩的SiO2质量分数为71.03%～74.39%,K2O质量分数为4.14%～5.07%,A/CNK=1.03～1.08,属弱过铝质高钾钙碱性I型花岗岩;（La/Yb）N为16.41～37.59,δEu=0.44～0.79,具轻稀土富集、重稀土相对亏损的特征;在原始地幔标准化蛛网图上,样品均明显富集K、Rb、Ba、Th等大离子亲石元素,亏损Ta、Nb、P、Ti等高场强元素。花岗岩岩浆源于下地壳的部分熔融,在熔融过程中源区残留石榴子石和斜长石。综合区域地质资料及前人成果,认为花岗岩形成的动力和热力来源与南天山洋向南俯冲有关,推测在早古生代南天山洋存在双向俯冲,并从奥陶纪开始向南俯冲消减,一直延续到早石炭世,到晚石炭世闭合。

... 郭瑞清等,2013a,2013b ...

... 郭瑞清等(2013b)报道了库鲁克塔格西段地区板块汇聚边缘火山弧性质的奥陶纪花岗岩,认为南天山洋盆向南俯冲至少在晚奥陶世已经开始 ...

2013

0.0

何碧竹, 焦存礼, 许志琴, 刘士林, 蔡志慧, 李海兵, 张淼. 2013. 不整合结构构造与构造古地理环境: 以加里东中期青藏高原北缘及塔里木盆地为例. 岩石学报, 29(6): 2184-2198.

[He B

, Jiao C

, Xu Z

, Liu S

, Cai Z

, Li H

, Zhang

. 2013. Unconformity structural architecture and tectonic paleo-geographic environment: A case of the Middle Caledonian on the northern margin of Tibet Plateau and Tarim Basin. Acta Petrologica Sinica, 29(6): 2184-2198]

... 何碧竹等,2013 ...

2001

0.0

姜常义, 穆艳梅, 赵晓宁, 白开寅, 张虹波. 2001. 塔里木板块北缘活动陆缘型侵入岩带的岩石学与地球化学. 中国区域地质, 20(2): 158-163.

[Jiang C

, Mu Y

, Zhao X

, Bai K

, Zhang H

. 2001. Petrology and geochemistry of an active continental-margin intrusive rock belt on the northern margin of the Tarim plate. Regional Geology of China, 20(2): 158-163]

在塔里木板块北缘，断续出露一条侵入岩带，总长度800多公里。岩石组合是：橄榄辉长岩-辉长岩-辉长闪长岩-闪长岩-石英闪长岩-花岗岩。各种类型岩石的化学组成显示了清晰的钙碱性岩浆演化趋势。稀土元素配分曲线均为轻稀土富集型，而且，重稀土元素配分曲线相对平坦。Sr、K、Rb、Ba、Th等大离子亲石元素强烈富集，而Ta、Nb、Zr、Hf、Ti等高场强元素显著贫化。这些岩石学与地球化学特征均证明，该侵入岩带形成于活动大陆边缘。

... 塔里木北缘发育有一系列近东西向断续出露的中酸性侵入岩,西起老虎台,向东延伸至库尔勒一带(姜常义等,2001 ...

2017

0.0

李路路, 杨宝忠, 尹永会, 刘龙龙, 王兵. 2017. 新疆柯坪地区下志留统柯坪塔格组物源分析: 来自地球化学、锆石U-Pb年代学的约束. 地质科技情报, 36(2): 1-12.

[Li L

, Yang B

, Yin Y

, Liu L

, Wang

. 2017. Geochemical characteristics and provenance analysis of sand stone in Silurian Kepingtage Formation in Keping area, Xinjiang. Geological Science and Technology Information, 36(2): 1-12]

以柯坪塔格组灰绿色砂岩为研究对象,开展了系统的岩石地球化学和同位素年代学研究。结果表明,砂岩SiO_2质量分数较高,Na_2O、CaO、TiO_2质量分数较低;轻稀土元素富集,具明显的Eu负异常。碎屑锆石U-Pb年龄集中分布于1 000~700,2 500~1 800 Ma 2个区间,可能分别对应新元古代晚期南华纪-青白口纪的构造抬升运动和古元古代早期的强烈构造运动及岩浆侵位,个别锆石颗粒年龄超过2 500 Ma,2颗锆石年龄数据偏小,仅在437~435 Ma之间,可能与南天山洋俯冲导致的岩浆活动有关。分析表明,早志留世柯坪地区处于稳定的被动大陆边缘,碎屑物源主要来自塔北隆起前寒武纪古老的克拉通基底岩类。

2009

0.0

李曰俊, 杨海军, 赵岩, 罗俊成, 郑多明, 刘亚雷. 2009. 南天山区域大地构造与演化. 大地构造与成矿学, 33(1): 94-104.

[Li Y

, Yang H

, Zhao

, Luo J

, Zheng D

, Liu Y

. 2009. Tectonic framework and evolution of south Tianshan, NW China. Geotectonica et Metallogenia, 33(1): 94-104]

塔里木和中天山之间的南天山造山带,经历了复杂的构造演化与地壳增生过程.综合分析南天山造山带的构造、地层、古生物、岩石、地球化学和同位素年代学等方面的资料,特别是放射虫、蛇绿岩、蓝片岩等方面的最新研究成果,讨论了南天山的区域构造格局和演化过程.南天山主体为一上百公里宽的增生-碰撞混杂带-南天山(蛇绿)混杂带;其北侧为中天山岛弧,是仰冲壳楔;南侧为塔里木陆块,是俯冲壳楔.古南天山洋为一广阔的大洋,南天山碰撞造山作用起始于二叠纪末-三叠纪初,新近纪-第四纪进入陆内造山作用阶段.

... 李曰俊等,2009 ...

2011

0.0

林畅松, 李思田, 刘景彦, 钱一雄, 罗宏, 陈建强, 彭莉, 芮志峰. 2011. 塔里木盆地古生代重要演化阶段的古构造格局与古地理演化. 岩石学报, 27(1): 210-218.

[Lin C

, Li J

, Liu J

, Qian Y

, Luo

, Chen J

, Peng

, Rui Z

. 2011. Tectonic framework and paleogeographic evolution of the Tarim Basin during the Paleozoic major evolutionary stages. Acta Petrologica Sinica, 27(1): 210-218]

Tarim basin underwent several major evolutionary stages during the Paleozoic, including the periods at the end of the Middle to early Late Ordovician, the end of the Late Ordovician and the end of the Middle Devonian or Early Carboniferous, and resulted in a series of important unconformities. The tectonic movement occurred in the Middle to the early Late Ordovician led to the development of the central paleo-uplift belt composed of the Bachu paleo-slope, the Tazhong uplift and the Hetianhe uplift, the relatively subsidence Northern depression belt and the Tangguzibasi depression formed due to compressive flexural subsidence. Constrained by the paleo-uplift, the Tazhong uplift belt of the Late Ordovician formed a peninsula-shaped carbonate platform which narrowed eastwards. The Majiaer depression, which generated in Sinian, and the Tangguzibasi depression received several thousand meters of deep water muddy and turbidite deposits during the Middle to Late Ordovician. At the end of the Ordovician, formed the Tarbei paleo-uplift belts along the northwestern basin margin and the Southeastern paleouplift belt along the southwest to southeastern basin margin. The resulted tectonic geomorphology controlled the Early Silurian depositional framework of the neritic terrigenous elastic basin extended northeast-eastwards. At the end of the Middle Devonian, the basin experienced an intense uplifting and suffered strong denudation, and formed an extensive angular unconformity surface along the Tabei and the Tadong paleo-uplifts. The tectonic geomorphology of the basin during this period changed from lower to higher in the east and higher to lower in the west, which made a significant influence on the paleogeographic pattern of the Late Devonian and Early Carboniferous. The study show that the deformation occurred at the end of the Middle to early Late Ordovician might have resulted from the northward collision and extrusion of the North Kunlun orogenics. At the end of the Middle Devonian, the intensively uplifting of the Tabei uplifts and the folding and uplifting of the Manjiaer depression might be attributed to the collision of the southern Tianshan Ocean.

塔里木盆地在古生代经历了中-晚奥陶世、晚奥陶世末、中泥盆世末等多个重要的盆地变革期,形成了多个重要的不整合,盆地构造古地理发生了重要的变化。中、晚奥陶世盆地的变革形成了由巴楚古斜坡-塔中隆起-和田河隆起构成的大型古隆起带、相对沉降的北部坳陷带以及由于挤压挠曲沉降形成的塘古孜巴斯坳陷带。中部古隆起带制约着晚奥陶世东窄西宽的弧立碳酸盐岩台地体系的发育,而开始形成于震旦纪的满加尔拗拉槽及东南侧的塘古孜巴斯坳陷接受了巨厚的中、晚奥陶世重力流沉积。奥陶纪末的盆地变革形成了北东东向展布的西南-东南缘和西北缘的强烈隆起带,总体的古构造地貌控制着早志留世北东东向展布的滨浅海陆源碎屑盆地的沉积格局。中泥盆纪世末期的盆地强烈隆升并遭受了夷平化的剥蚀作用,形成了大范围分布的角度不整合面,并以塔北隆起和塔东隆起的强烈抬升为显著特征。盆地古构造地貌从东低西高转为东高、西低,制约着晚泥盆和早石炭世由东向西南方向从滨岸到浅海的古地理分布。中、晚奥陶世主要不整合及其剥蚀量的分布反映出北昆仑向北碰撞和挤入是造成盆地南缘、东南缘及盆内隆起的主要原因。南天山洋的俯冲、碰撞在奥陶世末至早志留世已对盆地西北缘产生影响,导致塔北英买力隆起的抬升和遭受剥蚀。

... 研究区下志留统柯坪塔格组与下伏上奥陶统之间为平行不整合接触,发育有风化壳,前人在相邻区域内也有大量的报道(林畅松等,2011 ...

2012

0.0

刘景彦, 杨海军, 杨永恒, 蔡振忠, 刘永权, 芮志峰, 苏真真. 2012. 塔里木盆地东北缘志留纪构造活动的U-Pb年代证据及盆内响应. 中国科学: 地球科学, 42(8): 1218-1233.

[Liu J

, Yang H

, Yang Y

, Cai Z

, Liu Y

, Rui Z

, Su Z

. 2012. The U-Pb chronologic evidence and sedimentary responses of Silurian tectonic activities at northeastern margin of Tarim Basin. Science China: Earth Science, 42(8): 1218-1233]

关于塔里木盆地志留纪周边构造活动背景一直存在多种看法.本研究利用LA-ICP-MS测试技术获得了塔北隆起泥盆系碎屑锆石的U-Pb年龄,揭示塔北周缘460～414Ma存在强烈的构造事件,其中436～423Ma左右的锆石年龄最为集中,结合前人在盆缘造山带的研究成果,认为奥陶纪末至早、中志留世盆地东北缘存在强烈的构造活动这一期构造活动在盆内有明显的沉积响应:(1)上奥陶统及志留系内部存在多期明显的不整合,反映周边挤压过程在盆内形成的局部隆起;(2)在盆地北部柯坪、英买力、哈得、草湖等地区志留系都发现有由东北向西南注入的河流-三角洲体系,反映盆地东北缘的局部隆升和提供物源;(3)重矿物分析表明志留纪沉积期主要来自再旋回造山带物源.此外,志留系中上部大面积分布的红层可能与周边及盆地的构造隆升、海平面的快速下降等有关.

... 海退序列,以塔塔埃尔塔格组紫红色砂岩的出现作为转折,砂岩整体颜色由灰绿色转变为紫红色,说明气候由温暖湿润向干旱炎热转化(刘景彦,2012) ...

... 刘景彦等,2012 ...

2013

0.0

刘晓煌, 牛树银, 张雄华, 李保飞, 张新勇, 宋贺民, 鲁世鹏, 刘玖芬. 2013. 新疆西南天山哈拉奇地区古生代地层剖面中3个不整合面的确定及其意义. 西北地质, 46(4): 115-130.

[Liu X

, Niu S

, Zhang X

, Li B

, Zhang X

, Song H

, Lu S

, Liu J

. 2013. The identification and its significance of the three unconformity surfaces of the Paleozoic stratigraphic profile in Halaqi area in southwestern Tianshan, Xinjiang. Northwestern Geology, 46(4): 115-130]

Halaqi region is located in Southwest Tianshan-Northwest Tarim Basin. It's the front region of collision between Tarim Block and Kazakhstan-Siberia Block. Cambrian-Permian strata with slight metamorphism outcropped in this area, where we discover three unconformity surfaces, namely angular unconformity in Permian-Cenozoic, parallel unconformity in Ordovician-Silurian and parallel unconformity in Devonian-Carboniferous. The unconformity is bordered by A'erpaqueyiqieke vault anticlinorium. The sedimentary environment on both sides of Silurian-Permian is greatly different. The metamorphism in Ordovician and Cambrian composed of anticline is different from that of overlying strata. According to regional geology and evolution, the parallel unconformity in Ordovician-Silurian was corresponding to the regional Qilian Movement. The parallel unconformity in Devonian-Carboniferous was corresponding to the middle Tianshan Movement. The angular unconformity in Permian-Cenozoic was influenced by the end of Tianshan Movement.

哈拉奇地区位于西南天山南侧、塔里木盆地西北缘，是塔里木板块和哈萨克斯坦-西伯利亚板块碰撞的前锋区域。出露了寒武纪—二叠纪变质程度较浅的地层；新发现其存在奥陶系—志留系平行不整合、泥盆系—石炭系平行不整合和二叠系—中、新生界角度不整合共3个不整合面，并以阿尔帕确依切克穹窿式复背斜为界，两侧志留系—二叠系沉积环境存在较大差异，组成背斜的奥陶系、寒武系与上覆地层变质作用也不同。奥陶系—志留系平行不整合与区域上祁连运动相对应；泥盆系—石炭系平行不整合同天山运动中期相吻合；二叠系—中、新生界角度不整合为天山运动末期的影响造成。

... 刘晓煌等,2013) ...

2011

0.0

... REE和Zr、Th、Sc、Y等一些微量元素在风化、搬运和成岩过程中相对不易迁移,能提供物源区成分的信息,并且包括物源区地质体成分随时间变化的信息(毛光周和刘池洋,2011 ...

2013

0.0

牛露, 于炳松, 张文博. 2013. 塔里木盆地北部地区下志留统柯坪塔格组物源分析与物源区母岩年龄确定. 沉积学报, 31(3): 421-429.

[Niu

, Yu B

, Zhang W

. 2013. Provenance analysis and dating of parent rocks of the sand stones from Kepingtage Formation(Silurian)in the northern Tarim Basin. Acta Sedimentologica Sinica, 31(3): 421-429]

According to the observation of petrographic thin sections, the approaches of the heavy mineralogy analysis and the analysis of SHRIMP UPb ages of detrital zircons, which is of the sandstone samples taken from the Dawangou outcrops of Keping area and the drill cores of TP3,TP7 and KQ1 in northern Tarim Basin, as well as using the classic Dickinson Ternary Diagram method and combining with regional geology background analysis, we make a conclusion that the provenance of the sandstones in the Kepingtage Formation of Silurian in the west area of northern Tarim Basin is different from that in the center and east area of northern Tarim Basin. The tectonic setting of the former provenance is the continental island arc environment, and it is composed of the materials from the Proterozoic upper crust. Thus the provenance is inferred to be Tabei uplift. However, the tectonic setting of the latter provenance is the recycled orogens environment and it is composed of the Ordovician materials. So, the provenance is inferred to be Kuluketage uplift. The type of provenance is widely igneous rock. Compared with the center and east area of northern Tarim Basin, the west area is farther to the provenance. These conclusions are of great importance to the reconstruction of paleogeography deposition environment and the analysis of the type and evolution of Tarim Basin.

根据柯坪（KP）大湾沟剖面及塔北地区TP3，TP7和KQ1等井下志留统柯坪塔格组砂岩样品岩石薄片、重矿物、锆石SHRIMP U—Pb测年分析结果，应用Dickinson三角图法，结合区域地质背景分析，认为塔北西部地区和中东部地区的志留系柯坪塔格组砂岩物源明显不同。西部地区物源构造背景为大陆岛弧环境，物源物质为大陆上地壳，年代为元古代，推测物源区为塔北隆起；中东部地区物源构造背景为再旋回造山带环境，年代为奥陶纪，推测物源区为库鲁克塔格隆起带。物源母岩普遍含深成中酸性侵入岩。塔北西部物源距离远于塔北中东部地区，这对于恢复当时的沉积古地理环境以及塔里木盆地的类型和盆地演化有重要意义。

... 牛露等,2013 ...

2009

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王超, 罗金海, 车自成, 刘良, 张敬艺. 2009. 新疆欧西达坂花岗质岩体地球化学特征和锆石LA-ICP-MS定年: 西南天山古生代洋盆俯冲作用过程的启示. 地质学报, 83(2): 272-283.

[Wang

, Luo J

, Che Z

, Liu

, Zhang J

. 2009. Geochemical characteristics and U-Pb LA-ICP-MS zircon dating of the Oxidaban pluton from Xinjiang, China: Implications for a Paleozoic oceanic subduction process in southwestern Tianshan. Acta Geologica Sinica, 83(2): 272-283]

本文对出露于南天山南缘断裂带的欧西达坂岩体进行了系统的岩石学、地球化学和锫石U-Pb年代学研究,重点讨论了其岩石成因、源区性质及其大地构造意义.岩体主要由石英闪长岩、二长花岗岩和花岗斑岩组成,并且显示了强烈的后期变形特征.LA-ICP-MS微区定年获得了两组年龄:421±3Ma,273士2Ma,前者为二长花岗岩结晶年龄,而后者则代表了南天山后碰撞伸展走滑作用的时代.地球化学特征显示,二长花岗岩的SiO2含量介于65.16%～75.50%之间,Mg#值低(0.23～0.41),A/CNK-0.86～1.15,为过铝一强过铝质,钙碱-高钾钙碱系列花岗岩;(La/Yb)N为4.40～6.32,Eu=0.58～0.77.与二长花岗岩相比,石英闪长岩的SiO2含量较低(55.46%～58.29%),相对富钛、钙、铁、铝和MgO等;铝饱和指数A/CNK-0.88～1.04,Mg#值高(0.45～0.50),为钙碱性系列.二长花岗岩的(La/Yb)N为7.84～9.48,Eu=0.52～0.78.在原始地幔标准化蛛网图上,样品均明显富集Rb、Ba、Th、K等大离子亲石元素和LREE,亏损Nb、Ta、P、Ti等高场强元素.而二长花岗岩表现为更加亏损Nb、Ta、P、Ti等元素,并具有明显的Sr负异常.该岩体高的Al2O3、La/Nb、Th/Ta值和原始地幔标准化图解中Nb--Ti的负异常说明该套岩石形成于板块边缘环境或来自岛弧环境下的陆壳源区.石英闪长岩可能来源于镁铁质岩浆底侵导致的下地壳部分熔融,二长花岗岩可能是来自于中下地壳的无水熔融.欧西达坂岩体体现了南天山洋早古生代向南短暂而局部的平坦的低角度板片俯冲.综合区域地质资料分析推测在早古生代南天山洋可能存在双向俯冲,从而形成同一洋盆中的蛇绿岩在南天山南北两侧的就位;而在晚古生代南天山洋一直向北俯冲,具有长期、多阶段的特征.

... 8,Ma,均具有大陆弧花岗岩的性质,说明至少在志留纪塔里木北缘已转化为主动大陆边缘,南天山洋盆向南俯冲到塔里木板块之下(王超等,2009 ...

2014

0.0

王庆同, 杨宝忠, 姜文钦, 周发侨, 张枭, 王卫国. 2014. 新疆色帕巴衣地区志留纪柯坪塔格组笔石的发现. 地质通报, 33(1): 19-25.

[Wang Q

, Yang B

, Jiang W

, Zhou F

, Zhang

, Wang W

. 2014. The discovery of Silurian graptolites from the Kepingtage Formation in Sepabayi area, Xinjiang. Geological Bulletin of China, 33(1): 19-25]

2014

0.0

王松. 2014. 南天山晚古生代—新生代沉积记录及其对构造演化的制约. 合肥工业大学博士论文: 1-126.

[Wang

. 2014. Late Paleozoic to Cenozoic Sedimentary Record of the South Tianshan and Its Implications for Tectonic Evolution. Doctoral Dissertation of Hefei University of Technology: 1-126]

南天山地区石炭系—新近系地层发育齐全,主要由碎屑岩和碳酸盐岩组成。本文以野外地质调查和镜下微相分析为基础,对南天山石炭系—新近系岩相做了系统的划分,对石炭系—新近系的沉积体系进行了研究,并利用碎屑组分统计、全岩地球化学、单颗粒矿物地球化学和碎屑锆石U-Pb定年等方法,对沉积物源进行了详细探讨,阐述了石炭系—新近系碎屑岩的物源区及其构造背景,并进一步对南天山造山带的碰撞、隆升剥露历史提供制约。研究区石炭系—新近系发育碳酸盐岩、碎屑岩、石膏岩和煤,其中碳酸盐岩包括砾屑灰岩、(含陆源碎屑)鲕粒灰岩、蜓灰岩、生物碎屑颗粒灰岩、生物碎屑泥粒灰岩、生物碎屑粒泥灰岩、灰泥石灰岩和礁灰岩,碎屑岩主要包括粗砾岩、中砾岩、细砾岩、石英(杂)砂岩、岩屑石英(杂)砂岩、岩屑(杂)砂岩、长石岩屑(杂)砂岩、粉砂岩、泥岩,共17种主要岩石类型。沉积体系分析表明,南天山及南缘石炭系—新近系主要发育9种沉积体系,包括碎屑滨岸沉积体系、碳酸盐台地沉积体系、碳酸盐斜坡沉积体系、大陆斜坡沉积体系、盆地沉积体系、冲积扇沉积体系、河流沉积体系、三角洲沉积体系和湖泊沉积体系,并可细分为14种沉积相类型。海相沉积体系主要发育于石炭系—中二叠统,陆相沉积体系主要见于中二叠世—新近纪的地层中。碎屑岩的岩石学、地球化学分析表明,天山南缘石炭系、三叠系砂岩成分成熟度和结构成熟度均不高,杂基含量较高,从石炭系至三叠系砂岩不稳定组分依次增加。石炭系、二叠系具有相似的稀土元素含量特征,三叠系稀土元素含量明显低于石炭系和二叠系,石炭系—三叠系轻、重稀土元素分馏程度依次减弱,La/Th、La/Y比值依次增大,Th/U比值减小,来自再旋回的物质依次增多。综合碎屑组分、常量元素、稀土元素及微量元素特征的判别,天山南缘石炭系物源区构造背景为既有指示大陆岛弧、活动大陆边缘的证据,也有指示为被动大陆边缘,二叠系物源区示为大陆岛弧,三叠系物源区示为大陆岛弧和含有古老沉积岩的陆块。石炭系碎屑物源具有多种不同的构造属性,显示了双向物源的特点,这种物源特征恰是前陆盆地的典型特征。因此,塔里木板块与伊犁—中天山板块应于石炭纪之前开始碰撞,石炭纪时期南天山地区已经进入了前陆盆地演化阶段。碎屑单矿物化学成分和碎屑锆石年代学分析表明,天山南缘石炭系碎屑物质主要源自中天山南缘及南天山的早古生代中—高级变质岩、花岗岩、基性—超基性火山岩,部分源自塔里木北缘的变质基底；二叠系碎屑物质主要来源于天山的变质沉积岩、花岗岩,此外,塔里木盆地基性火山岩也作为一个重要的源岩；三叠系物源稍显复杂,主要为中天山南缘及南天山的低级—高级变质岩、酸性岩浆岩、岛弧及洋岛玄武岩,而且,从早三叠世到晚三叠世,低级变质岩供应减少,花岗岩及高级变质岩供给增加；侏罗系源岩主要为中天山南缘及南天山的中—高级变质岩、花岗岩和基性—超基性火山岩；新近系碎屑物质可能主要来自于低级变质岩、花岗岩和高压—超高压变质岩,相对缺少中、高级变质岩来源。此外,西南天山榴辉岩中石榴子石成分对比结果表明,南天山剪切带的高压变质岩在晚石炭世时期已经开始遭受剥蚀。研究区石炭系-三叠系中均存在与大洋岛弧玄武岩尖品石成分类似的碎屑铬尖品石,具大洋岛弧构造属性,这为南天山属多岛海造山提供了沉积学证据。南天山造山带开始碰撞时问可以限定在早泥盆世末—中泥盆世,至少在南天山中段及东部已经开始碰撞。这一认识主要基于以下几点：(1)上石炭统阿依里河组最年轻的一组碎屑锆石年龄为404-542Ma；(2)南天山中段上石炭统阿依里河组碎屑岩的物源的构造背景主要显示为大陆岛弧、活动大陆边缘、被动大陆边缘,具有双向物源特征；(3)南天山泥盆纪属于比较典型的海退层序,转折点应该在早泥盆世末；(4)石炭纪时期,南天山已经处于前陆盆地演化阶段,碰撞造山应发生于石炭纪之前；(5)在南天山,早石炭世地层不整合超覆在元古宇到下泥盆统不同时代地层之上,属于区域性不整合。沉积特征和物源分析表明,南天山造山带的初步隆升应发生在石炭纪,上古生界的大规模剥蚀应该发生在三叠纪；早侏罗世时期,南天山和中天山已有较大规模剥露,西南天山高压变质岩遭受剥蚀；中侏罗世—早白垩世早期,南天山发生小规模隆升,南天山北缘高压变质带供应减少,物源以南天山下古生界及泥盆系为主；早白垩世—始新世早期,随着南天山的进一步夷平,北缘的高压变质带和中天山南缘石炭—二叠纪碱性花岗岩带成为库车坳陷主要的物源供给区；由于欧亚大陆与印度大陆碰撞的远程效应,使得南天山在始新世晚期—上新世强烈隆升,阻挡北部高压变质带和中天山南缘石炭—二叠系花岗岩带的物质供给,库车坳陷在此时期以南天山下古生界为主要物源。可是,在南天山西段南缘乌恰一带新近系中发现大量源自于高压变质岩碎屑石榴子石,表明了南天山西段在新近纪时期并未大规模隆起,也未阻挡高压变质岩物质的供给。这表明南天山造山带在东西方向上存在差异隆升。

2009

0.0

邬光辉, 张宝收, 郭春利, 王成林, 高辉. 2009. 塔里木盆地北部志留系碎屑锆石测年及其地质意义. 大地构造与成矿学, 33(3): 418-426.

[Wu G

, Zhang B

, Guo C

, Wang C

, Gao

. 2009. Detrital zircon U-Pb dating for the Silurian in northern Tarim Basin and its significance. Geotectonica et Metallogenia, 33(3): 418-426]

... 在前人(邬光辉等,2009,2010 ...

2010

0.0

邬光辉, 孙建华, 郭群英, 唐涛, 陈志勇, 冯晓军. 2010. 塔里木盆地碎屑锆石年龄分布对前寒武纪基底的指示. 地球学报, 31(1): 65-72.

[Wu G

, Sun J

, Guo Q

, Tang

, Chen Z

, Feng X

. 2010. The distribution of detrital zircon U-Pb ages and its significance to Precambrian basement in Tarim Basin. Acta Geoscientica Sinica, 31(1): 65-72]

In order to get the information concerning the relationship between the Tarim Precambrian basement and the supercontinent, the authors analyzed the U-Pb isotopic ages of zircons from 11 clastic rocks in different areas of Tarim Basin in situ by means of LA-ICP-MS. The results show that there existed Early Paleoproterozoic provenance in northern Tarim and Middle Mesoproterozoic provenance in southern Tarim. An analysis of detrital zircon ages and data of surrounding orogenic belts indicates that a uniform Tarim basement did not exist in Paleo-proterozoic and Mesoproterozoic, during which the North and South Tarim continents had different evolution events. The North Tarim continent probably had the same tectonic event as the breakup of Columbia superconti-nent. The collision between North and South Tarim continents took place in Early Neoproterozoic, resulting in the formation of a uniform Tarim basement. All of the clastic rocks have Nanhuan ages, which indicates that there was a large scale breakup of the Tarim continent in Nanhuan period. The thermo-tectonic event in Nanhuan period provided widespread provenance of the cap rocks. The Tarim continent might have had the same tectono-thermal events as the breakup of the Rodinia supercontinent. These results have yielded new intraplate evidence for con-straining the relation between the Tarim plate and the supercontinent.

应用碎屑锆石LA-ICP-MS U-Pb定年方法研究塔里木盆地前寒武纪基底与超大陆的关系, 对盆地内部不同地区井下11个碎屑岩样品进行锆石年代学分析。塔里木盆地南部与北部分别检测到早元古代、中元古代产生的物源, 结合周边造山带测年资料分析佐证了早中元古代塔里木南北块体演化有差异, 北部大量的中元古代早期年代数据可能预示塔北微块体存在与Columbia超大陆裂解时间相近的构造－热事件。南北塔里木在新元古代早期才发生碰撞拼合形成统一的基底与演化进程, 所有样品都检测到南华纪年龄数据证实塔里木板块及其周缘在此期发生大规模裂解事件, 南华纪大规模火成岩活动形成了盆地显生宙碎屑岩最主要的蚀源, 塔里木板块存在与Rodinia超大陆裂解时间相当的构造－热事件。碎屑锆石测年资料为研究塔里木板块与超大陆的关系提供了来自盆地内部的证据。

... 在前人(邬光辉等,2009,2010 ...

2011

0.0

熊小辉, 肖加飞. 2011. 沉积环境的地球化学示踪. 地球与环境, 39(3): 405-414.

[Xiong X

, Xiao J

. 2011. Geochemical indicators of sedimentary environments: A Summary. Earth and Environment, 39(3): 405-414]

运用地球化学的方法,通过研究沉积岩或沉积物中各常量、微量元素及各种同位素特征,来示踪古沉积环境,以了解当时的沉积特征。通过Sr/Ba法、硼元素法、碳氧同位素法等地球化学指标判定海相沉积还是陆相沉积及了解古盐度信息;不同气候条件下特定元素(如P、Sr等)含量及元素比值(如Sr/Cu、Mg/Ca)可指示特定的古气候条件;沉积水体的氧化还原状态可通过氧化还原敏感元素(如Mo、U、V、Ni、Ce、Eu等)的分析得到较好的恢复;古水深以及海平面的相对变化则利用了元素迁移能力的差异,通过查明不同深度带沉积的元素组合(Fe族、Mn族)、比值(Sr/Ba、Sr/Ca)及同位素(87Sr/86Sr比值)的不同加以判定。沉积环境的地球化学特征同样可以用来判定沉积物源、物源岩性和构造背景及热水沉积。

... 熊小辉和肖加飞,2011 ...

2014

0.0

张斌, 陈文, 喻顺, 尹继元, 李洁, 孙敬博, 杨莉, 杨静. 2014. 南天山洋古生代期间俯冲作用过程探讨. 岩石学报, 30(8): 2351-2362.

[Zhang

, Chen

, Yu

, Yin J

, Li

, Sun J

, Yang

. 2014. Subduction process of South Tianshan Ocean during Paleozoic. Acta Petrologica Sinica, 30(8): 2351-2362]

The subduction process of South Tianshan Ocean is a significance aspect of Central-Asian Orogenic Belt research and there still exists a controversy concerning the way of subduction. A series of nearly east-west distribution of intermediate-acid intrusive rocks are exposed in southern margin of the South Tianshan and selected as the object of this research. Ouxidaban quartz diorite, located in the region, i. e. the north of Kuqa foreland basin, is studied in detail in this paper. Geochemical characteristics suggest that Ouxidaban quartz diorite has SiO2 (54.23% similar to 56.27%), Al2O3 (15.15% similar to 16.03%), CaO (6.44% similar to 7.56%), K2O (1.51% similar to 2.08%) and Na2O (2.30% similar to 2.62%) with A/NCK (0.77 similar to 0.91), high Al and low Ti with obvious depletion of Nb and Ta. Besides, the Ouxidaban pluton is enriched in large ion lithophile elements (K, Rb, Ba and Pb) and depleted in high field strength elements (Nb, Ta, Zr, Hf, Ti and P), with relatively more light rare earth elements than heavy rare earth elements with the chondritenormalized rare earth element patterns of slightly right-dipping V-type. These features indicated that Ouxidaban quartz diorite is typical calcium-alkali magmatic rocks which was formed in a subduction stage with a zircon LA -ICP-MS micro area (206)pb/(238) weighted average age of 418. 4 +/- 2. 2Ma. It' s widely acknowledged that the north Tarim craton and the south Central-Yili block all have lots of rocks produced by subduction. The ages of the rocks distributed in the southern part of Central-Yili block, ranges from Precambrian to Late Carboniferous and this region does not have an obvious silent time of magma activity. However, the rocks distributed in north Tarim craton whose ages concentrate on 426 similar to 418Ma, except for a granite of 386Ma which is located in east of Ouxidaban pluton and produced by subduction as well. At the same time, there are not a broader magma arc and a peaceful magma activity time in the north Tarim craton. Although a complex tectonic deformation existed there, it wasn't caused by the southward subduction of South Tianshan Ocean. In conclusion, this paper proposes that northern Tarim plate has been transformed from the passive continental margin to active continental margin in Silurian at latest and then it returned to the passive continental margin in Devonian. The evolution of the South Tianshan Ocean during Early Paleozoic was dominated by bidirectional subduction but the southward subduction was short, intermittent or pulse type subduction process until the end of middle Devonian, and the north subduction was a long-term and multi-stage process until the beginning of collision between Central-Yili block and Tarim plate. It should also be noted that the southward subduction process of South Tianshan Ocean was mostly like a normal high-angle subduction.

南天山洋的演化历史是中亚造山带研究中关键的问题，目前对古生代期间南天山洋的俯冲极性、俯冲方式等问题仍然存在着争议。南天山造山带南部地区近东西向出露一系列中酸性侵入岩，本文以其中的欧西达坂石英闪长岩为对象，开展了系统的岩石学、地球化学和同位素年代学研究。地球化学特征显示其富集Rb、Ba、K、Pb等大离子亲石元素，亏损Nb、Ta、Zr、Hf等高场强元素，轻稀土元素较重稀土元素富集，稀土配分曲线呈右倾的"海鸥"型，为典型的俯冲成因钙碱性系列岩浆岩，锆石LA-ICP-MS微区定年获得418.4±2.2Ma的 206 Pb/ 238 U加权平均年龄。结合区域地质背景及前人成果，初步认为塔里木板块北缘至少在志留纪时期已由被动大陆边缘转变成活动大陆边缘，中泥盆世开始又转变为被动大陆边缘；早古生代阶段南天山洋的演化以双向俯冲为主，向南为短期、脉冲式或间歇式的正常高角度俯冲过程，至中泥盆世结束；向北则为长期、多阶段性的俯冲。

... 张斌等,2014) ...

2007

0.0

张鑫, 张金亮, 覃利娟. 2007. 塔里木盆地志留系柯坪塔格组砂岩岩石学特征与物源分析. 矿物岩石, 27(3): 106-115.

[Zhang

, Zhang J

, Qin L

. 2007. Petrological characteristics and provenance analysis of sand stones in the Kepingtage Formation of Silurian in the Tarim Basin. Journal of Mineralogy and Petrology, 27(3): 106-115]

... Eu)可以灵敏地反映体系内的地球化学状态,并可作为鉴别物质来源的重要参数(张鑫等,2007) ...

... 9,张鑫等,2007) ...

2014

0.0

张英利, 王宗起, 闫臻, 王涛. 2014. 新疆库鲁克塔格早志留世地层沉积学、物源分析新认识. 地质学报, 88(10): 1970-1980.

[Zhang Y

, Wang Z

, Yan

, Wang

. 2014. New insights on sedimentology, provenance analysis of the Early Silurian in the Quruqtagh area, Xinjiang. Acta Geologica Sinica, 88(10): 1970-1980]

库鲁克塔格地区早志留世地层主要由灰绿色砂岩和粉砂岩组成,为浊流成因,沉积环境为海底扇。运用LA-ICP-MS U-Pb方法,对早志留世2件砂岩碎屑锆石进行U-Pb年龄测定,共获得了89组U-Pb有效年龄,获得了地层的物源、研究区区域对比和早古生代的构造演化资料。碎屑锆石的谐和年龄表明,689~836Ma为早志留世地层的主要物源区,866~986Ma、1055~1463Ma和1708~2490Ma 为次要物源区,部分为二次搬运。志留纪碎屑锆石的年龄概率图指出,早志留世可能为岩浆活动的安静期,早志留世之后,库鲁克塔格地区中—晚奥陶世岩石大规模隆升。碎屑锆石年龄和CL图像揭示,新元古代时期发育大量岩浆活动,可能与南天山洋向塔里木板块俯冲相关。区域变质作用同样在碎屑锆石中有所反映。

... 张英利等,2014) ...

2012

0.0

张宇航, 汤良杰, 云露, 谢大庆, 邱海峻, 蒋华山. 2012. 塔里木盆地关键构造变革期不整合特征及其地质意义. 世界地质, 31(2): 306-314.

[Zhang Y

, Tang L

, Yun

, Xie D

, Qiu H

, Jiang H

. Unconformity characteristics and geological significance in key tectonic revolution stage of Tarim Basin. Global Geology, 31(2): 306-314]

Tarim Basin suffered seven key tectonic revolution stages since Ordovician，including the episode Ⅰ of middle Caledonian，episode Ⅲ of middle Caledonian，early Hercynian，late Hercynian，Indo-Chinese，middle Yanshan and late Yanshan-Himalayan，and generated seven important unconformities with different types and characteristics． Through seismic profile recognition，logging analysis and core observation，the authors considered that these unconformities appeared in parallel，superimposed，folded，fault-folded，ancient karst and palaeo-erosion unconformities in type． Associated with the evolution of the Tarim Basin，unconformities changed constantly in geometric shape，space and time． According to these changes，the authors considered that the unconformities were characterized by superimposition and composition in geometric shape，lamination and difference in space，and migration in time． The unconformities characteristics in Tarim Basin had close relationship with tectonic movement，erosion time and palaeo-sedimentary environment．

塔里木盆地自奥陶纪以来，先后经历了加里东中期Ⅰ幕、加里东中期Ⅲ幕、海西早期、海西晚期、印支期、燕山中期及燕山晚期--喜马拉雅期等7 次关键构造变革期，并且形成7 个重要不整合界面，这些不整合具有各自不同的类型和特征。通过地震剖面识别、测井分析和岩心观察等手段分析，认为这些不整合面现今在盆地内主要表现为平行不整合、叠合不整合、褶皱不整合、断褶不整合、古岩溶和古侵蚀不整合。随着盆地的演化，这些不整合面在几何形态、空间位置和时间上不断发生变化。根据这些变化，认为塔里木盆地这些主要不整合在几何形态上具有叠合、复合特征，空间上具有分层、差异的特征，时间上表现为迁移特征。不整合与所经历的构造运动强弱，剥蚀时间长短，沉积时的气候、环境有着密切关系

... 张宇航等,2012 ...

2014

0.0

周科. 2014. 常量元素与微量元素特征在物源分析中的应用. 辽宁化工, 43(4): 515-520.

[Zhou

. 2014. Application of the characteristics of major elements and trace elements in provenance analysis. Liaoning Chemical Industry, 43(4): 515-520]

... 周科,2014) ...

2002

0.0

周新源, 李曰俊, 王招明, 李宇平, 罗俊成, 张博. 2002. 塔里木盆地西北缘下志留统沉积构造背景初探. 地质科学, 37(S1): 57-63.

[Zhou X

, Li Y

, Wang Z

, Li Y

, Luo J

, Zhang

. 2002. A preliminary study on tectonic setting of the Lower Silurian in NW Tarim. Chinese Journal of Geology, 37(S1): 57-63]

塔里木盆地西北缘柯坪塔格组中段的浊积岩(灰-灰绿色砂-泥岩)时代属早志留世.12个样品的岩石化学分析结果表明其形成的大地构造背景为被动大陆边缘,物源区性质函数判别图则指示了一个成熟大陆石英质物源区.据此认为塔里木盆地西北缘志留纪时发育被动大陆边缘.

... 末志留世研究区碎屑物质更可能来源于相对稳定的陆源区或继承性的、更老的沉积岩再旋回堆积的产物(Roser and Korsch,1988),研究结果与东部乌什南索格当他乌剖面志留系的沉积物源分析结果一致(周新源等,2002) ...

1978

0.0

1983

0.0

1986

0.0

2011

0.0

... Charvet et al ...

1992

0.0

... 11)之间,说明砂岩成熟度增加(Condie et al ...

2002

0.0

... Gu et al ...

2011

0.0

... Han et al ...

2013

0.0

... Ma et al ...

... 另有部分学者通过对南天山造山带南缘及塔里木板块北缘出露的岩浆岩研究发现,南天山洋在构造演化过程中存在双向俯冲,在向北俯冲的同时,向南短暂地俯冲到塔里木板块之下,塔里木板块北缘在早古生代存在活动大陆边缘(Ma et al ...

1986

0.0

... Roser和Korsch(1986)利用砂泥岩中K₂O/Na₂O值与SiO₂含量的变化规律,提出了K₂O/Na₂O-SiO₂构造环境判别图解 ...

1988

0.0

... Al₂O₃/SiO₂值可以作为碎屑沉积物成熟度的指标(Roser and Korsch,1988),样品Al₂O₃/SiO₂值在0 ...

1989

0.0

1985

0.0

... 超基性与酸性物质成分的指标(Taylor and Mclennan,1985 ...

2014

0.0

... Xia et al ...

2013

0.0

... Xiao et al ...