-
黄土高原沉积了巨厚的黄土—古土壤风尘沉积序列,记录了第四纪以来多尺度的气候变化及环境信息[1⁃6]。黄土粉尘来源和搬运机制的研究,对了解第四纪以来亚洲季风乃至全球气候的演化具有重要意义。
关于黄土物源,前人利用多种手段进行了研究[7⁃28]。刘东生[7]依据黄土高原周围的地形和现代季风方向以及粒度变化,认为黄土主要来自西北三大内陆盆地及周边戈壁沙漠；Sun[9]通过对比多个样品的Sr-Nd同位素、稀土元素等特征,认为黄土主要来自蒙古国南部以及附近的戈壁沙漠地区,而非内陆三大盆地；陈骏等[10]通过黄土中的Sr-Nd同位素以及碳酸盐等特征,认为黄土主要来自青藏高原北部和中亚造山带以及中间的沙漠地带。Stevens et al.[13]对末次冰期黄土进行锆石年代学分析,认为塔克拉玛干沙漠和祁连山可能是黄土的潜在物源区。Xiao et al.[14]通过多剖面的锆石年代学研究,认为黄土物源具有一定的时空差异性。第四纪以来气候波动频繁,冬、夏季风的循环交替伴随了冰期—间冰期旋回的出现。有学者认为,黄土粉尘来源可能随冰期—间冰期近地面季风强度及方向的周期性演化而改变[10⁃11,29⁃31]；另一部分学者通过黄土中Sr-Nd同位素以及矿物学特征的研究,认为物源在轨道尺度上并未发生变化[32⁃35]；Pullen et al.[15]通过碎屑锆石U-Pb年代学的研究,认为黄土物源在冰期—间冰期发生了变化；Xiao et al.[14]则进一步指出西风风暴路径在冰期和间冰期之间发生变化,冰期黄土来自柴达木盆地,间冰期则来自更北的地区；而Fenn et al.[36]通过对北郭塬碎屑锆石U-Pb年代学和石榴子石矿物学研究,认为轨道尺度上物源并未发生变化,次峰的分布差异是由人为挑选造成的；Bird et al.[19]则认为冰期—间冰期内黄土锆石U-Pb年龄的差异是由古气候的变化造成的,这一观点与Nie et al.[37]基于重矿物组合的分析结果相同。笔者注意到上述研究存在的不足之处,例如Pullen et al.[15]在洛川采集的黄土样品,年代跨度较大、缺少部分间冰期古土壤层位的信息,且部分层位锆石年龄数量较少。此外,部分研究中锆石年龄谱中的差异,可能是由于人为挑选以及样本数量偏少造成的,不能完全确定物源是否发生变化[36,38]；基于石英释光灵敏度的研究,则未能完全排除沉积速率以及矿物风化的影响[31]；同时有学者提出Sr-Nd同位素比值的差异,是风力的分选作用以及风化作用造成的,而非物源变化导致[17]。因此,黄土高原黄土物源在轨道尺度上是否发生变化仍需进一步研究。
与传统全岩物源示踪方法相比,碎屑锆石U-Pb年代学,能够更好地避免源区信息的均一化、体现混合源区特征,同时反映源区多阶段的造岩信息[24,39⁃43]。因此,基于上述研究中存在的问题,本文选取灵台—任家坡及洛川—黑木沟两个研究程度高、层序完整的典型剖面,进行锆石U-Pb定年学研究。通过与潜在物源区数据进行对比,分析黄土的主要物源区域以及可能存在的时间变化,并结合前人的研究成果,探讨轨道尺度内冰期、间冰期沉积物物源是否发生变化。
-
选取黄土高原中南部、六盘山以东的洛川—黑木沟和灵台—任家坡剖面为研究对象（图1）。黑木沟剖面位于陕西省洛川县以南约5 km的黑木沟（35°45′ N,109°25′ E）,总厚度约140 m,其中130 m为第四纪黄土沉积层,下部为新近纪红黏土；灵台剖面位于甘肃省灵台县以南约13 km的任家坡（35°04' N,107°39' E）,晚新生代以来共沉积了约300 m的风成沉积,其中第四纪风成黄土厚为170 m。
利用前人划分的地层成果[13,15,44⁃45],在两个研究剖面分别采集黑垆土（S0）、马兰黄土（L1）、第二层黄土（L2）、第二层古土壤（S2）及洛川黄土—古土壤剖面的第一层古土壤（S1）共9个样品（图2）,每个层位的采样重量大于10 kg。将采集到的样品送至河北省廊坊地质大队进行锆石挑选作业,每个样品挑选出500粒以上的锆石。为避免因锆石统计数量的原因造成数据误差,随机选择约120粒碎屑锆石进行试验[46]。
图 2 样品采集位置地层柱状图
Figure 2. Stratigraphic histogram of the study sections
锆石U-Pb年龄的测定在西北大学大陆动力学国家重点实验室进行,采用激光剥蚀—电感耦合等离子体质谱仪（LA-ICPMS）,激光光束直径30 μm,频率10 Hz,剥蚀物载气采用He。锆石U-Pb年龄采用29Si为内标,NIST610为外标,Harvard锆石91500为元素分馏效应的外部矫正标准。锆石U-Pb年龄协和度的计算采用Isoplot4.5。锆石数据采用直方图、概率密度图（Probability Density Plot,PDP）以及核密度估计图（Kernal Density Estimate,KDE）呈现[47]。因数据量大,采用非矩阵多维标度统计分析（Multi-Dimensional Scaling,MDS）对数据进行相关度分析以期确定黄土物源[48⁃49]。
-
洛川黄土—古土壤的锆石U-Pb年龄分布图（图3）显示,洛川剖面5个样品的主要年龄分布在200~600 Ma,呈双峰分布,峰值主要分布在300 Ma和450 Ma左右。其中第一峰值（300 Ma）占比略低于第二峰值（450 Ma）,第二峰值（450 Ma）为优势峰值；次要年龄分布在900~1 200 Ma、1 800~2 100 Ma、2 400~2 700 Ma,除S2层位的样品次要年龄主要分布在1 800~2 100 Ma外,其他层位在三个次年龄段的分布较为均匀。
图 3 洛川黄土—古土壤碎屑锆石U⁃Pb年龄分布图
Figure 3. Distribution of detrital zircon U⁃Pb ages from Luochuan loess⁃paleosol samples
灵台黄土—古土壤剖面的碎屑锆石U-Pb年龄分布图（图4）显示,4个样品的主要年龄分布在200~600 Ma年龄段,呈双峰分布,峰值主要分布在270 Ma和450 Ma左右,其中第一峰值（270 Ma）占比略低于第二峰值（450 Ma）,第二峰值（450 Ma）为优势峰值。次要年龄主要分布在900~1 200 Ma、1 800~2 100 Ma以及2 400~2 700 Ma,其中S0~L1的主要分布在600~900 Ma,而L2~S2则主要分布在900~1 200 Ma,2 100 Ma以后分布较少。尽管在600~2 700 Ma的年龄分布存在一定差异,但4个样品的主要年龄（200~600 Ma）的分布较为一致。
图 4 灵台黄土—古土壤碎屑锆石U⁃Pb年龄分布图
Figure 4. Distribution of detrital zircon U⁃Pb ages from Lingtai loess⁃paleosol samples
-
黄土作为风力作用的结果,其潜在物源区应该是黄土高原周边的造山带、戈壁沙漠以及河流阶地沉积物[14⁃15,19⁃21]。为了更好地研究黄土高原洛川与灵台剖面黄土—古土壤沉积物质的来源,选择了一些潜在物源区,包括发源于祁连山的弱水河下游冲积扇样品（RSH）[38]、东西毛乌素沙漠样品[13]、黄河河床沉积物样品（YR）[16]、阿尔泰山脉冲积扇样品（GAM）[20,38]、腾格里沙漠样品（TD）[13,20]和柴达木盆地样品（QB）以及松潘甘孜样品（SP）[15]等（图5）。
利用MDS进行数据的相关性分析,绘制出样品与各潜在物源区的相似/相异图,图中实线连接相近样品,虚线连接次相近样品。结果表明（图6）,本次采集的9个样品与弱水河下游沉积物、西毛乌素沙漠、黄河以及松潘、柴达木盆地的样品具有更好的相关性。
图 6 灵台—洛川样品及潜在物源区碎屑锆石U⁃Pb年龄数据非矩阵多维标度（MDS）统计分析图
Figure 6. Multi⁃dimensional scaling（MDS）plots of statistical analysis of detrital zircons U⁃Pb age data from the layers of the Lingtai⁃Luochuan profile and the samples of potential provenance regions in the Loess Plateau
通过对比样品与潜在物源区域的锆石U-Pb年龄分布特征（图7）,发现弱水河下游冲积扇（RSH）、西毛乌素沙漠（W-MUS）以及黄河（YR）三个物源区的样品在主要及次要年龄的分布上均与黄土—古土壤样品较为一致。洛川和灵台各样品的主要年龄分布在200~600 Ma且呈双峰分布,其中第一峰值（250~300 Ma）略低于第二峰值（350~600 Ma）；次要年龄分布在900~1 200 Ma、1 800~2 100 Ma。而柴达木盆地及东毛乌素沙漠（E-MUS）的主要年龄分布与本研究的数据存在一定差异：东毛乌素沙漠样品的优势峰值分布在200~360 Ma,且明显具有更多的1 800 Ma以后的碎屑锆石。柴达木盆地样品的主要年龄分布在200~600 Ma,但其第一峰值（250~300 Ma）与第二峰值（350~600 Ma）占比差异较大,且大于900 Ma的年龄分布占比过小,与本次研究采集样品的锆石年龄分布存在较大差异。同时,有研究认为第四纪以来柴达木盆地没有足够的碎屑物质输送到黄土高原[50],而东毛乌素沙漠两段不同的年龄分布代表着不同的沉积物来源,其中较年轻的沉积物来自中亚造山带,较老的沉积物来自基底的华北克拉通[13,51⁃52]。因此,东毛乌素沙漠以及柴达木盆地并不是黄土高原的主要物源区域。
图 7 黄土高原潜在物源区锆石U⁃Pb年龄分布图
Figure 7. Distribution of detrital zircon U⁃Pb ages from the samples of potential provenance regions in the Loess Plateau
由于弱水河流经祁连山至阿尔泰山中间的阿拉善区域,且在MDS图中与腾格里沙漠样品（TD）表现出较好的相关性（图6）,因此将弱水河下游沉积物样品（RSH）与腾格里沙漠样品（TD）共同作为阿拉善区域的混合沉积物代表。黄河发源于青藏高原并流经黄土高原西北部的中央沙漠地带。且西毛乌素沙漠样品（W-MUS）和黄河样品（YR）的碎屑物质与青藏高原东北部的松潘甘孜（SP）在锆石年龄的分布上表现出较好的一致性,因此推论前者的碎屑物质同样来自青藏高原东北部。综上,研究区内黄土的粉尘物质来自青藏高原东北部、阿拉善区域以及西毛乌素沙漠。
-
本次研究采集的黄土—古土壤样品的锆石U-Pb年龄（图3,4）显示,黄土层位L1、L2与古土壤层位S0、S1、S2之间,锆石年龄的分布较为一致,均为双峰分布,且优势峰值为360~600 Ma。尽管在灵台剖面的S0、L1与L2、S2之间在900~1 200 Ma分布存在一定差异,但这种差异可能是因为在L2沉积过程中,弱水河流域以及松潘甘孜贡献了更多的粉尘物质,在潜在物源区域的锆石U-Pb年龄图（图7）中,只有这两个样品在900~1 200 Ma分布较多。而反映冰期—间冰期物源的黄土—古土壤层位S0、L1、S1与L2、S2之间,锆石U-Pb年龄的分布则较为一致,指示轨道尺度内物源并未发生改变。
有学者认为锆石的统计数目会影响锆石年龄谱所反映的各年龄组分的真实丰度[40,53]。因此,将采集的各层位的数据按黄土、古土壤分为两个单元整理,根据锆石U-Pb年龄特征（图8）对黄土—古土壤的主要年龄进行统计。统计结果（表1）显示,锆石年龄主要分布在200~360 Ma、360~600 Ma、750~1 200 Ma、1 800~2 100 Ma以及大于2 400 Ma五个年龄段。在黄土与古土壤两个单元之间,年龄的分布较为一致,200~360 Ma、360~600 Ma两个年龄段占总体年龄的50%以上,且优势峰值位于360~600 Ma。为更直观地呈现黄土与古土壤锆石年龄的分布特征,绘制了锆石年龄的累计分布图（Cumulative Age Distribution,CAD）,结果显示黄土与古土壤两个数据集的累计增长趋势基本一致,甚至在部分年龄段出现重合（图9）。反映黄土与古土壤的锆石U-Pb年龄组成较为一致,指示冰期—间冰期内黄土物源未发生变化。
图 8 黄土—古土壤锆石U⁃Pb年龄概率密度（KDE）图
Figure 8. Kernal density estimate（KDE）diagram of detrital zircon U⁃Pb age in loess⁃paleosol
表 1 黄土—古土壤碎屑锆石主要年龄分布及百分比统计
Table 1. Main age distribution and percentage statistics of detrital zircon in loess⁃paleosol
类型 200~360 Ma 360~600 Ma 750~1 200 Ma 1 800~2 100 Ma >2 400 Ma 共计 黄土 18.8% 33.0% 14.5% 10.1% 5.3% 81.7% 古土壤 23.0% 31.8% 13.5% 12.3% 5.1% 85.7% 
图 9 黄土—古土壤碎屑锆石U⁃Pb年龄累计分布（CAD）图
Figure 9. Cumulative U⁃Pb age distribution (CAD) of detrital zircon in loess⁃paleosol
-
黄土高原是青藏高原隆升和东亚季风系统演化的协同产物[54]。中更新世气候转型事件（Mid-Pleistocene Transition,MPT）以来,全球冰量增加、CO2浓度降低,亚洲内陆的干旱化进一步加剧[2]。同一时期黄土粉砂层中的沉积速率以及粉尘通量的急剧增加[55⁃56],表明黄土的沉积需要大量的碎屑物质。1.2 Ma左右,青藏高原进入快速隆升的“昆—黄运动”阶段[57],在构造运动以及风化作用的影响下,周围的造山带产生了大量的碎屑物质。而东亚冬季风的增强以及河流侵蚀作用的加剧为粉尘的搬运创造了良好的外部条件。黄土样品、西毛乌素沙漠以及黄河的锆石年龄分布特征均与青藏高原东北缘表现出一定的相似性[16,18,37],说明大量的碎屑物质首先被搬运到邻近的山前冲洪积扇以及戈壁沙漠,而后在季风以及河流的共同搬运作用下运输至黄土高原（图10）。前人基于亚洲风尘系统的源—汇系统研究,认为中亚造山带与青藏高原东北部之间的干旱区既是黄土的物源区域,也是粉尘物质搬运的周转区域[58⁃59]。因此,黄土高原粉尘物质的形成是青藏高原东北部、阿拉善区域、黄河流域以及西毛乌素沙漠的多源混合的结果,是“山脉—河流—沙漠”的复合产物[60]。
在冰期—间冰期尺度上,此次研究的结果表明,黄土在冰期—间冰期内的粉尘物源保持稳定。黄土高原的粉尘物质主要受东亚季风以及西风的搬运作用[61]。近缘的粗粒粉尘搬运受近地面的西北风（冬季风）影响,而远距离的细粒粉尘搬运则主要由高空西风完成[62⁃63]。孙东怀等[55]对洛川黄土粒度的研究表明,约1.2 Ma以来高空西风环流对黄土高原风尘贡献减少,低空季风环流的贡献逐渐增多。而东亚季风产生的主要原因在于亚洲与太平洋之间的海陆热力差异。在冰期和间冰期,因为蒙古西伯利亚高压与阿留申低压和海洋大陆低压的位置大致稳定,且黄土高原周围地形相对稳定,东亚冬季风的风向是相似的。尽管高纬度气团扩张下的高低压系统对比增加,东亚冬季风在冰期增强,但总体而言,冰期—间冰期交替期间冬、夏季风的形成过程和大气环流在整个华北高原大致保持不变[64⁃65]。而样品数据的部分差异可能是因为季风风场的转变造成了个别源区对黄土高原提供碎屑物质的贡献差异。除此之外,黄土与古土壤之间较为一致的重矿物组合（Nie et al.[37]以及本文未发表数据）进一步支持古土壤是黄土在间冰期经历较强的风化、成壤作用的继承产物[1,66]。综上,黄土高原的粉尘物源在冰期—间冰期内来源一致。
-
（1） 0.2 Ma以来,六盘山东部黄土高原的粉尘物质来自青藏高原东北部、阿拉善区域、黄河流域及西毛乌素沙漠,表明黄土高原的粉尘堆积是西北向多源混合的产物。
（2） 样品的各层黄土与古土壤之间并未发现明显的锆石U-Pb年龄分布差异,指示冰期—间冰期内粉尘来源较为稳定。
Zircon U-Pb Ages Provenance Research of Glacial-interglacial Sediments from the Eastern Liupanshan Region of the Loess Plateau
-
摘要: 目的 黄土高原在冰期—间冰期沉积的黄土物源变化特征存在较大争议,仍需进一步研究。 方法 选取黄土高原中南部的洛川、灵台黄土—古土壤剖面,分别采集黑垆土（S0）、马兰黄土（L1）、第二层黄土（L2）、第二层古土壤（S2）及洛川黄土—古土壤剖面的第一层古土壤（S1）共9个样品,进行碎屑锆石U-Pb年代学研究。通过对比不同层位之间以及潜在物源区的锆石U-Pb年龄组合,并利用非矩阵多维标度统计分析（Multi-Dimensional Scaling,MDS）技术分析数据的相关性。 结果 发现两个黄土—古土壤剖面样品的锆石U-Pb年龄分布特征与青藏高原东北部、阿拉善区域以及西毛乌素沙漠锆石U-Pb年龄分布特征更为相似；代表冰期的黄土与代表间冰期的古土壤之间,碎屑锆石U-Pb年龄分布特征基本一致。 结论 综合研究认为,受青藏高原隆起以及东亚季风增强的影响,亚洲内陆干旱区持续扩大,六盘山以东黄土高原的粉尘物质主要来源于青藏高原东北部、阿拉善区域及西毛乌素沙漠的混合物质,且冰期—间冰期内的季风演化并未造成黄土物源发生分异。Abstract: Objective The Chinese Loess Plateau （CLP） preserves the most widely distributed, thickest, and continuous aeolian dust deposits in the world. Studying the evolution of loess provenance is important for deducing climate change in inland Asia. Predecessors have made a series of achievements, but the Quaternary climate changed quickly during the glacial-interglacial period accompanied by alternating winter-summer monsoon. Therefore, the source of loess is likely to change with the monsoon； however, there is still controversy regarding the change of loess sources in the glacial-interglacial period due to the lack of evidence of continuous strata. Methods Therefore, in this study, we collected nine loess-paleosol layers from Luochuan （S0, L1, S1, L2, and S2 ） and Lingtai （S0, L1, L2 and S2） for detrital zircon U-Pb dating study. Zircon U-Pb ages were determined at the State Key Laboratory of Continental Dynamics, Northwest University. The U-Pb ages of detrital zircons of the samples are displayed in PDP （Probability Density Plot）, KDE （Kernal Density Estimate）, and CAD （Cumulative Age Distribution） diagrams. By comparing the zircon age combinations between the different layers an potential source regions, we used MDS （multi-dimensional scaling） technology to analyze the data correlation. Results Based on the results, the correlation analysis of the data using MDS showed that nine samples had better correlation with the loess-paleosol samples, including the Ruoshui River, Western Mu Us Desert, Yellow River, and Songpan and Qaidam Basins. However, we found several differences in the KDE and PDP diagrams and indicating that the main age distribution of the samples was 200-600 Ma and the secondary age distributions were between 900-1 200 Ma, 1 800-2 100 Ma, and>2 700 Ma. The U-Pb age characteristics of the Lingtai and Luochuan samples were similar to those of the Songpan Basin, Ruoshui River, Western Mu Us Desert, and Yellow River samples. The Qaidam Basin and Eastern Mu Us Desert showed different age characteristics with our samples. Thus, the Qaidam Basin and Eastern Mu Us Desert were not the main source area of the loess, and we concluded that the dust material was mainly derived from the northwest mixture source, including northeast of the Tibetan Plateau, Alxa region, and Western Mu Us Desert. In addition, no significant difference was found between the loess-paleosol layers during the glacial-interglacial period. To avoid errors caused by data volume, we divided the sample data into two units, namely loess and paleosol, for analysis. The cumulative growth trend of the sample age was analyzed using the CAD diagram, and the results showed that there were not enough data differences, suggesting the provenance remained stable between the glacial and interglacial periods. Conclusions Based on the above research and analysis, we draw the following conclusions： （1） Affected by Asian climate drought and Tibetan Plateau uplift, the dust material is mainly derived from the northwest mixture source, including northeast of the Tibetan Plateau, Alxa region, and Western Mu Us Desert； （2） The source of loess indicating the glacial-interglacial period did not change significantly.
-
Key words:
- Loess Plateau /
- Quaternary loess /
- zircon U-Pb age /
- provenance identification
-
图 3 洛川黄土—古土壤碎屑锆石U⁃Pb年龄分布图
Figure 3. Distribution of detrital zircon U⁃Pb ages from Luochuan loess⁃paleosol samples
图 4 灵台黄土—古土壤碎屑锆石U⁃Pb年龄分布图
Figure 4. Distribution of detrital zircon U⁃Pb ages from Lingtai loess⁃paleosol samples
图 6 灵台—洛川样品及潜在物源区碎屑锆石U⁃Pb年龄数据非矩阵多维标度（MDS）统计分析图
Figure 6. Multi⁃dimensional scaling（MDS）plots of statistical analysis of detrital zircons U⁃Pb age data from the layers of the Lingtai⁃Luochuan profile and the samples of potential provenance regions in the Loess Plateau
图 7 黄土高原潜在物源区锆石U⁃Pb年龄分布图
Figure 7. Distribution of detrital zircon U⁃Pb ages from the samples of potential provenance regions in the Loess Plateau
图 8 黄土—古土壤锆石U⁃Pb年龄概率密度（KDE）图
Figure 8. Kernal density estimate（KDE）diagram of detrital zircon U⁃Pb age in loess⁃paleosol
图 9 黄土—古土壤碎屑锆石U⁃Pb年龄累计分布（CAD）图
Figure 9. Cumulative U⁃Pb age distribution (CAD) of detrital zircon in loess⁃paleosol
表 1 黄土—古土壤碎屑锆石主要年龄分布及百分比统计
Table 1. Main age distribution and percentage statistics of detrital zircon in loess⁃paleosol
类型 200~360 Ma 360~600 Ma 750~1 200 Ma 1 800~2 100 Ma >2 400 Ma 共计 黄土 18.8% 33.0% 14.5% 10.1% 5.3% 81.7% 古土壤 23.0% 31.8% 13.5% 12.3% 5.1% 85.7% 
下载: 导出CSV
-
[1] An Z S, Kukla G J, Porter S C, et al. Magnetic susceptibility evidence of monsoon variation on the Loess Plateau of central China during the last 130,000 years[J]. Quaternary Research, 1991, 36(1): 29-36. [2] Ding Z, Yu Z, Rutter N W, et al. Towards an orbital time scale for Chinese loess deposits[J]. Quaternary Science Reviews, 1994, 13(1): 39-70. [3] Ding Z L, Rutter N W, Sun J M, et al. Re-arrangement of atmospheric circulation at about 2.6Ma over northern China: Evidence from grain size records of loess-palaeosol and red clay sequences[J]. Quaternary Science Reviews, 2000, 19(6): 547-558. [4] An Z S, Kutzbach J E, Prell W L, et al. Evolution of Asian monsoons and phased uplift of the Himalaya-Tibetan Plateau since Late Miocene times[J]. Nature, 2001, 411(6833): 62-66. [5] Ding Z L, Derbyshire E, Yang S L, et al. Stepwise expansion of desert environment across northern China in the past 3.5 Ma and implications for monsoon evolution[J]. Earth and Planetary Science Letters, 2005, 237(1/2): 45-55. [6] 陈洪云,孙有斌. 黄土高原风尘沉积的物质来源研究：回顾与展望[J]. 第四纪研究,2008,28（5）：892-900. Chen Hongyun, Sun Youbin. Study on provenance of eolian dust deposits on the Chinese Loess Plateau: Retrospects and prospects[J]. Quaternary Sciences, 2008, 28(5): 892-900. [7] 刘东生. 黄土与环境[M]. 北京：科学出版社,1985：31-48. Liu Tunsheng. Loess and the environment[M]. Beijing: Science Press, 1985: 31-48. [8] Sun D H, Bloemendal J, Rea D K, et al. Bimodal grain-size distribution of Chinese loess, and its palaeoclimatic implications[J]. Catena, 2004, 55(3): 325-340. [9] Sun J M. Provenance of loess material and formation of loess deposits on the Chinese Loess Plateau[J]. Earth and Planetary Science Letters, 2002, 203(3/4): 845-859. [10] 陈骏,李高军. 亚洲风尘系统地球化学示踪研究[J]. 中国科学：地球科学,2011,41（9）：1211-1232. Chen Jun, Li Gaojun. Geochemical studies on the source region of Asian dust[J]. Science China: Earth Sciences, 2011, 41(9): 1211-1232. [11] Sun Y B, Tada R, Chen J, et al. Tracing the provenance of fine‐grained dust deposited on the central Chinese Loess Plateau[J]. Geophysical Research Letters, 2008, 35(1): L01804. [12] Li G J, Chen J, Ji J F, et al. Natural and anthropogenic sources of East Asian dust[J]. Geology, 2009, 37(8): 727-730. [13] Stevens T, Palk C, Carter A, et al. Assessing the provenance of loess and desert sediments in northern China using U-Pb dating and morphology of detrital zircons[J]. GSA Bulletin, 2010, 122(7/8): 1331-1344. [14] Xiao G Q, Zong K Q, Li G J, et al. Spatial and glacial-interglacial variations in provenance of the Chinese Loess Plateau[J]. Geophysical Research Letters, 2012, 39(20): L20715. [15] Pullen A, Kapp P, McCallister A T, et al. Qaidam Basin and northern Tibetan Plateau as dust sources for the Chinese Loess Plateau and paleoclimatic implications[J]. Geology, 2011, 39(11): 1031-1034. [16] Stevens T, Carter A, Watson T P, et al. Genetic linkage between the Yellow River, the Mu Us desert and the Chinese Loess Plateau[J]. Quaternary Science Reviews, 2013, 78: 355-368. [17] Bird A, Millar I, Rodenburg T, et al. A constant Chinese Loess Plateau dust source since the Late Miocene[J]. Quaternary Science Reviews, 2020, 227: 106042. [18] Zhang H Z, Nie J S, Liu X J, et al. Spatially variable provenance of the Chinese Loess Plateau[J]. Geology, 2021, 49(10): 1155-1159. [19] Bird A, Stevens T, Rittner M, et al. Quaternary dust source variation across the Chinese Loess Plateau[J]. Palaeogeography, Palaeoclimatology, Palaeoecology, 2015, 435: 254-264. [20] Zhang H Z, Lu H Y, Xu X S, et al. Quantitative estimation of the contribution of dust sources to Chinese loess using detrital zircon U‐Pb age patterns[J]. Journal of Geophysical Research: Earth Surface, 2016, 121(11): 2085-2099. [21] 马榕,张婉莹,何梦颖. 基于碎屑锆石U-Pb年龄对黄土高原黄土的空间物源差异分析[J]. 海洋地质前沿,2019,35（1）：35-42. Ma Rong, Zhang Wanying, He Mengying. Spatial provenance difference of the loess on Loess Plateau based on detrital zircon U-Pb age[J]. Marine Geology Frontiers, 2019, 35(1): 35-42. [22] Rittner M, Vermeesch P, Carter A, et al. The provenance of Taklamakan desert sand[J]. Earth and Planetary Science Letters, 2016, 437: 127-137. [23] Zhang H Z, Lu H Y, He J, et al. Large-number detrital zircon U-Pb ages reveal global cooling caused the formation of the Chinese Loess Plateau during Late Miocene[J]. Science Advances, 2022, 8(41): eabq2007. [24] Yan Y, Ma L, Sun Y B. Tectonic and climatic controls on provenance changes of fine-grained dust on the Chinese Loess Plateau since the Late Oligocene[J]. Geochimica et Cosmochimica Acta, 2017, 200: 110-122. [25] 王苗苗,弓虎军. 基于锆石U-Pb年龄的洛川黄土物源示踪[J]. 西北大学学报（自然科学版）,2021,51（4）：695-708. Wang Miaomiao, Gong Hujun. Tracing the provenance of Luochuan loess based on zircon U-Pb ages[J]. Journal of Northwest University (Natural Science Edition), 2021, 51(4): 695-708. [26] Zhang H Z, Lu H Y, Stevens T, et al. Expansion of dust provenance and aridification of Asia since ~ 7.2 Ma revealed by detrital zircon U‐Pb dating[J]. Geophysical Research Letters, 2018, 45(24): 13437-13448. [27] Gong H J, Xie W B, Wang J D, et al. Zircon U-Pb ages of Quaternary loess-paleosol sequences from the Luochuan section: Implication for sediment provenance[J]. Acta Geologica Sinica (English Edition), 2017, 91(1): 357-358. [28] 杨光亮,范育新,蔡青松,等. 第四纪黄土物源的时空差异研究现状及展望[J]. 古地理学报,2021,23（5）：1020-1037. Yang Guangliang, Fan Yuxin, Cai Qingsong, et al. Progress and prospect of research on temporal and spatial differences of the Quaternary loess provenance[J]. Journal of Palaeogeography (Chinese Edition), 2021, 23(5): 1020-1037. [29] Zhang X Y, Arimoto R, An Z S. Dust emission from Chinese desert sources linked to variations in atmospheric circulation[J]. Journal of Geophysical Research: Atmospheres, 1997, 102(D23): 28041-28047. [30] 孙博亚,张云翔,弓虎军,等. 洛川黄土碎屑锆石的粒度特征及其古气候意义[J]. 西北大学学报（自然科学版）,2011,41（1）：119-126. Sun Boya, Zhang Yunxiang, Gong Hujun, et al. The grain size of the detrital zircon of Luochuan and its paleoclimate implication[J]. Journal of Northwest University (Natural Science Edition), 2011, 41(1): 119-126. [31] 李娇. 黄土高原西峰剖面末次间冰期以来石英光释光灵敏度变化研究[D]. 西安：西北大学,2020. Li Jiao. The variation of quartz optically stimulated luminescence sensitivity in Xifeng section of Chinese Loess Plateau since the last interglacial[D]. Xi’an: Northwest University, 2020. [32] Gallet S, Jahn B M, Torii M. Geochemical characterization of the Luochuan loess-paleosol sequence, China, and paleoclimatic implications[J]. Chemical Geology, 1996, 133(1/2/3/4): 67-88. [33] Jahn B M, Gallet S, Han J M. Geochemistry of the Xining, Xifeng and Jixian sections, Loess Plateau of China: Eolian dust provenance and paleosol evolution during the last 140 ka[J]. Chemical Geology, 2001, 178(1/2/3/4): 71-94. [34] 杨杰东,陈骏,张兆峰,等. 距今7 Ma以来甘肃灵台剖面Nd和Sr同位素特征[J]. 地球化学,2005,34（1）：1-6. Yang Jiedong, Chen Jun, Zhang Zhaofeng, et al. Variations in 143Nd/144Nd and 87Sr/86Sr of Lingtai profile over the past 7 Ma[J]. Geochimica, 2005, 34(1): 1-6. [35] Jeong G Y, Hillier S, Kemp R A. Changes in mineralogy of loess-paleosol sections across the Chinese Loess Plateau[J]. Quaternary Research, 2011, 75(1): 245-255. [36] Fenn K, Stevens T, Bird A, et al. Insights into the provenance of the Chinese Loess Plateau from joint zircon U-Pb and garnet geochemical analysis of last glacial loess[J]. Quaternary Research, 2018, 89(3): 645-659. [37] Nie J S, Peng W B. Automated SEM–EDS heavy mineral analysis reveals no provenance shift between glacial loess and interglacial paleosol on the Chinese Loess Plateau[J]. Aeolian Research, 2014, 13: 71-75. [38] Che X D, Li G J. Binary sources of loess on the Chinese Loess Plateau revealed by U-Pb ages of zircon[J]. Quaternary Research, 2013, 80(3): 545-551. [39] Lee J K W, Williams I S, Ellis D J. Pb, U and Th diffusion in natural zircon[J]. Nature, 1997, 390(6656): 159-162. [40] 彭文彬. 利用黄土—红粘土重矿物组合和锆石U-Pb年代研究黄土高原物源及古气候变化[D]. 兰州：兰州大学,2017. Peng Wenbin. Paleoclimate and provenance changes on the Chinese Loess Plateau based on heavy mineral and zircon U-Pb ages of loess and red clay[D]. Lanzhou: Lanzhou University, 2017. [41] 郭佩,刘池洋,王建强,等. 碎屑锆石年代学在沉积物源研究中的应用及存在问题[J]. 沉积学报,2017,35（1）：46-56. Guo Pei, Liu Chiyang, Wang Jianqiang, et al. Considerations on the application of detrital-zircon geochronology to sedimentary provenance analysis[J]. Acta Sedimentologica Sinica, 2017, 35(1): 46-56. [42] 谢静,杨石岭,丁仲礼. 黄土物源碎屑锆石示踪方法与应用[J]. 中国科学：地球科学,2012,42（6）：923-933. Xie Jing, Yang Shiling, Ding Zhongli. Methods and application of using detrital zircons to trace the provenance of loess[J]. Science China: Earth Sciences, 2012, 42(6): 923-933. [43] Pell S D, Williams I S, Chivas A R. The use of protolith zircon-age fingerprints in determining the protosource areas for some Australian dune sands[J]. Sedimentary Geology, 1997, 109(3/4): 233-260. [44] 丁仲礼,孙继敏,杨石岭,等. 灵台黄土—红粘土序列的磁性地层及粒度记录[J]. 第四纪研究,1998,18（1）：86-92. Ding Zhongli, Sun Jimin, Yang Shiling, et al. Magnetostratigraphy and grain size record of a thick red clay-loess sequence at Lingtai, the Chinese Loess Plateau[J]. Quaternary Sciences, 1998, 18(1): 86-92. [45] 杨杰东,陈骏,刘连文,等. 2.5 Ma以来黄土高原灵台剖面黄土—古土壤87Sr/86Sr比值的变化[J]. 南京大学学报（自然科学）,2003,39（6）：731-738. Yang Jiedong, Chen Jun, Liu Lianwen, et al. Variations in 87Sr/86Sr ratios of loess-paleosols of Lingtai section over the past 2.5 Ma[J]. Journal of Nanjing University (Natural Sciences), 2003, 39(6): 731-738. [46] Vermeesch P. How many grains are needed for a provenance study?[J]. Earth and Planetary Science Letters, 2004, 224(3/4): 441-451. [47] Vermeesch P. On the visualisation of detrital age distributions[J]. Chemical Geology, 2012, 312-313: 190-194. [48] Vermeesch P. Multi-sample comparison of detrital age distributions[J]. Chemical Geology, 2013, 341: 140-146. [49] Vermeesch P. IsoplotR: A free and open toolbox for geochronology[J]. Geoscience Frontiers, 2018, 9(5): 1479-1493. [50] 吴磊,胡晓燚. 第四纪柴达木盆地是黄土高原的主要物源区吗?[J]. 第四纪研究,2022,42（4）：939-947. Wu Lei, Hu Xiaoyi. Was the Qaidam Basin major source of the Chinese Loess Plateau in the Quaternary?[J]. Quaternary Sciences, 2022, 42(4): 939-947. [51] Enkelmann E, Weislogel A, Ratschbacher L, et al. How was the Triassic Songpan‐Ganzi Basin filled? A provenance study[J]. Tectonics, 2007, 26(4): TC4007. [52] 谢静,吴福元,丁仲礼. 浑善达克沙地的碎屑锆石U-Pb年龄和Hf同位素组成及其源区意义[J]. 岩石学报,2007,23（2）：523-528. Xie Jing, Wu Fuyuan, Ding Zhongli. Detrital zircon composition of U-Pb ages and Hf isotope of the Hunshandake sandland and implications for its provenance[J]. Acta Petrologica Sinica, 2007, 23(2): 523-528. [53] Pullen A, Ibáñez-Mejía M, Gehrels G E, et al. What happens when n= 1000? Creating large-n geochronological datasets with LA-ICP-MS for geologic investigations[J]. Journal of Analytical Atomic Spectrometry, 2014, 29(6): 971-980. [54] 安芷生,王苏民,吴锡浩,等. 中国黄土高原的风积证据：晚新生代北半球大冰期开始及青藏高原的隆升驱动[J]. 中国科学：地球科学,1998,28（6）：481-490. An Zhisheng, Wang Sumin, Wu Xihao, et al. Eolian evidence from the Chinese Loess Plateau: The onset of the Late Cenozoic Great Glaciation in the northern Hemisphere and Qinghai-Xizang Plateau uplift forcing[J]. Science China: Earth Sciences, 1998, 28(6): 481-490. [55] 孙东怀,安芷生,苏瑞侠,等. 最近2.6 Ma中国北方季风环流与西风环流演变的风尘沉积记录[J]. 中国科学：地球科学,2003,33（6）：497-504. Sun Donghuai, An Zhisheng, Su Ruixia, et al. Eolian sedimentary records for the evolution of monsoon and westerly circulations of northern China in the last 2.6 Ma[J]. Science China: Earth Sciences, 2003, 33(6): 497-504. [56] Sun Y B, Clemens S C, An Z S, et al. Astronomical timescale and palaeoclimatic implication of stacked 3.6-Myr monsoon records from the Chinese Loess Plateau[J]. Quaternary Science Reviews, 2006, 25(1/2): 33-48. [57] Li J J, Fang X M, Song C H, et al. Late Miocene-Quaternary rapid stepwise uplift of the NE Tibetan Plateau and its effects on climatic and environmental changes[J]. Quaternary Research, 2014, 81(3): 400-423. [58] Sun Y B, Yan Y, Nie J S, et al. Source-to-sink fluctuations of Asian Aeolian deposits since the Late Oligocene[J]. Earth-Science Reviews, 2020, 200: 102963. [59] Chen J, Li G J. Geochemical studies on the source region of Asian dust[J]. Science China Earth Sciences, 2011, 54(9): 1279-1301. [60] Li Y R, Shi W H, Aydin A, et al. Loess genesis and worldwide distribution[J]. Earth-Science Reviews, 2020, 201: 102947. [61] 孙东怀,鹿化煜. 晚新生代黄土高原风尘序列的粒度和沉积速率与中国北方大气环流演变[J]. 第四纪研究,2007,27（2）：251-262. Sun Donghuai, Lu Huayu. Grain-size and dust accumulation rate of Late Cenozoic aeolian deposits and the inferred atmospheric circulation evolutions[J]. Quaternary Sciences, 2007, 27(2): 251-262. [62] 孙有斌. 探寻中更新世气候转型之谜[J]. 地球环境学报,2019,10（2）：210. Sun Youbin. Explore the mystery of the mid-Pleistocene climate transition[J]. Journal of Earth Environment, 2019, 10(2): 210. [63] 刘海娇,于学峰,孙有斌. 亚洲风尘：来自何方、飘向何处?[J]. 地球环境学报, 2020, 11(3): 335-342. Liu Haijiao, Yu Xuefeng, Sun Youbin. Asian dust: Where does it come from and where does it drift?[J]. Journal of Earth Environment, 2020, 11(3): 335-342. [64] An Z S. Late Cenozoic climate change in Asia: Loess, monsoon and monsoon-arid environment evolution[M]. Dordrecht: Springer, 2014. [65] Lu H Y, Wang X Y, Wang Y, et al. Chinese loess and the Asian monsoon: What we know and what remains unknown[J]. Quaternary International, 2022, 620: 85-97. [66] Liu T S, Ding Z L. Chinese loess and the paleomonsoon[J]. Annual Review of Earth and Planetary Sciences, 1998, 26: 111-145. -
点击查看大图
图(10) / 表 (1)
计量
- 文章访问数: 28
- HTML全文浏览量: 9
- PDF下载量: 4
- 被引次数: 0
