Provenance study of the Xining loess in the Northeastern Tibetan Plateau, China
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摘要: 碎屑锆石U-Pb年代学被认为是研究沉积物物源的有效手段。然而，应用碎屑锆石U-Pb年代学对中国黄土高原进行物源研究时却获得了非常复杂的物源信息。西宁黄土沉积于青藏高原东北缘地区，对其开展碎屑锆石U-Pb年代学研究不仅可以获得其物源信息，同时可以为探讨青藏高原北缘碎屑物质对黄土高原的贡献提供重要依据。碎屑锆石形貌学研究结果表明其可能经历了强烈的物理风化以及多次再循环，同时也可能暗示了物源的高度复杂性。来自不同沉积层位的碎屑锆石U-Pb年龄结果表明，西宁黄土碎屑物质的最终来源可能是青藏高原北缘和中亚造山带，且物源区自约1.3 Ma以来可能没有显著变化，但是两者对西宁黄土的相对贡献可能在不同的时期具有微弱的差异。西宁黄土与中国黄土高原中、西部典型剖面的碎屑锆石年龄分布具有高度相似性，暗示了两者的物源区可能很大程度上具有一致性，但具少量差异。Abstract: Single-grain U-Pb dating of detrital zircons is regarded as an efficient and effective technique to differentiate the contribution of discrete sources. However, its application to the extensive Chinese Loess Plateau (CLP) yields rather complex information in provenance discrimination. The Xining loess was deposited in the Northeastern Tibetan Plateau (NETP), and the detrital zircon U-Pb chronology study can not only obtain provenance information but also provide an important basis to discuss the contribution of the detrital materials from the Northern Tibetan Plateau (NTP) to the CLP. Results of the detrital zircon morphology suggest that zircons may have undergone intense physical weathering and multiple recirculations, and may also indicate the high complexity of the source. Detrital zircon U-Pb age results from different sedimentary layers of the Xining loess reveal there are no obvious temporal variations in the provenance of the Xining loess since ~1.3 Ma and materials may ultimately be eroded from the NTP and the Central Asian Orogenic Belt (CAOB), although the relative contribution of detritus from the two sources may slightly vary through time. The U-Pb age spectra of the Xining loess are highly similar to that of typical loess sites in the western-central CLP, suggesting that the provenance areas of the CLP and the Xining loess may be largely consistent, but the possibility of a small difference of provenance cannot be ruled out.
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Key words:
- Xining /
- detrital zircon /
- U-Pb ages /
- provenance /
- Chinese Loess Plateau /
- Northeastern Tibetan Plateau
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0. 引言
中国黄土高原的风尘堆积记录了第四纪时期最高分辨率的全球气候变化(Liu and Ding, 1998; An, 2000; Maher, et al., 2010)。刘东生(1985)发现中国黄土高原的黄土堆积自西北部至东南部，厚度逐渐变薄，粒度逐渐变细，暗示了风尘可能主要来源于黄土高原西北部广大的戈壁、沙漠地区。来自地球化学、矿物学方面的证据表明蒙古戈壁-沙漠南部和阿拉善干旱区是亚洲风尘主要物源地，其碎屑物质最终来源于中亚造山带的戈壁阿尔泰山脉和青藏高原北缘(Ji, et al., 1999; Chen, et al., 2007; Li, et al., 2007; Sun, et al., 2008; Li, et al., 2009; Chen and Li, 2011)。
碎屑锆石U-Pb年代学分析为沉积物物源的研究做出了巨大的贡献(郭佩等，2017；程瑜等，2018；林旭等，2021)。然而，该技术在黄土物源的研究中提供了有力地证据，同时也带来了更加复杂的物源信息。黄土高原西北部北郭塬黄土的碎屑锆石年代学研究表明其与近源的沙漠没有单一的亲缘关系，主要来自于祁连山脉和塔克拉玛干沙漠(Stevens et al., 2010)。Pullen et al.(2011)发现洛川黄土与柴达木盆地第四纪沉积物具有一致的碎屑锆石年龄分布特征，表明青藏高原北缘，尤其是柴达木盆地，对黄土高原的碎屑物质具有重要的贡献。随后的一些研究进一步支持了包括柴达木盆地的青藏高原北缘是黄土高原重要的物源区的观点(Cheand Li, 2013; Bird et al., 2015; Licht et al., 2016; Zhang et al., 2016, 2018; Fenn et al., 2018)。近年来，一些研究基于黄土高原、西毛乌素沙地、黄河沉积物与青藏高原东北缘具有相似的碎屑锆石年龄分布，认为青藏高原东北缘剥蚀下来的碎屑物质通过黄河的搬运被输送至毛乌素沙地和黄土高原(Stevens et al., 2013a; Nie et al., 2015; Zhang et al., 2021)。基于塔里木盆地、准噶尔盆地、柴达木盆地沉积物和黄土高原北部靖边黄土的碎屑锆石年龄分析，Sun et al.(2018)提出黄土的物源区主要是中亚造山带、祁连山脉和华北克拉通，而不是塔里木盆地、准噶尔盆地和柴达木盆地。Sun et al.(2020)对黄土源-汇系统综合分析提出亚洲风尘具有3个主要物源(青藏高原北缘、中亚造山带和鄂尔多斯高原)及10个次要物源(古尔班通右特沙漠、蒙古戈壁沙漠、塔克拉玛干沙漠、巴丹吉林沙漠、腾格里沙漠、柴达木盆地、库布奇沙漠、毛乌素沙地、浑善达克沙地和科尔沁沙地)。
除了主要物源区对黄土沉积的相对贡献具有争论外，黄土高原的物源是否具有空间一致性也具有争议(Jahn et al., 2001; Maher et al., 2009; Xiao et al., 2012;Che and Li., 2013 ; Bird et al., 2015; Zhang et al., 2021)。来自于黄土高原不同黄土剖面的碎屑锆石年代学研究提出了黄土高原不同地区的黄土可能来自不同的物源区，这明显不同于基于地球化学、同位素等证据提出的黄土高原物源区具有空间一致性的观点(Jahn et al., 2001; Maher et al., 2009)。此外，黄土高原物源的时间变化同样是一个具有争议的问题。Xiao et al. (2012)基于碎屑锆石U-Pb年代学研究认为黄土-古土壤层位的物源具有差异，而Che and Li(2013)基于同样的研究方法不认为存在黄土-古土壤层位物源差异。Stevens et al.(2013b)和Fenn et al.(2017)利用地球化学与矿物学研究发现在北郭塬~20 ka时期物源发生突变。另外，黄土-古土壤层位锆石U-Pb年龄和重矿物组分的统计研究表明这些矿物的物源并未发生变化(Nie et al., 2014; Licht et al., 2016)。因此，黄土-古土壤序列物源是否具有时间差异需要更多证据的支持。
西宁盆地位于黄土高原东邻，保存有青藏高原东北缘地区最大、最厚的黄土堆积。矿物学研究认为青藏高原东北缘的黄土堆积主要来自于青藏高原内部(李珍和聂树人，1999)。然而，碎屑锆石年代学研究发现末次冰期的西宁黄土与黄土高原内部黄土具有可对比性(李高军等，2013)。西宁黄土位于青藏高原东北缘的碎屑物质向东输送至黄土高原的重要路径上，对西宁黄土的碎屑锆石年代学研究，不仅能反映其本身的物源信息，同时对黄土高原的物源研究具有重要意义。基于此，选择西宁黄土1.3 Ma以来不同黄土层位进行碎屑锆石形貌学及U-Pb年龄分析，通过对比，研究西宁黄土主要物源区及其可能存在的时间变化，以及探讨青藏高原东北缘黄土与黄土高原内部黄土物源的空间差异。
1. 样品采集与实验方法
1.1 研究区概况及样品采集
研究区位于青藏高原东北缘西宁盆地内，盆地北、西、南侧被祁连山及其支脉——拉脊山、日月山包围，东侧与黄土高原相邻(图 1)。在自然地理区域上，西宁盆地位于西北内陆干旱区、东部季风区与高原季风影响的边界地带。盆地平均海拔约2000 m，全年平均气温约6 ℃，平均降水量约400 mm(中国气象数据网)。湟水自西向东穿过西宁盆地中心，切穿盆地内新生代地层。第四纪黄土沉积于湟水阶地之上，尤以西宁城北大墩岭沉积的黄土地层最厚、最具代表性。
图 1 研究区自然地理背景及碎屑锆石样品位置Figure 1. Geographical setting of the research area and detrital zircon sample sites在大墩岭顶部稳定塬面(36.65°N；101.79°E)进行科学钻探，钻井海拔为2740 m，深度为261 m。钻探获得260.4 m厚的黄土-古土壤沉积序列以及底部的冲积砾石层岩芯。将岩芯从中间剖开，以10 cm间距采样进行磁化率测试。结合Lu et al.(2012)的岩性和古地磁学研究，以及此次的磁化率研究结果，对岩芯进行地层学划分，结果表明大墩岭黄土-古土壤序列底部为S16，年龄为约1.3 Ma(图 2)。在S2LL1(2.2~4.6 m)、L5(56~57.5 m)、L7(118~120 m)、L9(150~152.5 m)和L13(210~212.5 m)等层位采集5个混合样品，命名为DL-1、DL-2、DL-3、DL-4和DL-5，进行碎屑锆石U-Pb年代学分析。
图 2 大墩岭钻探岩芯的土壤地层和磁化率随深度变化Figure 2. Pedostratigraphy and magnetic susceptibility variations with depth in the Dadunling core1.2 测试方法
每个样品均取约5 kg黄土，采用常规浮选与磁选法进行矿物分选，得到数百颗锆石颗粒，再在显微镜下挑选出200颗左右锆石颗粒制靶，拍摄锆石反射光、透射光和阴极发光(CL)显微照片。选择锆石无裂隙区域作为靶区，使用Agilent7900 MS等离子体质谱仪与ESI NWR 193 nm激光剥蚀系统进行锆石U-Pb测年。使用NIST 610作为校正U、Th和Pb含量的标准样品，GJ-1作为校正仪器偏差的标准样品，91500作为校正同位素分馏的标准样品。每个样品测试了120颗碎屑锆石，去掉谐和度＜90%的锆石，5个样品分别获得了111、117、112、107和108个有效年龄。对于206Pb/238U年龄＜1000 Ma的锆石颗粒，采用206Pb/238U年龄，对于206Pb/238U年龄＞1000 Ma的锆石颗粒，采用207Pb/206Pb年龄。使用DensityPlotter程序(Vermeesch, 2012)绘制锆石U-Pb年龄的直方图与核密度估计(KDE)图。
1.3 锆石形貌学
锆石阴极发光照片可以观察锆石的结构和环带特征。分析的锆石粒径为约40~200 μm，通过锆石CL图反映的内部结构，可将锆石分为岩浆锆石、变质锆石和继承锆石(图 3a)。反射光图可清晰地反映锆石表面的磨圆情况，绝大多数锆石具有不同程度的磨圆。根据锆石表明磨圆程度不同，将锆石分为棱角状、次棱角状、次圆状、圆状和浑圆状5类(图 3b)，对反射光图中所有的碎屑锆石进行磨圆度统计，结果见表 1。西宁黄土中锆石棱角状占比5.9%~13.9%，次棱角状占比27.5%~48.7%，次圆状占比24.5%~37.6%，圆状占比8.8%~22.0%，浑圆状占比1.5%~5.9%。整体来看，棱角状与次棱角状的碎屑锆石占全部样品总数的49.0%，可能暗示了西宁黄土存在一个距离较近的物源区。西宁黄土碎屑锆石具有多种类型的混合、复杂的磨圆度与裂隙的发育等特征，表明锆石颗粒可能经历了强烈的物理风化以及多次再循环，同时也可能暗示了多物源的混合。
图 3 西宁黄土代表性碎屑锆石显微照片a—阴极发光(CL)图；b—反射光图Figure 3. Micrographs of representative detrital zircons from the Xining loess(a)Cathode luminescence (CL) images; (b)Reflected light images表 1 西宁黄土碎屑锆石磨圆度统计结果Table 1. Statistical results of detrital zircon roundness of the Xining loess棱角状 次棱角状 次圆状 圆状 浑圆状 总数目 DL-1 7.9% 45.3% 31.8% 11.2% 3.7% 267 DL-2 9.0% 27.5% 37.6% 22.0% 3.9% 255 DL-3 5.9% 38.1% 35.9% 14.3% 5.9% 273 DL-4 13.9% 48.7% 24.5% 8.8% 3.3% 271 DL-5 11.4% 38.5% 35.2% 13.6% 1.5% 273 2. 结果与讨论
从不同层位采集的5个样品具有基本一致的锆石U-Pb年龄分布，可划分为4个年龄组：早中生代—古生代(200~540 Ma)，新元古代(540~1000 Ma)，中元古代早期—古元古代中期(1400~2050 Ma)和古元古代早期—新太古代(2300~2800 Ma)(图 4)。5个样品共555个锆石，年龄只有3个＜200 Ma：197±4 Ma(DL-1)，190±3 Ma(DL-4)和195±4 Ma(DL-4)。显生宙年龄组在西宁黄土中占大多数，占比约42%~58%，且具有显著的双峰特征，峰值年龄分别为约250 Ma和约420 Ma，其余3个年龄组占比分别为11%~22%(540~1000 Ma)、13%~19%(1400~2050 Ma)和8%~12%(2300~2800 Ma)。西宁黄土除具约250 Ma和约420 Ma主要年龄峰值外，还具有800 Ma、1800 Ma和2500 Ma次要年龄峰值。5个样品不同年龄组的相对含量具有轻微的差异。与其他峰值年龄相比，约250 Ma峰值年龄的锆石相对含量具有更明显的变化。此外，样品DL-1中元古代早期(约1500 Ma)锆石含量明显较其他层位少。这种在基本一致的锆石年龄分布下，不同年龄组相对含量的轻微差异，可能反映了不同物源在不同时期对西宁黄土的贡献具有轻微的变化。西宁黄土与黄土高原中—西部已报道黄土剖面的锆石年龄谱高度相似(图 5)，年龄分布基本一致，均具有约250 Ma、约420 Ma、约800 Ma、约1850 Ma和约2450 Ma的峰值年龄。但是，在<190 Ma组分含量上，西宁黄土和黄土高原黄土具有差异。在黄土高原腹地的黑木沟、灵台、西峰和渭南黄土剖面中含有少量该年龄组分锆石(图 5a—5d)，在黄土高原西部的曹岘黄土剖面，该年龄组分锆石相比黄土高原腹地的黄土剖面含量显著减少(图 5e)，而在更往西的西宁黄土，则未发现该年龄组分锆石(图 5f)。这种碎屑锆石年龄分布基本一致，但是在<190 Ma组分含量存在差异的情况，可能暗示了西宁黄土和黄土高原黄土的物源区在基本一致的情况下，存在一处物源区为黄土高原提供了少量碎屑物质，造成<190 Ma锆石含量差异。
图 4 西宁黄土碎屑锆石U-Pb年龄结果(n为锆石数目)Figure 4. Detrital zircon U-Pb age histograms of the Xining loess
图 5 碎屑锆石U-Pb年龄直方图及KDE图(n为锆石数目)a—黑木沟剖面(Pullen et al., 2011)；b—灵台剖面(Bird et al., 2015)；c—西峰剖面(Che and Li, 2013)；d—渭南剖面(Xiao et al., 2012)；e—曹岘剖面(Che and Li, 2013)；f—西宁黄土Figure 5. Detrital zircon U-Pb age histograms and KDE diagrams(a) The Heimugou section (Pullen et al., 2011); (b) The Lingtai section (Bird et al., 2015); (c) The Xifeng section (Che and Li, 2013); (d) The Weinan section (Xiao et al., 2012); (e) The Caoxian section (Che and Li, 2013); (f) The Xining loess200~300 Ma和400~500 Ma分别是海西—印支期造山运动和加里东期造山运动活跃的时期。西宁黄土与中国黄土高原的锆石年龄以200~300 Ma和400~500 Ma为主(图 6a、6b)，暗示了物源区在这两个时期具有大规模的构造运动。大量的研究表明，祁连山脉、柴达木盆地、库木塔格沙漠、阿拉善干旱区和毛乌素沙漠碎屑锆石年龄以约200~500 Ma为主，其中阿拉善干旱区、西毛乌素沙地以约200~300 Ma峰值为主，祁连山脉和柴达木盆地以约400~500 Ma为主(图 6c—6h；Stevens, et al., 2010; Pullen et al., 2011; Che and Li, 2013; Licht et al., 2016; Zhang et al., 2016)。西宁盆地位于毛乌素沙地的西南方，并不处于毛乌素沙地碎屑物质随冬季风搬运的沉积区，因此毛乌素沙地不太可能是西宁黄土的主要物源。阿拉善干旱区沉积物的Sr-Nd同位素研究表明其是来自于青藏高原北缘和中亚造山带碎屑物质的混合(Li et al., 2011)。青藏高原北缘作为黄土的潜在物源区，其碎屑物质可能来源于柴达木盆地、祁连山脉以及阿尔金山脉。对于祁连山脉与阿尔金山脉，在早古生代时期的俯冲、碰撞事件中可能发生了大规模的岩浆、变质活动(Wu et al., 2009, 2018; Song et al., 2013, 2014; Yang et al., 2015; 夏林圻等, 2016, Yu et al., 2018)。祁连山脉内河流沉积物的碎屑锆石年龄谱具有显著的约439 Ma年龄峰值，并指示沉积物中含有少量的200~300 Ma锆石(Zhang et al., 2020)。柴达木盆地沉积物碎屑锆石年龄谱的约431 Ma主要峰值和约264 Ma次要峰值，表明其含有的约380~490 Ma锆石主要来自于祁连山脉与阿尔金山脉(Pullen et al., 2011; Licht et al., 2016)。
图 6 西宁黄土、黄土高原及潜在物源区沉积物的碎屑锆石U-Pb年龄直方图与KDE图(n为锆石数目)a—西宁黄土样品；b—黑木沟、西峰、灵台、渭南、曹岘5个黄土剖面综合数据；c—祁连山麓沉积物(Zhang et al., 2016)；d—柴达木盆地沉积物(Pullen et al., 2011; Licht et al., 2016)；e—西毛乌素沙地沉积物(Stevens et al., 2013a; Nie et al., 2015)；f—东毛乌素沙地沉积物(Stevens et al., 2010, 2013; Nie et al., 2015)；g—阿拉善干旱区(综合的腾格里沙漠、弱水河床沉积物样品数据，引自Stevens et al., 2010; Che and Li, 2013; Licht et al., 2016; Zhang et al., 2016)；h—戈壁阿尔泰山麓沉积物(Che and Li, 2013; Zhang et al., 2016)Figure 6. Detrital zircon U-Pb chronology of the Xining loess, the CLP and potential provenances and KDE diagrams(a) Samples from the Xining loess; (b) Combined data of the five loess sections of the CLP in Figure 4; (c) Sediments from the piedmont of the Qilian mountains (Zhang et al., 2016); (d) Sediments from the Qaidam Basin(Pullen et al., 2011; Licht et al., 2016); (e) Sediments from the western Mu Us desert(Stevens et al., 2013a; Nie et al., 2015); (f) Sediments from the eastern Mu Us desert(Stevens et al., 2010, 2013; Nie et al., 2015); (g) Alxa arid areas (Combined data from the Tengger Desert and the Ruoshui River, after Stevens et al., 2010; Che and Li, 2013; Licht et al., 2016; Zhang et al., 2016); (h) Sediments from the piedmont of the Gobi Altay mountains (Che and Li, 2013; Zhang et al., 2016)中亚造山带作为地球上最大的显生宙增生造山带(Windley et al., 2007)，含有3个二叠纪—三叠纪拼贴系统(Zhang et al., 2009; Xiao et al., 2009, 2015)。中亚造山带二叠纪—三叠纪时期广泛发育的岩浆活动(Miao et al., 2007; Jian et al., 2008; Chu et al., 2013; Zheng et al., 2014; 贺昕宇等, 2022)可以为附近的沙漠提供约200~300 Ma锆石。中亚造山带的戈壁-阿尔泰山脉被认为是黄土高原主要的物源区(Chen et al., 2007; Li et al., 2009, 李高军等, 2013; Che and Li, 2013; Zhang et al., 2016, 2018)，其山麓沉积物的碎屑锆石年龄以250~400 Ma为主(图 6h；Che and Li, 2013; Zhang et al., 2016)。相较于大规模的晚古生代岩浆活动，中亚造山带早古生代岩浆活动则分布有限。在中国西北部，中亚造山带的早古生代的岩浆活动主要分布于北山造山带和天山山脉(徐学义等，2008; Li et al., 2016; Yuan et al., 2018)。天山山脉早古生代岩浆活动主要发育于300~400 Ma(Li et al., 2016)，山脉北麓准噶尔盆地新生代沉积物碎屑锆石年代学研究表明主要年龄组分为300~350 Ma(陈熠等，2012)。结合Sr-Nd同位素研究结果及黄土潜在物源区沉积物、其他黄土剖面的碎屑锆石年代学研究结果(Gehrels et al., 2003; 谢静等, 2007; Stevens et al., 2010; Xie et al., 2012; Xiao et al., 2012; Che and Li, 2013; Licht et al., 2016)，西宁黄土主要的年龄组分约200~500 Ma的碎屑锆石可能主要来自中亚造山带和青藏高原北缘。鉴于近青藏高原北缘地区沉积物中含有大量早古生代碎屑锆石，近中亚造山带地区沉积物中含有大量晚古生代碎屑锆石(图 6)，因此西宁黄土中200~300 Ma年龄组分的碎屑锆石可能主要由中亚造山带提供，而400~500 Ma年龄组分的碎屑锆石则主要由青藏高原北缘提供。
西宁黄土L9样品中的约250 Ma峰值年龄的锆石含量较约420 Ma峰值年龄的锆石含量高，而其他样品则是约250 Ma峰值年龄的锆石含量较少。由于L9是1.1 Ma以来厚度最大、粒度最粗的黄土层位，代表了一个非常严酷的冰期环境(Liu，1985；Guo et al., 1998)，L9中较高含量的200~300 Ma碎屑锆石可能反映了显著增强的来自西北的冬季风输送了更多的来自于中亚造山带的粗颗粒碎屑，并沉积于西宁盆地中，导致了晚古生代锆石含量的增加。
西宁黄土中前寒武纪碎屑锆石含量占48%~52%，如此之高的含量在探讨物源过程中无法忽视。阿拉善干旱区、戈壁阿尔泰山南麓、祁连山北麓和柴达木盆地沉积物中均含有新元古代和古元古代锆石，但不同时期锆石的含量是有差别的。阿拉善干旱区和戈壁阿尔泰山南麓沉积物中具有约1800 Ma锆石年龄峰值(图 6g)，柴达木盆地沉积物中600~1000 Ma锆石含量较高(图 6d)，祁连山北麓沉积物中则600~1000 Ma和约1800 Ma锆石含量较高。祁连山北麓与柴达木盆地较高的600~1000 Ma锆石含量可能是祁连造山带中发育大规模与新元古代罗迪尼亚超大陆裂解相关的岩浆活动所导致的(Song et al., 2013; 夏林圻等，2016；Zuza et al., 2017)。祁连山北麓、柴达木盆地沉积物与西宁黄土新元古代碎屑锆石相对含量比阿拉善干旱区和戈壁阿尔泰山南麓沉积物的高，暗示了青藏高原北缘可能对西宁黄土中新元古代碎屑锆石的贡献更高。古元古代锆石的来源则较为复杂。大量的研究表明古元古代锆石广泛分布在阿拉善干旱区基岩中，如阿拉善地块的龙首山岩群(修群业等，2004；耿元生等，2006；Tung et al., 2007a)与敦煌地块的TTG岩系(Zhang et al., 2013；Zhao et al., 2015)，祁连地区的结晶基底、水系沉积物中(Li, et al., 2007; Tung et al., 2017b; Zhang et al., 2020)，中亚造山带的基岩、沉积物中(Che and Li, 2013; Wang et al., 2014; Xu et al., 2015; Zhang et al., 2016; 苏茂荣等, 2020)，不利于更好地识别西宁黄土古元古代锆石的主要物源。
3. 结论
对西宁黄土不同层位黄土样品开展碎屑锆石U-Pb年代学研究，探讨其碎屑物质来源，并与黄土高原中—西部典型剖面进行差异对比，获得以下认识。
(1) 来自西宁黄土5个不同层位黄土样品的碎屑锆石具有多类型混合、磨圆度复杂、裂隙发育等特征，表明锆石颗粒可能经历了强烈的物理风化以及多次再循环，同时也可能暗示了西宁黄土为多物源混合。
(2) 5个样品的碎屑锆石U-Pb年龄谱分布特征较一致，均具有早中生代—古生代(200~500 Ma)、新元古代(540~1000 Ma)、中元古代早期—古元古代中期(1400~2050 Ma)和古元古代早期—新太古代(2300~2800 Ma)的锆石年龄组，表明西宁黄土物源在1.3 Ma以来没有显著变化。
(3) 西宁黄土与黄土高原典型黄土剖面的碎屑锆石年龄分布对比表明青藏高原东北缘的黄土堆积与黄土高原中—西部黄土的物源区应该是高度重合的，但具有略微差异。
(4) 西宁黄土的碎屑锆石U-Pb年代学数据证明了青藏高原东北缘是中国黄土除中亚造山带之外另一处主要物源区，同时也支持了中国黄土堆积是来自多个物源区的碎屑物质均匀混合的观点。
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图 1 研究区自然地理背景及碎屑锆石样品位置
Figure 1. Geographical setting of the research area and detrital zircon sample sites
图 2 大墩岭钻探岩芯的土壤地层和磁化率随深度变化
Figure 2. Pedostratigraphy and magnetic susceptibility variations with depth in the Dadunling core
图 3 西宁黄土代表性碎屑锆石显微照片
a—阴极发光(CL)图；b—反射光图
Figure 3. Micrographs of representative detrital zircons from the Xining loess
(a)Cathode luminescence (CL) images; (b)Reflected light images
图 4 西宁黄土碎屑锆石U-Pb年龄结果(n为锆石数目)
Figure 4. Detrital zircon U-Pb age histograms of the Xining loess
图 5 碎屑锆石U-Pb年龄直方图及KDE图(n为锆石数目)
a—黑木沟剖面(Pullen et al., 2011)；b—灵台剖面(Bird et al., 2015)；c—西峰剖面(Che and Li, 2013)；d—渭南剖面(Xiao et al., 2012)；e—曹岘剖面(Che and Li, 2013)；f—西宁黄土
Figure 5. Detrital zircon U-Pb age histograms and KDE diagrams
(a) The Heimugou section (Pullen et al., 2011); (b) The Lingtai section (Bird et al., 2015); (c) The Xifeng section (Che and Li, 2013); (d) The Weinan section (Xiao et al., 2012); (e) The Caoxian section (Che and Li, 2013); (f) The Xining loess
图 6 西宁黄土、黄土高原及潜在物源区沉积物的碎屑锆石U-Pb年龄直方图与KDE图(n为锆石数目)
a—西宁黄土样品；b—黑木沟、西峰、灵台、渭南、曹岘5个黄土剖面综合数据；c—祁连山麓沉积物(Zhang et al., 2016)；d—柴达木盆地沉积物(Pullen et al., 2011; Licht et al., 2016)；e—西毛乌素沙地沉积物(Stevens et al., 2013a; Nie et al., 2015)；f—东毛乌素沙地沉积物(Stevens et al., 2010, 2013; Nie et al., 2015)；g—阿拉善干旱区(综合的腾格里沙漠、弱水河床沉积物样品数据，引自Stevens et al., 2010; Che and Li, 2013; Licht et al., 2016; Zhang et al., 2016)；h—戈壁阿尔泰山麓沉积物(Che and Li, 2013; Zhang et al., 2016)
Figure 6. Detrital zircon U-Pb chronology of the Xining loess, the CLP and potential provenances and KDE diagrams
(a) Samples from the Xining loess; (b) Combined data of the five loess sections of the CLP in Figure 4; (c) Sediments from the piedmont of the Qilian mountains (Zhang et al., 2016); (d) Sediments from the Qaidam Basin(Pullen et al., 2011; Licht et al., 2016); (e) Sediments from the western Mu Us desert(Stevens et al., 2013a; Nie et al., 2015); (f) Sediments from the eastern Mu Us desert(Stevens et al., 2010, 2013; Nie et al., 2015); (g) Alxa arid areas (Combined data from the Tengger Desert and the Ruoshui River, after Stevens et al., 2010; Che and Li, 2013; Licht et al., 2016; Zhang et al., 2016); (h) Sediments from the piedmont of the Gobi Altay mountains (Che and Li, 2013; Zhang et al., 2016)
表 1 西宁黄土碎屑锆石磨圆度统计结果
Table 1. Statistical results of detrital zircon roundness of the Xining loess
棱角状 次棱角状 次圆状 圆状 浑圆状 总数目 DL-1 7.9% 45.3% 31.8% 11.2% 3.7% 267 DL-2 9.0% 27.5% 37.6% 22.0% 3.9% 255 DL-3 5.9% 38.1% 35.9% 14.3% 5.9% 273 DL-4 13.9% 48.7% 24.5% 8.8% 3.3% 271 DL-5 11.4% 38.5% 35.2% 13.6% 1.5% 273 
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