DmitrienkoLiudmila Valer′evna, 王鹏程, 李三忠, 曹现志, 周在征, 胡梦颖, 索艳慧, 郭玲莉, 王永明, 李玺瑶, 刘鑫, 于胜尧. 东亚大汇聚与中—新生代地球表层系统演变[J]. 海洋地质与第四纪地质, 2017, 37(4): 33-64. DOI: 10.16562/j.cnki.0256-1492.2017.04.003
引用本文: DmitrienkoLiudmila Valer′evna, 王鹏程, 李三忠, 曹现志, 周在征, 胡梦颖, 索艳慧, 郭玲莉, 王永明, 李玺瑶, 刘鑫, 于胜尧. 东亚大汇聚与中—新生代地球表层系统演变[J]. 海洋地质与第四纪地质, 2017, 37(4): 33-64. DOI: 10.16562/j.cnki.0256-1492.2017.04.003
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Dmitrienko Liudmila Valer′evna, WANG Pengcheng, LI Sanzhong, CAO Xianzhi, ZHOU Zaizheng, HU Mengying, SUO Yanhui, GUO Lingli, WANG Yongming, LI Xiyao, LIU Xin, YU Shengyao. Meso-Cenozoic Evolution of Earth Surface System Under the East Asian Tectonic Superconvergence[J]. Marine Geology & Quaternary Geology, 2017, 37(4): 33-64. DOI: 10.16562/j.cnki.0256-1492.2017.04.003
Citation: Dmitrienko Liudmila Valer′evna, WANG Pengcheng, LI Sanzhong, CAO Xianzhi, ZHOU Zaizheng, HU Mengying, SUO Yanhui, GUO Lingli, WANG Yongming, LI Xiyao, LIU Xin, YU Shengyao. Meso-Cenozoic Evolution of Earth Surface System Under the East Asian Tectonic Superconvergence[J]. Marine Geology & Quaternary Geology, 2017, 37(4): 33-64. DOI: 10.16562/j.cnki.0256-1492.2017.04.003
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东亚大汇聚与中—新生代地球表层系统演变

  • 1.

    海底科学与探测技术教育部重点实验室，中国海洋大学海洋地球科学学院，青岛 266100

  • 2.

    青岛海洋科学与技术国家实验室海洋地质功能实验室，青岛 266237

基金项目: 

国家自然科学基金项目 U1606401

国家海洋局重大专项 GASI-GEOGE-01

国家重点研发计划项目 2017YFC0601401

国家自然科学基金项目 41190072

国家自然科学基金项目 41502185

山东省泰山学者特聘教授项目 

国家自然科学基金项目 41502321

国家自然科学基金项目 41402172

国家重点研发计划项目 2016YFC0601002

鳌山卓越科学家计划 2015ASTP-0S10

国家自然科学基金杰出青年基金 41325009

详细信息
    作者简介:

    Dmitrienko Liudmila Valer′evna(1989—)，女，博士生，从事构造地质学研究，E-mail：lvliude@163.com

    通讯作者:

    李三忠(1968—)，男，教授，博导，从事构造地质学、海洋地质学研究，E-mail：sanzhong@ouc.edu.cn

  • 中图分类号: P542

Meso-Cenozoic Evolution of Earth Surface System Under the East Asian Tectonic Superconvergence

  • 1.

    Key Lab of Submarine Geosciences and Prospecting Techniques, MOE, College of Marine Geosciences, Ocean University of China, Qingdao 266100, China

  • 2.

    Laboratory for Marine Geology, Qingdao National Laboratory for Marine Science and Technology, Qingdao 266237, China

摘要

    摘要
  • 摘要: 东亚长期处于古亚洲洋、特提斯洋和古太平洋三大构造域的大汇聚构造背景之下。印支运动后，东亚东缘形成了统一的被动大陆边缘，随着晚三叠世古太平洋板块俯冲的启动，东亚东缘的被动大陆边缘转化为主动大陆边缘，发育了与俯冲相关的蛇绿岩、Ⅰ型花岗岩。晚三叠世—中侏罗世，古太平洋俯冲带持续向西迁移，板块俯冲产生的挤压应力影响到了东亚内部，发生广泛构造变形，构造体制从受E—W向特提斯构造域和古亚洲洋构造域控制逐渐向受NE向的古太平洋构造域控制转变。晚侏罗世—早白垩世早期(160~135 Ma)，古太平洋板块继续西进，东亚被挤压-走滑的应力场控制，安第斯型主动大陆边缘和华北东部高原最终形成，发育少量的埃达克岩。早白垩世晚期(135~90 Ma)，古太平洋俯冲带向东后撤，东亚陆缘由挤压-走滑应力场转变为拉张-走滑应力场，安第斯型大陆边缘被破坏，华北东部高原开始垮塌，伴随大量的埃达克岩、变质核杂岩的出现。在晚白垩世，随着俯冲带的后撤，东亚内部伸展作用减弱。新生代东亚发生了巨型的地形倒转，印度板块与欧亚板块碰撞最终导致中国西部的青藏高原隆升，相反，中国东部渤海湾盆地和海区的盆地群形成；构造-盆地-岩浆带体现出自西向东迁移的特征，盆地群起始时代主要在古近纪，形成了新生代西高东低的台阶式地貌格局。在新近纪盆地群由断陷转为快速拗陷，同时东亚内部的伸展构造主要受青藏高原隆起制约。
    Abstract: East Asia has suffered for a long duration under the superconvergence system of the Paleo-Asian, Tethyan and Paleo-Pacific tectonic domains. The Indosinian Movement for the first time made an unified passive continental margin in East Asia. The intrusion of ophiolites and Ⅰ-type granites associated with the subduction of the Paleo-Pacific Plate in Late Triassic suggests a transition from passive to active continental margins. In the process of the westward migration of the Paleo-Pacific Subduction Zone, the sinistral transpressional stress field dominated the intraplate deformation during the period from Late Triassic to Middle Jurassic. The E-W-trending structural system controlled by Tethys and Paleo-Asian oceans started changing to the N-E-trending structural system caused by the Paleo-Pacific Ocean subduction. The continuously westward migration of the subduction zones resulted in the transpressional stress field in East Asia marked by the emergence of the Eastern North China Plateau and the formation of the Andean-type of active continental margin from Late Jurassic to Early Cretaceous (160~135 Ma), accompanied by the development of a small amount of adakites. In Late Cretaceous (135~90 Ma), due to the eastward retreat of the Paleo-Pacific Subduction Zone, the regional stress field was changed from sinistral transpression to transtension. Since a large amount of late-stage adakites and metamorphic core complexes was developed, the Andean-type of active continental margin was destroyed and the Eastern North China Plateau started to collapse. In Late Cretaceous, the extension in East Asia gradually decreased eastward with the retreat of the Paleo-Pacific subduction zones. Futhermore, a significant topographic inversion took place in Cenozoic resulted from a rapid uplift of the Tibet Plateau owing to the India-Eurasian collision and the formation of the Bohai Bay Basin and other basins in the East Asian continental margin. The inversion has a remarkable eastward migration of deformation, basin formation and magmatism. Meanwhile, the basins mainly developed in Paleogene which caused the formation of the three-stepping topography with dropping altitude eastward. In Neogene, most of the basins underwent rapid subsidence under the control of faulting, as well as the intracontinental extension in East Asia, which also made substantial contribution to the uplifting of the Tibet Plateau.
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  • 第四纪气候变化与人类生存和发展关系密切，是当今地学研究的重点和热点之一。洞庭盆地是长江中游重要的第四纪沉积盆地，地理位置恰处我国东西、南北自然环境过渡地带，对环境变化具有高度敏感性，是研究第四纪古气候变化的理想区域。前人在洞庭盆地已经开展了全面且深入的古气候与环境的研究，并取得了显著的学术成果[1-13]。这些研究广泛聚焦于多个维度，包括但不限于岩性岩相特征分析[2-4]、地球化学组成探讨[4-6]、磁化率变化解析[7-8]、古野火活动记录重建[9]以及孢粉组合与古植被变化[2, 10-13]等多个方面，共同构成了对洞庭盆地古气候变迁多维度、综合性的认知体系。关于洞庭盆地第四纪之前的古气候研究较少，研究认为白垩纪和古近纪气候整体呈干旱-半干旱状态[14]。全新世气候变化由于人类活动的显著影响[11, 15]，往往需结合历史文献记载与人类活动遗迹进行综合分析[16-18]。故第四纪之前和全新世气候变化不在本文探讨范围。本文着眼于第四纪以来较长时间尺度下洞庭盆地的古气候变化特征，使用定量重建的方法，以期为理解该区域乃至全球气候变化历史提供新的视角与数据支持。

    1.   洞庭盆地概况

    洞庭盆地位于长江中游荆江段南侧（图1），地跨湘鄂两省，东、南、西分别以幕阜山隆起、雪峰隆起、武陵隆起为界；北与江汉盆地以华容次级隆起相隔，仅在西段相接。洞庭盆地是叠覆在早中生代陆内挤压造山带基底之上，经白垩纪-古近纪伸展断陷和第四纪早期断陷、晚期拗陷所形成的大型内陆盆地[19-21]，第四纪地层可划分为覆盖区和露头区两个系统。覆盖区地层自下而上划分为早更新世早期华田组（Qp1ht）湖相黏土沉积、汨罗组（Qp1m）河流相砂砾层，中更新世洞庭湖组（Qp2d）砂-粉砂-黏土韵律层，晚更新世坡头组（Qp3p）土黄色黏土以及全新统。露头区自下而上划分为早更新世华田组（Qp1ht）、晚期汨罗组（Qp1m），中更新世新开铺组（Qp2x）、白沙井组（Qp2b）、马王堆组（Qp2mw），晚更新世白水江组（Qp3b），以及全新统。新开铺组、白沙井组、马王堆组、白水江组分别发育一套具明显二元结构堆积，下部为河床相砂砾石层，上部为河漫滩相沉积物风化形成的棕红色网纹状黏土[22]。针对洞庭盆地覆盖区的松散沉积层，进行系统性地层学和年代学研究的工作相对较少，仅有少量绝对年代数据[23]和古地磁测年[6]结果。赵举兴等[24]系统地进行了古地磁、ESR、AMS 14C等测试，建立了洞庭盆地相对完整可靠的年代地层序列，为后续研究的年代确定和地层对比提供了依据。

    图  1  洞庭盆地地质简图及钻孔位置
    Figure  1.  Geological map of the Dongting Basin and locations of boreholes
    下载: 全尺寸图片 幻灯片

    现代洞庭湖地区属于中亚热带季风性湿润气候，年平均气温约为17.4℃，年平均降水量约为1400 mm，四季分明，雨热同期[25]。植物区系属于亚热带常绿落叶林区，主要植被类型包括暖性针叶林、针阔混交林、阔叶林、落叶阔叶灌丛、草甸和水生沼泽植被等,针叶树以马尾松（Pinus massoniana）、杉木（Cunninghamia lanceolata）等为主；阔叶树包括锥属（Castanopsis）、栎属（Quercus）、栗属（Castanea）、化香树（Platycarya strobilacea）、水青冈（Fagus longipetiolata）、 鹅耳枥（Carpinus turczaninowii）、黄连木（Pistacia chinensis）、朴树（Celtis sinensis）等；灌木包括蔷薇属（Rosa）、杜鹃花属（Rhododendron）、绣线菊（Spiraea salicifolia）、桃金娘（Rhodomyrtus tomentosa）、黄栌（Cotinus coggygria）、雀梅藤（Sageretia thea）、胡枝子（Lespedeza bicolor）等；草本植物主要有禾本科（Poaceae）、伞形科（Apiaceae）、蓼科（Polygonaceae）、菊科（Asteraceae）、莎草科（Cyperaceae）等[15, 26]。河道切割使得洞庭湖的泥沙不规则堆积形成了各种形状不同的洲滩，这些洲滩依地形而发育相应的植物群落，植被在大区域范围内形成了插花式镶嵌分布的特点；而在一些小区域或内湖、沼泽等特定条件下呈同心圆分布的特点[27]。洞庭湖湿地植被以被子植物为主，在植物群落构成中，禾本科、伞形科、蓼科、菊科、莎草科、十字花科（Brassicaceae）、眼子菜科（Potamogetonaceae）、小二仙草科（Haloragidaceae）、龙胆科（Gentianaceae）、金鱼藻科（Ceratophyllaceae）、水鳖科（Hydrocharitaceae）、唇形科（Lamiaceae）等占有重要的地位[28]。

    2.   洞庭盆地第四纪古气候研究简述

    过去四十余年间，众多学者围绕洞庭盆地的第四纪古气候重建开展了广泛而深入的研究，取得了丰硕成果。景存义[4]较早对洞庭湖第四纪气候演变进行了系统阐述（图2），但其气候特征主要是在沉积相的基础上判断，仅在更新世早期和全新世中期有孢粉样品参考。蔡述明等[2]和杨达源等[13]的研究均主要依据沅江市华田村田11孔及常德市安乡县CK10孔（图1）的孢粉样品（分别为6个与3个），但对洞庭湖第四纪植被与气候变化的解析存在着差异，如前者认为晚更新世晚期气候较暖而后者认为当时气候冷干（图2）。可见定性或半定量的描述受主观因素影响较大。前者还参考了其他孢粉样品，认为早更新世早期气候湿热，而后者综合了其他多个钻孔的地球化学分析及黏土矿物组成等资料，认为当时应处于温湿环境（图2）。这些早期研究结果普遍存在样品分辨率较低的问题，且相比于温度的变化通常容易忽视湿度的变化，或在低分辨率下降水的小幅变化不容易被识别（图2）。

    图  2  洞庭盆地第四纪古气候不同研究结果对比
    小方块颜色示冷暖干湿程度。蓝框：冷期，黄框：暖期。
    Figure  2.  Comparison of results of different Quaternary paleoclimate studies in the Dongting Basin
    Different colors of cubes show different levels in temperature and humidity. Blue bars: cold period,yellow bars: warm period.
    下载: 全尺寸图片 幻灯片

    湖南省地质矿产局水文地质工程地质二队（简称水文二队）[22]系统研究了洞庭盆地第四纪地质，包括地层对比、沉积环境、新构造运动等。综合孢粉组合、黏土矿物组合、重矿物组合、沉积物的颜色特征等各方面资料，划分了洞庭盆地第四纪时期的古气候旋回（图2）。这份报告综合性较高、内容详实，可惜部分进行磁性地层学研究的钻孔，如常德市澧县ZK16孔、常德市汉寿县ZK124孔（图1），缺乏高精度的孢粉分析，孢粉数据分散来自不同钻孔，未形成完整序列，现有的样品精度只能进行定性的对比讨论。张建新等[6]构建第四纪环境气候变化序列的工作也较为综合，其最主要的依据是环境地球化学。其中年龄最老的连续钻孔（岳阳市湘阴县仁寿村ZK3孔、常德市澧县周家港村ZK5孔）可达早更新世晚期，早更新世早期的资料结合了其他不连续钻孔及前人研究。

    连续采样的钻孔资料包括常德市汉寿县CZ04孔[12] 和两护村ZKC01孔[7, 10]（图1），分别识别出16个和10个孢粉带，以较高的分辨率重塑了洞庭盆地第四纪气候演变过程，进一步丰富了该区域古气候研究的数据库。当分辨率提高时，气候的变化波动体现出了更强的一致性（图2）。

    对上述各项研究结果进行分析与统计，可以得出一些共有的大趋势（图2），可能代表了幅度较大、易于识别的冷暖波动，与全球气候变化一致。如更新世最早期，孢粉、环境地球化学等证据表明洞庭湖地区气候较为寒凉[4, 6, 10, 12]。在全球范围内，上新世–更新世之交（深海氧同位素阶段MIS 100—104，约2.6～2.5 Ma[29]）是冰川活动广泛分布的主要时期之一[30]，北半球冰盖作用发育[31-32]，是从上新世末期相对温暖的气候条件到更新世期间大规模冷暖交替变化的关键时期[33]。另一个降温的阶段是更新世千叶期早期，可能对应了MIS 16的冰期（约0.7～0.63 Ma），即昆仑冰期[34]。华田组顶部沉积时期除杨达源等[13]外，其他研究均存在一个较为温暖的时期，可能代表了MIS 49和55两个时代相隔较近的超级间冰期[35]。洞庭湖组顶部的网纹红土研究一致认为其产生于湿热的气候环境（图2）[8, 36-38]。

    然而，不同指标或者相同指标的不同研究所反映的干湿冷暖变化存在一定差异，并不完全和谐一致（图2），其成因可能主要源于两个方面：一是年代学的精确度不够，使得各个研究之间无法在统一的年代标尺下进行对比和讨论，除部分钻孔采用了ESR、OSL测年[10]、古地磁测年[6]之外，大部分古气候研究仅通过岩石地层学划分和区域对比得到相对年代参考。二是气候数据分辨率过低且不一致，早期以岩石地层组或段为单位的低分辨率研究[2, 4, 13]无法反映气候环境更高频率的波动和变化。深海氧同位素和其他证据显示第四纪气候存在频繁冷暖波动[35, 39-40]，若样品精度达不到气候波动的频率，则可能得到与实际不符甚至相反的结果。

    3.   材料和方法

    针对上述年代学和样品分辨率两个问题，理想的状态是在时代确定的同一钻孔中采集高分辨率的样品，进行综合性研究。在洞庭盆地众多第四纪古气候恢复研究中，孢粉分析是最重要的研究手段之一，其他技术手段恢复古气候与古环境时也几乎都借助了孢粉学数据作为参考。孢粉能够记录母体植物所处的不同气候环境背景，且拥有耐腐蚀的外壁，易于保存为化石，其分布广泛、产量丰富，是研究古植被、古气候演化的良好载体。柏道远等[10] 对第四纪洞庭盆地ZKC01孔以及向轲等[12] 对CZ04孔进行了系统的孢粉学研究，其钻孔剖面连续完整，样品采集分辨率较高，在定性或半定量的孢粉组合分析的基础之上，应能挖掘出更多有用的信息。但后者缺乏年龄数据，而前者的样品[10]有ESR、OSL定年数据的支持，与古地磁研究进行对比[24]建立年代地层框架，因此本文以ZKC01钻孔的孢粉原始数据为基础，重建洞庭盆地第四纪古气候与古环境演化。ZKC01钻孔岩性以黏土、粉砂含量较高为特征，偶夹砂砾石层。其中华田组和汨罗组以过水性湖泊为主，洞庭湖组上部、坡头组和全新统总体属河漫滩-湖泊相沉积，仅洞庭湖组中下部河流相沉积较为发育。现代沉积物研究表明在冲积物中主流相沉积花粉较少，漫滩、心滩沉积花粉较多，类型丰富[41]。ZKC01钻孔孢粉样品主要采集灰色黏土、粉砂以及粗碎屑中的细碎屑沉积夹层，尽量避免或降低沉积相的变化对孢粉组合的影响。ZKC01钻孔剖面共取孢粉样品258个，采用传统的HCl-HF和重液浮选方法处理，共计212个样品含有孢粉化石，分为16个孢粉带（图3）[10]。

    图  3  ZKC01孔主要孢粉图式[10]
    Figure  3.  Palynological diagram of ZKC01 borehole[10]
    下载: 全尺寸图片 幻灯片

    近年来，随着定量重建技术的不断发展，孢粉-古植被、孢粉-古气候研究领域逐渐超越了传统的定性或半定量研究方法，追求更为精确和深入的理解。用定量方法重新处理历史数据，可以帮助我们更准确地从孢粉数据中提取环境信息，定量重建古气候参数，从而提高重建结果的准确度和精度。通过定量处理，不同研究之间的孢粉数据可以更加标准化，便于进行跨地区、跨时间的综合分析和比较。孢粉-古植被重建方法包括使用相对花粉产量[42-44]的景观重建算法（Landscape Reconstruction Algorithm，LRA）[45-46]和植物功能型（Plant Functional Types，PFTs）的生物群区化法（Biamisation）[47]。将孢粉化石数据和古气候直接建立联系的方法有指示种法、集合法、多元回归函数法、贝叶斯法、古植被模型反演方法等，每种方法均具其独特优势与局限性[48-51]。多元回归函数法是用现代数据建立孢粉类群相对丰度与气候因子的转换函数，问题在于这一函数实际上是非线性的，且不同的区域之间常有差别[52]。指示种法的原理是古气候参数值至少应该在已知化石类群的气候适应范围内，只考虑物种存在与否而不考虑丰度，通常适用于没有丰度数据或缺乏现代组合参照物的情况，存在对变化不敏感和假设过于理想的问题[53]。相较之下，集合法将化石组合视为整体，考虑各分类群的相对丰度，广泛应用于定性及半定量分析。定量的集合法，包括现代类比法（Modern Analogue Technique，MAT）、响应曲面法（Response Surface Method）等，进一步提升了分析精度。现代类比法的基本思路是使用相异系数（如平方弦距离）将化石与现代组合在数值上进行比较，在找到与化石组合最相似的一个或几个现代样本后，古气候即可推断为与这些现代样本相关气候变量的状态相似[54-55]。

    本文选取直接将孢粉化石数据和古气候建立联系的定量方法——现代类比法对ZKC01钻孔孢粉数据进行处理，去除苔藓类、蕨类孢子后以花粉为基础重建气候的变量，包括年平均温度（Tann）和每年的总降水量（Pann）。该方法无需在区域上建立孢粉各分类群的含量与气候因子之间的转换函数，现代孢粉库的发展和气候数据更新保证了该方法现代类比物的数据充足和可靠。本文现代孢粉数据主要来自曹现勇等[56]的亚洲现代花粉数据集，同时参考了陈海燕等[57]的中国现代花粉数据集，并做了必要的筛选，选取亚洲地区花粉数据点5792个，参考孢粉类群56个；采用的气候数据来自Hijmans等的World-Clim资料集[58]；花粉收集样点的气候参数插值使用的是Diva-GIS 软件提供的薄板样条插值法；在Polygon 中的类比采用主因子（占到90%）的孢粉而不是全部孢粉，类比计算采用的是方差距离。为评估模型性能的优劣，使用留一法（Leave One Out，LOO）进行交叉验证，决定系数R2（预测值和实测值相关系数的平方）越接近1，则模型拟合越好[59-60]。以上过程利用Polygon软件完成。

    4.   结果与讨论

    最佳类比法通常被应用于晚第四纪研究中，而在冰期-间冰期长周期的序列中可能会出现在现代数据集中找不到相应类比结果的情况[61]。ZKC01孔孢粉数据在长时间尺度下仍能找到较好的现代类比结果，除250.63～251.23 m外，其他样品存在非相似性距离阈值（T）小于0.2的最佳样点均可以达到8个。

    基于最佳类比法分析得到的年平均温度（图4 b）和年平均降水（图4 c）变化曲线，体现了冰期和间冰期波动变化的特征。冰期年平均温度约为0～5℃，通常伴随着湿度的降低，年平均降水约为300～600 mm，但也存在寒凉湿润的阶段（图4 F阶段）。间冰期年平均温度约为10～15℃，年平均降水约为600～1000 mm。气候的波动在华田组沉积时期频繁，而在汨罗组、洞庭湖组沉积时期幅度变大而频率变低，此等变化可能归因于采样间隔的不均一性以及化石产出情况的差异，如65.58～100.03 m较长间断内无孢粉化石产出，这可能是由于河流相粗碎屑沉积较高的水动力条件不利于孢粉保存为化石。这段缺乏化石的地层降低了气候重建的分辨率，且可能错过重要的气候变化信号，需结合其他材料互相印证，或补充更多新材料以待后续研究。此外，中更新世转型期（Mid-Pleistocene Transition，MPT）对气候波动幅度和频率改变的影响亦不容忽视，即在0.8～1.2 Ma时期，气候周期由41 ka向100 ka转变，伴随着冰期-间冰期旋回幅度增大，全球冰量明显增加，海洋表面温度下降，东亚季风显著增强，陆地干旱化程度加强[35, 62-65]。

    图  4  根据ZKC01孔孢粉定量研究重建的洞庭盆地古气候演化
    a：深海氧同位素，b： 年平均气温，c： 年平均降水，d： 岩性、孢粉和测年数据，e. 古地磁。a据Lisiecki & Raymo[40]，b–d据柏道远等[10]修改，e据赵举兴等[24]。A–G：蓝色示冰期，粉红色示间冰期；具体阶段详见文本。灰色区域为无孢粉化石产出层段。
    Figure  4.  Reconstruction of paleoclimate evolution in the Dongting Basin based on quantitative pollen analysis of ZKC01 borehole
    a:Deep-sea oxygen isotopes; b: Annual mean temperature; c: Annual mean precipitation; d: Lithology, pollen, and dating data; e:Paleomagnetism. a :After Lisiecki & Raymo[40], b–d: modified after Bai et al.[10], e: after Zhao et al.[24]. A–G: blue bands show glacial periods, pink bands are interglacial periods; see text for details. Grey shades represent the interval of no palynomorphs.
    下载: 全尺寸图片 幻灯片

    总体而言，洞庭盆地上新世和更新世之交气候较为干冷（图4 A阶段），杰拉期早期气温逐渐回暖，降水始终较少，直至约2.0～2.2 Ma为温暖湿润的间冰期（图4 B阶段）。随后气候在凉干-温暖半干旱之间频繁波动，1.6 Ma左右进入另一个间冰期紧随一个显著的冰期（图4 C、D阶段）。此后冰期-间冰期的波动频率降低，但幅度升高。卡拉布里雅期晚期气候温暖湿润，在约1 Ma有一次降温同时伴随着湿度的降低（图4 E阶段）。千叶期早期缺乏孢粉样品，推测应有一个干凉的阶段；升温后中期约0.4 Ma又有一个温凉湿润的冰期（图4 F阶段）；晚期气候逐渐转为湿热，该阶段区内发育大量网纹化红土。更新世晚期是一个逐渐降温的过程（图4 G阶段），全新世则在较为温暖湿润的基础上存在气候波动。

    4.1   模型的现代检验

    利用留一法获得的交叉检验结果如图5所示。可以看出，基于现代类比法模型对于重建年均降水和年均温度均具有较高的可靠性。其中，年均降水的预测能力更佳，决定系数R2为0.8554；模型对于年均温度的预测能力次之，决定系数R2为0.8148。

    图  5  基于现代类比法模型的年均温度（a）和年均降水（b）的观测值与预测值散点图
    Figure  5.  Scatter plots of observed values and estimated values of annual mean temperature (Tann) (a) andannual mean precipitation (Pann) (b) based on MAT (Modern Analogue Technique) quantitative models
    下载: 全尺寸图片 幻灯片

    4.2   华田组沉积期古气候

    在气候波动的背景下，洞庭盆地的第四纪气候可细分为多个变化阶段。具体而言，华田组下段下部沉积时期气候干冷，并有逐渐变暖的趋势。即孢粉带I—II[10]，孢粉组合面貌以蒿属（Artemisia）、藜科、禾本科、蓼科、葎草属（Humulus）、石竹科（Caryophyllaceae）、十字花科等草本植物为主（图3），代表了较为寒凉且干燥的气候环境。年平均气温为0～8℃，年平均降水为250～570 mm。其中最底部相对最冷的阶段可能对应了上新世–更新世之交（图4 A阶段；深海氧同位素阶段MIS 100—104），该阶段是北半球冰川作用增强（iNHG）的时期[30, 66]，中高纬度地区出现冰川沉积物和冰筏碎片[67-68]，北极锋面和北大西洋洋流的南移[69]，气候季节性显著增强[70]。此转变的机制涉及全球变冷的渐进过程[71-72]，大气环流的改变[73-74]，海洋永久性强烈分层和冷舌的出现[75-77]，优势轨道参数的变化[78-79]，pCO2的下降[80-82]以及巴拿马地峡的闭合对太平洋和大西洋之间交流的限制等多种因素[83-85]。这一寒冷阶段较为显著，在多数研究中都能被识别（图2）[4, 6, 22]。

    洞庭盆地华田组沉积时期年均降水量普遍偏低（图4 c），平均约为500 mm，仅在超级间冰期出现小范围高值，可达600～800 mm，这与中国陆地孢粉记录显示的2.5～1.5 Ma期间气候偏干现象一致[86]。北太平洋及黄土高原的风尘记录进一步印证了在距今约2.7 Ma，亚洲地区干旱化加剧[87]。这一干旱化影响的范围较广，在亚洲各地的发生时间具有较高的一致性，西伯利亚南部贝加尔湖地区由于降水减少，大面积的开阔草原和岩石草原植被在 2.62 Ma 后永久建立[88]，西伯利亚东北部埃尔古古伊恩湖（Lake El’gygytgyn）的降温和干旱加剧也发生在2.6 Ma[35, 89-90]。这一干旱化事件与上新世–更新世之交降温事件有关或受相关的机制驱动。

    华田组沉积中期，两次显著冰期之间有一段持续时间较长的间冰期相隔，表现为温度处在较高位置（年平均气温8～10℃）小幅度波动，且降水也相应增加（图4 B阶段）。对应的孢粉组合IV草本植物含量下降，而常绿栎（Quercus）、枫香树属（Liquidambar）等阔叶乔木增加（图3），揭示了较为温暖且干旱有所缓解的气候特征。对俄罗斯埃尔古古伊恩湖沉积物的研究表明，深海氧同位素阶段MIS 11c、31、49、55、77、87、91和93存在超级间冰期[35]。尽管该湖芯剖面的孢粉数据显示MIS 77没有预想中的极端温暖，也是一个相对显著的间冰期[91]。洞庭盆地ZKC01孢粉带IV[10]的暖湿阶段可能是对这一超级间冰期的响应。向轲等[12]CZ04孔孢粉组合带II早期也存在枫香树属等热带、亚热带树种产出、中旱生草本花粉的百分含量大幅减少的温湿阶段。水文二队[22]报道的沅江华田ZK176、沅江塞坡咀ZK172等多个钻孔剖面中反映温湿-暖湿气候的孢粉组合可能也是在这一超级间冰期产出的。同时在留尼汪极性事件（Réunion event）[92] 发生时期附近，多条剖面的黄土记录显示S27古土壤层磁化率较高，且与S28相连的较长时间间隔内古土壤粒度较小 [93-95]。这与地磁极性发生变化[24]的阶段B显示出的温暖湿润的间冰期特征相符。

    4.3   汨罗组沉积期古气候

    华田组与汨罗组之交再次展现出显著的间冰期特征，年平均气温上升约6℃，可达11℃，年平均降水增加约800 mm，可达1200 mm（图4 C阶段），栗属、胡桃属（Juglans）等阔叶树和松属（Pinus）、铁杉属（Tsuga）等针叶树形成针阔叶混交林（图3）。这与水文二队[22]得出的结论更新世华田沉积晚期早时为温凉气候、晚时渐转湿热-干热气候基本一致（图2）。埃尔古古伊恩湖沉积物中Mg/Fe和Si/Ti指标识别出MIS 49和MIS 55两个时代相隔较近的超级间冰期[35]，其中MIS 55相对较为凉爽[96]。意大利Stirone剖面Picea+Tsuga的孢粉指标识别出MIS 49和MIS 55两个明显的低值，Vrica剖面MIS 47～55在较低的范围内波动，指示了较长一段时间内温暖适宜的气候[97]。洞庭盆地华田组和汨罗组之交的温暖湿润阶段即对应MIS 49—55（约1.5～1.6 Ma）这一段连续的显著间冰期。

    汨罗组沉积时期，在上述间冰期之后进入了一个相对寒冷的阶段，年平均温度8～10℃，降幅可达8℃，同时伴随着干旱的发生，年平均降水减少300 mm至500 mm左右（图4 D阶段），孢粉组合上表现为十字花科、蒿属等草本植物占主导地位。北太平洋中部的风尘通量自1.5 Ma开始又逐渐增加[87]，印证了这一干旱化趋势。同时在1.3～1.2 Ma左右，黄土记录显示L16—L14黄土层粒度显著增大，指示了沙漠的南移，夏季风的减弱[94]。随后升温进入一个较长时间的温暖湿润阶段，年平均温度11～14℃，年平均降水900～1100 mm，可能包含了MIS 31超级间冰期（约1.1 Ma）。汨罗组沉积后期再次经历了降温和升温的过程，其中干冷阶段处于中更新世转型过程中，通常冰期的持续时间增加[98] （图4 E阶段）。向轲等[12]报道的汨罗组孢粉组合反映出经历了凉干（带III）-温暖湿润-温凉半干旱（带IV、带V）-温湿（带VI）的变化，与本文得到的温湿曲线的变化趋势基本相符。

    4.4   洞庭湖组沉积期以来古气候

    洞庭湖组下部有较长间隔（65.58～100.03 m）无孢粉化石产出，根据岩性岩相、地球化学特征、磁化率、化学风化指数等指标，这一时间段内存在一个气候干旱寒冷的阶段[6-8, 13]。蔡述明等[2]报道了千叶期（中更新世）早期一个以冷杉属（Abies）、云杉属（Picea）为优势类群的孢粉样品，指示了寒凉湿润的气候。这与洞庭湖组沉积中期温凉湿润的冰期阶段表现相似（图4 F阶段），孢粉组合面貌不同于其他草本植物占优势地位的冰期，而以针叶类裸子植物为主，发育云杉属、铁杉属等花粉。这一阶段可能对应了MIS 12，在青藏高原地区发育为中梁赣冰期[99]。洞庭湖组沉积中后期气候温暖湿润，广泛发育了网纹红土。洞庭湖组和坡头组之间存在着沉积间断，坡头组沉积时期的降温可能标志着末次冰期（MIS 2—4）的到来（图4 G阶段），藜科、蒿属、葎草属等草本植物为主，间有蔷薇科（Rosaceae）、木樨科（Oleaceae）、麻黄属（Ephedra）等灌木形成的灌丛草原再次占领了洞庭盆地。环境地球化学特征变化也记录到了此次降温事件（图2）[6]。

    5.   结论和展望

    本研究基于ZKC01钻孔的孢粉数据，采用最佳类比法对洞庭盆地第四纪古气候进行了定量重建，初步识别出多个与深海氧同位素阶段（MIS）相对应的关键气候事件。研究结果表明，洞庭盆地第四纪气候演化具有显著的阶段性特征，主要包括：（1）上新世至更新世之交（MIS 100—104）的冰期；（2）更新世初期的干旱事件；（3）MIS 77—81与MIS 49—57期间的两次超级间冰期；（4）中梁赣冰期（MIS 12）以及（5）末次冰期（MIS 2—4）。这些气候事件的识别为理解洞庭盆地乃至东亚季风区第四纪气候演变提供了新的高分辨率证据。

    尽管本研究在长时间尺度、高分辨率定量分析方面取得了初步进展，但仍存在一些局限性。例如，部分层段样品稀缺导致气候波动信息缺失，部分样品的孢粉统计量不足，限制了分析的全面性。未来研究需结合更多高分辨率、精确定年的地质记录（如湖泊沉积、黄土序列等），并辅以多指标（如地球化学、微生物标志物等）综合分析，以更全面地恢复和解析洞庭盆地第四纪古气候的演变过程及其驱动机制。此外，加强区域与全球气候记录的对比研究，将有助于进一步揭示洞庭盆地对全球气候变化的响应特征。

  • 图  1   中新生代东亚地区微陆块划分及块体迁移

    Figure  1.   Schematic tectonic map showing Mesozoic-Cenozoic blocks migration in the East Asia

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    图  2   中侏罗世(165 Ma)东亚构造和地貌重建

    1-渤海湾盆地；2-鄂尔多斯盆地；3-海拉尔-塔木察格盆地；4-蒙古-鄂霍茨克造山带；5-松辽盆地；6-西萨彦岭；7-东萨彦岭；8-准噶尔盆地；9-车尔臣断裂

    Figure  2.   Tectonic and geomorphological reconstruction of Jurassic East Asia at ca 165 Ma

    1-Bohai Bay Basin; 2-Ordos Basin; 3-Hailar-Tamsag Basin; 4-Mongolian-Okhotsk Orogenic Belt; 5- Songliao Basin; 6-Western Sayan Mountains; 7-Eastern Sayan Mountains; 8-Junggar Basin; 9-Cherchen Fault Zone

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    图  3   早白垩世早期(140 Ma)东亚构造和地貌重建

    1-渤海湾盆地；2-鄂尔多斯盆地；3-海拉尔-塔木察格盆；4-蒙古-鄂霍茨克造山带；5-松辽盆地；6-西萨彦岭；7-东萨彦岭；8-准噶尔盆地；9-车尔臣断裂；10-戈壁-鄂嫩断裂；11-蒙古-鄂霍次克缝合

    Figure  3.   Tectonic and geomorphological reconstruction of early Early Cretaceous East Asia at ca 140 Ma

    1-Bohai Bay Basin; 2-Ordos Basin; 3-Hailar-Tamsag Basin; 4-Mongolian-Okhotsk Orogenic Belt; 5- Songliao Basin; 6- Western Sayan Mountains; 7- Eastern Sayan Mountains 8-Junggar Basin; 9- Cherchen Fault Zone; 10- Gobi-Onon Fault; 11-Mongolian-Okhotsk Suture

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    图  4   早白垩世晚期(125Ma)东亚构造和地貌重建

    1-渤海湾盆地；2-鄂尔多斯盆地；3-海拉尔-塔木察格盆；4-蒙古-鄂霍茨克造山带；5-松辽盆地；6-西萨彦岭；7-东萨彦岭；8-准噶尔盆地；9-车尔臣断裂；10-漠河盆地；11-依兰-伊通断；12-敦化-密山断裂

    Figure  4.   Tectonic and geomorphological reconstruction of late Early Cretaceous East Asia at ca 125 Ma

    1-Bohai Bay Basin; 2-Ordos Basin; 3-Hailar-Tamsag Basin; 4-Mongolian-Okhotsk Orogenic Belt; 5-Songliao Basin; 6-Western Sayan Mountains; 7-Eastern Sayan Mountains; 8-Junggar Basin; 9-Cherchen Fault Zone; 10-Mohe Basin; 11-Ilan-Yitong Fault; 12-Dunhua-Mishan fault

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    图  5   晚白垩世(90 Ma)东亚构造和地貌重建

    1-渤海湾盆地；2-鄂尔多斯盆地；3-海拉尔-塔木察格盆；4-蒙古-鄂霍茨克造山带；5-松辽盆地；6-西萨彦岭；7-东萨彦岭；8-准噶尔盆地；9-车尔臣断裂；10-漠河盆地；11-依兰-伊通断；12-敦化-密山断裂

    Figure  5.   Tectonic and geomorphological reconstruction of Late Cretaceous East Asia at ca 90 Ma

    1-Bohai Bay Basin; 2-Ordos Basin; 3-Hailar-Tamsag Basin; 4-Mongolian-Okhotsk Orogenic Belt; 5-Songliao Basin; 6-Western Sayan Mountains; 7-Eastern Sayan Mountains; 8-Junggar Basin; 9-Cherchen Fault Zone; 10-Mohe Basin; 11-Ilan-Yitong Fault; 12-Dunhua-Mishan fault

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    图  6   古近纪(60 Ma)东亚构造和地貌重建

    1-渤海湾盆地；2-鄂尔多斯盆地；3-海拉尔-塔木察格盆；4-蒙古-鄂霍茨克造山带；5-松辽盆地；6-西萨彦岭；7-东萨彦岭；8-准噶尔盆地；9-车尔臣断裂；10-漠河盆地；11-依兰-伊通断；12-敦化-密山断裂；13-索伦-西拉木伦-长春断裂

    Figure  6.   Tectonic and geomorphological reconstruction of Paleogene East Asia at ca 60 Ma

    1-Bohai Bay Basin; 2-Ordos Basin; 3-Hailar-Tamsag Basin; 4-Mongolian-Okhotsk Orogenic Belt; 5-Songliao Basin; 6-Western Sayan Mountains; 7-Eastern Sayan Mountains; 8-Junggar Basin; 9-Cherchen Fault Zone; 10-Mohe Basin; 11-Ilan-Yitong Fault; 12-Dunhua-Mishan fault; 13-Solon-Xar Moron-Changchun fault

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    图  7   古近纪(35 Ma)东亚构造和地貌重建

    1-渤海湾盆地；2-鄂尔多斯盆地；3-海拉尔-塔木察格盆；4-蒙古-鄂霍茨克造山带；5-松辽盆地；6-西萨彦岭；7-东萨彦岭；8-准噶尔盆地；9-车尔臣断裂；10-漠河盆地；11-依兰-伊通断；12-敦化-密山断裂；13-索伦-西拉木伦-长春断裂；14-阿尔金断裂；15-贝加尔裂谷；16-山西地堑；17-秦岭-大别造山带；18-南黄海盆地；19-台西南盆地；20-珠江口盆地；21-琼东南盆地；22-莺歌海盆地；23-冲绳海槽

    Figure  7.   Tectonic and geomorphological reconstruction of Neogene East Asia at ca 35 Ma

    1-Bohai Bay Basin; 2-Ordos Basin; 3-Hailar-Tamsag Basin; 4-Mongolian-Okhotsk Orogenic Belt; 5-Songliao Basin; 6-Western Sayan Mountains; 7-Eastern Sayan Mountains; 8-Junggar Basin; 9-Cherchen Fault Zone; 10-Mohe Basin; 16-Shanxi Graben; 17-Qinling-Dabie orogenic belt; 18-South Yellow Sea Basin; 19-Southwest Taiwan Basin; 20-Pearl River Mouth Basin; 21-Qiongdongnan Basin; 22-Yinggehai Basin; 23-Okinawa Trough

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    图  8   新近纪(25 Ma)东亚构造和地貌重建

    1-渤海湾盆地；2-鄂尔多斯盆地；3-海拉尔-塔木察格盆；4-蒙古-鄂霍茨克造山带；5-松辽盆地；6-西萨彦岭；7-东萨彦岭；8-准噶尔盆地；9-车尔臣断裂；10-漠河盆地；11-依兰-伊通断；12-敦化-密山断裂；13-索伦-西拉木伦-长春断裂；14-阿尔金断裂；15-贝加尔裂谷；16-山西地堑；17-秦岭-大别造山带；18-南黄海盆地；19-台西南盆地；20-珠江口盆地；21-琼东南盆地；22-莺歌海盆地；23-冲绳海槽

    Figure  8.   Tectonic and geomorphological reconstruction of Neogene East Asia at ca 25 Ma

    1-Bohai Bay Basin; 2-Ordos Basin; 3-Hailar-Tamsag Basin; 4-Mongolian-Okhotsk Orogenic Belt; 5-Songliao Basin; 6-Western Sayan Mountains; 7-Eastern Sayan Mountains; 8-Junggar Basin; 9-Cherchen Fault Zone; 10-Mohe Basin; 16-Shanxi Graben; 17-Qinling-Dabie Orogenic Belt; 18-South Yellow Sea Basin; 19-Southwest Taiwan Basin; 20-Pearl River Mouth Basin; 21-Qiongdongnan Basin; 22-Yinggehai Basin; 23-Okinawa Trough

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  • 被引次数: 11
出版历程
  • 收稿日期:  2017-05-30
  • 修回日期:  2017-06-18
  • 刊出日期:  2017-08-27

目录

摘要
HTML全文

  • 1.   洞庭盆地概况

  • 2.   洞庭盆地第四纪古气候研究简述

  • 3.   材料和方法

  • 4.   结果与讨论

  • 4.1   模型的现代检验

  • 4.2   华田组沉积期古气候

  • 4.3   汨罗组沉积期古气候

  • 4.4   洞庭湖组沉积期以来古气候

  • 5.   结论和展望

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