闽西仙云洞高分辨率石笋记录的东亚夏季风CIS-8事件及亚旋回特征^*

East Asian Summer Monsoon CIS-8 event and its sub-cycle features recorded by precisely-dated high-resolution stalagmite from Xianyun Cave,western Fujian Province,China

摘要

基于福建仙云洞石笋(XY2-10)的9个高精度²³⁰Th年龄和442个氧同位素数据,重建了38.20—36.10ka B.P.平均分辨率达5 yr的东亚夏季风(East Asian Summer Monsoon,EASM)强度演变历史。福建仙云洞石笋 δ¹⁸O 值在CIS-8(Chinese Interstadial 8)时期整体呈现出稳定的偏负特征,与同一时期中国季风区内葫芦洞、永兴洞、小白龙洞石笋 δ¹⁸O 记录趋势较为一致,但该石笋 δ¹⁸O 记录的夏季风强度在CIS-8期间整体偏强的趋势,与格陵兰冰芯 δ¹⁸O 记录的降温趋势不同。分析表明,在CIS-8事件期间,南极变冷,其通过增强南半球马斯克林高压(Mascarene High,MH)和越赤道气流,使中国南方地区石笋 δ¹⁸O 记录的EASM整体保持较强态势。此外,仙云洞石笋 δ¹⁸O 记录还揭示了CIS-8事件内部存在21次百年至十年际尺度的夏季风增强事件,这与格陵兰NEEM(Northern Greenland Eemian Ice Drilling)冰芯 δ¹⁸O 记录、阿拉伯海海盆岩心反照率记录的亚旋回事件相对应,表明EASM增强(减弱)、北高纬温度升高(降低)和赤道辐合带(Intertropical Convergence Zone,ITCZ)北移(南移)在百年至十年际尺度上存在紧密的联系,而这种联系可能是源于北大西洋经向翻转环流(Atlantic Meridional Overturning Circulation,AMOC)变化引起的北半球高纬与低纬地区的快速海气耦合。

Abstract

The Greenland Interstadial 8(GIS-8)event during Marine Isotope Stage 3(MIS3)is characterized by significant warming at northern high latitudes. However,relatively few high-resolution geological records have been used to reveal its detailed structure and global response. In this study,nine high-precision ²³⁰Th ages and 442 oxygen isotope(δ¹⁸O)data were measured from a stalagmite(XY2-10) collected from Xianyun Cave in Fujian Province. These data enable us to reconstruct the evolution of the East Asian Summer Monsoon(EASM)intensity with an average temporal resolution of 5 years over the period of 38.20-36.10ka B.P.(Before Present,“Present”refers to 1950 AD),which covers the Chinese Interstadial 8(CIS-8)event. The δ¹⁸O time series exhibit a stable negative characteristic during the CIS-8 period,consistent with the trends observed in δ¹⁸O records from other stalagmites in the Chinese monsoon region,such as those from Hulu Cave,Yongxing Cave,and Xiaobailong Cave. However,the strengthening trend in summer monsoon intensity recorded by the stalagmite in Xianyun Cave during CIS-8 contrasts with the cooling trend evident in the Greenland ice core δ¹⁸O record. The analysis suggests that during CIS-8,enhanced cooling in Antarctica strengthened the Mascarene High and the transequatorial flow in the Southern Hemisphere,resulting in an overall stronger EASM in southern China, as reflected in the stalagmite δ¹⁸O records. Our sub-decadal resolution record also identifies 21 centennial- to interdecadal-scale summer monsoon enhancement events within the CIS-8 interval. These events correlate well with corresponding events in the Greenland NEEM(Northern Greenland Eemian Ice Drilling)ice-core δ¹⁸O record and the core albedo record from the Arabian Sea Basin. This correlation indicates that the EASM enhancement(weakening),warming(cooling)of northern high latitudes,and northward(southward)shift of the Intertropical Convergence Zone(ITCZ)are strongly linked on centennial- to interdecadal-scales. These connections are likely driven by rapid air-sea coupling mechanism,which is influenced by changes in the Atlantic Meridional Overturning Circulation(AMOC) in the North Atlantic.

Graphical abstract

关键词

CIS-8事件 / 石笋 / 东亚夏季风 / 福建仙云洞 / 亚旋回

Key words

Chinese Interstadial 8 event / stalagmite / East Asian summer monsoon / Xianyun Cave of Fujian Province / sub-cycles

1 概述

末次冰期深海氧同位素第3阶段(Marine Isotope Stage 3,MIS3)以一系列典型的千年尺度Dansgaard-Oeschger(DO)旋回为标志(Dansgaard et al., 1993;Hinnov et al., 2002),全球冰量、太阳辐射及CO₂浓度均处于中等水平(McManus et al., 1999;Sachs and Lehman,1999),北大西洋洋流不稳定,易发生千年尺度气候震荡(Dansgaard et al., 1993)。格陵兰冰芯与中国季风区石笋分别记录了北半球高纬度地区(后文简称“北高纬”)温度快速变暖与东亚夏季风(East Asian Summer Monsoon,EASM)快速增强的气候突变事件,分别被称为格陵兰间冰阶(Greenland Interstadials,GIS)与中国间冰阶(Chinese Interstadials,CIS)(Johnsen et al.,1992;Cheng et al., 2006)。研究发现,千年时间尺度上GIS与CIS事件具有良好的一一对应关系(Wang et al.,2001,2005)。依据高分辨率的格陵兰冰芯记录发现在GIS事件内部存在百年至十年际尺度的亚旋回事件,表明冰期中的暖事件气候变化也不稳定(Capron et al., 2010,2012;Rasmussen et al., 2014)。该冰芯记录中,末次冰期千年尺度气候突变事件的亚旋回事件是否在亚洲季风区也存在,对于理解气候突变事件的驱动机制具有重要意义。此外,CIS事件在起始过程方面与格陵兰冰芯快速突变并不完全一致,而是表现出类似南极冰芯缓慢变化的特征,说明中国季风区气候会受到南半球气候的强有力调控(Rohling et al., 2003;Cai et al., 2006;Chen et al., 2016;Wu et al., 2020)。

GIS-8事件在格陵兰冰芯 δ¹⁸O 记录中的持续时间接近1700 yr,振幅达4‰(Andersen et al., 2006),是MIS3阶段最典型的GIS事件之一。中国季风区的三星洞、小白龙洞、雾露洞、葫芦洞和永兴洞石笋 δ¹⁸O 记录都捕捉到了CIS-8事件(Cai et al., 2006;何尧启和姜修洋,2012;Duan et al., 2014;Cheng et al., 2016;Liang et al., 2022)。其中,西南雾露洞石笋 δ¹⁸O 记录的CIS-8事件开始与南极冰芯 δ¹⁸O 记录存在着类似的缓慢变化特征,说明中国季风区在CIS-8事件初始时受到与南极温度相关的南半球水汽输送的影响(Duan et al.,2014)。贵州三星洞石笋 δ¹⁸O 记录显示CIS-8内部还存在4次亚旋回事件,在定年误差范围内分别与格陵兰NGRIP冰芯 δ¹⁸O 记录及Cariaco海盆沉积物反射比记录一一对应,表明亚洲夏季风与北极温度、赤道辐合带(Intertropical Convergence Zone,ITCZ)位置在千年至百年尺度上存在遥相关(何尧启和姜修洋,2012)。然而,上述石笋记录的氧同位素分辨率较低,且位于中国西南地区或长江中下游地区。因此,为了更准确地还原EASM在CIS-8时期的时空变化特征,了解其与南、北极气候的联系,有必要获取更多区域高精度定年的高分辨率古气候记录并对其进行更深入的研究。

文中选取位于东亚季风区前沿地带的中国东南地区福建仙云洞的1根石笋(编号XY2-10),通过精确的²³⁰Th测年和氧同位素测试,重建了中国东南地区38.20—36.10ka B.P. 期间平均分辨率达5 yr的东亚夏季风时间演化序列,揭示出中国东南地区CIS-8事件期间EASM的变化特征。通过与已发表的古气候记录对比,探讨其内部特征及可能存在的驱动机制。

2 研究区域概况、材料与方法

石笋样品采自福建西部龙岩市连城县城东南15km处的仙云洞(25°33'N,116°59'E)(图1-A),洞口海拔约为968m。仙云洞所在的连城县处于浙闽丘陵,受典型的东亚夏季风影响,因地形因素兼具山地气候特征,全年气候温和,降水充沛。距仙云洞59km的永安气象站自1989至2018年年平均气温为20℃,平均降水量1552mm,5-9月份降水量约占全年总降水量的60%(图1-C)。溶洞发育于二叠系栖霞组石灰岩中,自洞口向内呈阶梯状下延,全长2470m(张富强等,2018)。洞穴封闭性较好,洞内实测气温为17.5℃,湿度常年接近100%。洞内有若干大小不等的洞厅,滴水点众多,次生碳酸盐发育良好。洞穴上覆土壤为黄壤,植被繁茂,主要以毛竹林、林下草本植物为主。

样品XY2-10采自仙云洞右支洞的中部大厅(图1-B),整体外形呈圆柱状,长532mm,底部直径约为58mm(图2-A)。将石笋沿着中心生长轴切开、抛光,抛光面光滑且无溶孔。在距顶部41mm、70mm及515mm处分别存在1个风化层面,有可能为沉积间断。

在石笋抛光面上,使用直径为0.5mm的牙钻,沿生长轴钻取11个样品用于²³⁰Th定年。化学前处理和分析方法参照Shen等(2012),分析仪器为MC-ICP-MS Neptune,在台湾大学高精度质谱与环境变迁实验室(HISPEC)完成测试。

使用直径为0.3mm的牙钻,沿生长轴方向,每间隔1mm采集1个氧同位素样品,共获取442个样品进行稳定同位素测试。每9个样品插入1个标准样品(NBS-19),通过碳酸盐自动进样装置Kiel-Ⅳ与Finnigan MAT-253 Plus型质谱仪联机测试完成。氧同位素样品的采集与测试工作在福建师范大学地理科学学院稳定同位素实验室完成。

3 结果

3.1 U/Th年代

表1给出了XY2-10石笋在41~530mm层段的11个U-Th实测年龄以及误差范围(±2σ)。定年结果显示,XY2-10石笋²³⁸U含量高(8.7~29.0 μg/g),²³²Th含量低(33.5~12924.1 pg/g),测年误差为13~104 a,测年精度高。结合定年结果和岩性特征分析,认为在70mm、515mm处可能存在沉积间断(图2-A)。文中主要分析距顶部70~511mm的石笋层段。在研究层段,根据9个²³⁰Th定年点,采用线性内插方法,建立了年龄—深度模型(图2-B),由此构建了38.20—36.10ka B.P.分辨率达5 yr的氧同位素序列,该时段生长速率为0.13~0.30mm/yr(图2-C)。

3.2 石笋氧同位素记录

图3给出了覆盖CIS-8及间断面下海因里希冰阶4(Heinrich Stadial 4,HS4)时期的仙云洞XY2-10及已发表的同一洞穴XY-1(Zhang et al., 2021)石笋氧同位素记录随时间演化序列。由图3可以看出,XY2-10与 XY-1氧同位素在重叠生长时段重现性较好,说明XY2-10没有发生显著的动力分馏。在HS4时期,XY2-10石笋氧同位素在-7.43‰~-7.08‰之间波动,平均值为-7.24‰。CIS-8事件时期,氧同位素整体在-8.65‰~-7.30‰之间波动,平均值为-8.13‰。整个CIS-8时段XY2-10氧同位素值较为偏负,相比于HS4时期偏负约1‰,与同一时期XY-1石笋氧同位素振幅相一致。38.19±0.10ka B.P.左右XY2-10石笋氧同位素快速负偏,时间上与XY-1石笋氧同位素记录的CIS-8开始时快速负偏在定年误差范围内一致。2支石笋精确地标定了CIS-8事件开始时间为38.19±0.10ka B.P., 这与由葫芦洞校正的格陵兰冰芯GICC05(Greenland Ice Core Chronology 2005,GICC05)时标下CIS-8的开始时间(38.34±0.07ka B.P.)(Cheng et al., 2021)及永兴洞(38.18ka B.P.)(Liang et al.,2022)、小白龙洞(38.21ka B.P.)(Cai et al.,2006)、雾露洞(38.27ka B.P.)(Duan et al., 2014)记录的CIS-8事件开始时间在定年误差范围内一致。38.19—36.29ka B.P.,氧同位素呈稳定的水平波动,并叠加了众多百年至十年际尺度的震荡。自36.29ka B.P.开始,石笋 δ¹⁸O 值迅速偏正,直到36.19ka B.P.达到极大值之后趋于稳定波动。根据气候突变过程中间点的位置,标定CIS-8事件的结束时间为36.24±0.02ka B.P.。CIS-8事件的持续时间为2ka左右。

4 讨论

4.1 仙云洞石笋氧同位素指示意义

研究认为,中国石笋 δ¹⁸O 在轨道至百年时间尺度上反映了平均气候状态下的夏季风强度或大尺度范围内水汽整体运移状况(Liu et al., 2014;Cheng et al., 2016),但目前对于夏季风强度的解释存在不同认识,例如夏季降水量与全年降水量的比值(Wang et al., 2001;Zhang et al.,2020)、水汽源变化(Tan,2014)、传输路径上雨除效应强度(Yuan et al.,2004;Ruan et al., 2019)等。针对中国东南地区的石笋 δ¹⁸O 记录,前人研究表明其在十年至年际时间尺度上主要受控于厄尔尼诺/南方涛动(El Niño-Southern Oscillation,ENSO)调控的夏季/非夏季降水比例(Zhang et al., 2018a,2018b;Lu et al., 2021)。最近,Qiu 等(2023)基于福建西部玉华洞11 yr的现代监测,认为与ENSO有关的上游对流和雨除效应调控了中国东南地区年际至季节降水 δ¹⁸O 值。据此,结合先前的解释(Qiu et al., 2022,2024;Zhang et al., 2024),笔者认为中国东南地区仙云洞石笋 δ¹⁸O 在千年至百年时间尺度上反映了大尺度环流和降水变化的信号,即EASM的强度。当 δ¹⁸O 值越正(负),EASM越弱(强)。

4.2 CIS-8事件特征及演化机制

GIS-8事件在格陵兰冰芯记录中呈现快速升温—持续降温—快速降温的“锯齿状”变化模式(Dansgaard et al., 1993;Wolff et al., 2010),表明北高纬温度在GIS-8事件开始后会持续降低直至事件结束(图4-A)。图4-D代表的XY2-10石笋 δ¹⁸O 序列在CIS-8完全开始后呈现出持续偏负的特征,说明仙云洞石笋记录的东亚夏季风强度在事件期间是逐渐增强的,这与北高纬温度变化趋势不一致。将中国季风区不同石笋记录的CIS-8事件氧同位素变化序列进行对比,发现虽然各石笋 δ¹⁸O 记录变化细节存在一定差异,这可能与样品的氧同位素分辨率及定年精度不同有关,也可能是受局地气候的影响或者由石笋记录的信噪比不同引起,但在事件整体变化趋势上,可以较为明显地看出葫芦洞(图4-B)和小白龙洞(图4-E)石笋 δ¹⁸O 值在CIS8事件期间始终较为偏负,永兴洞(图4-C)和仙云洞(图4-D)类似,表现出明显的负偏趋势,说明中国季风区石笋记录的EASM整体较为强劲。已有研究表明,石笋记录的EASM在千年尺度上响应北高纬气候强迫(Wang et al., 2001;Cheng et al., 2009),但地理空间和影响因素的区域差异性可能会使低纬夏季风和北高纬温度在CIS变化模式上呈现出不同的变化特征(Han et al., 2016;Duan et al., 2018)。

因此,CIS-8时期EASM强度与北高纬温度不一致的整体变化趋势,可能暗示了其他驱动力的作用。将仙云洞石笋 δ¹⁸O 记录(图4-D)与南极冰芯WDC的 δ¹⁸O 记录(图4-F)进行比较,南极冰芯表现出的持续变冷与EASM的整体较强趋势在反相位关系下具有更强的一致性。从中国石笋、黄土与南极冰芯、南半球湖泊等古气候地质证据的对比中已经发现,EASM作为全球气候系统的一个组成部分,充当了北半球和南半球气候相互作用的 “桥梁”角色,会受到南半球气候“推力”的影响(An,2000,2015;Rohling et al., 2009)。当CIS-8开始后,南高纬地区温度持续降低,加大了南半球温度梯度,这会导致马斯克林高压(Mascarene High,MH)的增强。而MH对东亚夏季风环流有重要引导作用,MH的增强会改变对流层低层大气环流,增强跨赤道的索马里急流,使南印度洋水汽更多输送至东亚地区,从而加强EASM(Xue et al., 2004;Cai et al., 2006;崔英方等,2011;Chen et al., 2016;Wu et al., 2020)。因此,虽然北高纬地区温度在CIS-8时期逐渐降低,但是南极降温引起的自南向北更强的越赤道气流会增强亚洲夏季风强度,从而削弱了北高纬地区气候对中国季风区的影响,使得EASM呈现出整体较强的趋势。

4.3 CIS-8时期百年至十年际尺度气候亚旋回事件

高分辨率的格陵兰NEEM冰芯(Gkinis et al., 2021)与阿拉伯海海盆岩心(Deplazes et al., 2013),不仅记录了CIS-8千年尺度气候振荡,更揭示出事件内的亚旋回震荡特征。对格陵兰NEEM冰芯δ¹⁸O、阿拉伯海海盆岩心反照率及XY2-10石笋 δ¹⁸O 记录分别进行6点、6点及4点滑动平均处理以达到相近分辨率后进行对比,结果如图5所示。由图5可以看出,EASM在长期趋势上未响应ITCZ南移及北高纬地区变冷信号,这也在一定程度上说明了EASM还受到南半球越赤道气流的调控,因此3个记录在整体变化趋势上并未显示出完全一致的变化特征。而在百年至十年际时间尺度上,平滑后的石笋 δ¹⁸O 发生了21次明显负偏(图5-B),指示了东亚季风区共发生了21次季风增强的亚旋回事件,这与格陵兰冰芯 δ¹⁸O 正偏指示的北极温度升高(图5-A)和阿拉伯海海盆岩心反照率降低指示的ITCZ北移(图5-C)相对应。研究发现,全新世(张春霞等,2010)、末次冰消期(姜修洋等,2015)及末次冰期其他CIS事件中(Liu et al., 2010;王晓艳等,2015;车印平等,2020),也存在这种百年至十年际时间尺度高低纬联系。而末次冰期气候不稳定背景下的MIS3时期,海气耦合系统可能会放大微弱气候信号,导致大气系统随机共振,引起高低纬一致变化(刘殿兵等,2008;Ganopolski and Rahmstorf,2002;Willeit et al., 2024)。整个CIS-8期间,大气CO₂浓度下降,冰盖体积减小,这可能使北大西洋经向翻转环流(Atlantic Meridional Overturning Circulation,AMOC)的活动敏感性增强(Arz et al., 2007;Bauska et al., 2021;Sun et al., 2022)。因此,这一时期北高纬地区冰量的短时间变化可能会引起北大西洋淡水注入发生变化,并影响到北大西洋北部深层水的形成,从而导致AMOC增强(减弱)(Rahmstorf,2002),北高纬地区的气温升高(降低)。这一认识一方面会使指示数十年时间尺度上北大西洋海温非周期性波动的大西洋多年代际变率(Atlantic Multidecadal Variability,AMV)正(负)位相转变(Zhang and Delworth,2005;Sutton et al., 2018;Zhang et al., 2019),从而引起南、北半球海洋温度梯度异常,哈德莱环流圈与ITCZ位置北(南)移; 另一方面会经北半球西风将北高纬地区气候信号向低纬传递,最终导致东亚夏季风强度增强(减弱)(Broccoli et al.,2006;Cosford et al., 2008;Schneider et al.,2014;Guo et al., 2024;丁一汇等,2020;姜大膀等,2024)。因此,东亚季风CIS-8内部百年至十年际尺度的亚旋回特征可能是受到AMOC变化引起的北高纬与低纬地区的快速海气耦合影响。

5 结论

本研究基于福建西部仙云洞石笋9个高精度²³⁰Th年龄和442个氧同位素分析,获得了38.20—36.10ka B.P.平均分辨率达5 yr的CIS-8时期东亚夏季风强度变化信息。

1)CIS-8时期,仙云洞石笋XY2-10 的 δ¹⁸O 值整体表现出稳定的负偏趋势,与同一时期中国季风区葫芦洞、永兴洞、小白龙洞石笋 δ¹⁸O 记录相似,说明空间尺度上中国南方地区石笋记录的EASM在事件期间整体较为强劲,这可能是由于南极变冷,南半球马斯克林高压和越赤道气流增强,进而加强了EASM。

2)高分辨率的仙云洞石笋 δ¹⁸O 记录揭示出CIS-8事件内存在21个EASM 增强的亚旋回气候事件,这与格陵兰NEEM冰芯及阿拉伯海海盆岩心反照率记录有相对应的关系。表明在末次冰期典型CIS季风增强事件气候背景下,受到北大西洋气候波动的影响,EASM在百年至十年际尺度上具有不稳定的强弱变化,这可能源于AMOC变化引起的北大西洋海温异常经海气耦合系统将北高纬信号传递至低纬地区。

参考文献

[1] 车印平, 肖海燕, 姜修洋, 蔡炳贵. 2020. DO4事件的精确定年及亚旋回特征: 来自福建龙岩仙云洞石笋的证据. 古地理学报, 22(2): 377-384.

[2] [Che Y P, Xiao H Y, Jiang X Y, Cai B G. 2020. Precise dating of the Dansgaard-Oeschger event 4 and its sub-cycles: evidence from a stalagmite from Xianyun cave in Longyan City, Fujian. Province. Journal of Palaeogeography(Chinese Edition), 22(2): 377-384]

[3] 崔英方, 汪永进, 刘殿兵. 2011. 黔西南雾露洞石笋记录的MIS3晚期亚洲季风变化和南北极气候的联系. 海洋地质与第四纪地质, 31(3): 101-107.

[4] [Cui Y F, Wang Y J, Liu D B. 2011. High-resolution stalagmite δ¹⁸O records of Asian monsoon changes in southwest Guizhou during the late episode of MIS3: a test of the bi-polar see-saw model at centennial scale. Marine Geology & Quaternary Geology, 31(3): 101-107]

[5] 丁一汇, 李怡, 王遵娅, 司东, 柳艳菊. 2020. 亚非夏季风的年代际变化: 大西洋多年代际振荡与太平洋年代际振荡的协同作用. 大气科学学报, 43(1): 20-32.

[6] [Ding Y H, Li Y, Wang Z Y, Si D, Liu Y J. 2020. Interdecadal variation of Afro-Asian summer monsoon: coordinated effects of AMO and PDO oceanic modes. Transactions of Atmospheric Sciences, 43(1): 20-32]

[7] 何尧启, 姜修洋. 2012. 黔北洞穴石笋记录的GIS-8事件亚旋回特征. 第四纪研究, 32(3): 561-562.

[8] [He Y Q, Jiang X Y. 2012. Sub-Greenland-Interstadial 8 Event of Asianmonsoon from a stalagmite record in northern Guizhou Province. Quaternary Sciences, 32(3): 561-562]

[9] 姜大膀, 司东, 缪家鹏. 2024. 大西洋多年代际振荡对东亚气候影响的综述. 大气科学, 48(1): 261-272.

[10] [Jiang D B, Si D, Miao J P. 2024. Impacts of Atlantic multidecadal oscillation on the east Asian climate: a review. Chinese Journal of Atmospheric Sciences, 48(1): 261-272]

[11] 姜修洋, 杨邦, 王晓艳, 何尧启, 段福才, 李志忠, 沈川洲. 2015. 黔北洞穴石笋记录的末次冰消期至早全新世百年-十年际气候变化. 地理科学, 35(6): 773-781.

[12] [Jiang X Y, Yang B, Wang X Y, He Y Q, Duan F C, Li Z Z, Shen C Z. 2015. The centennial to decadal scale variation of summer monsoon precipitation in northern Guizhou Province during the last deglacial. Scientia Geographica Sinica, 35(6): 773-781]

[13] 刘殿兵, 汪永进, 陈仕涛, 程海, R. L. Edwards. 2008. 东亚季风MIS3早期DO事件的亚旋回及全球意义. 第四纪研究, 28(1): 169-176.

[14] [Liu D B, Wang Y J, Chen S T, Cheng H, R. L. Edwards. 2008. Sub-Dansgaard-Oeschger events of east Asian monsoon and their global significance. Quaternary Sciences, 28(1): 169-176]

[15] 王晓艳, 何尧启, 姜修洋. 2015. CIS 24事件的精确定年及亚旋回特征: 以黔北三星洞石笋为例. 第四纪研究, 35(6): 1418-1424.

[16] [Wang X Y, He Y Q, Jiang X Y. 2015. Precise dating of the Chinese-Interstadial 24 event and its sub-cycles inferred from a high resolution stalagmite δ¹⁸O record in northern Guizhou Province. Quaternary Sciences, 35(6): 1418-1424]

[17] 张春霞, 张茂恒, 李偏, 孔兴功, 朱正坤, 姜修洋, 汪永进. 2010. 2592-1225a BP湖北神农架石笋氧同位素记录及区域气候意义. 地理科学, 30(6): 950-954.

[18] [Zhang C X, Zhang M H, Li P, Kong X G, Zhu Z K, Jiang X Y, Wang Y J. 2010. Stalagmite δ¹⁸O record 2592-1225 aBP from Mt. Shennongjia and its regional climate significance. Scientia Geographica Sinica, 30(6): 950-954]

[19] 张富强, 李苗发, 曹奇, 雷国良, 王芳, 蔡炳贵. 2018. 闽西仙云洞空间结构特征及其影响因素浅析. 亚热带资源与环境学报, 13(1): 88-94.

[20] [Zhang F Q, Li M F, Cao Q, Lei G L, Wang F, Cai B G. 2018. Spatial structure and influencing factors of the Xianyun cave in western Fujian Province. Journal of Subtropical Resources and Environment, 13(1): 88-94]

[21] Arz H W, Lamy F, Ganopolski A, Nowaczyk N, Pätzold J. 2007. Dominant Northern Hemisphere climate control over millennial-scale glacial sea-level variability. Quaternary Science Reviews, 26(3): 312-321.

[22] An Z S. 2000. The history and variability of the East Asian paleomonsoon climate. Quaternary Science Reviews, 19(1): 171-187.

[23] An Z S, Wu G X, Li J P, Sun Y B, Liu Y M, Zhou W J, Cai Y J, Duan A M, Li L, Mao J Y, Cheng H, Shi Z G, Tan L C, Yan H, Ao H, Chang H, Feng J. 2015. Global monsoon dynamics and climate change. Annual Review of Earth and Planetary Sciences,43: 29-77.

[24] Andersen K K, Svensson A, Johnsen S J, Rasmussen S O, Bigler M, Röthlisberger R, Ruth U, Siggaard-Andersen M L, Steffensen J P, Dahl-Jensen D, Vinther B M, Clausen H B. 2006. The Greenland Ice Core Chronology 2005,15-42 ka. Part 1: constructing the time scale. Quaternary Science Reviews, 25(23-24): 3246-3257.

[25] Bauska T K, Marcott S A, Brook E J. 2021. Abrupt changes in the global carbon cycle during the last glacial period. Nature Geoscience, 14(2): 91-96.

[26] Broccoli A J, Dahl K A, Stouffer R J. 2006. Response of the ITCZ to Northern Hemisphere cooling. Geophysical Research Letters, 33(1): L01702.

[27] Buizert C, Cuffey K M, Severinghaus J P, Baggenstos D, Fudge T J, Steig E J, Markle B R, Winstrup M, Rhodes R H, Brook E J, Sowers T A, Clow G D, Cheng H, Edwards R L, Sigl M, McConnell J R, Taylor K C. 2015. The WAIS Divide deep ice core WD2014 chronology-Part 1: methane synchronization(68-31 ka BP)and the gas age-ice age difference. Climate of the Past, 11(2): 153-173.

[28] Cai Y J, An Z S, Cheng H, Edwards R L, Kelly M J, Liu W G, Wang X F, Shen C C. 2006. High-resolution absolute-dated Indian Monsoon record between 53 and 36 ka from Xiaobailong Cave,southwestern China. Geology, 34(8): 621-624.

[29] Capron E, Landais A, Chappellaz J, Schilt A, Buiron D, Dahl-Jensen D, Johnsen S J, Jouzel J, Lemieux-Dudon B, Loulergue L, Leuenberger M, Masson-Delmotte V, Meyer H, Oerter H, Stenni B. 2010. Millennial and sub-millennial scale climatic variations recorded in polar ice cores over the last glacial period. Climate of the Past, 6(3): 345-365.

[30] Capron E, Landais A, Chappellaz J, Buiron D, Fischer H, Johnsen S J, Jouzel J, Leuenberger M, Masson-Delmotte V, Stocker T F. 2012. A global picture of the first abrupt climatic event occurring during the last glacial inception. Geophysical Research Letters, 39(15): L15703.

[31] Chen S T, Wang Y J, Cheng H, Lawrence Edwards R, Wang X F, Kong X G, Liu D B. 2016. Strong coupling of Asian monsoon and Antarctic climates on sub-orbital timescales. Scientific Reports, 6(1): 32995.

[32] Cheng H, Edwards R L, Wang Y J, Kong X G, Ming Y F, Kelly M J, Wang X F, Gallup C D, Liu W G. 2006. A penultimate glacial monsoon record from Hulu cave and two-phase glacial terminations. Geology, 34(3): 217-220.

[33] Cheng H, Edwards R L, Broecker W S, Denton G H, Kong X G, Wang Y J, Zhang R, Wang X F. 2009. Ice age terminations. Science, 326(5950): 248-252.

[34] Cheng H, Edwards R L, Shen C C, Polyak V J, Asmerom Y, Woodhead J, Hellstrom J, Wang Y J, Kong X G, Spötl C, Wang X F, Alexander E C. 2013. Improvements in ²³⁰Th dating,²³⁰Th and ²³⁴U half-life values,and U-Th isotopic measurements by multi-collector inductively coupled plasma mass spectrometry. Earth and Planetary Science Letters, 371-372: 82-91.

[35] Cheng H, Edwards R L, Sinha A, Spötl C, Yi L, Chen S T, Kelly M, Kathayat G, Wang X F, Li X L, Kong X G, Wang Y J, Ning Y F, Zhang H W. 2016. The Asian monsoon over the past 640,000 years and ice age terminations. Nature, 534(7609): 640-646.

[36] Cheng H, Xu Y, Dong X Y, Zhao J Y, Li H Y, Baker J, Sinha A, Spötl C, Zhang H W, Du W J, Zong B Y, Jia X, Kathayat G, Liu D B, Cai Y J, Wang X F, Strikis N M, Cruz F W, Auler A S, Gupta A K, Singh R K, Jaglan S, Dutt S, Liu Z Y, Edwards R L. 2021. Onset and termination of Heinrich Stadial 4 and the underlying climate dynamics. Communications Earth & Environment, 2(1): 230.

[37] Cosford J, Qing H R, Yuan D X, Zhang M L, Holmden C, Patterson W, Hai C. 2008. Millennial-scale variability in the Asian monsoon: evidence from oxygen isotope records from stalagmites in southeastern China. Palaeogeography,Palaeoclimatology,Palaeoecology, 266(1): 3-12.

[38] Dansgaard W, Johnsen S J, Clausen H B, Dahl-Jensen D, Gundestrup N S, Hammer C U, Hvidberg C S, Steffensen J P, Sveinbjörnsdottir A E, Jouzel J, Bond G. 1993. Evidence for general instability of past climate from a 250-kyr ice-core record. Nature, 364(6434): 218-220.

[39] Deplazes G, Lückge A, Peterson L C, Timmermann A, Hamann Y, Hughen K A, Röhl U, Laj C, Cane M A, Sigman D M, Haug G H. 2013. Links between tropical rainfall and North Atlantic climate during the last glacial period. Nature Geoscience, 6(3): 213-217.

[40] Duan F C, Liu D B, Cheng H, Wang X F, Wang Y J, Kong X G, Chen S T. 2014. A high-resolution monsoon record of millennial-scale oscillations during Late MIS 3 from Wulu Cave,south-west China. Journal of Quaternary Science, 29(1): 83-90.

[41] Duan F C, Wang Y J, Liao Z B, Chen S T, Zhang W H, Shao Q F. 2018. Divergent influences of the Greenland and Antarctica climates on the Asian monsoon during a stadial to interstadial cycle. Journal of Asian Earth Sciences,159: 69-73.

[42] Ganopolski A, Rahmstorf S. 2002. Abrupt glacial climate changes due to stochastic resonance. Physical Review Letters, 88(3): 038501.

[43] Gkinis V, Vinther B M, Popp T J, Quistgaard T, Faber A K, Holme C T, Jensen C M, Lanzky M, Lütt A M, Mandrakis V, Ørum N O, Pedersen A S, Vaxevani N, Weng Y B, Capron E, Dahl-Jensen D, Hörhold M, Jones T R, Jouzel J, Landais A, Masson Delmotte V, Oerter H, Rasmussen S O, Steen-Larsen H C, Steffensen J P, Sveinbjörnsdóttir Á E, Svensson A, Vaughn B, White J W C. 2021. A 120,000-year long climate record from a NW-Greenland deep ice core at ultra-high resolution. Scientific Data, 8(1): 141.

[44] Guo F, Clemens S C, Du X, Liu X, Liu Y, Sun J, Fan H, Wang T, Sun Y. 2024. North Atlantic influence on the glacial amplitude of East Asian millennial-scale monsoon variability. Journal of Climate, 37(15): 3903-3915.

[45] Han L Y, Li T Y, Cheng H, Edwards R L, Shen C C, Li H C, Huang C X, Li J Y, Yuan N, Wang H B, Zhang T T, Zhao X. 2016. Potential influence of temperature changes in the Southern Hemisphere on the evolution of the Asian summer monsoon during the last glacial period. Quaternary International,392: 239-250.

[46] Hiess J, Condon D J, McLean N, Noble S R. 2012. ²³⁸U/²³⁵U systematics in terrestrial uranium-bearing minerals. Science, 335(6076): 1610-1614.

[47] Hinnov L A, Schulz M, Yiou P. 2002. Interhemispheric space-time attributes of the Dansgaard-Oeschger oscillations between 100 and 0 ka. Quaternary Science Reviews, 21(10): 1213-1228.

[48] Jaffey A H, Flynn K F, Glendenin L E, Bentley W C, Essling A M. 1971. Precision measurement of half-lives and specific activities of ²³⁵U and ²³⁸U. Physical Review C, 4(5): 1889-1906.

[49] Johnsen S J, Clausen H B, Dansgaard W, Fuhrer K, Gundestrup N, Hammer C U, Iversen P, Jouzel J, Stauffer B, Steffensen J P. 1992. Irregular glacial interstadials recorded in a new Greenland ice core. Nature, 359(6393): 311-313.

[50] Liang Y J, Chen S T, Wang Y J, Zhao K, Yang S H, Wang Z J, Huang Y Z, Cheng H, Edwards R L. 2022. Asian monsoon intensity coupled to Antarctic climate during Dansgaard-Oeschger 8 and Heinrich 4 glacial intervals. Communications Earth & Environment, 3(1): 298.

[51] Liu D B, Wang Y J, Cheng H, Edwards R L, Kong X G, Wang X F, Hardt B, Wu J Y, Chen S T, Jiang X Y, He Y Q, Dong J G, Zhao K. 2010. Sub-millennial variability of Asian monsoon intensity during the early MIS3 and its analogue to the ice age terminations. Quaternary Science Reviews, 29(9): 1107-1115.

[52] Liu Z Y, Wen X Y, Brady E C, Otto-Bliesner B, Yu G, Lu H Y, Cheng H, Wang Y J, Zheng W P, Ding Y H, Edwards R L, Cheng J, Liu W, Yang H. 2014. Chinese cave records and the East Asia Summer Monsoon. Quaternary Science Reviews,83: 115-128.

[53] Lu J Y, Zhang H W, Li H Y, Sha L J, Zhao J Y, Li Y W, Wang J, Dong X Y, Edwards R L, Qian Z, Cheng H. 2021. A 120-year seasonally resolved speleothem record of precipitation seasonality from southeastern China. Quaternary Science Reviews,264: 107023.

[54] McManus J F, Oppo D W, Cullen J L. 1999. A 0.5-million-year record of millennial-scale climate variability in the North Atlantic. Science, 283(5404): 971-975.

[55] North Greenland Ice Core Project members. 2004. High-resolution record of Northern Hemisphere climate extending into the last interglacial period. Nature,431: 147-151.

[56] Qiu W Y, Zhang X, Jiang X Y, Hu H M, Ma L, Xiao H Y, Cai B G, Shen C C. 2022. Double-plunge structure of the East Asian summer monsoon during Heinrich stadial 1 recorded in Xianyun cave,southeastern China. Quaternary Science Reviews,282: 107442.

[57] Qiu W Y, Yang Y Y, Jiang X Y, Wang X F, Wang Y, Cai J R, Liao Y S, Feng T H, Gao K, Zhai S J. 2023. Oxygen isotope variability in precipitation,dripwater,and modern calcite responding to ENSO based on 11 years’ monitoring in Yuhua cave,Southeast China. Journal of Hydrology,624: 129937.

[58] Qiu W Y, Zhang X, Wang X F, He S N, Yuan S F, Che Y P, Cai B G, Jiang X Y. 2024. Synchronous anti-phase variations between the East Asian summer monsoon and South America Summer Monsoon during Heinrich stadial 2. Quaternary Science Reviews,323: 108434.

[59] Rahmstorf S. 2002. Ocean circulation and climate during the past 120,000 years. Nature, 439(6903): 207-214.

[60] Rasmussen S O, Bigler M, Blockley S P, Blunier T, Buchardt S L, Clausen H B, Cvijanovic I, Dahl-Jensen D, Johnsen S J, Fischer H, Gkinis V, Guillevic M, Hoek W Z, Lowe J J, Pedro J B, Popp T, Seierstad I K, Steffensen J P, Svensson A M, Vallelonga P, Vinther B M, Walker M J C, Wheatley J J, Winstrup M. 2014. A stratigraphic framework for abrupt climatic changes during the Last Glacial period based on three synchronized Greenland ice-core records: refining and extending the INTIMATE event stratigraphy. Quaternary Science Reviews,106: 14-28.

[61] Rohling E, Mayewski P, Challenor P. 2003. On the timing and mechanism of millennial-scale climate variability during the last glacial cycle. Climate Dynamics, 20(2): 257-267.

[62] Rohling E J, Liu Q S, Roberts A P, Stanford J D, Rasmussen S O, Langen P L, Siddall M. 2009. Controls on the East Asian monsoon during the last glacial cycle,based on comparison between Hulu Cave and polar ice-core records. Quaternary Science Reviews, 28(27-28): 3291-3302.

[63] Ruan J Y, Zhang H Y, Cai Z Y, Yang X Q, Yin J. 2019. Regional controls on daily to interannual variations of precipitation isotope ratios in Southeast China: implications for paleomonsoon reconstruction. Earth and Planetary Science Letters,527: 115794.

[64] Sachs J P, Lehman S J. 1999. Subtropical north Atlantic temperatures 60,000 to 30,000 years ago. Science, 286(5440): 756-759.

[65] Schneider T, Bischoff T, Haug G H. 2014. Migrations and dynamics of the intertropical convergence zone. Nature, 513(7516): 45-53.

[66] Shen C C, Wu C C, Cheng H, Edwards R L, Hsieh Y T, Gallet S, Chang C C, Li T Y, Lam D D, Kano A, Hori M, Spötl C. 2012. High-precision and high-resolution carbonate ²³⁰Th dating by MC-ICP-MS with SEM protocols. Geochimica et Cosmochimica Acta,99: 71-86.

[67] Sun Y C, Knorr G, Zhang X, Tarasov L, Barker S, Werner M, Lohmann G. 2022. Ice sheet decline and rising atmospheric CO₂ control AMOC sensitivity to deglacial meltwater discharge. Global and Planetary Change,210: 103755.

[68] Sutton R T, McCarthy G D, Robson J, Sinha B, Archibald A T, Gray L J. 2018. Atlantic multidecadal variability and the U.K. ACSIS Program. Bulletin of the American Meteorological Society, 99(2): 415-425.

[69] Tan M. 2014. Circulation effect: response of precipitation δ¹⁸O to the ENSO cycle in monsoon regions of China. Climate Dynamics, 42(3): 1067-1077.

[70] WAIS Divide Project Members. 2015. Precise interpolar phasing of abrupt climate change during the last ice age. Nature,520: 661-665.

[71] Wang Y J, Cheng H, Edwards R L, An Z S, Wu J Y, Shen C C, Dorale J A. 2001. A high-resolution absolute-dated Late Pleistocene monsoon record from Hulu cave,China. Science,294: 2345-2348.

[72] Wang Y J, Cheng H, Edwards R L, He Y Q, Kong X G, An Z S, Wu J Y, Kelly M J, Dykoski C A, Li X D. 2005. The Holocene Asian monsoon: links to solar changes and North Atlantic climate. Science, 308(5723): 854-857.

[73] Willeit M, Ganopolski A, Edwards N R, Rahmstorf S. 2024. Surface buoyancy control of millennial-scale variations in the Atlantic meridional ocean circulation. Climate of the Past, 20(2): 2719-2739.

[74] Wolff E W, Chappellaz J, Blunier T, Rasmussen S O, Svensson A. 2010. Millennial-scale variability during the last glacial: the ice core record. Quaternary Science Reviews, 29(21): 2828-2838.

[75] Wu Y, Li T Y, Yu T L, Shen C C, Chen C J, Zhang J, Li J Y, Wang T, Huang R, Xiao S Y. 2020. Variation of the Asian summer monsoon since the last glacial-interglacial recorded in a stalagmite from southwest China. Quaternary Science Reviews,234: 106261.

[76] Xue F, Wang H J, He J H. 2004. Interannual variability of Mascarene High and Australian High and their influences on East Asian summer monsoon. Journal of the Meteorological Society of Japan,82: 1173-1186.

[77] Yuan D X, Cheng H, Edwards R L, Dykoski C A, Kelly M J, Zhang M L, Qing J M, Lin Y S, Wang Y J, Wu J Y, Dorale J A, An Z S, Cai Y J. 2004. Timing,duration,and transitions of the last interglacial Asian monsoon. Science, 304(5670): 575-578.

[78] Zhang H W, Cheng H, Cai Y J, Spötl C, Kathayat G, Sinha A, Edwards R L, Tan L C. 2018a. Hydroclimatic variations in southeastern China during the 4.2 ka event reflected by stalagmite records. Climate of the Past, 14(1): 1805-1817.

[79] Zhang H W, Cheng H, Spötl C, Cai Y J, Sinha A, Tan L C, Yi L, Yan H, Kathayat G, Ning Y F, Li X L, Zhang F, Zhao J Y, Edwards R L. 2018b. A 200-year annually laminated stalagmite record of precipitation seasonality in southeastern China and its linkages to ENSO and PDO. Scientific Reports, 8(1): 12344.

[80] Zhang H W, Cheng H, Cai Y J, Spötl C, Sinha A, Kathayat G, Li H Y. 2020. Effect of precipitation seasonality on annual oxygen isotopic composition in the area of spring persistent rain in southeastern China and its paleoclimatic implication. Climate of the Past, 16(1): 211-225.

[81] Zhang R, Delworth T L. 2005. Simulated tropical response to a substantial weakening of the Atlantic thermohaline circulation. Journal of Climate, 18(12): 1853-1860.

[82] Zhang R, Sutton R, Danabasoglu G, Kwon Y O, Marsh R, Yeager S G, Amrhein D E, Little C M. 2019. A review of the role of the Atlantic meridional overturning circulation in Atlantic multidecadal variability and associated climate impacts. Reviews of Geophysics, 57(2): 316-375.

[83] Zhang X, Qiu W Y, Jiang X Y, Hu H M, Xiao H Y, Cai B G, Shen C C. 2021. Three-phase structure of the East Asia summer monsoon during Heinrich Stadial 4 recorded in Xianyun Cave,southeastern China. Quaternary Science Reviews,274: 107267.

[84] Zhang X, Qiu W Y, Jiang X Y, Cai B G, Shen C C. 2024. East Asian summer monsoon evolution during Heinrich Stadial 5. Palaeogeography, Palaeoclimatology,Palaeoecology,654: 112467.

基金资助

*国家自然科学基金项目(42377440)