Holocene Precipitation Change in the Middle and Lower Reaches of the Yangtze River and Its Forcing Mechanisms
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摘要: 为调和不同研究重建的全新世长江中下游地区降水演化之间的矛盾，集成分析了具有年代可靠、指示意义明确的12条全新世长江中游降水记录和18条全新世长江下游降水记录. 结果显示，长江中下游地区降水自全新世伊始逐步增多，中全新世后降水逐渐减少；晚全新世，长江中下游地区降水演化模式出现分异：长江中游整体重新转为湿润，长江下游在波动中趋于干旱. 机制方面，全新世长江中下游地区降水演化总体受控于北半球夏季太阳辐射影响. 晚全新世，ENSO活动显著增强，亚洲西风急流位置偏南，叠加印度夏季风环流异常，不仅导致长江中下游地区降水演化模式偏离北半球夏季太阳辐射变化趋势，也造成长江中游相对于长江下游形成更为湿润的气候.Abstract: In order to reconcile the contradictions among the Holocene precipitation records retrieved from different nature archives in the middle and lower reaches of the Yangtze River (MLRYR), this study analyzed 12 Holocene precipitation records in the middle reaches of the Yangtze River and 18 Holocene precipitation records in the lower reaches of the Yangtze River. The results show that the precipitation in the MLRYR has gradually increased since the onset of the Holocene, and then decreased after the middle Holocene. During the late Holocene, the precipitation evolution pattern in the MLRYR was decoupled: the precipitation in the middle reaches of the Yangtze River increased again, while the precipitation in the lower reaches of the Yangtze River tended to decrease with fluctuations. In terms of mechanisms, the Holocene precipitation evolution in the MLRYR was generally controlled by the Northern Hemisphere summer insolation (NHSI). During the late Holocene, the ENSO activity increased significantly, and the position of the Asian westerly jet was shifted to the south, superimposed on the anomalies of the Indian summer monsoon circulation, which not only led to the deviation of the precipitation pattern in the MLRYR from the variation trend of NHSI, but also resulted in the formation of a more wet climate in the middle reaches of the Yangtze River relative to the lower reaches of the Yangtze River.
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图 1 研究区范围及降水记录位置点
紫色图形表示长江中游降水记录；红色图形表示长江下游降水记录；蓝色轮廓为长江中下游流域边界，数据来源于国家科技基础条件平台-国家地球系统科学数据中心（
http://www.geodata.cn ）；红色虚线表示长江中游与长江下游分界线Fig. 1. Extent of the study area and location points of precipitation records
图 2 长江中下游地区全新世湿润度变化
横坐标0.5代表 1.0~0.0ka BP的时间阶段，1.5代表 2.0~1.0 ka BP的时间阶段，依此类推，11代表 11.7~10.0 ka BP的时间阶段. 每个时间阶段湿润度的误差用标准误差（Standard Error）表示
Fig. 2. Holocene wetness changes in the middle and lower reaches of the Yangtze River
图 3 长江中下游地区全新世湿润期对比
蓝色矩形表示原始文献所指湿润期，红色虚线以下为长江下游降水记录，以上为长江中游降水记录
Fig. 3. Comparison of Holocene wet periods in the middle and lower reaches of the Yangtze River
图 4 长江中游地区湿润度变化与同区域古气候指标对比
a. 大九湖泥炭正构烷烃碳优势指数（He et al.，2015）；b. 大九湖地下水位深度（Liu et al.，2019）；c. 和尚洞石笋中细菌3-羟基脂肪酸重建水文记录（Wang et al.，2018）；d. 长江中游地区湿润度变化（本研究）；记录下方以以区间形式展示记录所用原始年龄数据与误差范围
Fig. 4. Comparison of wetness changes in the middle reaches of the Yangtze River with paleoclimate indicators in the same region
图 5 长江下游地区湿润度变化与同区域古气候指标对比
a. TraCE-21ka模拟的全新世新街钻孔周边区域夏季降水变化（Liu et al.，2009）；b. 长江三角洲YZ07岩芯中值粒径Md（μm）（Wang et al.，2012）；c. 南漪湖钻孔中青冈花粉含量（Chen et al.，2021）；d. 长江下游地区湿润度变化（本研究）. 记录下方以区间形式展示记录所用原始年龄数据与误差范围
Fig. 5. Comparison of wetness changes in the lower reaches of the Yangtze River with paleoclimate indicators in the same region
图 6 长江中下游地区湿润度变化序列与主要驱动机制对比
a. 30°N6月太阳辐射变化（Laskar et al.，2004）；b. 全新世以来北美洲冰盖消融面积百分比（Dyke，2004）；c. Niño 3.4指数反映赤道东太平洋ENSO强度变化（Liu et al.，2014）；d. 长江中游与长江下游湿润度变化时间序列（本研究）
Fig. 6. Comparison of the wetness change sequence and the main forcing mechanism in the middle and lower reaches of the Yangtze River
图 7 晚全新世长江中下游地区降水变化驱动机制示意图
黄色虚线表示亚洲夏季风北界（Chen et al.，2008）；红色虚线表示东亚夏季风与印度夏季风边界；白色箭头表示印度夏季风、东亚夏季风（Xu et al.，2014）和西风急流（Yang et al.，2014）；紫色和灰色区域分别表示ENSO活动增强时西太副高与雨带位置（Liu et al.，2019）
Fig. 7. Schematic diagram of the forcing mechanism of precipitation changes in the middle and lower reaches of the Yangtze River in the Late Holocene
表 1 本研究中使用的降水记录详细信息
Table 1. Details of precipitation records used in this study
地点序号 地点 经度（°E） 纬度（°N） 海拔（m） 地貌类型 时间阶段（ka BP） 测年材料和方法 全新世内年代控制点数量 指标类型 参考文献 1 神农洞、九龙洞 117.250
113.90028.700
27.800383
162山地 14.0~0.0 石笋，230Th 15 562 δ18O和δ13C Zhang et al.(2021a) 2 神农洞 117.250 28.700 383 山地 14.0~0.9 石笋，230Th 48 δ18O和δ13C Zhang et al.(2021c) 3 巢湖 117.375 31.530 5 平原 10.5~2.0 木炭（2）、植物残体（3）、粘土（3）、贝壳（2），AMS14C 10 孢粉 Chen et al.（2009） 4 巢湖 117.394 31.562 5 盆地 10.0~0.0 有机沉积物（7），AMS14C 7 木炭浓度、磁化率 Wu et al.（2019） 5 南漪湖 119.054 31.156 2.2 盆地 11.5~0.0 植物残体（4）、有机沉积物（3），AMS14C 7 地球化学指标 Liu et al.(2021) 6 南漪湖 119.055 31.156 2.3 盆地 9.0~0.0 有机沉积物（5）、木炭（2），AMS14C 6 孢粉 Chen et al.(2021) 7 新街 119.483 31.433 6 平原 12.5~0.0 有机沉积物（5）、木炭（3）、泥炭（2），AMS14C 10 孢粉 Lu et al.(2019) 8 高淳剖面 119.092 31.307 5 平原 13.2~0.0 有机沉积物（11），AMS14C 10 孢粉、木炭浓度、腐殖化程度（DOH）、烧失量（LOI） Yao et al.(2017) 9 长江下游集成a 118.935 31.304 - 平原 10.0~0.0 - - 孢粉 Li et al.(2018) 10 青浦 121.184 31.134 2.67 平原 8.5~0.0 泥炭（3）、贝壳（1）、植物残体（1）有机沉积物（7），AMS14C 12 孢粉、地球化学指标 Tao et al.（2006） 11 卜弋桥b - - 3 平原 11.0~0.0 有机沉积物（5），AMS14C
有机沉积物（1），
传统测年6 孢粉、磁化率、粒度 舒军武等(2007) 12 平望 120.579 30.976 1.31 平原 11.0~0.0 含碳屑沉积物，AMS14C 4 孢粉 李冰等(2018) 13 北湖桥 119.940 30.379 7 平原 11.3~4.2 泥炭（4）、有机沉积物（5）、贝壳（2）、木头（1）、碳酸盐（1），AMS14C 12 粒度、孢粉、地球化学指标 Ye et al.(2018) 14 长江三角洲 119.754
121.38332.307
31.6177.2
2.48平原 13.0~0.0 岩芯（5），210Pb软体动物壳（10），AMS14C 15 粒度、物源 Wang et al.(2013) 15 长江三角洲北部海岸 121.597 32.084 -5 平原 10.3~0.0 石英，OSL 30 孢粉 Ye et al.(2022) 16 长江三角洲
东海大陆架c121.383
121.78231.617
27.7232.48 平原大陆架 10.0~0.0 软体动物壳（12），AMS14C
软体动物壳（8），AMS14C20 粒度、地球化学指标 Bi et al.(2017) 17 长江水下三角洲c 122.383 31.000 - 大陆架 9.5~0.0 腹足类动物（8）、软体动物壳（5）、植物残体（2），AMS14C 15 粒度、地球化学指标 Xu et al.(2020) 18 长江水下三角洲c 122.383 30.717 - 大陆架 13.2~0.0 植物残体（5）、贝壳碎片(5)、木头碎片（1），AMS14C 7 C/N、δ13C Zhan et al.(2012) 19 和尚洞 110.419 30.446 294 山地 9.0~0.0 石笋，U-Th 21 δ13C Li et al.(2014a) 20 和尚洞 110.419 30.446 294 山地 9.0~0.0 石笋，U-Th 21 矿物磁记录 Zhu et al.(2017) 21 大九湖和尚洞 110.003
110.41931.481
30.4461 700
294盆地山地 13.0~0.0 植物残体，AMS14C石笋，U-Th 1221 好氧微生物矿物磁记录 Xie et al.(2013) 22 和尚洞 110.419 30.446 294 山地 9.0~0.0 石笋，U-Th 21 革兰氏阴性细菌3-羟基脂肪酸 Wang et al.(2018) 23 落水洞 109.117 29.733 975 山地 23.5~0.2 石笋，230Th 14 δ18O和δ13C Wang et al.(2022) 24 大九湖 110.003 31.481 1 758 盆地 18.0~1.0 有机沉积物（20），AMS14C 13 δ2H、δ13C、δ18O Huang et al.(2018) 25 大九湖 109.999 31.482 1 758 盆地 13.0~0.0 有机沉积物（20），AMS14C 13 植硅体 Liu et al.(2019) 26 大九湖地区集成 109.996 31.491 1 760 盆地 16.0~0.0 泥炭（10），AMS14C 10 孢粉 Sun et al.(2019( 27 洞庭湖地区集成a 112.956 29.295 20 盆地 10.0~4.0 - - 孢粉 Liu et al.(2012) 28 江西大湖 115.034 24.751 246 盆地 16.5~1.0 有机沉积物，AMS14C 12 矿物磁记录 Wei et al.(2018) 29 江汉平原 112.367 30.184 42.32 平原 12.7~0.0 泥炭(3)、有机沉积物(3)，AMS14C 5 粒度、磁化率、地球化学指标 Li et al.(2014b) 30 江汉平原b - - 28.2 平原 15.0~0.0 有机沉积物（4），AMS14C 4 植硅体 Gu et al.(2012) 注：a. 记录为多个地点集成，具体信息中只显示时间阶段与指标类型, 图 1中地点10以固城湖经纬度表示，地点27以洞庭湖经纬度表示; b. 记录所用钻孔为地质调查项目钻取，具体经纬度不予显示; c. 采样地点位于东海大陆架（水下），海拔不予显示 
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