地球科学进展

地球科学进展 ›› 2025, Vol. 40 ›› Issue (11): 1183 -1195. doi: 10.11867/j.issn.1001-8166.2025.087

研究论文 上一篇    下一篇

渭河盆地河湖相磁化率揭示中布容事件前后季风气候变化与沉积响应
何旭科1,2(), 宋友桂1(), 李越1, 许建红3, 王庆良3   
  1. 1.中国科学院地球环境研究所 黄土科学全国重点实验室，陕西 西安 710061
    2.中国科学院大学 地球与行星科学学院，北京 100049
    3.中国地震局第二监测中心，陕西 西安 710054
  • 收稿日期:2025-08-29 修回日期:2025-10-21 出版日期:2025-11-10
  • 通讯作者: 宋友桂 E-mail:hexuke@chd.edu.cn;syg@ieecas.cn
  • 基金资助:
    国家自然科学基金重大项目(42494911);中国地震局第二监测中心项目(E390020006)

Lacustrine-Fluvial Magnetic Susceptibility Records from the Weihe Basin Reveal Monsoonal Climate Change and Sedimentary Response across the Mid-Brunhes Event

Xuke HE1,2(), Yougui SONG1(), Yue LI1, Jianhong XU3, Qingliang WANG3   

  1. 1.State Key Laboratory of Loess Science, Institute of Earth Environment, Chinese Academy of Sciences, Xi’an 710061, China
    2.College of Earth and Planetary Sciences, University of Chinese Academy of Sciences, Beijing 100049, China
    3.The Second Monitoring and Application Center, China Earthquake Administration, Xi’an 710054, China
  • Received:2025-08-29 Revised:2025-10-21 Online:2025-11-10 Published:2025-12-31
  • Contact: Yougui SONG E-mail:hexuke@chd.edu.cn;syg@ieecas.cn
  • About author:HE Xuke, research areas include sedimentary environment and paleoclimate. E-mail: hexuke@chd.edu.cn
  • Supported by:
    the National Natural Science Foundation of China(42494911);The Second Monitoring and Application Center, China Earthquake Administration(E390020006)
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中布容事件（约430 ka）之后全球冰期—间冰期气候振幅显著增大。为深入研究该事件前后东亚季风气候变率及河湖相沉积演化对东亚季风气候变化的响应，对渭河盆地23GL钻孔记录的过去1.18 Ma以来河湖相—风成相的磁化率变化机理进行了探讨；综合黄土高原古气候记录，研究了MIS 12~10期间钻孔磁化率揭示的东亚夏季风降水变化，并对其进行周期分析。结果表明，浅湖环境中低磁化率与粗碎屑输入较低及成岩过程中强磁性矿物可能发生还原性溶解有关；滨湖环境中磁化率总体升高，且异常高的磁化率峰值与古湖萎缩使得钻孔位置更加接近岸边有关，这导致强磁性粗碎屑颗粒增加；河流沉积物中磁化率波动与不稳定的沉积环境及氧化—还原条件有关。周期分析表明，东亚夏季风降水受岁差主导的夏季日照驱动。MIS 12期间东亚地区发生了2次（451 ka和460 ka）明显的季风降水减少事件；中布容事件前后浅湖—滨湖—河流环境的演化与MIS 12晚期至MIS 9期间季风降水减少、长冰期和较高蒸发的综合作用有关。

关键词: 中布容事件, 渭河盆地, 河湖相, 磁化率, 东亚季风降水, MIS 12

The Mid-Brunhes Event (MBE, ~430 ka) marks a pronounced amplification of global glacial-interglacial climate amplitude and a fundamental reorganization of the Earth system. Palaeoclimatic proxies from the Chinese Loess Plateau indicate that Marine Isotope Stage (MIS) 13a, immediately preceding the MBE, was the warmest and wettest interglacial of the Middle–Late Quaternary in East Asia, whereas global marine and other terrestrial archives consistently identify the post-MBE MIS 11c as the humid and thermally optimal interglacial worldwide. To investigate the variability of the East Asian monsoon climate and the response of fluvial-lacustrine sedimentary sequences to East Asian monsoon climate change across the event, we analyzed the mechanisms governing down-core variations in volumetric magnetic susceptibility (κ, 10-5 SI) preserved in the lacustrine-fluvial-aeolian succession preserved of core 23GL from the Weihe Basin over the past 1.18 Ma. By integrating previously published paleoclimate proxies from the loess-paleosol sequence of the Chinese Loess Plateau, we investigated variations in East Asian Summer Monsoon (EASM) precipitation as recorded by κ during MIS 12~10 and analyzed their orbital periodicities. Results show that the low κ in the shallow-lake setting is related to (i) the low input of coarse debris flux and (ii) possible reductive dissolution of ferrimagnetic minerals during early diagenesis. In the littoral settings, the κ values are systematically higher; exceptional κ peaks coincide with lake-level fall that shifted the depositional site closer to the paleo-shoreline, thereby increasing the flux of ferrimagnetic coarse detritus. In fluvial settings, high-amplitude κ variability is primarily controlled by unstable sedimentary environments and variable oxidation-reduction conditions associated with intermittent subaerial exposure. Within the overlying aeolian sequence, κ clearly defines two intervals: (i) a low-κ interval (~30~12 ka) correlative with the MIS 2 loess sub-layer L1LL1, and (ii) a high-κ paleosol layer S0 (<12 ka) formed during the Holocene. Spectral analysis of the κ series for the 500~320 ka window reveals a statistically significant precession cycle (~20 ka), demonstrating that EASM precipitation is paced by precession-dominated boreal summer insolation. During MIS 12, two pronounced precipitation minima occurred at ~460 ka and ~451 ka across East Asia—expressed in the core as 30- to 50-cm-thick sand beds that coincide with high κ and mean-grain-size values. The transition from shallow-lake to littoral-lake and finally to fluvial settings across the MBE is attributed to the combined effects of (i) the reduced EASM precipitation from late MIS 12 to MIS 9, (ii) the longer glacial stages after the MBE, and (iii) the enhanced evaporation during the extended MIS 11c interglacial.

Key words: Mid-Brunhes Event, Weihe Basin, Fluvial-lacustrine facies, Magnetic susceptibility, East Asian monsoon precipitation, Marine Isotope Stage 12

中图分类号: 

图1 渭河盆地及其邻区地形地貌和大气环流示意图
Fig. 1 Topography and atmospheric circulation of the Weihe Basin and its adjacent regions
图2 23GL钻孔中不同沉积环境的磁化率和平均粒径指标与黄土高原气候—环境代用指标的对比
（a）黄土高原灵台剖面磁化率［29］；（b）靖远剖面黄土碳酸盐δ13CIC［40］；（c）钻孔磁化率；（d）和（e）分别为钻孔平均粒径记录和沉积环境演化序列①。
Fig. 2 Comparison of magnetic susceptibility and mean grain size records of different sedimentary settings in core 23GL with climatic-environmental proxies from the Chinese Loess Plateau
（a） Magnetic susceptibility record of the Lingtai section on the Chinese Loess Plateau （CLP）［29］； （b） δ13CIC record of loess carbonate of the Jingyuan profile from the CLP［40］； （c） Core’s magnetic susceptibility proxy； （d） and （e） Mean grain-size record and sedimentary-environment evolution sequence of the core， respectively①.
图3 MIS 13~11期间23GL钻孔的岩心扫描图像
MIS 12期间2个砂质沉积层（约460 ka和约450 ka）指示2次东亚夏季风降水减少，此时钻孔位置更靠近湖岸。约460 ka的砂层厚约30 cm，约450 ka的砂质沉积层厚约50 cm。
Fig. 3 Photograph of the core 23GL showing the sedimentary sequence deposited during MIS 13~11
The two sandy interbeds （white labels） correspond to two pronounced precipitation-reduction events during Marine Isotope Stage 12 （~460 ka and ~450 ka）， when the borehole site was situated closer to the paleo-lakeshore. The sand layer at ~460 ka is about 30 cm thick， and the sandy deposit at ~450 ka is approximately 50 cm thick.
图4 23GL钻孔粒径和磁化率记录与中国黄土高原气候—环境代用指标的比较
（a）草滩剖面赤铁矿含量［56］；（b）彬县黄土赤铁矿/针铁矿比值［1］；（c）宝鸡剖面基于10Be的降水量重建［57］；（d）靖远剖面黄土平均粒径［40］；（e）驿马关剖面>32 μm的组分含量［58］；（f）靖远剖面黄土碳酸盐δ13CIC［40］；（g）23GL钻孔的磁化率记录；（h）和（i）为23GL钻孔平均粒径记录①；（j）中国南方石笋δ18O合成记录［59］；（k）全球底栖有孔虫δ18O堆叠曲线［3］。深海氧同位素亚阶段的划分依据Railsback等［38］的方案：MIS 12c（478~457 ka），MIS 12b（457~442 ka），MIS 12a（442~424 ka），MIS 11（424~374 ka），MIS 10（374~337 ka），MIS 9（337~300）；MIS 11c为417~396 ka。红色高亮圆圈指示以23GL钻孔年代为基准，MIS 12内部发生的2次气候波动事件。
Fig. 4 Comparison of mean grain size and magnetic susceptibility from the 23GL core with climatic-environmental proxies from the Chinese Loess Plateau
（a） Hematite content from the Caotan section［56］； （b） Hematite/goethite ratio of the Binxian loess［1］； （c） Precipitation reconstruction based on 10Be from the Baoji section［57］； （d） Mean grain-size record of the Jingyuan loess［40］； （e） >32 µm fraction content from the Yimaguan section［58］； （f） δ13CIC record of loess carbonate in the Jingyuan section［40］； （g） Magnetic-susceptibility record from core 23GL； （h） and （i） Linear and logarithmic scale variations of the mean grain-size record from core 23GL， respectively①； （j） Composite speleothem δ18O record from southern China［59］； （k） Stack of global benthic foraminiferal δ18O records［3］. Marine oxygen-isotope substages follow the scheme of Railsback et al.［38］： MIS 12c （478~457 ka）， MIS 12b （457~442 ka）， MIS 12a （442~424 ka）， MIS 11 （424~374 ka）， MIS 10 （374~337 ka）， and MIS 9 （337~300 ka）， with MIS 11c specifically defined as 417~396 ka. Red-highlighted circles denote two intra-MIS 12 climatic oscillations， anchored to the 23GL core chronology.
图5 钻孔磁化率、粒度指标与岁差曲线和中国南方合成石笋δ18O记录的对比
（a）岁差记录［67］；（b）钻孔磁化率记录（橙色）及其拟合曲线（蓝色）；（c）钻孔平均粒径记录；（d）中国南方石笋δ18O合成记录［59］。
Fig. 5 Comparison of magnetic susceptibility， grain size proxies and precession curve with composite stalagmite δ18O record from southern China
（a） Precession record［67］； （b） Magnetic-susceptibility （κ） record from the core （orange） with its fitted curve （blue）； （c） Mean grain-size record from the core； （d） Composite speleothem δ¹⁸O record from southern China［59］.
图6 500~320 ka期间钻孔体积磁化率的小波分析及功率谱分析结果
（a）小波分析结果；（b）功率谱分析。
Fig. 6 The results of wavelet analysis and power spectrum analysis of core magnetic susceptibility during 500~320 ka
（a） Results of wavelet analysis； （b） Results of power spectrum analysis.
图7 中布容事件前后东亚夏季风指标与CO2 浓度的对比
（a）灵台剖面东亚夏季风指数［29］；（b） 靖远剖面黄土磁化率［40］；（c）草滩黄土频率磁化率［56］；（d）南极冰芯CO2浓度记录（品红）［4］和重建的CO2浓度记录（蓝色）［14］；（e）23GL钻孔磁化率。
Fig. 7 Comparison of East Asian summer monsoon proxies with atmospheric CO2 concentrations across the Mid-Brunhes Event
（a） East Asian summer monsoon index from the Lingtai section［29］； （b） Loess magnetic susceptibility from the Jingyuan section［40］； （c） Frequency-dependent magnetic susceptibility of the Caotan loess［56］； （d） Atmospheric CO₂ concentration from Antarctic ice cores （magenta）［4］ and a reconstructed CO₂ record （blue）［14］； （e） Magnetic-susceptibility record from the core 23GL.
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