重庆金佛洞石笋δ<sup>13</sup>C记录的Heinrich6期间气候环境变化

组里塞斯; 杨勋林; 王勇; 胡明广; 许奕滨

doi:10.11932/karst2023y008

重庆金佛洞石笋δ¹³C记录的Heinrich6期间气候环境变化

doi: 10.11932/karst2023y008

组里塞斯¹,
杨勋林^{1, 2, 3, ,},
王勇¹,
胡明广¹,
许奕滨¹

1.
西南大学地理科学学院/重庆金佛山喀斯特生态系统国家野外科学观测研究站, 重庆 400715
2.
重庆岩溶环境开放实验室, 重庆 400715
3.
自然资源部岩溶生态环境——重庆南川野外基地, 重庆 400715

基金项目: 国家自然科学基金项目(41971109，41572158)；国家重点研发计划项目(2016YFC0502301)

详细信息

作者简介:
组里塞斯（1996－），女，硕士研究生，研究方向：岩溶记录与全球变化。E-mail:1977166588@qq.com

通讯作者:
杨勋林(1974-)，男，教授，主要从事亚洲季风气候历史重建等研究工作。E-mail：xlyang@swu.edu.cn

中图分类号: P532
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出版历程
- 收稿日期: 2022-06-20
- 网络出版日期: 2023-02-28
- 刊出日期: 2023-06-30

Climatic and environmental changes during Heinrich 6 recorded by δ¹³C in stalagmites from Jinfo Cave, Chongqing

Zulisaisi¹,
YANG Xunlin^{1, 2, 3
, ,},
WANG Yong¹,
HU Mingguang¹,
XU Yibin¹

1.
School of Geographical Sciences, Southwest University / National Observation and Research Station of Karst Ecosystem in Jinfo Mountain of Chongqing, Chongqing 400715, China
2.
Chongqing Key Laboratory of Karst Environment, Chongqing 400715, China
3.
Nanchuan Field Scientific Observation & Research Base of Karst Eco-environment, Ministry of Natural Resources of the People’s Republic of China, Chongqing 400715, China

摘要

摘要: 在末次冰期发生的6次海因里希事件(Heinrich事件,简称H事件)中，H6事件发生年代最早，对其研究较少，利用高分辨率石笋记录研究H6事件期间的气候环境变化，有助于理解高低纬度气候变化对H事件的响应过程。本文基于重庆市金佛洞石笋JF2017铀系测年数据和碳同位素数据，重建H6事件期间中国西南地区季风气候环境的演化过程。结果显示：石笋JF2017的δ¹³C值在61 811±204 a B.P.~59 716±159 a B.P.时段显著偏重，持续大约2 095 a，暗示该时段季风减弱和生态植被退化，对应北大西洋H6事件。H6事件期间，石笋JF2017的δ¹³C记录在61 811~60 848 a B.P.期间开始先逐渐偏重至最大值，随后发生短时间尺度的波动变化；最后在60 848~59 716 a B.P.期间缓慢偏轻至H6事件结束，整体呈现先逐渐偏重后又缓慢偏轻的趋势，内部存在百年际尺度的气候震荡，表明H6事件期间当地气候不稳定。石笋JF2017记录的百年际尺度的季风气候变化可能与热带辐合带和北大西洋经向翻转环流密切相关。
- 亚洲季风 /
- Heinrich 6 /
- 石笋δ¹³C /
- 金佛洞 /
- 中国西南
Abstract: Of the six Heinrich events (H event for short) occurring during the last glacial period, H6 event has been less studied due to its earliest occurrence time. However, using high-resolution stalagmite records to study climate and environmental changes during H6 event can help people understand the response of climate change at high and low latitudes to the H events. In recent years, much progress has been made in terms of studies on paleoclimate and environmental changes with use of stalagmite δ¹³C records. Besides, some stalagmite δ¹³C records have been used to study the climate change of the events on a millennium scale during the last glacial period, but there is no detailed record of the high-resolution climate change in Southwest China during the H6 event. In this case, the JF2017 stalagmite δ¹³C may provide an excellent proxy for exploring the climate and environmental change during H6 event. Based on the dating data of uranium series and carbon isotope data of JF2017 stalagmite in Jinfo Cave, we analyzed the climate significance indicated by stalagmite δ¹³C, and reconstructed the evolution process of the monsoon climate environment in Southwest China during H6 event.Developed from the Jinfo-Yangzi Cave system, Jinfo Cave is located in Jinfo Mountain, Nanchuan district, Chongqing, Southwest China, with an altitude of 2,080 m. The Jinfo Mountain area belongs to subtropical humid monsoon climate, which is jointly affected by the Indian Summer Monsoon and the East Asian Summer Monsoon (ASM). In this study, the age samples of stalagmites were tested by Neptune Plus Multi-receiver Plasma Inductively Coupled Mass Spectrometry (MC-ICP-MS), and the carbon isotopes of stalagmites were tested by Delta-V-Plus gas isotope ratio mass spectrometer and carbonate automatic sampling device Kiel-IV online. The experimental results are based on Vienna Pee Dee Belemnite (V-PDB) with δ¹³C experimental analysis error<0.06 ‰(2σ). According to data analysis, the variation range of stalagmite JF2017 δ¹³C is from -1.44 ‰ to -4.92 ‰, with an average value of -3.40 ‰. JF2017 stalagmite δ¹³C fluctuates significantly, and change amplitude is -3.48 ‰. JF2017 stalagmite δ¹³C records show that the value mainly presents a negative-positive-negative-positive trend during the period of 63,000-58,000 a B.P. Due to the complex influence factors of stalagmite δ¹³C, we compared JF2017 stalagmite δ¹³C records with JFYK7 stalagmite δ¹⁸O records in Yangkou Cave which belongs to the same cave system as Jinfo Cave in order to further analyze the climate significance of stalagmite JF2017 δ¹³C. The comparison indicates a similar variation between the stalagmite stable isotope records of Yangkou Cave and JF2017 stalagmite δ¹³C records. Through previous research, JFYK7 stalagmite δ¹⁸O is indicative of variations in ASM intensity, and the positive shift in stalagmite δ¹⁸O corresponds to weakened ASM. In this study, we observed that the stalagmite JF2017 δ¹³C value was slightly positive, corresponding to the positive JFYK7 stalagmite δ¹⁸O. Therefore, under the background of weakening ASM, JF2017 stalagmite δ¹³C records can reflect the change of ecological environment caused by the change of regional hydrological climate. In addition, the comparison between JF2017 stalagmite and the stalagmites from other caves indicate that JF2017 stalagmite δ¹³C records were comparable with other climate records during H6 event. From 61,811 a B.P.to 60,848 a B.P., the values gradually became heavier, reaching to the maximum, and then fluctuated on a short-time scale. Finally, from 60,848 a B.P. to 59,716 a B.P., they became slightly lighter to the end of H6 event. The comparison between JF2017 stalagmite δ¹³C and other relevant records in the rest of the world shows fluctuations in the stalagmite δ¹³C record, so do the corresponding ITCZ and AMOC.This study shows that the stalagmite JF2017 δ¹³C value was significantly heavier during the 61,811 ± 204 a B.P.-59,716 ± 159 a B.P. period, lasting for about 2,095 a, which may suggest that the monsoon weakened and the ecological vegetation degraded during this period. This result corresponds to the North Atlantic H6 event. During H6 event, stalagmite JF2017 δ¹³C records became heavy to the maximum value during the period of 61,811-60,848 a B.P., followed by the fluctuation change on the short-time scale. During the period of 60,848-59,716 a B.P., the values slowly became lighter to the end of the H6 event. The trend of becoming light after a gradual increase of weight and a climate shock inside on a centennial scale indicate that the local climate was unstable during H6 event. The monsoon climate change on a centennial scale recorded by stalagmite JF2017 may be closely related to the Intertropical Convergence Zone (ITCZ) and the North Atlantic meridional overturning circulation (AMOC).
- Asian monsoon /
- Heinrich 6 /
- stalagmite δ¹³C /
- Jinfo Cave /
- Southwest China

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图 1 重庆金佛洞地理位置示意图(图中黑色五角星指示金佛洞位置)

注：审图号：GS(2020)4619号

Figure 1. Geographical location of Jinfo Cave in Chongqing (Black star indicates the location of Jinfo Cave)

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图 2 石笋JF2017剖面图

注：红色实线表示U-Th 测年采样点。

Figure 2. Profile of stalagmite JF2017

Note: Solid in red indicates U-Th dating sampling point.

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图 3 石笋JF2017年代模型图

注：深蓝色圆点表示U-Th测年点的年代及深度，深蓝色误差棒表示测年误差(±2σ)；红色实线表示年代模型曲线，蓝色实线表示95%的置信界限。

Figure 3. Chronological model of stalagmite JF2017

Note: Dark blue dots indicate the age and depth of the U-Th dating points; error bars in dark blue indicate the dating error (±2σ); solid line in red indicates the chronological model curve; solid line in blue indicates the 95% confidence limit.

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图 4 石笋JF2017 δ¹³C记录

注：深蓝色曲线为该数据20点滑动平滑，黑色虚线为数据平均值，红色误差棒表示测年误差(±2σ)。

Figure 4. δ¹³C records of stalagmite JF2017

Note: Dark blue curve indicates that the record is smoothed using a 20-point running mean; the black dotted line indicates the average value of the data; the error bars in red represent dating errors (±2σ).

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图 5 石笋JF2017的平衡分馏检验

注：(a)深度为70 mm处生长层的δ¹³C和δ¹⁸O；(b) 深度为81 mm处生长层的δ¹³C和δ¹⁸O (红色点线图为δ¹³C；深蓝色点线图为δ¹⁸O)。

Figure 5. Equilibrium fractionation tests of stalagmite JF2017.

Note: (a) δ¹³C and δ¹⁸O values with a depth of 70 mm; (b) δ¹³C and δ¹⁸O values with a depth of 81 mm (red dotted line: δ¹³C; dark blue dotted line: δ¹⁸O.

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图 6 JF2017石笋δ¹³C记录与其他石笋记录对比

注：(a) 金佛洞石笋JF2017 δ¹³C(本研究)；(b) 和(c)羊口洞石笋JFYK7 δ¹⁸O和 δ¹³C^[9]；(d)和(e) 羊子洞石笋YZ1 δ¹⁸O和δ¹³C^[21]；(f)和(g) 永兴洞石笋YX55 δ¹⁸O和δ¹³C^[23]；黄色阴影部分表示H6发生的时间段。

Figure 6. Comparison of JF2017 stalagmite δ¹³C record with other stalagmite records

Note: (a) JF2017 stalagmite δ¹³C in Jinfo Cave; (b) and (c) JFYK7 stalagmites δ¹⁸O and δ¹³C^[9] in Yangkou Cave; (d) and (e) YZ1 stalagmites δ¹⁸O and δ¹³C^[21]in Yangzi Cave; (f) and (g) YX55 stalagmites δ¹⁸O and δ¹³C^[23] in Yongxing Cave; yellow shadow: the time when H6 occurred.

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图 7 JF2017石笋δ¹³C记录与全球其他气候记录对比

注：(a)金佛洞JF2017石笋δ¹³C记录(本研究)； (b)羊口洞JFYK7石笋δ¹⁸O记录^[9] ；(c)65°N夏季太阳辐射^[53]；(d)格陵兰冰芯δ¹⁸O记录^[54]； (e) 北大西洋MD95-2040沉积岩芯SST记录^[55]；(f) 北大西洋KNR191-CDH19沉积岩芯²³¹Pa/²³⁰Th记录(误差棒表示年代误差)^[56]；(g)卡里亚科盆地MD03-2621沉积岩芯反射率记录^[57]；橙色虚线表示H6的开始和结束。

Figure 7. Comparison of JF2017 stalagmite δ¹³C record with other climate records in the rest of world

Note: (a) JF2017 stalagmite δ¹³C in Jinfo Cave; (b) JFYK7 stalagmite δ¹⁸O in Yangkou Cave^[9]; (c) summer solar radiation at 65°N^[53]; (d) ice core δ¹⁸O record in Greenland^[54]; (e) SST record of MD95-2040 sediment core in North Atlantic Ocean^[55] ; (f) ²³¹Pa/²³⁰Th record of KNR191-CDH19 sediment core in North Atlantic Ocean (error bar: age error)^[56]; (g) reflectivity of MD03-2621 sediment core in Cariaco Basin^[57]; dotted line in orange: the beginning and the end of H6.

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表 1 金佛洞石笋JF2017 ²³⁰Th测年结果

Table 1. ²³⁰Th dating results of stalagmite JF2017

样品编号	深度 /mm	²³⁸U /ppb	²³²Th /ppt	d²³⁴U* (measured)	²³⁰Th/²³⁸U (activity)	²³⁰Th Age (a B.P.) (corrected)
JF2017-1	23.0	50 639±100	42±39	−118.1±1.1	0.361 7±0.0010	58 368±235
JF2017-2	28.5	35 390±71	163±41	−120.6±1.1	0.363 7±0.0010	59 050±248
JF2017-3	42.0	52 946±106	2±39	−118.6±1.2	0.365 9±0.0010	59 345±244
JF2017-4	49.0	50 680±59	98±15	−116.1±1.0	0.368 8±0.0006	59 728±159
JF2017-5	61.5	39 643±67	61±33	−113.5±1.1	0.371 6±0.0009	60 076±217
JF2017-6	71.5	38 075±48	182±19	−109.8±1.1	0.376 1±0.0006	60 681±177
JF2017-7	73.5	27 942±57	610±47	−110.5±0.8	0.377 3±0.0011	61 018±261
JF2017-8	88.5	57 510±98	32±31	−119.4±1.1	0.374 6±0.0008	61 339±219
JF2017-9	93.0	34 514±51	383±26	−116.1±1.1	0.378 1±0.0007	61 769±204
JF2017-10	107.5	49 708±94	91±36	−119.5±1.1	0.379 0±0.0010	62 332±248
注：衰变常数取值为λ²³⁰Th=9.157 7×10⁻⁶a⁻¹；λ²³⁴U=2.826 3×10⁻⁶a⁻¹；λ²³⁸U=1.551 25×10⁻¹⁰a⁻¹；δ²³⁴U = ([²³⁴U/²³⁸U]$_ {\rm{activity}}^{-1}$)×10³，δ²³⁴U_初始值是根据²³⁰Th 年龄获得，即δ²³⁴U_初始值=δ²³⁴U_测量值×e^λ234×T；初始²³⁰Th年龄校正采用地壳²³⁰Th/²³²Th平均比值: 4.4×10⁻⁶±2.2×10⁻⁶。 Note: The value of the decay constant is λ²³⁰Th=9.1577×10⁻⁶a⁻¹; λ²³⁴U=2.8263×10⁻⁶a⁻¹; λ²³⁸U=1.55125×10⁻¹⁰a⁻¹; δ²³⁴U = ([²³⁴U/²³⁸U]$_ {\rm{activity}}^{-1}$) x 10³, δ²³⁴U_{initial value} is obtained based on ²³⁰Th age, i.e. δ²³⁴U_{initial value} = δ²³⁴U_{measured value}×e^λ234×T; The initial ²³⁰Th age adjustment was based on the average ratio of ²³⁰Th/²³²Th in the earth's crust: 4.4×10⁻⁶±2.2×10⁻⁶.

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