410 ka weak monsoon event recorded by stalagmites in Jinfo Cave of Chongqing
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Abstract:
The freshwater discharge from melting ice sheets in the deglaciation or glaciation is prone to anomalies in ocean−atmosphere transport between different latitudes, which can lead to a series of abrupt millennial-scale climate events, either obvious or not, such as the Younger Dryas (YD) events and YD-like events. Marine Isotope Stage 11c (MIS 11c) serves as one of the best references for the current Holocene, and the studies of possible YD-like events and their triggering mechanisms during Holocene are conducive to the understanding of the occurrence pattern of extreme climate events. In this paper, the results of the study on the J33 δ18O sequence records of stalagmites in Jinfo Cave, Chongqing, are shown: (1) Stalagmites in the Asian monsoon climate zone reveal a millennial-scale weak monsoon event that occurred around 410 ka BP prior to the Glacial Maximum of MIS 11 interglacial period. (2) Both the 410 ka weak monsoon event and the YD event occurred during the gradual strengthening of the monsoon and ascending branch of summer insolation in the Northern Hemisphere prior to the Glacial Maximum of interglacial period. This was also a time when Atlantic Meridional Overturning Circulation (AMOC) disturbance occurred. The duration, internal structure, and pattern of the events were similar, with differences in the change magnitude and ice volume conditions. (3) The weak monsoon event that occurred in 410 ka BP was primarily influenced by the combined effects of insolation and AMOC. This event was characterized by a sustained warming process that accelerated the melting of the Greenland ice sheet, leading to the destabilization of this ice sheet. The continuous flowing of freshwater into the North Atlantic resulted in a short-lived AMOC oscillation. The weakening of the AMOC resulted in a cold anomaly over the North Atlantic. As a result of atmospheric telecorrelation, the weaker AMOC led to a weaker Asian Summer Monsoon (ASM)
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Key words:
- Asian Summer Monsoon /
- MIS 11c /
- stalagmite δ18O /
- weak monsoon event /
- Jinfo Cave /
- Southwest China
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Table 1. 230Th date results for stalagmite J33 (‘*’ indicates the new measured data.)
Sample
NumberDepth
(mm)238U
(ppb)232Th
(ppt)230Th / 232Th
(atomic×10−6)δ234U
(measured)230Th / 238U
(activity)Age (ka BP)
(uncorrected)Age (ka BP)
(corrected)δ234UInitial
(corrected)J33-1 144.9 2516.4±0.1 884.9±10.2 72003.1±832.5 424.5±0.3 1.536±0.001 393.5±2.0 393.5±2.0 1288.5±7.5 J33-2 185.7 2875.4±0.1 429.4±10.7 167329.4±4184.0 406.4±0.3 1.516±0.001 400.6±1.5 400.6±1.5 1258.9±5.3 J33-3 196.9 2158.7±0.1 2182.9±11.0 24635.3±127.0 402.8±0.3 1.511±0.002 400.9±3.2 400.9±3.2 1248.6±11.2 J33-4 230.9 3113.8±0.2 1397.6±9.8 55814.2±391.3 406.0±0.3 1.519±0.001 409.4±1.6 409.4±1.6 1288.8±5.9 J33-5 268.7 2791.5±0.2 738.7±28.7 95730.9±3715.6 416.4±0.3 1.536±0.001 415.6±1.6 415.6±1.6 1345.7±6.1 J33-6 301.2 2906.0±0.1 479.0±8.4 154689.1±2718.8 422.2±0.3 1.546±0.001 420.5±1.8 420.5±1.8 1383.2±7.1 J33-7* 306.0 3621.9±8.7 672.0±1.6 137821.0±39.0 425.2±0.3 1.551±0.000 421.1±1.3 421.1±1.3 1395.4±5.3 J33-8* 333.0 3173.3±7.7 607.6±1.5 134437.0±38.0 431.6±0.4 1.561±0.000 425.2±1.5 425.2±1.5 1432.7±6.2 U decay constants: λ238 = 1.55125×10−10[13] and λ234 = 2.82206×10−6[9]. Th decay constant: λ230 = 9.1705×10−6[11]. δ234U = ([234U/238U] activity − 1) ×1000. δ234Uinitial was calculated based on 230Th age (T), i.e., δ234Uinitial = δ234Umeasured×eλ234×T. Corrected 230Th ages assume the initial 230Th/232Th atomic ratio of 4.4±2.2×10−6. Those are the values for a material at secular equilibrium, with the bulk earth 232Th/238U value of 3.8. The errors are arbitrarily assumed to be 50%. "BP" stands for "Before Present" where the "Present" is defined as the year 1950 CE. 
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