High resolution climatic and environmental changes in Shandong Peninsula during the last glacial maximum
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摘要:
末次冰盛期是末次冰期以来地球表面最寒冷的时期。通过对山东半岛地下画廊溶洞石笋DXHL3进行高精度230Th定年和高分辨率氧-碳稳定同位素分析，重建了该地区23.2～18.8 ka时期高分辨率夏季风气候环境变化历史。结果发现，山东半岛末次冰盛期夏季风气候存在显著的千年尺度波动；REDFIT分析表明，氧、碳同位素值均存在显著的2.2 ka周期。末次冰盛期山东半岛总体处于冷干状态，具体又可细分为4个阶段，即冷干（23.2～22 ka）-相对暖湿（22～21 ka）-冷干（21～19 ka）-相对暖湿（19～18.8 ka）。石笋DXHL3的δ18O变化趋势总体上与亚洲季风区内其他石笋记录相似，也与西太平洋暖池婆罗洲的石笋记录类似。这反映了末次冰盛期西太平洋暖池气候环境变化可能对山东半岛的夏季风气候变化产生了重要影响，推测西太平洋暖池表层海水温度变化引起的大气环流和黑潮的变化，是将气候环境变化信号从低纬地区传递到中高纬地区的纽带。
Abstract:The last glacial maximum is the most cold-dry period on the Earth's surface since the last glaciation. We reconstructed high-resolution summer monsoon changes over the Shandong Peninsula during the period of 23.2～18.8 ka using precisely-dated high-resolution oxygen and carbon isotopes (δ18O and δ13C). Results show that the summer monsoon climate in the last glacial maximum in Shandong Peninsula had significant millennial scale fluctuations, and REDFIT analysis shows a significant 2.2 ka cycle in both oxygen and carbon isotopes, which was in a cold-dry state in general, and can be subdivided into four stages, namely, cold and dry (23.2～22 ka), relatively warm and wet (22～21 k), cold and dry (21～19 ka), and relatively warm and wet (21～19 ka). The newly obtained δ18O record is generally similar to other records of stalagmite δ18O from monsoonal China, as well as the stalagmite δ18O records from northern Borneo in the Western Pacific Warm Pool (WPWP). The climate and environment changes in the WPWP might have exerted a substantial impact on summer monsoon climate over the Shandong Peninsula during the last glacial maximum. It is speculated that temperature change at sea surface of WPWP affected the atmospheric circulation and Kuroshio, which should be the main mechanism sending climate and environment signals from low latitude to middle-high latitude zones in the northern hemisphere.
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表 1 石笋DXHL3的U-230Th年代数据
Table 1. U-230Th dating results of stalagmite DXHL3
样品号 深度/mm 238U/10−9 232Th/10−12 实测 δ234U [230Th/238U]活度比 [230Th/232Th]/10−6 未校正年龄/aBP 校正年龄/aBP δ234Ui DXHL-1 3.5 24467±21 2220±8 3015.5±4.5 0.67890±0.00072 123563±448 19774±33 19774±33 3188.8±4.7 DXHL-3 7.0 22657±28 635±22 3147.5±5.5 0.73498±0.00097 432661±14833 20794±42 20794±42 3338.0±5.8 DXHL-4 10.0 19816±26 56±7 3189.6±6.4 0.77094±0.00106 4531392±550191 21654±48 21654±48 3390.9±6.8 DXHL-5 26.5 18180±25 165±16 3120.4±6.8 0.77806±0.00114 1413001±138238 22270±53 22270±53 3323.2±7.2 DXHL-6 31.0 29792±43 128±21 3118.2±8.0 0.78114±0.00124 3004717± 499744 22379±61 22379±61 3321.8±8.6 DXHL-7 59.0 27930±33 323±15 3115.6±6.5 0.78600±0.00099 1120882±50279 22545±49 22545±49 3320.6±6.9 DXHL-8 64.2 24744±32 621±23 3051.2±6.2 0.77506±0.00111 509515±18740 22591±51 22591±51 3252.4±6.6 DXHL-9 90.0 23807±23 66±20 3054.3±4.6 0.77846±0.00116 4609934±1361855 22680±46 22680±46 3256.5±5.0 DXHL-10 111.0 35390±39 293±18 3186.8±5.5 0.80779±0.00136 1609388±97936 22793±53 22793±53 3398.8±5.9 DXHL-2 132.8 31713±32 50±9 3113.7±5.1 0.80362±0.00091 8416357±1550677 23106±42 23106±42 3323.8±5.4 注: λ230=9.1599×10−6 a−1 ；λ234=2.8263×10−6 a−1 ；λ238=1.55125×10−10 a−1 。δ234U=([234U/238U]活度比−1)×1000；234U初始值是根据230Th年龄获得的，即δ234U初始值=δ234U测量值×eλ234×t。校正230Th年龄假设初始的230Th/232Th摩尔比为(4±2)×10−6。 
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