Luminescence chronology constraints on the sedimentary stratigraphy of the Yangtze River delta since the last interglacial
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摘要:
长江三角洲是我国东部陆架-海岸沉积体系的重要组成部分, 是研究三角洲环境演化和人类活动的理想区域之一。前期大量的研究成果主要聚焦于冰后期和全新世长江三角洲响应海面上升的演进过程, 而冰期-间冰期尺度的长江三角洲地区沉积环境变化的研究因年代学工作薄弱而进展缓慢。本文在近年来对长江三角洲地区晚第四纪沉积物开展一系列石英OSL和钾长石(混合矿物)红外释光(pIRIR)测年研究, 且已取得一定的释光测年数据的基础上, 简要地梳理和总结长江三角洲末次间冰期以来区域沉积环境演化的研究进展, 着重分析晚更新世以来长江三角洲南北两翼沉积地层的年代框架异同、释光年代约束下末次冰期长江古下切河谷的演化历史及成因。释光测年及区域地层对比研究结果表明: 1)氧同位素(MIS)5e阶段(130~120ka)和全新世, 长江三角洲地区沉积环境受海洋作用影响比较明显。2)MIS 3阶段是否存在海侵环境, 不同测年技术得出了不同的年代学结论。且认为14C和常规的石英OSL测年得到的末次冰期早期地层(MIS 3~4)的年龄很可能都存在低估, 而钾长石或混合矿物红外释光测年可以发挥一定的测年优势。这也需要后期继续强化区域地层的年代学测试和对比研究。3)在MIS 4/2阶段, 长江三角洲南北两侧及主体平原均以陆相沉积环境为主。本研究结果可为全球或区域性大河三角洲及海岸系统响应末次间冰期以来海面变化的沉积历史对比研究提供参考。
Abstract:The Yangtze River delta region is a significant section of Chinese coastal-shelf sedimentary system and one ideal place to investigate delta sedimentary evolution and human activities. In past decades, numerous studies have focused on the post-glacial estuary and Holocene delta sedimentary processes in response to rapid sea-level rise. However, there has been limited research work about the sedimentary evolution of the delta on glacial-interglacial timescales. Based on quartz optically stimulated luminescence(OSL)and K-feldspar/polymineral post-infrared(IR)infrared stimulated luminescence(pIRIR)dating of six long sediment cores(JCP01, YZ07, YD006, YD014, EGQD14 and YD016), together with a compilation of regional chronostratigraphy from previous studies, this study explored the sedimentary history of the Yangtze Delta and the sedimentary stratigraphy evolution in this region(31°~34°N, 119°~120°E)since Marine Isotope Stage(MIS)5. In particular, we analyzed the similarities and differences of the sedimentary environments between the southern and northern delta plain as well as possible reasons. Our results showed that two distinct transgressive events around the northern Yangtze River delta plain were recorded in the MIS5 and Holocene stratigraphy, influenced by relatively high sea level at then. However, it seems to have no consistent dating or reliable chronological evidence for the "MIS3 transgression" in the northern Yangtze Delta because both 14C and quartz OSL ages are closed to saturation and thus age underestimation. In contrast, K-feldspar or polymineral pIRIR dating has advantage for sediments dating in this region. Thus, a ca. 130ka terrestrial-marine interaction sedimentary history of the northern Yangtze River coastal plain was achieved. In addition, the complex sedimentary stratigraphy of the paleo-Yangtze incised valley since the last glacial were investigated. We concluded that the basal MIS3 fluvial deposits might represent the earlier infilling over another incised valley, which might be formed during MIS4 although our data have not reached yet. In general, it suggested the sedimentary environments over the Yangtze Delta region were terrestrial environments during the MIS4 and MIS2, in contrast to the MIS5/MIS1marine-influenced deposition and the debatable sedimentary environments in MIS3. This will provide a case for global or regional comparison for delta-coastal sedimentary systems in response to sea-level fluctuations in glacial-interglacial scales.
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Key words:
- Late Quaternary /
- Yangtze River delta /
- sedimentary evolution /
- luminescence chronology
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图 3
(a) JCP01孔石英OSL释光信号生长曲线[32]；(b)JCP01孔石英OSL信号饱和分析[32]；(c)JCP01孔代表性样品红外释光信号恢复比和残余剂量[32]；(d)JCP01孔代表性样品NL-718红外释光信号校正及对应年龄[32]
Figure 3.
(a)Dose response curves of quartz OSL signals from core JCP01[32]; (b)OSL signal saturation of quartz fractions from core JCP01[32]; (c)Dose recovery and residual doses of IRSL signals for samples from core JCP01[32]; (d)Fading correction of pIRIR260 signal from representative sample NL-718 and luminescence age from core JCP01[32]
表 1
本文使用的钻孔岩芯资料来源
Table 1.
Data source of cores used in this study
钻孔名称 纬度(N) 经度(E) 高程(m) 芯长(m) 钻孔岩芯时间序列长度及测年方法 钻孔来源 JCP01 33.2° 120.02° 约3 30.0 约130ka；OSL & pIRIR 文献[32] By1 33.2° 119.37° 约3 30 约39ka；14C 文献[40] LG 约33.3° 约119.5° 4.25 28 约23ka；14C 文献[41] YC01 约33.3° 约119.5° 4.25 33.11 约40ka；14C 文献[41] TZK9 32.6° 120.2° 2 286.86 166ka；14C/OSL 文献[42] CSJA3 约32.62° 约120.13° 约2 74 约70ka；14C/OSL 文献[39] SM 32.54° 121.31° 3.1 60.3 >35 ka；14C 文献[43] QC5 32.33 121.18 3.04 393.8 33ka；14C/TL 文献[44] SR11 32.15° 121.55° 0.00 71.0 45ka；14C 文献[43] YD016 31.77° 121.67° 3.00 78.0 约29ka；OSL 文献[33] YD014 31.83° 121.68° 2.00 75.2 约31ka；OSL 文献[33] YD006 32.0° 121.47° 4.00 68.78 约8.5ka；OSL 文献[33] EGQD14 31.82° 121.68° 2.00 60.0 约53ka；OSL 文献[30] YZ07 32.08° 121.60° 0.00 100.0 约50ka；OSL & pIRIR 文献[31] CM97 31.62° 121.38° 2.48 66.15 约14ka；14C 文献[45] MFC 31.24° 121.46° — 112.0 约116ka；OSL 文献[46] ZK01 31.83° 121.55° 2.05 112.0 约13ka；14C 文献[20] SG7 31.00° 121.95° 2.3 约101 约148ka；OSL/铀系 文献[47] FX 31.20° 121.25° 3.0 102 129ka；OSL 文献[46] HYZ16 30.58° 121.92° -3.6 44 约36.8 ka；14C/OSL 文献[48] QP88 31.08° 120.98° 2.0 105 约134ka；OSL/铀系 文献[47] WJ 31.17° 120.63° 3.0 51.2 约100ka；14C/OSL 文献[47] 
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