High-resolution climate evolution derived from the sediment records of Erlongwan Maar Lake since 14 ka BP

You, Hongjian; Liu, Jiaqi

doi:10.1007/s11434-012-5244-6

Cited by 20 publications

(8 citation statements)

References 31 publications

(50 reference statements)

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“…1C) offer excellent opportunities for detailed palaeoenvironmental reconstructions 114 with a temporal resolution of few years to several decades and an excellent time control far 115 back into the last glacial (Mingram et al, 2004;Schettler et al, 2006;Stebich et al, 2007 Stebich et al, , 116 2009 Chu et al, 2011Chu et al, , 2014You and Liu, 2012; Li et al, 2013;Zhu et al, 2013; Xu et al, 117 2014). However, interpretation results presented in these publications are not always 118 consistent.…”

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Holocene vegetation and climate dynamics of NE China based on the pollen record from Sihailongwan Maar Lake

Stebich¹,

Rehfeld

Schlütz³

et al. 2015

Quaternary Science Reviews

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The East Asian summer monsoon (EASM) plays a major role in the global climate 63 system (Wang, 2009). In mid-latitude and southern Asia, ecosystems, rain-fed agriculture and 64 economic prosperity critically depend on the amount and distribution of monsoonal 65 precipitation (Yasuda and Shinde, 2004). Therefore, detailed knowledge of the monsoon 66 system variability is essential for understanding global climate processes and is of societal and 67 economic interest, particularly with regard to existing uncertainties in future rainfall 68 projections (Stocker et al., 2013). 69A large number of palaeoenvironmental records have already been generated to better 70 understand the spatio-temporal variability and control mechanisms of the Asian monsoon (e.g. 71 Wang et al., 2010;Cao et al., 2013;Ran and Feng, 2013;An, 2014;Yang et al., 2014). In 72 general, these studies primarily invoke local or regional moisture changes as most indicative 73 of variations in monsoon strength and large-scale circulation patterns. Particularly, oxygen 74 isotope records from speleothems in S/E China have substantially influenced palaeo-monsoon 75 research as they are well dated and widely considered to be high-resolution summer monsoon 76 proxies (e.g., Wang et al., 2005; Liu et al., 2014 suggesting a similar moisture evolution across the monsoon-influenced regions of China 82 (Zhao et al., 2009a; Zhang et al., 2011;Ran and Feng, 2013). 83However, other studies point to much more variability of the summer monsoon in space 84 and time. In particular, towards its northern margin, proxy records reveal region-specific 85 palaeoenvironmental changes, suggesting a complex interplay between the Indian summer 86 monsoon (ISM), the EASM and other major climatic factors, including topography and 87 vegetation (Hu et al., 2003; Maher and Hu, 2006;An et al., 2006;Zhao and Yu, 2012; Ran 88 and Feng, 2013). 89To reveal coherent spatio-temporal patterns of climate evolution in monsoonal Asia and 90 adjacent regions, available proxy data were used for summarizing compilations, over-regional 91 correlations, for constructing 'monsoon/moisture indices' and data-model comparisons (An, 92 2000;Ren and Beug, 2002; Morrill et al., 2003;An et al., 2006;Herzschuh, 2006; Chen et al., 93 2008; Zhao et al., 2009a,b;Cai et al., 2010;Wang et al., 2010; Kleinen et al., 2011; Zhao and 94 Yu, 2012;Cao et al., 2013, Dallmayer et al., 2013 Leipe et al., 2014;Yang et al., 2014). 95However, the regional behaviour of the summer monsoon and its over-regional linkages is far 96 from being well understood. This is reflected in ongoing debates regarding (i) the regional 97 impact of the major atmospheric circulation systems controlling moisture distribution patterns 98 in China (e.g. Clemens et al., 2010;Ran and Feng, 2013), (ii) the phase 99 relationships between these systems (e.g. He et al., 2004;Zhao et al., 2009a; Wang et al., 100 2010;Cai et al., 2010; Clemens et al., 2010; Zhang et al., 2011; Ran and 101 Feng, 2013; Li et al., 2014;Yang et al., 2014),...

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confidence: 99%

“…yr BP (Xu et al, 2014), from alkenone 126 based temperature reconstructions for the past 1600 cal. yr BP (Chu et al, 2011), and from 127 multi-proxy analysis for the entire Holocene (You et al, 2012). However, the reconstructed 128 shifts and short-term events appear not always synchronous and yield different cyclicity 129 patterns.…”

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confidence: 99%

Holocene vegetation and climate dynamics of NE China based on the pollen record from Sihailongwan Maar Lake

Stebich¹,

Rehfeld

Schlütz³

et al. 2015

Quaternary Science Reviews

Self Cite

261

164

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“…For lakes in NEC, this can be explained by the relatively high sediment and C accumulation in the early Holocene. Most of lakes there had an accumulation peak in the late Holocene due to human activities and a subpeak in the early Holocene as a result of warm and wet climate (Liu et al ., , ; You & Liu, ) (Figs S3, S8). For lakes in EP, the sediment and C accumulation did not have an obvious increasing trend may be due to the lack of the early Holocene data, as most of them initiated in the middle or late Holocene (Figs.…”

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confidence: 97%

Carbon accumulation and sequestration of lakes in China during the Holocene

Wang

Chen

et al. 2015

Global Change Biology

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Understanding the responses of lake systems to past climate change and human activity is critical for assessing and predicting the fate of lake carbon (C) in the future. In this study, we synthesized records of the sediment accumulation from 82 lakes and of C sequestration from 58 lakes with direct organic C measurements throughout China. We also identified the controlling factors of the long-term sediment and C accumulation dynamics in these lakes during the past 12 ka (1 ka = 1000 cal yr BP). Our results indicated an overall increasing trend of sediment and C accumulation since 12 ka, with an accumulation peak in the last couple of millennia for lakes in China, corresponding to terrestrial organic matter input due to land-use change. The Holocene lake sediment accumulation rate (SAR) and C accumulation rate (CAR) averaged (mean ± SE) 0.47 ± 0.05 mm yr(-1) and 7.7 ± 1.4 g C m(-2) yr(-1) in China, respectively, comparable to the previous estimates for boreal and temperate regions. The SAR for lakes in the East Plain of subtropical China (1.05 ± 0.28 mm yr(-1) ) was higher than those in other regions (P < 0.05). However, CAR did not vary significantly among regions. Overall, the variability and history of climate and anthropogenic interference regulated the temporal and spatial dynamics of sediment and C sequestration for lakes in China. We estimated the total amount of C burial in lakes of China as 8.0 ± 1.0 Pg C. This first estimation of total C storage and dynamics in lakes of China confirms the importance of lakes in land C budget in monsoon-influenced regions.

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“…Recently, a variety of proxy records has been reported to document climate change in NE China (Chu et al 2009;Hong et al 2005Hong et al , 2009Li et al 2011;Parplies et al 2007;Stebich et al 2009;Wang et al 2012b;You and Liu 2012). These studies mainly focused on the last deglaciation period (Parplies et al 2007;Stebich et al 2009) and the past millennium (Chu et al 2009;Sun et al 2013;Wang et al 2012b), but there are a limited number of Holocene palaeoclimatic records from the NE China (Hong et al 2005(Hong et al , 2009Li et al 2011;You and Liu 2012) that can provide insight into climate change and potential forcing mechanisms. Furthermore, these Holocene palaeoclimatic records display different patterns could be attributed to dating uncertainties, lowresolution and/or climate proxy implications remains uncertain.…”

Section: Introductionmentioning

confidence: 99%

Reconstructing Mid- to Late Holocene East Asian Monsoon Variability in the Jingpo Lake, Northeastern China

Chen

Shen

2015

Earth Surface Processes and Environmental Changes in East Asia

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The Northeastern China involves complex interactions between the East Asian monsoon (EAM) circulation and the polar climate system, and plays a significant role as the bridge communicating low and high latitude climatic processes. High-resolution multi-proxy analysis of a robust AMS 14 C dated lacustrine sediment core recovered from Jingpo Lake in northeastern China provides a detailed history of East Asian monsoon (EAM) variability and vegetation changes during the Midto Late Holocene. The multi-proxy results show that the climate was relatively warm and humid during the period from 5100 to 3600 cal. yr BP, cool and dry between 3600 and 2100 cal. yr BP, and a strengthening of the EAM intensity during the period of 2100 to 150 cal. yr BP. After 150 cal. yr BP, the multi-proxy results reflecting the Jingpo Lake region is affected by intensive human activities. Our findings indicate that variability of the EAM during the Mid-to Late Holocene on multi-decadal to centennial scale are forced by changes in both solar output and oceanic-atmospheric circulations. Furthermore, we have found the evidence that abrupt climate changes coincides with the collapse or the beginning and the chaotically divided of some Chinese dynasties, which will need further research on the relationship between climate and human cultural changes.

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High-resolution climate evolution derived from the sediment records of Erlongwan Maar Lake since 14 ka BP

Cited by 20 publications

References 31 publications

Holocene vegetation and climate dynamics of NE China based on the pollen record from Sihailongwan Maar Lake

Holocene vegetation and climate dynamics of NE China based on the pollen record from Sihailongwan Maar Lake

Carbon accumulation and sequestration of lakes in China during the Holocene

Reconstructing Mid- to Late Holocene East Asian Monsoon Variability in the Jingpo Lake, Northeastern China

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