重庆地区石笋δ~(13)C记录的全新世气候环境变化
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摘要
本文利用重庆市青木关镇狮子洞石笋QM09铀系测年数据和氧碳稳定同位素数据,重建了研究区9.4~0 ka BP的古气候环境演化历史。依据狮子洞石笋δ~(13)C记录变化趋势,将其划分为2个阶段:(1)9.4~3.0 ka BP期间,狮子洞石笋δ~(13)C记录除了在4.2 ka BP附近发生一次短暂的偏重事件外,整体变化比较平缓,石笋δ~(13)C值比较偏轻;同时石笋δ~(18)O值在该期也较为偏轻,暗示了此时段季风强盛,气候温暖湿润,地表植被变化稳定。此时人类活动比较弱,对自然环境的影响小,植被变化主要受自然气候环境的影响;(2)3.0~0 ka BP期间,石笋δ~(13)C记录不再呈现如第一阶段般平稳变动的趋势,在3.0 ka BP时开始波动下降,在经历1.7 ka BP大幅下降后,δ~(13)C便频繁波动大幅升降。石笋δ~(18)O记录显示该时段季风减弱,气候变干,植被退化,土壤水中溶解的CO_2含量减少。加之该期人类活动剧烈,地表自然植被遭到破坏,当地无机环境更多的参与到地下水循环体系中来,使得石笋δ~(13)C逐渐加重。
High-resolution carbon isotope( δ~(13) C) profiles of stalagmites from Shizi Cave in Chongqing Area,China were established with 15 ~(230)Th ages and 315 carbon isotope data,providing a continuous history of the surface vegetation condition for the period of 9. 4-0 thousand years before present(ka BP,relative to AD1950). The δ~(13) C record includes two distinct stages along with the evolution of EASM:( 1) Lush vegetation period( 9. 4 ~ 3 ka BP); during this period,the monsoon climate had been warm and humid,and the vegetation had been luxuriant,with C_3 of surface vegetation cover. In the mid Holocene,δ~(13) C did not show a tendency to follow the trend of δ~(18) O,indicating that although the monsoon weakened,but the absolute humidity of ground surface environment had not changed but had been still suitable for C_3 growth of vegetation. The climate had changed from warm and humid to cold and humid.( 2) Environmental frequently changing period( 3 ~ 0 ka BP); during the late Holocene,the monsoon recorded by the δ~(18) O had been weak further,coupled with the impact of human activities,making the surface environment complex. Especially since 3 ka BP,the correlation between the δ~(13) C record and the content of organic carbon in the section of the Chongqing dam site has been obvious. A "natural profile"and"human site profile"correspond well. The results show that the vegetation types and their coverage have a profound influence on the changes of carbon isotope.
High-resolution carbon isotope( δ~(13) C) profiles of stalagmites from Shizi Cave in Chongqing Area,China were established with 15 ~(230)Th ages and 315 carbon isotope data,providing a continuous history of the surface vegetation condition for the period of 9. 4-0 thousand years before present(ka BP,relative to AD1950). The δ~(13) C record includes two distinct stages along with the evolution of EASM:( 1) Lush vegetation period( 9. 4 ~ 3 ka BP); during this period,the monsoon climate had been warm and humid,and the vegetation had been luxuriant,with C_3 of surface vegetation cover. In the mid Holocene,δ~(13) C did not show a tendency to follow the trend of δ~(18) O,indicating that although the monsoon weakened,but the absolute humidity of ground surface environment had not changed but had been still suitable for C_3 growth of vegetation. The climate had changed from warm and humid to cold and humid.( 2) Environmental frequently changing period( 3 ~ 0 ka BP); during the late Holocene,the monsoon recorded by the δ~(18) O had been weak further,coupled with the impact of human activities,making the surface environment complex. Especially since 3 ka BP,the correlation between the δ~(13) C record and the content of organic carbon in the section of the Chongqing dam site has been obvious. A "natural profile"and"human site profile"correspond well. The results show that the vegetation types and their coverage have a profound influence on the changes of carbon isotope.
引文
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[24]张华生,殷建军,程海,等.全新世早期弱夏季风事件的精确定位及机制探讨-以湖南莲花洞LHD5石笋为例[J].沉积学报,2016,34(2):281-291.
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[27]Maher B A,Thompson R.Oxygen isotopes from Chinese caves:Records not of monsoon rainfall but of circulation regime[J].Journal of Quaternary Science,2012,27(6):615–624.
[28]李廷勇,李红春,袁道先,等.重庆新崖洞XY6石笋4.5ka以来高分辨率δ18O、δ13C记录的气候变化[J].中国岩溶,2006,25(2):95-100.
[29]王绍武.4.2 ka BP事件[J].气候变化研究进展,2010,6(1):75-76.
[30]谭亮成,安芷生,蔡演军,等.4.2 ka BP气候事件在中国的降雨表现及其全球联系[J].地质论评,2008,54(1):94-104.
[31]Cheng Z,Ma C M,Yu S Y,et al.A detailed pollen record of vegetation and climate changes in Central China during the past 16 000 years[J].Boreas,2010,39(1):69-76.
[32]Bond G,Showers W,Cheseby M,et al.A pervasive millennial-scale cycle in North Atlantic Holocene and glacial climates[J].Science,1997,278(5341):1257-1266.
[33]葛倩,刘敬圃,初凤友,等.全新世事件3与古文化变迁[J].地质科技情报,2010,29(3):15-22.
[34]刘浴辉,孙霞,郭彩青.中国全新世4.2ka BP气候事件及其对古文明的影响[J].地质科技情报,2013(1):99-106.
[35]杨勋林,陈发虎,袁道先,等.高分辨率石笋记录的三峡库区小冰期气候变化[J].地理科学,2013,33(5):629-634.
[36]重庆文化遗产保护中心,重庆市文物考古所.重庆考古60年[J].四川文物,2009(6):32-45.
[37]Baldini J U L,Mcdermott F,Baker A,et al.Biomass effects on stalagmite growth and isotope ratios:A 20th century analogue from Wiltshire,England[J].Earth&Planetary Science Letters,2005,240(2):486-494.
[2]Wang Y J,Cheng H,Edwards R L,et al.A high-resolution absolute-dated late Pleistocene monsoon record from Hulu Cave,China[J].Science,2001,294(5550):2345-2348.
[3]Wang Y,Cheng H,Edwards R L,et al.The Holocene Asian monsoon:links to solar changes and North Atlantic climate[J].Science,2005,308(5723):854-857.
[4]Zhang P,Cheng H,Edwards R L,et al.A test of climate,sun,and culture relationships from an 1810-year Chinese cave record[J].science,2008,322(5903):940-942.
[5]Tan L,Cai Y,Cheng H,et al.Climate significance of speleothemδ18O from central China on decadal timescale[J].Journal of Asian Earth Sciences,2015,106:150-155.
[6]Cheng H,Edwards R L,Sinha A,et al.The Asian monsoon over the past 640,000 years and ice age terminations.[J].Nature,2016,534(7609):640-646.
[7]Genty D,Blamart D,Ouahdi R,et al.Precise dating of Dansgaard-Oeschger climate oscillations in western Europe from stalagmite data[J].Nature,2003,421(6925):833.
[8]李廷勇,李红春,向晓晶,等.碳同位素(δ13C)在重庆岩溶地区植被-土壤-基岩-洞穴系统运移特征研究[J].中国科学:地球科学,2012,42(4):526-535.
[9]Cruz F W,Burns S J,Karmann I,et al.A stalagmite record of changes in atmospheric circulation and soil processes in the Brazilian subtropics during the Late Pleistocene[J].Quaternary Science Reviews,2006,25(21-22):2749-2761.
[10]Frisia S,Fairchild I J,Fohlmeister J,et al.Carbon mass-balance modelling and carbon isotope exchange processes in dynamic caves[J].Geochimica Et Cosmochimica Acta,2011,75(2):380-400.
[11]Genty D.Palaeoclimate research in Villars Cave(Dordogne,SW-France)[J].International Journal of Speleology,2008,37(3):3.
[12]高华中,朱诚,孙智彬.三峡库区中坝遗址考古地层土壤有机碳的分布及其与人类活动的关系[J].土壤学报,2005,42(3):518-522.
[13]Baskaran M,Krishnamurthy R V.Speleothems as proxy for the carbon isotope composition of atmospheric CO2[J].Geophysical Research Letters,1993,20(24):2905-2908.
[14]Musgrove M L,Banner J L.Controls on the spatial and temporal variability of vadose dripwater geochemistry:Edwards aquifer,central Texas 1[J].Geochimica et Cosmochimica Acta,2004,68(5):1007-1020.
[15]Baker A,Ito E,Smart P L,et al.Elevated and variable values of13C in speleothems in a British cave system[J].Chemical Geology,1997,136(3–4):263-270.
[16]李玲珑,刘再华.不同植被条件下岩溶地下水δ13CDIC的差异研究-以贵州夜郎洞、天钟洞和普定岩溶水碳通量模拟试验场为例[J].第四纪研究,2015,35(4):913-921.
[17]Marion G M,Introne D S,Van Cleve K.The stable isotope geochemistry of Ca CO3on the Tanana River floodplain of interior Alaska,USA:Composition and mechanisms of formation[J].Chemical Geology:Isotope Geoscience Section,1991,86(2):97-110.
[18]张美良,朱晓燕,林玉石,等.桂林洞穴滴水及现代碳酸钙(Ca CO3)沉积的δ13C记录及其环境意义[J].地球学报,2009,30(5):634-642.
[19]覃嘉铭,袁道先.桂林44ka B.P.石笋同位素记录及其环境解译[J].地球学报,2000,21(4):407-416.
[20]Coplen T B.W inograd I J,Landwehr J M et al.500 000 years stable carbon isotopic record from Devils Hole,N evada[J].Nature,1994,263:3612365.
[21]Zhang H,Cai Y,Tan L,et al.Large variations ofδ13C values in stalagmites from southeastern China during historical times:Implications for anthropogenic deforestation[J].Boreas,2015,44(3):511-525.
[22]梁轩,汪智军,袁道先,等.岩溶区不同植被下土壤水溶解无机碳含量及其稳定δ13C组成特征[J].生态学报,2013,33(10):3031-3038.
[23]莫彬,曹建华,徐祥明,等.岩溶山区不同土地利用方式对土壤活性有机碳动态的影响[J].生态环境学报,2006,15(6):1224-1230.
[24]张华生,殷建军,程海,等.全新世早期弱夏季风事件的精确定位及机制探讨-以湖南莲花洞LHD5石笋为例[J].沉积学报,2016,34(2):281-291.
[25]邵晓华,汪永进,程海,等.全新世季风气候演化与干旱事件的湖北神农架石笋记录[J].科学通报,2006,51(1):80-86.
[26]Dorale J A,Liu Z.Limitations of Hendy Test criteria in judging the paleoclimatic suitability of speleothems and the need for replication[J].Journal of Cave&Karst Studies the National Speleological Society Bulletin,2009,71(1):73-80.
[27]Maher B A,Thompson R.Oxygen isotopes from Chinese caves:Records not of monsoon rainfall but of circulation regime[J].Journal of Quaternary Science,2012,27(6):615–624.
[28]李廷勇,李红春,袁道先,等.重庆新崖洞XY6石笋4.5ka以来高分辨率δ18O、δ13C记录的气候变化[J].中国岩溶,2006,25(2):95-100.
[29]王绍武.4.2 ka BP事件[J].气候变化研究进展,2010,6(1):75-76.
[30]谭亮成,安芷生,蔡演军,等.4.2 ka BP气候事件在中国的降雨表现及其全球联系[J].地质论评,2008,54(1):94-104.
[31]Cheng Z,Ma C M,Yu S Y,et al.A detailed pollen record of vegetation and climate changes in Central China during the past 16 000 years[J].Boreas,2010,39(1):69-76.
[32]Bond G,Showers W,Cheseby M,et al.A pervasive millennial-scale cycle in North Atlantic Holocene and glacial climates[J].Science,1997,278(5341):1257-1266.
[33]葛倩,刘敬圃,初凤友,等.全新世事件3与古文化变迁[J].地质科技情报,2010,29(3):15-22.
[34]刘浴辉,孙霞,郭彩青.中国全新世4.2ka BP气候事件及其对古文明的影响[J].地质科技情报,2013(1):99-106.
[35]杨勋林,陈发虎,袁道先,等.高分辨率石笋记录的三峡库区小冰期气候变化[J].地理科学,2013,33(5):629-634.
[36]重庆文化遗产保护中心,重庆市文物考古所.重庆考古60年[J].四川文物,2009(6):32-45.
[37]Baldini J U L,Mcdermott F,Baker A,et al.Biomass effects on stalagmite growth and isotope ratios:A 20th century analogue from Wiltshire,England[J].Earth&Planetary Science Letters,2005,240(2):486-494.