北疆黄土的磁化率各向异性揭示末次冰期以来古风向的变化
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摘要
黄土磁化率各向异性(AMS)被认为是重建古风向变化重要的指标之一,在黄土高原地区得到广泛的应用。然而新疆地区的黄土磁化率各向异性研究相对薄弱。通过对新疆塔城盆地库尔托别剖面磁化率各向异性参数和磁化率分析古风向和风力强度的变化,结果表明:塔城地区末次冰期以来以东南风为主,剖面从下至上,可分为5个阶段:第1阶段(12~14 m):对应MIS3c时期,磁组构特征受水流作用的影响明显,表现为东南风。第2阶段(6~12 m):对应MIS3b时期,出现西南风,但主要还是以东南风为主。第3阶段(4~6 m):对应MIS3a早中期,以东南风为主,西南风逐渐消失,并且风力强度逐渐减弱。第4阶段(0.5~4 m):对应MIS3a晚期和MIS2早期,表现为东南风,风力强度波动较大。第5阶段(0~0.5 m):磁组构特征受成壤作用影响强烈。
As a proxy of paleowind direction,the anisotropy of magnetic susceptibility( AMS) has been widely applied to reconstruct the paleowind history of aeolian loess deposits in Chinese Loess Plateau( CLP). However,fewer attentions have been paid to AMS in Xinjiang loess. In this study,we present AMS results from an aeolian loess section near Tacheng in North Xinjiang,China. Based on magnetic susceptibility and AMS,we discussed variations of paleowind intensity and direction. In general,SE paleowind dominatesin this area since Marine Isotope Stage( MIS) 3. According to magnetic fabric characteristics,we divide the section into five stages of paleowind variations.The stage 1( 12-14 m in depth),corresponding to late MIS3 c,is characterized by reworked aeolian sediment. The stage 2( 6-12 m in depth),corresponding to MIS3 b,is characterized by dominate SE wind with the appearance of SW wind. During MIS3 b,large-scale glaciers in Altay Mountains may cause stronger cold high pressure in the Junggar Basin. Undoubtedly,the pressure gap between Junggar Basin and Tacheng Basin will be enlarged,which will produce stronger SE wind in Tacheng Basin during MIS3 b. Glacier widely developed during MIS3 b in Tianshan can also push cold high pressure to expand to the north and close to Tacheng Basin,which is in favor to form stronger SW wind in Tacheng Basin. The stage 3( 4-6 m in depth),corresponding to early and middle MIS3 a,is characterized by decreasing intensity of wind and disappearing SW wind. Magnetic fabric characteristics is disturbed to some extent. During this stage,temperature increased and glaciers in Tianshan retreated because of gradually increasing high-latitude( 65°N) solar insolation. However,due to particular location,Altay glacier will still keep its larger scale under Mongolia and Siberian high-pressure system. Retreating glacier in Tianshan may cause gradually the disappearing of SW wind in Tacheng Basin. The stage 4( 0. 5-4 m in depth),corresponding to late MIS3 a and early MIS2,is characterized by completely disappeared SE wind and rapid fluctuating intensity of wind. The stage 5( 0-0. 5 m in depth),corresponding to topsoil,is characterized by that the magnetic fabric characteristics is totally disturbed by pedogenesis. Systematical AMS investigation of Tacheng loess will provide a new insight in understanding dust source and mechanisms of climate changes in Tacheng Basin.
As a proxy of paleowind direction,the anisotropy of magnetic susceptibility( AMS) has been widely applied to reconstruct the paleowind history of aeolian loess deposits in Chinese Loess Plateau( CLP). However,fewer attentions have been paid to AMS in Xinjiang loess. In this study,we present AMS results from an aeolian loess section near Tacheng in North Xinjiang,China. Based on magnetic susceptibility and AMS,we discussed variations of paleowind intensity and direction. In general,SE paleowind dominatesin this area since Marine Isotope Stage( MIS) 3. According to magnetic fabric characteristics,we divide the section into five stages of paleowind variations.The stage 1( 12-14 m in depth),corresponding to late MIS3 c,is characterized by reworked aeolian sediment. The stage 2( 6-12 m in depth),corresponding to MIS3 b,is characterized by dominate SE wind with the appearance of SW wind. During MIS3 b,large-scale glaciers in Altay Mountains may cause stronger cold high pressure in the Junggar Basin. Undoubtedly,the pressure gap between Junggar Basin and Tacheng Basin will be enlarged,which will produce stronger SE wind in Tacheng Basin during MIS3 b. Glacier widely developed during MIS3 b in Tianshan can also push cold high pressure to expand to the north and close to Tacheng Basin,which is in favor to form stronger SW wind in Tacheng Basin. The stage 3( 4-6 m in depth),corresponding to early and middle MIS3 a,is characterized by decreasing intensity of wind and disappearing SW wind. Magnetic fabric characteristics is disturbed to some extent. During this stage,temperature increased and glaciers in Tianshan retreated because of gradually increasing high-latitude( 65°N) solar insolation. However,due to particular location,Altay glacier will still keep its larger scale under Mongolia and Siberian high-pressure system. Retreating glacier in Tianshan may cause gradually the disappearing of SW wind in Tacheng Basin. The stage 4( 0. 5-4 m in depth),corresponding to late MIS3 a and early MIS2,is characterized by completely disappeared SE wind and rapid fluctuating intensity of wind. The stage 5( 0-0. 5 m in depth),corresponding to topsoil,is characterized by that the magnetic fabric characteristics is totally disturbed by pedogenesis. Systematical AMS investigation of Tacheng loess will provide a new insight in understanding dust source and mechanisms of climate changes in Tacheng Basin.
引文
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[2]吴海斌,陈发虎,王建民,等.现代风成沉积物磁化率各向异性与风向关系的研究[J].地球物理学报,1998,41(6):811-817.[WU Haibin,CHEN Fahu,WANG Jianmin,et al.A study on the relationship between magnetic anisotropy of modern eolian sediments and wind direction[J].Acta Geophysica Sinica,1998,41(6):811-817.]
[3]ZHU R,LIU Q,JACKSON M J.Paleoenvironmental significance of the magnetic fabrics in Chinese loess-paleosols since the last interglacial(<130 ka)[J].Earth and Planetary Science Letters,2004,221(1-4):55-69.
[4]ZHANG R,KRAVCHINSKY V A,ZHU R,et al.Paleomonsoon route reconstruction along a W-E transect in the Chinese Loess Plateau using the anisotropy of magnetic susceptibility:Summer monsoon model[J].Earth and Planetary Science Letters,2010,299(3-4):436-446.
[5]GONG H,ZHANG R,YUE L,et al.Magnetic fabric from red clay sediments in the Chinese Loess Plateau[J].Scientific Reports,2015,5:9706.
[6]HROUDA F,CHADIMA M,JEZEK J,et al.Anisotropy of out-ofphase magnetic susceptibility of rocks as a tool for direct determination of magnetic subfabrics of some minerals:An introductory study[J].Geophysical Journal International,2017,208(1):385-402.
[7]FRANCE L,SUBIR K B.Paleowind directions from the magnetic fabric of loess profiles in central Alaska[J].Earth and Planetary Science Letters,2002,195:99-112.
[8]XIE X,XIAN F,WU Z,et al.Asian monsoon variation over the late Neogene-early Quaternary recorded by anisotropy of magnetic susceptibility(AMS)from Chinese loess[J].Quaternary International,2016,399:183-189.
[9]DING Z L,RANOV V,YANG S L,et al.The loess record in southern Tajikistan and correlation with Chinese loess[J].Earth and Planetary Science Letters,2002,200:387-400.
[10]MACHALETT B,OCHES E A,FRECHEN M,et al.Aeolian dust dynamics in Central Asia during the Pleistocene:Driven by the long-term migration,seasonality,and permanency of the Asiatic polar front[J].Geochemistry,Geophysics,Geosystems,2008,9(8):1-22.
[11]李冠华,夏敦胜,赵爽,等.新疆塔城地区黄土沉积的磁学特征及其对古环境变化的指示[J].中国沙漠,2012,32(6):1565-1575.[LI Guanhua,XIA Dunsheng,ZHAO Shuang,et al.Magnetic properities and paleoclimatic implication of the loess deposits in Tacheng,northwest China[J].Journal of Desert Research,2012,32(6):1565-1575.]
[12]邓少福,杨太保,秦宏毅,等.新疆塔城黄土古土壤磁化率特征及其影响因素[J].中国沙漠,2011,31(4):848-854.[DENG Shaofu,YANG Taibao,QIN Hongyi,et al.Magnetic susceptibility and its influencing factors from loess-paleosol in Tacheng,Xinjiang,China[J].Journal of Desert Research,2011,31(4):848-854.]
[13]LI G,XIA D,JIN M,et al.Magnetic characteristics of loess-paleosol sequences in Tacheng,northwestern China,and their paleoenvironmental implications[J].Quaternary International,2015,372:87-96.
[14]李新东,马玲霞,张广兴,等.塔额盆地大风、沙尘天气统计特征分析[J].沙漠与绿洲气象,2008,2(6):19-23.[LI Xindong,MA Lingxia,ZHANG Guangxing,et al.Analysis of statistical characteristics on gale and sand-dust weather in Tacheng-Emin Basin[J].Desert and Oasis Meteorology,2018,2(6):19-23.]
[15]叶玮.新疆西风区黄土沉积特征与古气候[M].北京:海洋出版社,2001:1-179.[YE Wei.Loess deposition features and paleoclimate in the westerlies-dominated region of Xinjiang[M].Beijing:Ocean Press,2001:1-179.]
[16]高婧,井立军,井立红,等.新疆塔城地区大风年际振荡及环流背景[J].干旱区地理,2011,34(2):284-291.[GAO Jing,JING Lijun,JING Lihong,et al.Interannual oscillation and circulation features of gale weather in Tacheng Prefecture,Xinjiang[J].Arid Land Geography,2011,34(2):284-291.].
[17]李江风.新疆气候[M].北京:气象出版社,1991:17-18.[LI Jiangfeng.Xinjiang climate[M].Beijing:Meteorological Press,1991:17-18.].
[18]LI Y,SONG Y G,YAN L B,et al.Timing and spatial distribution of loess in Xinjiang,NW China[J].Plos One,2015,10(5):1-16.
[19]JELINEK V.Characterization of the magnetic fabric of rocks[J].Tectonophysics,1981,79(3):T63-T67.
[20]李云.新疆伊犁和塔城黄土记录的末次冰期以来的古气候变化[D].西安:中国科学院地球环境研究所,2014.[LI Yun.Paleoclimatic changes recorded in Tacheng and Ili loess-paleosol sequences in the Xinjiang area since the last glaciation[D].Xi’an:Institute of Earth Environment,Chinese Academy of Sciences,2014.]
[21]SONG Y,SHI Z,FANG X,et al.Loess magnetic properties in the Ili Basin and their correlation with the Chinese Loess Plateau[J].Science China Earth Sciences,2010,53(3):419-431.
[22]HAO Q,OLDFIELD F,BLOEMENDAL J,et al.Hysteresis and thermomagnetic properties of particle-sized fractions from loess and palaeosol samples spanning 22 Myr of accumulation on the Chinese Loess Plateau[J].Geophysical Journal International,2012,191(1):64-77.
[23]HAO Q,OLDFIELD F,BLOEMENDAL J,et al.The magnetic properties of loess and paleosol samples from the Chinese Loess Plateau spanning the last 22 million years[J].Palaeogeography,Palaeoclimatology,Palaeoecology,2008,260(3-4):389-404.
[24]DENG C,SHAW J,LIU Q,et al.Mineral magnetic variation of the Jingbian loess/paleosol sequence in the northern Loess Plateau of China:Implications for Quaternary development of Asian aridification and cooling[J].Earth and Planetary Science Letters,2006,241(1-2):248-259.
[25]LIU X M,HESSE P,ROLPH T,et al.Properties of magnetic mineralogy of Alaskan loess:Evidence for pedogenesis[J].Quaternary International 1999,62:93-102.
[26]ZHU R,KAZANSKY A,MATASOVA G,et al.Rock-magnetic investigation of Siberia loess and its implication[J].Chinese Science Bulletin,2000,45(23):2192-2198.
[27]CHLACHULA J.The Siberian loess record and its significance for reconstruction of Pleistocene climate change in north-central Asia[J].Quaternary Science Reviews,2003,22(18-19):1879-1906.
[28]JIA J,XIA D,WANG B,et al.The investigation of magnetic susceptibility variation mechanism of Tien Mountains modern loess:Pedogenic or wind intensity model?[J].Quaternary International,2013,296:141-148.
[29]LIU Y,SHI Z,DENG C,et al.Mineral magnetic investigation of the Talede loess-palaeosol sequence since the last interglacial in the Yili Basin in the Asian interior[J].Geophysical Journal International,2012,190(1):267-277.
[30]SONG Y,SHI Z,DONG H,et al.Loess magnetic susceptibility in Central Asia and its paleoclimatic significance[C]∥Geoscience and Remote Sensing Symposium,2008,2:1227-1230.
[31]BEGET J E,STONE D B,HAWKINS D B.Paleoclimatic forcing of magnetic susceptibility variations in Alaskan loess during the late Quaternary[J].Geology,1990,18(1):40.
[32]KRAVCHINSKY V A,ZYKINA V S,ZYKIN V S.Magnetic indicator of global paleoclimate cycles in Siberian loess-paleosol sequences[J].Earth and Planetary Science Letters,2008,265(3-4):498-514.
[33]CHLACHULA J,EVANS M E,RUTTER N W.A magnetic investigation of a late Quaternary loess/palaeosol record in Siberia[J].Geophysical Journal International,1998,132(1):128-132.
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