罗马尼亚Mircea Voda剖面黄土粒度特征及其成因指示
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摘要
Mircea Voda剖面是欧洲典型的黄土剖面之一,本文对Mircea Voda黄土剖面序列S0-S3进行了系统的粒度分析,并与中国黄土高原典型的黄土剖面洛川剖面、西峰剖面等进行了对比研究。结果显示,黄土粒度组成以粒径为4μm-63μm粉砂为主,其平均含量为78. 22%,呈现出风成成因的基本特征,且不同深度样品的粒度组成具有较高的均一性,显示该区黄土具有相同的物质来源。粒度频率曲线呈现为以突出的第一众数20μm～35μm,分选较好的单峰正偏态分布特征,说明粉尘在沉积之前经过了充分的混合。粒级主要组分集中在粗粒端,但在细粒端1μm附近存在第2个分量,这种特征与中国黄土高原黄土的粒度特征十分相似。计算得沉积物环境判别参数Y值均小于-2. 741 1,通过与水成沉积物判别值Y的比较,进一步证实了Mircea Voda剖面黄土为风成成因特征。
The Mircea Voda Loess paleosol sequence is one of the typical loess paleosol sequences in Europe.In the present work,the loess sequence of S0-S3 in Mircea Voda loess is carried out and compared with the typical loess sequence of the Loess Plateau of China,such as the Luochuan loess-paleosol sequence,the Xifeng loess-paleosol sequence. The results show that the main grain size is 4 μm ～ 63 μm,and the average content is 78. 22%,which show the basic characteristics of aeolian origin and the grain sizes of different depth samples are very similar,indicating that the loess has the same source. The grain size frequency curve appears as a prominent mode of 20 μm ～ 35 μm,indicating that the dust has been fully mixed before deposition. The main components of the grain size are concentrated in the coarse grain,but there is a second small mode near the fine grain about 1 μm. This characteristic is very similar to the grain size characteristics of the Loess Plateau in China. The sediment environment discriminant Y value is less than-2. 741 1,and through compare with the water origin sediment discriminant Y value is further confirmed that the Mircea Voda loess is characterized by eolian origin.
The Mircea Voda Loess paleosol sequence is one of the typical loess paleosol sequences in Europe.In the present work,the loess sequence of S0-S3 in Mircea Voda loess is carried out and compared with the typical loess sequence of the Loess Plateau of China,such as the Luochuan loess-paleosol sequence,the Xifeng loess-paleosol sequence. The results show that the main grain size is 4 μm ～ 63 μm,and the average content is 78. 22%,which show the basic characteristics of aeolian origin and the grain sizes of different depth samples are very similar,indicating that the loess has the same source. The grain size frequency curve appears as a prominent mode of 20 μm ～ 35 μm,indicating that the dust has been fully mixed before deposition. The main components of the grain size are concentrated in the coarse grain,but there is a second small mode near the fine grain about 1 μm. This characteristic is very similar to the grain size characteristics of the Loess Plateau in China. The sediment environment discriminant Y value is less than-2. 741 1,and through compare with the water origin sediment discriminant Y value is further confirmed that the Mircea Voda loess is characterized by eolian origin.
引文
[1]郭晖,刘秀铭,吕镔,等.罗马尼亚第四纪黄土沉积的岩石磁学特征及成土模式探讨[J].第四纪研究,2012,32(4):738-748.
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[19] Sun D,Su R,Bloemendal J,et al. Grain-size and accumulation rate records from Late Cenozoic aeolian sequences in northern China:Implications for variations in the East Asian winter monsoon and westerly atmospheric circulation[J]. Palaeogeography Palaeoclimatology Palaeoecology,2008,264(1-2):39-53.
[20] Ulrich H. On the superparamagnetic-stable single domain transition for magnetite,and frequency dependence of susceptibility[J]. Geophysical Journal of the Royal Astronomical Society,2010,133(1):201-206.
[21] Terry J P,Goff J. Megaclasts:Proposed Revised Nomenclature At the Coarse End of the Udden-Wentworth Grain-Size Scale for Sedimentary Particles[J]. Journal of Sedimentary Research,2014,84(3-4):192-197.
[22] Shepard F P. Nomenclature Based on Sand-silt-clay Ratios[J].Journal of sedimentary Research,1954,24(5):151-158.
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[24]叶玮.新疆伊犁地区黄土与黄土状土粒度对比[J].干旱区地理,2000(04):310-314.
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[26] Pye K. Aeolian Dust and Dust Deposits[J]. 1987,25(88):340.
[27]孙东怀.晚新生代黄土高原风尘序列的磁性地层与古气候记录[D].中国科学院研究生院(地球环境研究所),1997.
[28]成都地质学院陕北队.沉积岩(物)粒度分析及其应用[M].北京:地质出版社,1978.
[29]鹿化煜,安芷生.黄土高原红粘土与黄土古土壤粒度特征对比——红粘土风成成因的新证据[J].沉积学报,1999(2):61-67.
[30] Sahu B K. Depositional Mechanisms from the Size Analysis of Clastic Sediments[J]. Journal of Sedimentary Research,1964,34(1):2-24.
[31]李徐生,杨达源,鹿化煜.镇江下蜀黄土粒度特征及其成因初探[J].海洋地质与第四纪地质,2001(1):25-32.
[2] Kukla G J. Pleistocene land—sea correlations I. Europe[J].Earth Science Reviews,1977,13(4):307-374.
[3] Derbyshire E,Kemp R A,Meng X M. Climate change,loess and palaeosols:Proxy measures and resolution in North China[J]. Journal of the Geological Society,1997,154(5):793-805.
[4] Catt J A. Soils as indicators of quaternary climatic change in mid-latitude regions[J]. Geoderma,1991,51(1-4):167-187.
[5] Muhs D R,Benedict J B. Eolian Additions to Late Quaternary Alpine Soils,Indian Peaks Wilderness Area,Colorado Front Range[J]. Arctic Antarctic&Alpine Research,2006,38(1):120-130.
[6] Pye K. The nature,origin and accumulation of loess[J]. Quaternary Science Reviews,1995,14(7-8):653-667.
[7] Porter S C,An Z. Correlation between climate events in the North Atlantic and China during the last glaciation[J]. Nature,1995,375(6529):305-308.
[8] An Z S,Kukla G,Porter S C,et al. Late quaternary dust flow on the chinese Loess Plateau[J]. Catena,1991,18(2):125-132.
[9] Zhisheng A,Kutzbach J E,Prell W L,et al. Evolution of Asian monsoons and phased uplift of the Himalaya-Tibetan plateau since Late Miocene times[J]. Nature,2001,411(6833):62.
[10] Ding Z,Rutter N,Han J,et al. A coupled environmental system formed at about 2. 5 Ma in East Asia[J]. Palaeogeography Palaeoclimatology Palaeoecology,1992,94(1-4):223-242.
[11] Lu H,Liu X,Zhang F,et al. Astronomical calibration of loesspaleosol deposits at Luochuan,central Chinese Loess Plateau[J]. Palaeogeography Palaeoclimatology Palaeoecology,1999,154(3):237-246.
[12]孙东怀,鹿化煜,David Rea,等.中国黄土粒度的双峰分布及其古气候意义[J].沉积学报,2000(3):327-335.
[13] Prins A,Vandenberghe J,Weltje G J. Palaeoclimate signals in loess size distributions[G]. Int. Workshop HWK Delmenhorst April 15-18 2004. From Particle Size to Sediment Dynamics,2004. 123-125.
[14]鹿化煜,安芷生.黄土高原黄土粒度组成的古气候意义[J].中国科学(D辑:地球科学),1998(3):278-283.
[15]鹿化煜,安芷生.洛川黄土粒度组成的古气候意义[J].科学通报,1997(1):66-69.
[16]孙有斌,周杰.风化成壤对原始粉尘粒度组成的改造证据[J].中国沙漠,2002,22(1):16-20.
[17] Wang H,Mason J A,Balsam W L. The importance of both geological and pedological processes in control of grain size and sedimentation rates in Peoria Loess[J]. Geoderma,2006,136(1):388-400.
[18] Xiao J,Porter S C,An Z,et al. Grain Size of Quartz as an Indicator of Winter Monsoon Strength on the Loess Plateau of Central China during the Last 130,000 Yr[J]. Quaternary Research,1995,43(1):22-29.
[19] Sun D,Su R,Bloemendal J,et al. Grain-size and accumulation rate records from Late Cenozoic aeolian sequences in northern China:Implications for variations in the East Asian winter monsoon and westerly atmospheric circulation[J]. Palaeogeography Palaeoclimatology Palaeoecology,2008,264(1-2):39-53.
[20] Ulrich H. On the superparamagnetic-stable single domain transition for magnetite,and frequency dependence of susceptibility[J]. Geophysical Journal of the Royal Astronomical Society,2010,133(1):201-206.
[21] Terry J P,Goff J. Megaclasts:Proposed Revised Nomenclature At the Coarse End of the Udden-Wentworth Grain-Size Scale for Sedimentary Particles[J]. Journal of Sedimentary Research,2014,84(3-4):192-197.
[22] Shepard F P. Nomenclature Based on Sand-silt-clay Ratios[J].Journal of sedimentary Research,1954,24(5):151-158.
[23]刘东生.黄土与环境[M].北京:科学出版社,1985:191-379.
[24]叶玮.新疆伊犁地区黄土与黄土状土粒度对比[J].干旱区地理,2000(04):310-314.
[25]孙东怀.晚新生代黄土高原风尘序列的磁性地层与古气候记录[D].中国科学院研究生院(地球环境研究所),1997.
[26] Pye K. Aeolian Dust and Dust Deposits[J]. 1987,25(88):340.
[27]孙东怀.晚新生代黄土高原风尘序列的磁性地层与古气候记录[D].中国科学院研究生院(地球环境研究所),1997.
[28]成都地质学院陕北队.沉积岩(物)粒度分析及其应用[M].北京:地质出版社,1978.
[29]鹿化煜,安芷生.黄土高原红粘土与黄土古土壤粒度特征对比——红粘土风成成因的新证据[J].沉积学报,1999(2):61-67.
[30] Sahu B K. Depositional Mechanisms from the Size Analysis of Clastic Sediments[J]. Journal of Sedimentary Research,1964,34(1):2-24.
[31]李徐生,杨达源,鹿化煜.镇江下蜀黄土粒度特征及其成因初探[J].海洋地质与第四纪地质,2001(1):25-32.
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