汾渭盆地黄土剖面0.9 Ma前后的粒度突变及其环境意义

摘要/Abstract

摘要： 通过对汾渭盆地老庄黄土剖面的古地磁、磁化率、粒度分析,认为该剖面具有1.2 Ma以来的完整风成沉积系列。该剖面最为显著的特点为其粒度组成中粗粒组分含量较高,自L9（对应年龄约为0.9 Ma）以来粒度突然变粗并且地层中共发育了11层厚度较大的埋藏古风成砂,研究区远离沙漠,黄土中的砂粒及风成砂是近源搬运造成的,其中黄河河漫滩是其砂粒的主要供给源。这一特点显示汾渭盆地在距今0.9 Ma以来气候显著变干,冰期时发生严重土地沙漠化,这可能是汾渭盆地对中更新世气候转型的响应,还可能与当时青藏高原急剧隆升而激发的亚洲内陆干旱化加剧有关。

关键词: 汾渭盆地, 中更新世, 粒度特征, 风成砂, 环境意义

Abstract: The field investigations and the analyses of paleomagnetic polarity reversals, magnetic susceptibility and grain size on Laozhuang section which is on the fifth terrace of the Yellow River in Fenwei basin show that this section contains most of the aeolian stratigraphic units over the past 1.2 Ma. This section contains abundant sand (>63 μm) and the curve of the percentage of the grain size exhibits an abrupt shift around 0.9 Ma. And since then there are several aeolian sand units in loess. Because of far from the desert, the abundant sand ( >63 μm) and the aeolian sand units are caused by the sand from near source. The sand beach of the Yellow River is the main source of sand in loess in Laozhuang section. The abrupt shift recorded in the section around 0.9 Ma possibly responded to the world-wide middle Pleistocene climatic transition event. This transition event may be related to the aggravation of drought in interior Asian triggered by the accelerated uplift of the Tibetan plateau.

Key words: Fenwei basin, middle Pleistocene, grain size, aeolian sand, environmental effect

中图分类号:

P532

褚娜娜;潘保田;王均平;等. 汾渭盆地黄土剖面0.9 Ma前后的粒度突变及其环境意义[J]. 中国沙漠, 2008, 28(1): 50-56.

CHU Na na;PAN Bao tian;WANG Jun ping;et al.. Grain Size Abrupt Shift around 0.9 Ma in Loess and Its Environmental Effect in Fenwei Basin, China[J]. JOURNAL OF DESERT RESEARCH, 2008, 28(1): 50-56.

参考文献

[1]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,1976:90-100.
[2]Rea D K.The paleoclimatic record provided by eolian deposition in the deep sea：the geologic history of wind[J].Rev Geophys,1994,32:159-195.
[3]汪海斌,陈发虎,张家武.黄土高原西部地区黄土粒度的环境指示意义[J].中国沙漠,2002,22（1）：21-26.
[4]赵建华,张强,袁铁,等.沙粒启动机制的理论分析[J].中国沙漠,2005,25（6）：853-862.
[5]董光荣,李森,李保生,等.中国沙漠形成演化的初步研究[J].中国沙漠,1991,11(4):23-32.
[6]董光荣,李保生,高尚玉,等.鄂尔多斯高原的第四纪古风砂[J].地理学报,1983,38（4）：341-346.
[7]董光荣,高尚玉,金炯,等.毛乌素沙漠的形成、演变与成因[J].中国科学:B辑,1988(6)：633-642.
[8]董光荣,靳鹤龄,陈惠忠.末次间冰期以来沙漠黄土边界带移动与气候变化[J].第四纪研究,1997(2)：158-165.
[9]陈惠中,金炯,董光荣.全新世古尔班通古特沙漠演化和气候变化[J].中国沙漠,2001,21(1):333-339.
[10]闫满存,王光谦,董光荣,等.巴丹吉林沙漠沙山发育与环境演变研究[J].中国沙漠,2001,21(4):361-366.
[11]丁仲礼,孙继敏,刘东生.上新世以来毛乌素沙地阶段性扩张的黄土-红粘土沉积证据[J].科学通报,1999,44(3)：324-326.
[12]孙继敏,丁仲礼,刘东生,等.末次间冰期以来沙漠-黄土边界带的环境演变[J].第四纪研究,1995(2)：117-122.
[13]孙继敏,刘东生,丁仲礼,等.五十万年来毛乌素沙漠的变迁[J].第四纪研究,1996(4)：359-365.
[14]Sun J M,Ding Z L.Deposits and soils of the past 130 000 years at the desert-loess transition in northern China[J].Quaternary Research,1998,50：14-156.
[15]熊尚发,丁仲礼,刘东生,等.北京邻区112 Ma以来黄土沉积及其对东部沙漠扩张的指示[J].海洋地质与第四纪地质,1999,19(3)：67-73.
[16]Cande S C,Kent D V.Revised calibration of the geomagnetic polarity timescale for the late Cretaceous and Cenozoic[J].Journal of Geophysical Research,1995,100:603-609.
[17]岳乐平,薛祥熙. 中国黄土古地磁学[M]. 北京：地质出版社,1996: 63-64.
[18]刘秀铭,刘东生,Heller F,等.中国黄土磁化率与第四纪古气候研究[J].地质科学,1992,12（增刊）：279-285.
[19]王均平,潘保田,高红山,等.豫西黄土中砂粒含量及其环境意义[J].中国沙漠,2005,25（5）：629-634.
[20]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,1998,28（3）：278-283.
[21]Ding Z L,Derbyshire E, Yang S L,et al.Stacked 2.6 Ma grain size record from the Chinese loess based on five sections and correlation with the deep sea δ18O record[J].Paleoceanography,2002,17(3)：1-21.
[22]赖内克,辛格.陆源碎屑沉积环境[M]. 陈昌明等译.北京：石油工业出版社,1975:111-123.
[23]闫满存,董光荣,陶贞,等. 腾格里沙漠东南缘晚第三纪古风成砂及其环境[J].中国沙漠,1992,12（3）：10-15.
[24]Pye K,Tsoar H.The mechanics and geological implications of dust transport and deposition in deserts with particular reference to loess formation and dune sand diagnosis in northern Negev,Israel[J].Geological Society Publication,1987,35：139-156.
[25]邬光剑,潘保田,李吉均,等. 祁连山东段 0.83 Ma以来的构造气候事件[J].中国科学:D辑,2001,31(增刊)：202-208.
[26]丁仲礼,孙继敏,刘东生.联系沙漠黄土演变过程中耦合关系的沉积学指标[J].中国科学:D辑,1999,29(1):82-87.
[27]李容全,邱维理,张亚立,等.对黄土高原的新认识[J].北京师范大学学报:自然科学版,2005,41（4）：431-436.
[28]马志正,胡晓猛,李有利.禹门口南黄河东岸沙丘初步研究[J].中国沙漠,1999,19（2）：184-186.
[29]山西省土壤普查办公室.山西土壤[M].北京:科学出版社,1992:166-170.
[30]山西省农业区划委员会.山西省农业自然资源丛书(运城地区卷)[M].北京：中国地图出版社,1992:409-528.
[31]Mudelsee M, Stattegger K.Exploring the structure of the mid-Pleistocene revolution with advanced methods of time-series analysis[J].Geol Rundsch,1997,86:499-511.
[32]Mudelsee M,Schulz M. The Mid-Pleistocene climate transition: onset of 100 ka cycles lags ice volume build-up by 280 ka[J].Earth Planet Sci Lett,1997,151:117-123.
[33]Berger W H,Yasuda M K,Bickert T,et al.Quaternary time scale for the Ontong Java Plateau：Milankovitch template for Ocean Drilling Program Site 806 [J].Geology,1994,22：463-467.
[34]Maasch K A.Statistical detection of the mid-Pleistocene transition[J].Climatic Dynamic,1988,2：133-143.
[35]Ruddiman W F,Raymo M E, Martinson D G,et al.Pleistocene evolution：northern hemisphere ice sheets and North Atlantic Ocean[J].Paleoceanography,1989,4：353-412.
[36]Raymo M E,Oppo D W,Curry W.The mid-Pleistocene climate transition:A deep sea carbon isotope perspective[J]. Paleoceanography,1997,12：546-559.
[37]Wu F L,Fang X M,Ma Y Z,et al.A 1.5 Ma sporo-pollen record of paleoecologic environment evolution in the central Chinese Loess Plateau[J].Chinese Science Bulletin,2004,49(3)：295-301.
[38]方小敏,史正涛,杨胜利,等.天山黄土与古尔班通古特沙漠发育与北疆干旱化[J].科学通报,2002,47(7）：540-545.
[39]方小敏,吕连清,杨胜利,等.昆仑山黄土与中国西部沙漠发育和高原隆升[J].中国科学：D辑,2001,31（3）：177-184.
[40]杨东,方小敏,董光荣,等.1.8 Ma BP以来陇西断岘黄土剖面沉积特征及其反映的腾格里沙漠演化[J].中国沙漠,2006,26（1）：6-13.
[41]朱照宇,丁仲礼,等.中国黄土高原第四纪古气候与新构造演化[M].北京：地质出版社,1994.
[42]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.
[43]崔之久,吴永秋,刘耕年. 关于“昆仑黄河运动”[J] .中国科学:D辑,1998,16(1)：53-69.