| Paleoclimate and Environment Evolution |
|
|
|
|
| Differences in the Formation Environment of Loess and Paleosol in Ili Region, Xinjiang, China |
| LI Chuan-xiang1,2, SONG You-gui1 |
1.State Key Laboratory of Loess and Quaternary Geology, Institute of Earth Environment, Chinese Academy of Sciences, Xian 710075, China;
2.Graduate University of Chinese Academy of Sciences,Beijing 100049, China |
|
|
|
|
Abstract Based on grain size and geochemical analysis data, we compared the formation environment of loess and paleosol at the Zhaosu section in Ili, Xinjiang, China. Results indicate that the contents of coarse grain-size of >30 μm, >40 μm and >63 μm at the paleosol layer is higher than that of at the loess layer, especially the >63 μm component. A lot of near source coarse components accumulation in the paleosol layer resulted from the enhanced westerly circulation during the paleosol formation process, which indicated that there was a climate mutation and environmental change in this period. The westerly wind was weak when loess deposited, so the climate change was relatively slight. During the period of paleosol formation, the weathering process was not strong due to an enhanced westerly wind and a cold climate, although the rainfall was much. When loess deposited the precipitation equaled to or less than that during the paleosol formation process, but the weathering pedogenesis was relatively strong because of a warm climate. The combination of water and heat and their different weights in different periods had different impacts on the weathering process of loess and paleosol in Ili.
|
|
Received: 06 April 2012
Published: 20 September 2012
|
|
|
| [1]王永焱,林在贯.中国黄土的结构特征及物理力学性质[M].北京:科学出版社,1990:105.[2]路晶芳,向树元,江尚松,等.西藏日喀则末次冰期风成黄土粒度分析及其意义[J].干旱区资源与环境,2008,22(5):80-85.[3]李徐生,杨达源,鹿化煜.皖南风尘堆积序列氧化物地球化学特征与古气候记录[J].海洋地质与第四纪地质,1999,19(4):75-82.[4]刘志刚,潘保田,邬光剑,等.末次间冰期以来中国西北部沙漠边缘区夏季风变化初步研究[J].中国沙漠,2000,20(4):375-377.[5]强明瑞,李森,金明,等.60 ka来腾格里沙漠东南缘风成沉积与沙漠演化[J].中国沙漠,2000,20(3):256-259.[6]王建民,潘保田.青藏高原东部黄土沉积的基本特征及其环境[J].中国沙漠,1997,17(4):395-400.[7]史正涛,董铭,方小敏.伊犁盆地晚更新世黄土-古土壤磁化率特征[J].兰州大学学报(自然科学版),2007,43(2):8-10.[8]宋友桂,史正涛.伊犁盆地黄土分布和组成特征[J].地理科学,2010,31(2):267-272.[9]宋友桂,史正涛,方小敏,等.伊犁黄土的磁学性质及其与黄土高原对比[J].中国科学(D辑),2010,40(1):61-72.[10]叶玮.新疆伊犁地区自然环境特点与黄土形成条件[J].干旱区地理,1999,22(3):9-16.[11]叶玮.新疆伊犁地区黄土矿物特征与沉积环境[J].干旱区研究,2000,17(4):1-10.[12]叶玮,靳鹤龄.新疆伊犁地区黄土的粒度特征与物质来源[J].干旱区地理,1998,21(4):1-8.[13]叶玮,矢吹真代,赵兴有.中国西风区与季风区黄土沉积特征对比研究[J].干旱区地理,2005,28(6):789-794.[14]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,2001:49-62.[15]Mclennan S M.Weathering and global denudation[J].Journal of Geology,1993,101:295-303.[16]李传想,宋友桂.新疆伊犁黄土磁化率增强机制差异性分析[J].地球学报,2011,32(1):80-86.[17]史正涛,董铭,方小敏.天山黄土和西北内陆干旱化[D].兰州:兰州大学博士学位论文,2002.[18]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.[19]Pye K.Aeolian dust and dust deposit[M].Academic Press,1987:1-56.[20]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.[21]董光荣,叶玮, 袁玉江,等.新疆伊犁地区末次冰期气候的不稳定性[J].科学通报,2000,45(6):641-646.[22]刁桂仪,文启忠.渭南黄土剖面中的稀土元素[J].海洋地质与第四纪地质,2000,20(4):57-62.[23]刘东生.黄土与环境[M].北京:海洋出版社,1985:238-245.[24]杨红瑾,黄春长,庞奖励,等.宁夏长城塬全新世黄土土壤剖面元素地球化学特征研究[J].地理科学,2010,30(1):134-140.[25]张虎才,张林源,Mahaney W C.兰州九州台黄土剖面元素地化学研究[J].地球化学,1991,20(1):79-86.[26]李徐生,韩志勇.镇江下蜀土剖面的化学风化强度与元素迁移特征[J].地理学报,2007,62(11):1174-1184.[27]乔彦松,赵志中,王燕,等.川西甘孜黄土-古土壤序列的地球化学演化特征及其古气候意义[J].科学通报,2010,55(3):255-260.[28]Nesbitt H W,Young G M.Early Proterozoic climates and plate motions inferred from major element chemistry of lutites[J].Nature,1982,299:715-717.[29]文启忠.中国黄土地球化学[M].北京:科学出版社,1989:8-231.[30]李丽.大连地区滨海黄土古环境信息研究[D].辽宁师范大学硕士学位论文,2009.[31]李传想,宋友桂.新疆伊犁黄土化学风化特征及其控制因素[J].高校地质学报,2011,17(4):611-619.[32]庞奖励,张岩青,黄春长,等.宁夏长城塬全新世黄土-古土壤序列微形态特征及意义[J].中国沙漠,2010,30(6):1491-1496.[33]何忠,黄春长,周杰,等.淮河上游全新世黄土及其沉积动力系统研究[J].中国沙漠,2010,30(4):816-823. |
| No Suggested Reading articles found! |
|
|
Viewed |
|
|
|
Full text
|
|
|
|
|
Abstract
|
|
|
|
|
Cited |
|
|
|
|
| |
Shared |
|
|
|
|
| |
Discussed |
|
|
|
|
2012, Vol. 32 
