丹江谷地晚更新世黄土剖面微量元素地球化学特征研究
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摘要
文中以丹江河谷二级阶地前缘覆盖的黄土剖面为研究对象,研究Mn、Ni、Cu、Ba、La、Rb、Sr 7种微量元素在剖面中的波动特征,并对比黄土高原典型黄土,探讨其蕴含的古气候意义。结果显示:7种微量元素在剖面中的波动特征是气候变化的直接反映;Mn、Ni、Cu、Ba、Rb在古土壤层(S1、S0)出现高值,在黄土层(Lt、L2、L1)出现低值,La、Sr在黄土层(Lt、L2、L1)含量较高,在古土壤(S1、S0)层含量低,微量元素动态变化特征指示古土壤形成时期气候温暖湿润,成壤作用强,黄土堆积时期冬季风为主导,降水较少,成壤作用较弱;其中在马兰黄土形成时期,气候经历了短暂的温暖期;与黄土高原微量元素总体具有较好的相似性,指示两个区域受后期沉积环境影响基本相同,相比较而言,丹江地区的形成环境较黄土高原暖湿,风化成壤作用强于黄土高原地区。
Based on systematic experiment analysis of trace elements including Mn,Ni,Cu,Ba,La,Rb and Sr for Longquancun profile covered by the front edge of the second terrace in the Danjiang River Valley,these characteristics reveal the weathering intensity of Loess-paleosol sequence and its palaeoclimatic significance since late Pleistocene. At the same time,the typical loess on the loess plateau is compared. Results are shown as follows: the fluctuation characteristics of 7 trace elements in the profile are direct reflection of climate change. Mn,Ni,Cu,Ba and Rb have high values in paleosol layer( S1,S0),low values in the loess layer(Lt,L2,L1);However,La and Sr are high in loess layer( Lt,L2,L1),low in paleosol(S1,S0). The environment changes since late Pleistocene have been clearly recorded by the changes in the trace elements in this area. That is,the climate was warm and the pedogenesis was stronger in the period of the palaeosol formation. In the stage of the loess accumulation,the climate was cold and arid,so the weathering pedogenesis was very weak. Among them,during the period of the formation of Malan loess,the climate experienced a short period of warm. The trace elements in the Danjiang region are similar to those in the Loess Plateau,which indicates that the two regions are basically the same under the influence of the late sedimentary environment. The chemical weathering of LQC profile was stronger than that of the loess and paleosol in Luochuan.
Based on systematic experiment analysis of trace elements including Mn,Ni,Cu,Ba,La,Rb and Sr for Longquancun profile covered by the front edge of the second terrace in the Danjiang River Valley,these characteristics reveal the weathering intensity of Loess-paleosol sequence and its palaeoclimatic significance since late Pleistocene. At the same time,the typical loess on the loess plateau is compared. Results are shown as follows: the fluctuation characteristics of 7 trace elements in the profile are direct reflection of climate change. Mn,Ni,Cu,Ba and Rb have high values in paleosol layer( S1,S0),low values in the loess layer(Lt,L2,L1);However,La and Sr are high in loess layer( Lt,L2,L1),low in paleosol(S1,S0). The environment changes since late Pleistocene have been clearly recorded by the changes in the trace elements in this area. That is,the climate was warm and the pedogenesis was stronger in the period of the palaeosol formation. In the stage of the loess accumulation,the climate was cold and arid,so the weathering pedogenesis was very weak. Among them,during the period of the formation of Malan loess,the climate experienced a short period of warm. The trace elements in the Danjiang region are similar to those in the Loess Plateau,which indicates that the two regions are basically the same under the influence of the late sedimentary environment. The chemical weathering of LQC profile was stronger than that of the loess and paleosol in Luochuan.
引文
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[14]赵军,鹿化煜,王晓勇,等.东秦岭地区黄土堆积的岩石磁学特征及磁化率增强机制探索[J].沉积学报,2008,26(6):1052-1062.
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[18]庞奖励,黄春长,周亚利,等.郧县盆地风成黄土-古土壤与汉江I级阶地形成年龄研究[J].地理学报,2015,70(1):63-72.
[19]王恒松,黄春长,周亚利,等.渭河中游全新世黄土剖面光释光测年及记录的古洪水事件[J].地质学报,2012,86(6):994-1004.
[20]庞奖励,黄春长.黄土高原晚更新世黄土与古季风研究进展[J].干旱区地理,1996,19(2):1-8.
[21]聂高众,刘嘉麟,郭正堂.渭南黄土剖面十五万年以来的主要地层界线和气候事件-年代学方面的证据[J].第四纪研究,1996,16(3):221-231.
[22]Liu J Q,Nie G Z,Song C Y,et al. A high resolution time scale for the past 150 000 years at Weinan loess section,Central China[J]. Scientia Geologica Sinica,1995(1):9-22.
[23]陈骏,安芷生,刘连文,等.最近2. 5 Ma以来黄土高原风尘化学组成的变化与亚洲内陆的化学风化[J].中国科学(D辑),2001,31(2):136-145.
[24]Taylor S R,Mclennan S M. The Continental Crust:Its Composition and Evolution[M]. London:Blackwell,1985:277.
[25]李瑜琴.泾河上游全新世黄土-古土壤序列微量元素分布特征及环境变化[J].中国生态农业学报,2009,17(3):416-422.
[26]刁桂仪,文启忠,吴明清,等.黄土中游马兰黄土中若干微量元素的平均含量及相关性研究[J].海洋地质与第四纪地质,1996,16(2):85-92.
[27]陈俊,汪永进,季峻峰,等.陕西洛川黄土剖面的Rb/Sr值及其气候地层学意义[J].第四纪研究,1999,19(4):350-356.
[28]庞奖励,黄春长,张占平.陕西岐山黄土剖面Rb、Sr组成与高分辨率气候变化[J].沉积学报,2001,19(4):637-641.
[29]孙建中.黄土学[M].香港:香港考古学会出版社,2005:171-178.
[30]庞奖励,黄春长,张占平.陕西五里铺黄土微量元素组成与全新世气候不稳定性研究[J].中国沙漠,2001,21(2):151-156.
[2]田均良.黄土高原土壤地球化学[M].北京:科学出版社,1994:42-106.
[3]李传想,宋友桂.西风区末次冰期以来昭苏黄土剖面微量元素分布特征及其环境意义[J].地球环境学报,2014,5(2):56-66.
[4]郭利成,陈秀玲,宋友桂,等.新疆伊犁盆地昭苏黄土剖面稀土元素特征[J].干旱区研究,2013,30(6):1004-1012.
[5]张文翔,史正涛,张虎才,等.中国西风区伊犁盆地塔勒德黄土-古土壤元素地球化学特征及环境意义[J].第四纪研究,2011,31(5):812-821.
[6]文启忠,刁桂仪,余素华.黄河中游地区马兰黄土微量元素分布图[J].地球化学,1986(4):364-374.
[7]刁桂仪,文启忠.第四纪沉积物中的微量元素[J].地质地球化学,1979(5):62-67.
[8]Gallet S,Jahn B M,Torii M. Geochemical characterization of the Luochuan loess-paleosol sequence,China,and paleoclimatic implications[J]. Chemical Geology,1996,133(1-4):67-88.
[9]Yang J D,Chen J,An Z S,et al. Variations in 87Sr/86Sr ratios of calcites in Chinese loess:a proxy for chemical weathering associated with the East Asian summer monsoon[J]. Palaeogeography,Palaeoclimatology,Palaeoecology,2000,157(1-2):151-159.
[10]庞奖励,黄春长,刘安娜,等.黄土高原南部全新世黄土-古土壤序列若干元素分布特征及意义[J].第四纪研究,2007,27(3):357
[11]李艳华,庞奖励,黄春长,等.关中东部全新世黄土-古土壤序列微量元素分布特征及意义[J].土壤通报,2012,43(1):125-130.
[12]贾耀锋,黄春长,庞奖励,等.全新世黄土剖面Li/Ba值变化及其古气候意义[J].第四纪研究,2005,25(6):770-776.
[13]鹿化煜,张红艳,王社江,等.东秦岭南洛河上游黄土地层年代的初步研究及其在旧石器考古中的意义[J].第四纪研究,2007,27(4):559-567.
[14]赵军,鹿化煜,王晓勇,等.东秦岭地区黄土堆积的岩石磁学特征及磁化率增强机制探索[J].沉积学报,2008,26(6):1052-1062.
[15]雷祥义.秦岭黄土-古土壤发育时的植被与环境[J].海洋地质与第四纪地质,2000,20(1):73-79.
[16]雷祥义.商州黄土记录的最近六十万年来东秦岭古环境变迁[J].海洋地质与第四纪地质,1999,19(1):63-73.
[17]王社江,黄培华.洛南盆地旧石器遗址地层划分及年代研究[J].人类学学报,2001,20(3):229-237.
[18]庞奖励,黄春长,周亚利,等.郧县盆地风成黄土-古土壤与汉江I级阶地形成年龄研究[J].地理学报,2015,70(1):63-72.
[19]王恒松,黄春长,周亚利,等.渭河中游全新世黄土剖面光释光测年及记录的古洪水事件[J].地质学报,2012,86(6):994-1004.
[20]庞奖励,黄春长.黄土高原晚更新世黄土与古季风研究进展[J].干旱区地理,1996,19(2):1-8.
[21]聂高众,刘嘉麟,郭正堂.渭南黄土剖面十五万年以来的主要地层界线和气候事件-年代学方面的证据[J].第四纪研究,1996,16(3):221-231.
[22]Liu J Q,Nie G Z,Song C Y,et al. A high resolution time scale for the past 150 000 years at Weinan loess section,Central China[J]. Scientia Geologica Sinica,1995(1):9-22.
[23]陈骏,安芷生,刘连文,等.最近2. 5 Ma以来黄土高原风尘化学组成的变化与亚洲内陆的化学风化[J].中国科学(D辑),2001,31(2):136-145.
[24]Taylor S R,Mclennan S M. The Continental Crust:Its Composition and Evolution[M]. London:Blackwell,1985:277.
[25]李瑜琴.泾河上游全新世黄土-古土壤序列微量元素分布特征及环境变化[J].中国生态农业学报,2009,17(3):416-422.
[26]刁桂仪,文启忠,吴明清,等.黄土中游马兰黄土中若干微量元素的平均含量及相关性研究[J].海洋地质与第四纪地质,1996,16(2):85-92.
[27]陈俊,汪永进,季峻峰,等.陕西洛川黄土剖面的Rb/Sr值及其气候地层学意义[J].第四纪研究,1999,19(4):350-356.
[28]庞奖励,黄春长,张占平.陕西岐山黄土剖面Rb、Sr组成与高分辨率气候变化[J].沉积学报,2001,19(4):637-641.
[29]孙建中.黄土学[M].香港:香港考古学会出版社,2005:171-178.
[30]庞奖励,黄春长,张占平.陕西五里铺黄土微量元素组成与全新世气候不稳定性研究[J].中国沙漠,2001,21(2):151-156.
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