河北白洋淀老河头剖面25.5ka BP以来气候环境变化的沉积记录
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摘要
基于河北省白洋淀地区老河头剖面沉积物的粒度组成与磁化率特征,结合6个AMS14C测年结果,重建了该地区25.5 cal ka BP以来的气候环境变化历史。结果显示,25.5 cal ka BP以来可以划分为7个较大的气候阶段:25.5~20.9cal ka BP(610~515 cm),沉积环境以微弱的流水沉积和风力沉积为主;20.9~10.7 cal ka BP(515~388 cm),该区河流作用减弱,风力堆积加强;10.7~8.6 cal ka BP(388~335 cm),该区降水增加,白洋淀湖泊面积扩大,水位升高;8.6~7.2 cal ka BP(335~299 cm),风力作用加强,以风力堆积为主;7.2~3.2 cal ka BP(299~200 cm),沉积环境以稳定的湖相沉积为主,后期流水作用增强;3.2~1.3 cal ka BP(200~110 cm),该区流水作用显著,有泛滥性的洪水在此期间出现;1.3 cal ka BP至今(110~0 cm)降水减少,但流水作用仍然明显。
Laohetou profile is located in the west of Baiyangdian depression. A 610 centimeter-deep sediment profile was studied in this paper. The AMS14 C measured data revealed that the sediment profile deposited since25. 5 cal ka BP. Combined with chronological data,grain size characteristics,susceptibility and sedimentary characteristics,the evolutionary process and environment features during the past 25. 5cal ka BP were reconstructed. Results showed that there were seven stages as following. 25. 5- 20. 9 cal ka BP( 610- 515 cm) is a fluvial facies and wind accumulation period; in 20. 9- 10. 7 cal ka BP( 515- 388 cm),fluvial action is weakened,and wind accumulation may be strengthened; in 10. 7- 8. 6 cal ka BP( 388- 335 cm),precipitation increases and water accumulates,lakes expanding during this stage; 8. 6- 7. 2 cal ka BP( 335- 299 cm) is a wind accumulation period; 7. 2- 3. 2 cal ka BP( 299- 200 cm) is a lacustrine facies period; 3. 2- 1. 3 cal ka BP( 200- 110 cm) is a fluvial facies period; from 1. 3 cal ka BP to now( 110- 0 cm),the precipitation decreases,but fluvial function is still obvious.
Laohetou profile is located in the west of Baiyangdian depression. A 610 centimeter-deep sediment profile was studied in this paper. The AMS14 C measured data revealed that the sediment profile deposited since25. 5 cal ka BP. Combined with chronological data,grain size characteristics,susceptibility and sedimentary characteristics,the evolutionary process and environment features during the past 25. 5cal ka BP were reconstructed. Results showed that there were seven stages as following. 25. 5- 20. 9 cal ka BP( 610- 515 cm) is a fluvial facies and wind accumulation period; in 20. 9- 10. 7 cal ka BP( 515- 388 cm),fluvial action is weakened,and wind accumulation may be strengthened; in 10. 7- 8. 6 cal ka BP( 388- 335 cm),precipitation increases and water accumulates,lakes expanding during this stage; 8. 6- 7. 2 cal ka BP( 335- 299 cm) is a wind accumulation period; 7. 2- 3. 2 cal ka BP( 299- 200 cm) is a lacustrine facies period; 3. 2- 1. 3 cal ka BP( 200- 110 cm) is a fluvial facies period; from 1. 3 cal ka BP to now( 110- 0 cm),the precipitation decreases,but fluvial function is still obvious.
引文
[1]申洪源,贾玉连,郭峰.内蒙古黄旗海湖泊沉积物磁化率特征及其环境意义[J].干旱区地理,2010,33(2):151-157.
[2]张振克,吴瑞金,王苏民.岱海湖泊沉积物频率磁化率对历史时期环境变化的反映[J].地理研究,1998,17(3):297-302.
[3]吴旭东,沈吉,汪勇.广东湛江湖光岩玛珥湖全新世磁化率变化特征及其环境意义[J].热带地理,2011,31(4):346-352.
[4]李其华.沉积物粒度在古环境重建中的应用[J].巢湖学院学报,2003,5(3):26-28.
[5]Prins M A,Vriend M,Nugteren G,et al.Late Quaternary aeolian dust input variability on the Chinese Loess Plateau:inferences from unmixing of loess grain-size records[J].Quaternary Science Reviews,2007,26(1/2):230-242.
[6]Stuiver M,Grootes P M.GISP2 oxygen isotope ratios[J].Quaternary Research,2000,53(3):277-284.
[7]何乃华,朱宣清.白洋淀地区近3万年来的古环境与历史上人类活动的影响[J].海洋地质与第四纪地质,1992,12(2):79-88.
[8]王会昌.一万年来白洋淀的扩张与收缩[J].地理研究,1983,2(8):8-18.
[9]李月丛,王洪根,张翠莲,等.白洋淀地区古环境变迁与史前文化[J].同济大学学报:社会科学版,2000,11(4):22-27.
[10]段宏振.白洋淀地区史前环境考古初步研究[J].华夏考古,2008,2(1):39-47,152.
[11]河北省地质矿产局.河北省、北京市、天津市区域地质志[M].北京:地质出版社,1989:100-608.
[12]张秀芝,郭海全,李宏亮,等.河北省白洋淀洼地环境地球化学物源判断[J].地学前缘,2008,15(5):90-96.
[13]张静,徐建明,刘海坤,等.华北平原晚更新世以来岩石地层、生物地层及气候地层[J].现代地质,2009,23(1):64-74.
[14]张蕾,张绪教,武法东,等.太行山南缘晚更新世以来河流阶地的发育及其新构造运动意义[J].现代地质,2013,27(4):791-798.
[15]Stuiver M,Reimer P J,Bard E,et al.INTCAL98 Radiocarbon age calibration 24,000-0 cal BP.[J].Radiocarbon,1998,40:1041-1083.
[16]曹玲珑,王建华,王晓静,等.珠江口全新世沉积物粒度与磁化率的变化特征及其所反映的气候环境变化[J].海洋湖沼通报,2012,2(1):167-175.
[17]汪永进,王建,刘金陵.东太湖全新世水下河道沉积特征及环境演变[J].古生物学报,1996,35(2):224-233.
[18]Warrier A K,Shankar R.Geochemical evidence for the use of magnetic susceptibility as a paleorainfall proxy in the tropics[J].Chemical Geology,2009,265(3/4):553-562.
[19]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,1978:44-54.
[20]刘丹.廊坊市第四纪沉积物粒度特征及沉积环境分析[D].北京:中国地质大学,2012:17-26.
[21]付莉莉,冯秀丽,杨旭辉.沉积物粒度参数和频率曲线对粒级划分的响应[J].中国海洋大学学报:自然科学版,2011,41(9):83-89.
[22]冉敬,杜谷,潘忠习.沉积物粒度分析方法的比较[J].岩矿测试,2011,30(6):669-676.
[23]朱筱敏.沉积岩石学[M].第四版.北京:石油工业出版社,2008:73-85.
[24]McM anus J.Grain size determination and interpretation[M]//Tucker M.Techniques in Sedimentology.Oxford:Wiley-Blackwell,1988:63-85.
[25]黄思静.用EXCEL计算沉积物粒度分布参数[J].成都理工学院学报,1999,13(2):98-100.
[26]贾建军,高抒,薛允传.图解法与矩法沉积物粒度参数的对比[J].海洋与湖沼,2002,13(6):577-582.
[27]姚杜琳,王永,迟振卿,等.内蒙古东乌珠穆沁旗乌拉盖高毕湖泊沉积记录的5万年来环境演变[J].湖泊科学,2012,24(6):965-973.
[28]蒋庆丰,刘兴起,沈吉.乌伦古湖沉积物粒度特征及其古气候环境意义[J].沉积学报,2006,22(6):877-882.
[29]金秉福.粒度分析中偏度系数的影响因素及其意义[J].海洋科学,2012,36(2):129-135.
[30]陈冬梅,穆桂金.不同沉积环境下沉积物的粒度分形特征的对比研究[J].干旱区地理,2004,27(1):47-51.
[31]Sun D,Bloemendal J,Rea D K,et al.Grain-size distribution function of polymodal sediments in hydraulic and aeolian environments,and numerical partitioning of the sedimentary components[J].Sedimentary Geology,2002,152(3):263-277.
[32]张平,宋春晖,杨用彪,等.稳定湖相沉积物和风成黄土粒度判别函数的建立及其意义[J].沉积学报,2008,26(3):501-507.
[33]王会昌.一万年来白洋淀的扩张与收缩[J].地理研究,1983,2(8):8-18.
[34]林景星,张静,林防,等.西太平洋暖池扩张对华北平原气候变化的影响:华北平原4万年以来升温事件的新证据[J].地球学报,1998,19(4):18-21.
[35]Qin X.Loess record of the aerodynamic environment in the east Asia monsoon area since 60,000 years before present[J].Journal of Geophysical Research,2005,110(B1):1204.
[36]Zhou W,Yu X,Jull A J T,et al.High-resolution evidence from southern China of an early Holocene optimum and a mid-Holocene dry event during the past 18,000 years[J].Quaternary Research,2004,62(1):39-48.
[37]邵晓华,汪永进,程海,等.全新世季风气候演化与干旱事件的湖北神农架石笋记录[J].科学通报,2006,51(1):80-86.
[38]郭书元,詹伟,王强.河北省白洋淀地区中全新世丽蚌动物群及其生态环境意义[J].古地理学报,2014,16(3):335-346.
[39]吴忱,魏福利.华北地区晚全新世初期环境变化分析[J].地理与地理信息科学,2003,19(2):97-101.
[40]吴忱,朱宣清,何乃华,等.华北平原古河道研究[M].北京:中国科学技术出版社,1991:169-184.
[2]张振克,吴瑞金,王苏民.岱海湖泊沉积物频率磁化率对历史时期环境变化的反映[J].地理研究,1998,17(3):297-302.
[3]吴旭东,沈吉,汪勇.广东湛江湖光岩玛珥湖全新世磁化率变化特征及其环境意义[J].热带地理,2011,31(4):346-352.
[4]李其华.沉积物粒度在古环境重建中的应用[J].巢湖学院学报,2003,5(3):26-28.
[5]Prins M A,Vriend M,Nugteren G,et al.Late Quaternary aeolian dust input variability on the Chinese Loess Plateau:inferences from unmixing of loess grain-size records[J].Quaternary Science Reviews,2007,26(1/2):230-242.
[6]Stuiver M,Grootes P M.GISP2 oxygen isotope ratios[J].Quaternary Research,2000,53(3):277-284.
[7]何乃华,朱宣清.白洋淀地区近3万年来的古环境与历史上人类活动的影响[J].海洋地质与第四纪地质,1992,12(2):79-88.
[8]王会昌.一万年来白洋淀的扩张与收缩[J].地理研究,1983,2(8):8-18.
[9]李月丛,王洪根,张翠莲,等.白洋淀地区古环境变迁与史前文化[J].同济大学学报:社会科学版,2000,11(4):22-27.
[10]段宏振.白洋淀地区史前环境考古初步研究[J].华夏考古,2008,2(1):39-47,152.
[11]河北省地质矿产局.河北省、北京市、天津市区域地质志[M].北京:地质出版社,1989:100-608.
[12]张秀芝,郭海全,李宏亮,等.河北省白洋淀洼地环境地球化学物源判断[J].地学前缘,2008,15(5):90-96.
[13]张静,徐建明,刘海坤,等.华北平原晚更新世以来岩石地层、生物地层及气候地层[J].现代地质,2009,23(1):64-74.
[14]张蕾,张绪教,武法东,等.太行山南缘晚更新世以来河流阶地的发育及其新构造运动意义[J].现代地质,2013,27(4):791-798.
[15]Stuiver M,Reimer P J,Bard E,et al.INTCAL98 Radiocarbon age calibration 24,000-0 cal BP.[J].Radiocarbon,1998,40:1041-1083.
[16]曹玲珑,王建华,王晓静,等.珠江口全新世沉积物粒度与磁化率的变化特征及其所反映的气候环境变化[J].海洋湖沼通报,2012,2(1):167-175.
[17]汪永进,王建,刘金陵.东太湖全新世水下河道沉积特征及环境演变[J].古生物学报,1996,35(2):224-233.
[18]Warrier A K,Shankar R.Geochemical evidence for the use of magnetic susceptibility as a paleorainfall proxy in the tropics[J].Chemical Geology,2009,265(3/4):553-562.
[19]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,1978:44-54.
[20]刘丹.廊坊市第四纪沉积物粒度特征及沉积环境分析[D].北京:中国地质大学,2012:17-26.
[21]付莉莉,冯秀丽,杨旭辉.沉积物粒度参数和频率曲线对粒级划分的响应[J].中国海洋大学学报:自然科学版,2011,41(9):83-89.
[22]冉敬,杜谷,潘忠习.沉积物粒度分析方法的比较[J].岩矿测试,2011,30(6):669-676.
[23]朱筱敏.沉积岩石学[M].第四版.北京:石油工业出版社,2008:73-85.
[24]McM anus J.Grain size determination and interpretation[M]//Tucker M.Techniques in Sedimentology.Oxford:Wiley-Blackwell,1988:63-85.
[25]黄思静.用EXCEL计算沉积物粒度分布参数[J].成都理工学院学报,1999,13(2):98-100.
[26]贾建军,高抒,薛允传.图解法与矩法沉积物粒度参数的对比[J].海洋与湖沼,2002,13(6):577-582.
[27]姚杜琳,王永,迟振卿,等.内蒙古东乌珠穆沁旗乌拉盖高毕湖泊沉积记录的5万年来环境演变[J].湖泊科学,2012,24(6):965-973.
[28]蒋庆丰,刘兴起,沈吉.乌伦古湖沉积物粒度特征及其古气候环境意义[J].沉积学报,2006,22(6):877-882.
[29]金秉福.粒度分析中偏度系数的影响因素及其意义[J].海洋科学,2012,36(2):129-135.
[30]陈冬梅,穆桂金.不同沉积环境下沉积物的粒度分形特征的对比研究[J].干旱区地理,2004,27(1):47-51.
[31]Sun D,Bloemendal J,Rea D K,et al.Grain-size distribution function of polymodal sediments in hydraulic and aeolian environments,and numerical partitioning of the sedimentary components[J].Sedimentary Geology,2002,152(3):263-277.
[32]张平,宋春晖,杨用彪,等.稳定湖相沉积物和风成黄土粒度判别函数的建立及其意义[J].沉积学报,2008,26(3):501-507.
[33]王会昌.一万年来白洋淀的扩张与收缩[J].地理研究,1983,2(8):8-18.
[34]林景星,张静,林防,等.西太平洋暖池扩张对华北平原气候变化的影响:华北平原4万年以来升温事件的新证据[J].地球学报,1998,19(4):18-21.
[35]Qin X.Loess record of the aerodynamic environment in the east Asia monsoon area since 60,000 years before present[J].Journal of Geophysical Research,2005,110(B1):1204.
[36]Zhou W,Yu X,Jull A J T,et al.High-resolution evidence from southern China of an early Holocene optimum and a mid-Holocene dry event during the past 18,000 years[J].Quaternary Research,2004,62(1):39-48.
[37]邵晓华,汪永进,程海,等.全新世季风气候演化与干旱事件的湖北神农架石笋记录[J].科学通报,2006,51(1):80-86.
[38]郭书元,詹伟,王强.河北省白洋淀地区中全新世丽蚌动物群及其生态环境意义[J].古地理学报,2014,16(3):335-346.
[39]吴忱,魏福利.华北地区晚全新世初期环境变化分析[J].地理与地理信息科学,2003,19(2):97-101.
[40]吴忱,朱宣清,何乃华,等.华北平原古河道研究[M].北京:中国科学技术出版社,1991:169-184.