宁夏长城塬全新世黄土—土壤元素地球化学特征与成壤环境演变研究
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摘要
当今,一系列前所未有的重大的全球性环境问题对世界各国的经济发展和人类社会的生存产生了深远的影响,全球气候变化及其产生的影响更是与人类的生存息息相关。全新世作为与人类社会发展密切相关的一个时期,是国际过去气候变化研究中的重点,研究全新世气候变化对预测未来环境和气候演变具有重要的参考价值。至今许多研究方法和信息载体已经引入全新世环境演变的研究中,并且取得了很大的进展。黄土高原的黄土一土壤序列以其堆积完整、沉积连续的特点成为第四纪环境变迁研究中公认的良好信息载体之一,通过对黄土-土壤序列的高分辨率研究,学者们己经弄清楚了中国黄土高原地区风成黄土的形成机制、物质来源及其所反映的气候变迁历史。
本文在了解了国际国内地学界和环境学界第四纪环境演变进展的基础上,经过缜密的野外观察,选定宁夏彭阳长城塬地区一个典型的全新世黄土-土壤剖面进行高分辨率采样,确定磁化率、化学元素、粒度、烧失量、碳酸钙和吸湿水含量等环境指标进行室内测定分析,获得了宁夏长城塬全新世环境演变的高分辨率数据信息。实验数据分析表明磁化率、烧失量、吸湿水和粘粒高值均出现在土壤层,低值出现在黄土层。而碳酸钙、粗粉沙和沙级颗粒却在土壤层中含量低,黄土层中含量高。活动性较强的元素Na、Ca、Sr在土壤层中发生迁移淋失,从而在黄土层中出现高值。其他微量元素和大部分重金属元素(除Pb、V外)的含量分布特征反映了受气候变化的成土过程的影响,在土壤层中表现为高值,在黄土层中表现为低值。钾钠比、残积系数,Rb／Sr比值作为良好的气候代用指标在彭阳CCY剖面中呈现出有规律的变化：即最大值出现在古土壤层,最小值出现在黄土层；硅铝系数、钙镁比(CaO/MgO)、(CaO+Na2O+K2O)/Al2O3则表现出相反的变化规律。这些化学参数与磁化率、频率磁化率曲线形成很好的对比,表明黄土风化成壤过程中元素的迁移变化可以间接反映全新世以来的气候变化和成壤环境的变化。
元素对环境条件变化的响应表现在地球表生作用过程中化学元素的迁移富集。土壤发生的实质是各种化学元素的重新组合及其迁移淋失。因此,黄土-土壤序列中元素含量的动态变化、化学参数等地球化学特征都对环境变化有直接的指示意义,代表了研究区域土壤的化学风化强度及时空规律。本文结合数据分析对彭阳地区CCY黄土-土壤剖面的元素地球化学特征和风化成壤强度以及成壤环境演变进行了研究讨论,主要得出以下结论：
(1)相对马兰黄土层,其他黄土层中的常量元素和微量元素均没有发生明显的分异,反映了黄土物质组成的均一性和物质来源的统一性；而在古土壤层(So)中常量元素和微量元素发生了明显的分异,全新世大暖期,CCY剖面在土壤风化成壤过程中,常量元素中Ca, Mg、Na在化学风化过程中发生了迁移淋失,Si、Fe、K、则呈现出富集特征。常量元素的活动性大小为CaO>MgO>Na2O>SiO2Fe2O3>K2O。元素的迁移特征表明宁夏长城塬黄土只经历了早期的化学风化,应处在脱Ca、Na阶段,尚未进入去K风化阶段。微量元素中Sr发生了很明显的迁移淋失,大部分微量元素呈现富集特征,元素迁移序列由强至弱依次为Sr>Ba>V>Cu>Zn>Ni>Mn>Ti>Rb>Cr。因生物生命活动特别是植物生长吸收而应在地表大量富集的微量元素Cu、Zn,在CCY剖面中富集很弱,反映全新世宁夏长城塬地区风化成壤时期植物生命活动弱,植被生长状况较差。
(2)化学蚀变指数CIA和A-CN-K风化趋势图指示在全新世大暖期,黄土高原地区由北到南黄土化学风化程度逐渐增强,彭阳长城塬地区经历了低等的化学风化作用,与平凉地区黄土风化相似,而弱于关中扶风地区的黄土风化作用。彭阳地区黄土的化学风化过程及其与黄土高原其他地区黄土化学风化强度的差异主要受到气候条件的控制,气候条件通过年平均气温和年降水量对化学风化的地球化学环境起着重要的影响,其中降水在整体比较干旱的黄土高原地区的黄士化学风化过程中可能起着更为重要的制约作用。
(3)CCY全新世黄土-土壤剖面各项环境代用指标和元素地球化学特征揭示了全新世以来气候环境的演变,相应地宁夏长城塬地区的成壤环境表现出由全新世早期干冷气候条件下的沉积期(形成过渡层Lt)向全新世中期温湿气候条件下的强成壤期(形成古土壤S0)演变,再向全新世晚期冷干气候条件下的沉积期(形成全新世黄土L0)的演变规律。1500a B.P.以来,气候条件有所改善,在人类农业耕作扰动下,形成成壤作用较强的表土层(TS)。
(4)与黄土高原关中地区的磁化率、Rb／Sr值和CIA指数的比较发现,相对于南部关中地区的亚热带暖湿气候,彭阳地区在全新世大暖期可能为暖温带的气候环境。
(5)重金属元素的相关性分析与成壤环境演变研究表明在万年时间尺度上,彭阳长城塬地区土壤中重金属元素含量变化,从表面上看,受到土壤粒度成分和碳酸钙含量变化影响。深入分析发现,其中最根本的控制因素,还是季风气候的变化导致沙尘暴强度和堆积速率以及降水量变化。
Nowdays a series of global environment problems which have never occurred before, especially global changes in climate have deep impacts on both economic development of all the coutries and survival of human beings. The Holocene which is closely related to the development of human society is an essential part of PAGES. And study of the Holocene climate change has a viallty inportmant reference value to forcasting future environment changes. Many methods were introduced into the studies and great progress was made. The loess-paleosol sequence in the Loess Plteau which is located in Northwest China was accepted as a wonderful information carrier in Quaternary research. The formative mechanism, source of loess-paleosol and history of climatic changes in the Loess Plateau was made clear through the studies of the Loess-paleosol profile.
Through field exploration, systematical sampling and experimenting, we gained a lot of high-definition datum of magnetic susceptibility, partical size, chemical elements, content of calcium carbonate, loss-on-ignition and hygroscopic water which have an important indicative significance to paleoclimate evolution. The results show that the content of magnetic susceptibility, loss-on-ignition, hygroscopic water and clay in soil are higer than those in loess. But the content of calcium carbonate, coarse fraction and sand-size particles in soil are lower than those in loess. The elemet Na, Ca, Sr were obviously migrated and leached during the chemical weathering progress so that they had a high value in loess.The distribution characteristics of heavy metals (except Pb, V) and other trace elements reflect the effect of soil formation, so that they have a high value in soil and low value in loess. K2O/Na2O ratio, eluvial coefficient and Rb/Sr, as good proxy climate indexes,varied regularly in the CCY Holocene loess-soil profile, i.e. they peaked in the paleosol,and were lower in the loess,and reduced along with the intensity of pedogenesis decreasing.Whereas CaO/MgO ratio, SiO2/Al2O3 ratio and leaching coefficient went the other way in the profile,indicating that during the paleosol formation,the climate was warm and humid with abundant precipitation;while during the loess accumulation.the climate was relatively cold and arid.There is a good comparisons between these chemical parameters and magnetic susceptibility, frequency dependent susceptibility, showing that during the process of loess chemical weathering.elements seems to indirectly reflect the change of climate and pedogenic environment.
The migration and enrichment of chemical elements were related to the environment changes. The Holocene loess-soil in the Loess Plateau constituted an excellent record of climate evolution, aeolian dust and soil formation. The essential of soil was that the chemical elements reset and mignation. Therefore, the distribution of elements content in soil and the chemical parameter all can show the variety of environment and intension of chemical weathering in Pengyang. In paper, the element geochemical characteristics, intensity of chemical weathering and pedogenetic environment changes were studied and discussed. The conclusions maily are as follows:
(1)In relation to Malan loess layer, the major elements and trace elements in other loess layers were not obviously differentiated, which reflect the homogeneity and uniformity of loess material. But in Holocene Megatherma, the major elements and trace elements were differentiated in paleosoil (So). During the pedogenetic progress, Ca, Mg, Na were leached but Fe, Si, K were enriched. According to the migration ability, the major elements are ranked in the following order: Ca>Mg>Na>Mn>Si>Ti>Fe>K. The migration features of the macro-elements reveal that Holocene loess in Pengyang only experienced primary process of chemical weathering characterized by leaching of Ca、Na,and not reached the secondary process characterized by leaching of K.Most of the trace elements were enriched except the element Sr was obviously migrated and leached during the chemical weathering process. According to the migration ability, the major elements are ranked in the following order:Sr>Ba>V>Cu>Zn>Ni>Mn>Ti>Rb>Cr. Cu, Zn was faintly enriched in CCY profile, which indicated that the vegetation is poor during the chemical weathering progress in Pengyang.
(2) CIA and A-CN-K ternary diagram indicate that intensity of chemical weathering of loess in Loess Plateau was gradually increased from northwest to southeast. In Holocene Megatherma, the Pengyang loess underwent primary chemical weathering, which is similar to that of Pingliang loess, much weaker than that of Guangzhong loess. The chemical weathering differences among the studied Aeolian-dust deposits in Loess Plateau were mainly induced by the distinction of climate condition, which imposed important influence on the geochemical environment through the mean annual temperature and annual precipitation. It seems that the annual precipitation has more important influence on the chemical weathering process in arid Loess Plateau.
(3)The environmrnt proxy indicators and element geochemical characteristics in CCY Holocene loess-soil profile reveal the evolution of climatic environment. Pedogenetic environment in Pengyang underwent such process:the early Holocene with dry and cold climate deposited trasitional loess Lt, the middle Holocene with warm and humid climate developed paleosoil So, the late Holocene with dry and cold climate deposited Holocene loess Lo. Since 1500a B.P.,the climate condition had improved, and a potent soil layer TS was developed under the human farming perturbations.
(4)Comparison with magnetic susceptibility, Rb/Sr, CIA of JYC profile at Guangzhong basin, these values of CCY profile was obviously lower, showing that paleosol's intensity of pedogenesis in the CCY profile was significantly weaker than that in JYC profile, precipitation was on the low side, which indicating that in relation to the subtropical climate in Guangzhong basin, Changcheng loess tableland in Pengyang may only belong to warm temperate climate in Holocene Megathermal.
(5)Research in pedogenetic environment changes and correlation analysis between heavy metals and climatic index indicate that at a long-time scale particle-size distribution and content of calcium carbonate are the important factors that directly affect the distribution of heavy metals in the profile. However, these are ultimately affected by the changes in the intensity of dust storms and precipitation that controlled by monsoonal climatic changes during the Holocene.
本文在了解了国际国内地学界和环境学界第四纪环境演变进展的基础上,经过缜密的野外观察,选定宁夏彭阳长城塬地区一个典型的全新世黄土-土壤剖面进行高分辨率采样,确定磁化率、化学元素、粒度、烧失量、碳酸钙和吸湿水含量等环境指标进行室内测定分析,获得了宁夏长城塬全新世环境演变的高分辨率数据信息。实验数据分析表明磁化率、烧失量、吸湿水和粘粒高值均出现在土壤层,低值出现在黄土层。而碳酸钙、粗粉沙和沙级颗粒却在土壤层中含量低,黄土层中含量高。活动性较强的元素Na、Ca、Sr在土壤层中发生迁移淋失,从而在黄土层中出现高值。其他微量元素和大部分重金属元素(除Pb、V外)的含量分布特征反映了受气候变化的成土过程的影响,在土壤层中表现为高值,在黄土层中表现为低值。钾钠比、残积系数,Rb／Sr比值作为良好的气候代用指标在彭阳CCY剖面中呈现出有规律的变化：即最大值出现在古土壤层,最小值出现在黄土层；硅铝系数、钙镁比(CaO/MgO)、(CaO+Na2O+K2O)/Al2O3则表现出相反的变化规律。这些化学参数与磁化率、频率磁化率曲线形成很好的对比,表明黄土风化成壤过程中元素的迁移变化可以间接反映全新世以来的气候变化和成壤环境的变化。
元素对环境条件变化的响应表现在地球表生作用过程中化学元素的迁移富集。土壤发生的实质是各种化学元素的重新组合及其迁移淋失。因此,黄土-土壤序列中元素含量的动态变化、化学参数等地球化学特征都对环境变化有直接的指示意义,代表了研究区域土壤的化学风化强度及时空规律。本文结合数据分析对彭阳地区CCY黄土-土壤剖面的元素地球化学特征和风化成壤强度以及成壤环境演变进行了研究讨论,主要得出以下结论：
(1)相对马兰黄土层,其他黄土层中的常量元素和微量元素均没有发生明显的分异,反映了黄土物质组成的均一性和物质来源的统一性；而在古土壤层(So)中常量元素和微量元素发生了明显的分异,全新世大暖期,CCY剖面在土壤风化成壤过程中,常量元素中Ca, Mg、Na在化学风化过程中发生了迁移淋失,Si、Fe、K、则呈现出富集特征。常量元素的活动性大小为CaO>MgO>Na2O>SiO2Fe2O3>K2O。元素的迁移特征表明宁夏长城塬黄土只经历了早期的化学风化,应处在脱Ca、Na阶段,尚未进入去K风化阶段。微量元素中Sr发生了很明显的迁移淋失,大部分微量元素呈现富集特征,元素迁移序列由强至弱依次为Sr>Ba>V>Cu>Zn>Ni>Mn>Ti>Rb>Cr。因生物生命活动特别是植物生长吸收而应在地表大量富集的微量元素Cu、Zn,在CCY剖面中富集很弱,反映全新世宁夏长城塬地区风化成壤时期植物生命活动弱,植被生长状况较差。
(2)化学蚀变指数CIA和A-CN-K风化趋势图指示在全新世大暖期,黄土高原地区由北到南黄土化学风化程度逐渐增强,彭阳长城塬地区经历了低等的化学风化作用,与平凉地区黄土风化相似,而弱于关中扶风地区的黄土风化作用。彭阳地区黄土的化学风化过程及其与黄土高原其他地区黄土化学风化强度的差异主要受到气候条件的控制,气候条件通过年平均气温和年降水量对化学风化的地球化学环境起着重要的影响,其中降水在整体比较干旱的黄土高原地区的黄士化学风化过程中可能起着更为重要的制约作用。
(3)CCY全新世黄土-土壤剖面各项环境代用指标和元素地球化学特征揭示了全新世以来气候环境的演变,相应地宁夏长城塬地区的成壤环境表现出由全新世早期干冷气候条件下的沉积期(形成过渡层Lt)向全新世中期温湿气候条件下的强成壤期(形成古土壤S0)演变,再向全新世晚期冷干气候条件下的沉积期(形成全新世黄土L0)的演变规律。1500a B.P.以来,气候条件有所改善,在人类农业耕作扰动下,形成成壤作用较强的表土层(TS)。
(4)与黄土高原关中地区的磁化率、Rb／Sr值和CIA指数的比较发现,相对于南部关中地区的亚热带暖湿气候,彭阳地区在全新世大暖期可能为暖温带的气候环境。
(5)重金属元素的相关性分析与成壤环境演变研究表明在万年时间尺度上,彭阳长城塬地区土壤中重金属元素含量变化,从表面上看,受到土壤粒度成分和碳酸钙含量变化影响。深入分析发现,其中最根本的控制因素,还是季风气候的变化导致沙尘暴强度和堆积速率以及降水量变化。
Nowdays a series of global environment problems which have never occurred before, especially global changes in climate have deep impacts on both economic development of all the coutries and survival of human beings. The Holocene which is closely related to the development of human society is an essential part of PAGES. And study of the Holocene climate change has a viallty inportmant reference value to forcasting future environment changes. Many methods were introduced into the studies and great progress was made. The loess-paleosol sequence in the Loess Plteau which is located in Northwest China was accepted as a wonderful information carrier in Quaternary research. The formative mechanism, source of loess-paleosol and history of climatic changes in the Loess Plateau was made clear through the studies of the Loess-paleosol profile.
Through field exploration, systematical sampling and experimenting, we gained a lot of high-definition datum of magnetic susceptibility, partical size, chemical elements, content of calcium carbonate, loss-on-ignition and hygroscopic water which have an important indicative significance to paleoclimate evolution. The results show that the content of magnetic susceptibility, loss-on-ignition, hygroscopic water and clay in soil are higer than those in loess. But the content of calcium carbonate, coarse fraction and sand-size particles in soil are lower than those in loess. The elemet Na, Ca, Sr were obviously migrated and leached during the chemical weathering progress so that they had a high value in loess.The distribution characteristics of heavy metals (except Pb, V) and other trace elements reflect the effect of soil formation, so that they have a high value in soil and low value in loess. K2O/Na2O ratio, eluvial coefficient and Rb/Sr, as good proxy climate indexes,varied regularly in the CCY Holocene loess-soil profile, i.e. they peaked in the paleosol,and were lower in the loess,and reduced along with the intensity of pedogenesis decreasing.Whereas CaO/MgO ratio, SiO2/Al2O3 ratio and leaching coefficient went the other way in the profile,indicating that during the paleosol formation,the climate was warm and humid with abundant precipitation;while during the loess accumulation.the climate was relatively cold and arid.There is a good comparisons between these chemical parameters and magnetic susceptibility, frequency dependent susceptibility, showing that during the process of loess chemical weathering.elements seems to indirectly reflect the change of climate and pedogenic environment.
The migration and enrichment of chemical elements were related to the environment changes. The Holocene loess-soil in the Loess Plateau constituted an excellent record of climate evolution, aeolian dust and soil formation. The essential of soil was that the chemical elements reset and mignation. Therefore, the distribution of elements content in soil and the chemical parameter all can show the variety of environment and intension of chemical weathering in Pengyang. In paper, the element geochemical characteristics, intensity of chemical weathering and pedogenetic environment changes were studied and discussed. The conclusions maily are as follows:
(1)In relation to Malan loess layer, the major elements and trace elements in other loess layers were not obviously differentiated, which reflect the homogeneity and uniformity of loess material. But in Holocene Megatherma, the major elements and trace elements were differentiated in paleosoil (So). During the pedogenetic progress, Ca, Mg, Na were leached but Fe, Si, K were enriched. According to the migration ability, the major elements are ranked in the following order: Ca>Mg>Na>Mn>Si>Ti>Fe>K. The migration features of the macro-elements reveal that Holocene loess in Pengyang only experienced primary process of chemical weathering characterized by leaching of Ca、Na,and not reached the secondary process characterized by leaching of K.Most of the trace elements were enriched except the element Sr was obviously migrated and leached during the chemical weathering process. According to the migration ability, the major elements are ranked in the following order:Sr>Ba>V>Cu>Zn>Ni>Mn>Ti>Rb>Cr. Cu, Zn was faintly enriched in CCY profile, which indicated that the vegetation is poor during the chemical weathering progress in Pengyang.
(2) CIA and A-CN-K ternary diagram indicate that intensity of chemical weathering of loess in Loess Plateau was gradually increased from northwest to southeast. In Holocene Megatherma, the Pengyang loess underwent primary chemical weathering, which is similar to that of Pingliang loess, much weaker than that of Guangzhong loess. The chemical weathering differences among the studied Aeolian-dust deposits in Loess Plateau were mainly induced by the distinction of climate condition, which imposed important influence on the geochemical environment through the mean annual temperature and annual precipitation. It seems that the annual precipitation has more important influence on the chemical weathering process in arid Loess Plateau.
(3)The environmrnt proxy indicators and element geochemical characteristics in CCY Holocene loess-soil profile reveal the evolution of climatic environment. Pedogenetic environment in Pengyang underwent such process:the early Holocene with dry and cold climate deposited trasitional loess Lt, the middle Holocene with warm and humid climate developed paleosoil So, the late Holocene with dry and cold climate deposited Holocene loess Lo. Since 1500a B.P.,the climate condition had improved, and a potent soil layer TS was developed under the human farming perturbations.
(4)Comparison with magnetic susceptibility, Rb/Sr, CIA of JYC profile at Guangzhong basin, these values of CCY profile was obviously lower, showing that paleosol's intensity of pedogenesis in the CCY profile was significantly weaker than that in JYC profile, precipitation was on the low side, which indicating that in relation to the subtropical climate in Guangzhong basin, Changcheng loess tableland in Pengyang may only belong to warm temperate climate in Holocene Megathermal.
(5)Research in pedogenetic environment changes and correlation analysis between heavy metals and climatic index indicate that at a long-time scale particle-size distribution and content of calcium carbonate are the important factors that directly affect the distribution of heavy metals in the profile. However, these are ultimately affected by the changes in the intensity of dust storms and precipitation that controlled by monsoonal climatic changes during the Holocene.
引文
[1]符超峰,安芷生,强小科,等.全球变化研究进展和面临的挑战及应对策略[J].干旱区研究,2006,23(1)：1-7.
[2]安芷生,符宗斌.全球变化科学的进展[J].地球科学进展,2001,16(5)：671-680.
[3]叶笃正,符宗斌.全球变化的主要科学问题[J].大气科学,1994,18(4)：498-512.
[4]刘东生.黄土与环境[M].北京：科学出版社,1985,191-302
[5]孙建中.黄土学[M].香港：香港考古学会出版,2005：1-25.
[6]赵景波.中国黄土地环境的研究进展[J].干旱区地理,2000,23(2)：186-190.
[7]丁仲礼,刘东生.1.80Ma以来黄土-深海古气候记录对比[J].科学通报,1991(15)：1401-1403.
[8]丁仲礼,任剑璋,刘东生,等.晚更新世季风-沙漠系统千年尺度的不规则变化及其机制问题[J].中国科学(D辑),1996：385-391.
[9]An Z. S.,Kutzbach J.E.,Poter S.C. Evolution of Asian monsoons and phased up lift of the Himalaya-Tibetan plateau since Late Miocene times [J].Nature,2001, 411:62-66.
[10]岳乐平,杨利荣,李智佩,等.西北地区干枯湖床沉积粒度组成与东亚沙尘天气[J].沉积学报,2004,22(2)：325-331.
[11]Pan B.T.,Burbank D., Wang Y.X.,et al. A 900 k.y record of strath terrance formation during glacial-interglacial transitions in northwest China [J].Geology, 2003,30(11):957-960.
[12]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,1999,17(2)：226-232.
[13]Rea D.K.,Snoeckx H.,Joseph L.H. Late Genozoic eolian deposition in the North Pacific:Aisan drying, Tibetan up lift, and cooling of the northern hemisphere [J]. Plaeoceanography,1998,13(3):215-224.
[14]Guo Z.T.,Ruddiman W.F., Hao Q.Z.,et al. Onset of Asian desertification by 22 M yr ago inferred from loess deposits in China [J].Nature,2002,416(14):159-163.
[15]Chen J.,An Z. S.,Head J. Variation of Rb/Sr ratios in the loess-paleosol sequences of Central China during the last 130,000 years and implication for monsoon paleoclimatology [J].Quaternary Research,1999,51:215-219.
[16]马峰,刘立,王安平,等.图门江下游沙丘粒度分布与石英表面结构研究[J]. 沉积学报,2004,22(2)：261-266.
[17]Zhou L.P., Oldfield F.,Wintle A.G,et al. Partly pedogenic origin of magnetic variation in Chinese loess [J].Nature,1990,346:1-3.
[18]Xiao J.L., Poter S.C.,An Z.S.,et al. Grain size of quartz as indicator of wintermonsoon strength on the loess plateau of Central China during the last 130,000 yr[J].Quaternary Research,1995,43:22-29.
[19]Ding Zhongli, Yu Zhiwei, Ruter N W, et al.Towards an orbital time scale for Chinese loess deposits [J].Quaternary Sciences Review,1994,13:39-70.
[20]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,1997,42(1)：66-69.
[21]鹿化煜,安芷生.黄土高原粒度组成的古气候意义[J].中国科学(D辑),1998,28(3)：278-283.
[22]赵景波.黄土的本质与形成模式[J].沉积学报,2003,21(2)：198-204.
[23]隋玉柱.黄土不同指标的古环境意义探讨[J].中国沙漠,2006,26(1)：14-19.
[24]徐建树,潘保田,李琼,等.陇西贫地末次冰期黄土粒度特征及其环境意义[J].沉积学报,2005,23(4)：702-708.
[25]丁仲礼,余志伟,刘东生.中国黄土研究新进展(三)：时间标尺[J].第四纪研究,1991,(4)：336-347.
[26]安芷生,吴锡浩,汪品先,等.最近130ka中国的古季风-Ⅰ.古季风记录[J].中国科学(B辑),1991,10：1076-1081.
[27]安芷生,吴锡浩,汪品先,等.最近130ka中国的古季风-Ⅱ.古季风变迁[J].中国科学(B辑),1991,11：1209-1215.
[28]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.
[29]Lu Huayu, LiLi, An Zhisheng, et al. EastAsiawintermonsoon oscillation and its correlation with the North Atlantic Heinrich events during the last glaciation [J]. Progress in Natural Science,1996,6(6):711-717.
[30]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,2000,18(3)：327-335.
[31]Heller F, Liu T S.Magnetostratigraphical dating of loess deposits in China [J]. Nature,1982,300:431-433.
[32]刘秀铭,许同春,刘东生.中国黄土磁化率各向异性及成因及其对第四纪研究的意义[J].中国科学(B辑),1989,(4)：441-448.
[33]李吉均.中国西北地区晚更新世以来环境变迁模式[J].第四纪研究,1990,(3)：197-204.
[34]陈发虎.兰州黄土记录与万年尺度气候变化周期[J].科学通报,1992,(24)：2263-2265.
[35]Heller F, Shen C D, Beer J, et al. Quantitative estimates and palaeoclimatic implications of pedogenic ferromagnetic mineral formation in Chinese loess [J]. Earth Sci lett,1993,114:385-390.
[36]吕厚远,韩家懋,吴乃琴,等.中国现代土壤磁化率分析及其古气候意义[J].中国科学(B辑),1994,24(12)：1290-1297.
[37]郭正堂,魏兰英,吕厚远.晚第四纪风尘物质成分的变化及其环境意义[J].第四纪研究,1999,(1)：41-48.
[38]刘东生.黄土的物质成分和结构[M].北京：科学出版社,1966,59-71.
[39]文启忠.中国黄土地球化学[M].北京：科学出版社,1989,115-145.
[40]顾兆炎.黄土-古土壤序列碳酸盐同位素组成与古气候变化[J].科学通报,1991,36：767-770.
[41]卢演铸.黄土地层中CaCO3含量变化与更新世气候旋回[J].地质科学,1981,(2)：122-125.
[42]管东红,奚晓霞,郝永萍,等.北源剖面碳酸钙记录的末次间冰期气候不稳定性[J].冰川冻土,1996,(2)：119-124
[43]Fang X.M.,Li J.J.Millennial-scale monsoonal climatic change from paleosol sequences on the Chinese Loess Plateau and Tibetan Plateau:A brief summary and review, China[J].Sci. Bull,1999,44(1):38-52.
[44]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),2000,31(3)：177-184.
[45]张虎才,史正涛,戴雪荣.深海氧同位素第5阶段的气候记录：武都黄土剖面与极地冰心／深海沉积同位素记录的对比[J].兰州大学学报(自然科学版),1997,33(4)：107-115.
[46]刁桂仪,文启忠.渭南黄土剖面碳酸盐和铁变化的古气候记录[J].地球化学,1995,24(增)：77-82.
[47]刘丛强,张劲,李春来.黄土中碳酸钙及其Sr同位素组成变化与古气候波动记录[J].科学通报,1999,44(10)：1088-1092.
[48]孙建中,赵景波.黄土高原第四纪[M].北京：科学出版社，1991,89-143.
[49]郝永萍,方小敏,李吉均,等.干旱-半湿润区土壤-气候转化函数的研究[J]. 地理科学,1998,18(3)：248-256.
[50]郝永萍,奚晓霞,方小敏等.西北干旱-半湿润区土壤与气候间转化函数的初步研究[J].土壤地质,1997,(4)：12-19.
[51]赵景波.淀积理论与黄土高原环境演变[M].北京：科学出版社,2002,17-44.
[52]Zheng S H, Wang Y, Chen C Y.Studies on the stable isotopes in carbonates in Luochuan loess section:Applicability of the Ca daduies as paleoclimate indicators. In:Liu T S ed. Aspects of Loess Research. Beijing:China Ocean Press,1987, 283-290.
[53]Hendy C H. The isotope geochemistry of speleothems-I. The calculation of effects of different modes of formation on isotopic composition of speleothems and their applicability as paleoclimatic indicators [J].Geochimica et Cosmochimica Acta,1971,35:801-824.
[54]Gu Z Y. The carbonate isotopic composition of the loess-paleosol sequence and its implication of paleoclimatic change [J].Chinese Science Bulletin,1991,36(20): 1979-1983
[55]Gu Z Y, Liu R M, Liu Y.Response of the table isotopic composition of loess-paleosol carbonate to paleoenvironmental changes. In:Liu T S ed. Loess, Environment and Global Change. Beijing:Science Press,1991.82-92.
[56]Lin B H, Liu R M, An Z S.Preliminary research on stable isotopic compositions of Chinese loess. In:Liu T S ed. Loess, Environment and Global Change. Beijing: Science Press,1991,124-131.
[57]韩家懋,姜文英,吴乃琴,等.黄土中钙结核的碳氧同位素研究(一)氧同位素及其古环境意义[J].第四纪研究,1995,(2)：130-137.
[58]韩家懋,姜文英,吕厚远,等.黄土中钙结核的碳氧同位素研究(二)碳同位素及其古环境意义[J].第四纪研究,1995,(4)：367-377.
[59]Han J M, Jiang W Y, Liu T Set al. Carbonate isotope records of paleoclimate changes in Chinese loess.Science in China(Series D),1996,39(5):460-467.
[60]Han J M, Keppens E, Liu T S.Stable isotope composition of the carbonate concretion in loess and climate change [J].Quaternary International,1997,37: 37-43.
[61]顾兆炎,韩家懋,刘东生.中国第四纪黄土地球化学研究进展[J].第四纪研究,2000,20(1)：41-55.
[62]陈骏,王洪涛,鹿化煜.陕西洛川黄土沉积物中稀土元素及其它微量元素的 化学淋滤研究[J].地质学报,1996,70：61-72
[63]陈骏,李峻峰,仇纲,等.陕西洛川黄土化学风化程度的地球化学研究[J].中国科学(D辑),1997,27(5)：531-536.
[64]陈骏,安芷生,汪永进,等.最近800ka洛川黄土剖面中Rb／Sr分布和古季风变迁[J].中国科学(D辑),1998,28(5)：498-504.
[65]陈骏,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,(4)：350-356.
[66]Gu Z Y, Lal D, Liu T Set al. Weathering histories of Chinese loess deposits based on uranium and thorium series nuclides and cosmogeniclOBe [J].Geochimica et Cosmochimica Acta,1997,61:5221-5231.
[67]Liu T S, Guo Z T, Liu J Qet al.Variation of eastern Asian monsoon over the last 140000 years [J].Bulletin Societ geologique France,1995,166:221-229.
[68]Guo Z T, Liu T S, Guiot Jet al.High frequency pulses of East Asianmonsoon climate in the last two glaciations:Link with the North Atlantic [J].Climate Dynamics,1996,12:701-709.
[69]刘连文,陈骏,陈肠,等.最近13ka以来黄土中Zr／Rb值变化及其对冬季风的指示意义[J],科学通报,2002,47(9)：702-706.
[70]李徐生,韩志勇,杨守业,等.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.
[71]吕厚远,王永吉.晚更新世以来洛川黑木沟黄土地层中植物硅酸体研究及古植被演替[J].第四纪研究,1991,(1)：72-84.
[72]吕厚远,吴乃琴,刘东生,等.最近15万年以来宝鸡黄土剖面植物硅酸体组合所反映的季节性气候变化[J].中国科学(D辑),1996,26：131-137.
[73]夏应菲,汪永进,陈骏.李家岗下蜀黄土剖面的反射光谱[J].土壤学报,2000,37(4)：443-448.
[74]陈焕伟.从古土壤看北京环境变迁[J].土壤学报,2000,37(3)：306-315.
[75]李叙勇,李保国,石元春.土壤发育指数及其在黄土-古土壤序列中的应用[J].土壤学报,2001,38(2)：153-159.
[76]张宗枯,魏明建.黄土中全氧化铁与气候指标的定量关系[J].科学通报,1995,40(13)：191-222.
[77]吴乃琴,吕厚远,孙湘君.植物硅酸体-气侯因子转换函数及其在渭南晚冰期以来古环境研究中的应用[J].第四纪研究,1994,3：270-279.
[78]夏敦胜,马玉贞,陈发虎,等.秦安大地湾高分辨率全新世植被演变与气候变 迁初步研究[J].兰州大学学报(自然科学版),1998,34(1)：119-127.
[79]Huang C.C., Zhou J, Pang J.L.,et, al. Aregional aridity Phase and its possible culture impact during the Holocene Megathermal in Guangzhong Basin [J].The Holocene,2000,10(1):135-143.
[80]Huang C.C.,Pang J.L.,Zhao J.B. Chinese loess and evolution of the East Asian monsoon [J].Progress in Physical Geography,2000,24 (1):75-96.
[81]黄春长,庞奖励,张占平.黄土高原环境恶化的自然背景研究[J].陕西师范大学学报(自然科学版),2000,28(3)：110-114.
[82]黄春长.渭河流域3100年前的资源退化与人地关系演变[J].地理科学,2001,21(1)：29-35.
[83]黄春长,庞奖励,陈宝群,等.渭河流域先周一西周时代环境和水土资源退化及其社会影响[J].第四纪研究,2003,4：404-414.
[84]Huang C.C, Pang J L, Su H X, et, al.The Ustic Isohumisol (Chernozem) distributed over the Chinese Loess Plateau:Modern soil or palaeosol [J]? Geoderma,2009,150:344-358.
[85]庞奖励,黄春长,张占平,等.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.
[86]庞奖励,黄春长,张占平,等.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.
[87]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,2007,3：357-364.
[88]Huang C.C, Pang J L, Chen S E. Charcoal records of the fire history in the Holocene loess-soil sequences over the southern Loess Plateau of China [J]. Palaeogeography Palaeoecology Palaeoclimatology.2006,239:28-44.
[89]Huang C.C, Pang J L, Zhou Q Y, et al. Holocene pedogenic change and the emergence and decline of rain-fed cereal agriculture on the Chinese Loess Plateau [J].Quaternary Science Reviews,2004,23:2529-2539.
[90]Huang C.C, Jia Y F, Pang J.L, et al. Holocene colluviation and its implications for tracing human-induced soil erosion and redeposition on the piedmont loess lands of the Qinling mountains, Northern China [J].Geoderma.2006,136:838-851.
[91]Huang C.C, Zhao S.C, Pang J.L.,et al.Climatic aridity and the relocations of the Zhou Culture in the Southern Loess Plateau of China[J].Climatic Change.2003, 61(3):361-378.
[92]Huang C.C, Pang J.L, Chen S.E, et al. Holocene dust accumulation and the formation of policyclic cinnamon soils in the Chinese Loess Plateau [J].Earth Surface Processes and Landforms.2003,28(12):1259-1270.
[93]王建,刘泽纯,姜文英,等.磁化率与粒度、矿物的关系及其古环境意义[J].地理学报,1996,51(2)：155-162.
[94]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(增刊),1992,12：279-285.
[95]Mather B.A.,Thompson R. Mineral magnetic record of the Chinese loess [J]. Geology,1991,19:3-6.
[96]彭先芝,贾蓉芬,李荣森,等.趋磁细菌及磁小体对黄土-古土壤序列磁化率贡献的模拟实验研究[J].第四纪研究,2002,22(2)：188-194.
[97]Kukla G.Loess stragtigraphy in cetral China [J].Quaternary Science Reserch, 1987,6:191-219.
[98]Kukla G J. Correlation of Chinese, European and America loess series with deep-sea sediments. Loess Research [D].Beijing:China Ocean Press.1987,27-38.
[99]Kukla G,An Z S.,Melice J.L., et, al. Magnetic susceptibility record of Chinese loess [J].Translation of the Royal Society of Edinburgh. Earth Science,1990, 81:263-288.
[100]安芷生,Kukla G,刘东生.洛川黄土地层学[J].第四纪研究,1989,2：155-168.
[101]强小科,安芷生,常宏.佳县红粘土堆积序列频率磁化率的古气候意义[J].海洋地质与第四纪地质,2003,23(3)：91-96.
[102]刘秀铭,刘东生,F Heller,等.黄土频率磁化率与古气候冷暖转换[J].第四纪研究,1990,(1)：42-49.
[103]谭红兵,马海州,张西营.碳酸盐研究与其记录的环境变化[J].盐湖研究,2003,11(4)：21-27.
[104]刘东生,丁仲礼.二百五十万年来季风环流与大陆冰量变化的阶段性耦合过程[J].第四纪研究,1992,(1)：12-23.
[105]陈忠,马海州,曹广超,等.黄土碳酸盐的研究[J].盐湖研究,2004,14(4)：66-72.
[106]朱宏,赵成义,李军,等.土壤CaCO3淀积对降水量及环境变化的指示[J].土壤通报,2001,38(4)：810-812.
[107]刘安娜.渭河流域全新世剖面元素地球化学特征与成壤环境变化研究[D]. 中国优秀博硕士学位论文全文数据库(硕士),2006,(10).
[108]石建省,石迎春,叶浩,等.黄土堆积序列“高温烧失量”指标对古气候演化的指示意义[J].地理学与国土研究,2002,8(4)：104-106.
[109]张佳华,孔昭衰,杜乃秋.烧失量数值波动对北京地区过去气候和环境的特征响应[J].生态学报,1998,18(4)：343-347.
[110]莱尔曼A.,王苏民,等译.湖泊的化学地质学和地理学[M].北京：地质出版社,1989：132-133.
[111]黄麒.柴达木盆地察尔汗湖区气候波动模式的初步研究[J].中国科学(B辑),1990：652-66.
[112]李新艳.淮河上游全新世黄土-土壤剖面高分辨率地球化学研究[D].中国优秀博硕士学位论文全文数据库(硕士),2006,(10).
[113]朱士光,王元林,呼林贵.历史时期关中地区气候变化的初步研究[J].第四纪研究,1998,(1)：2-10.
[114]刘孝义,依艳丽,张大庚.土壤水分与植物生长[M].辽宁科学技术出版社,2007,49-50.
[115](苏)罗戴,A.A.著,巴逢辰等译.土壤水[M].科学出版社,1964,300-340.
[116]任明达,王乃梁.现代沉积环境概论[M].北京：科学出版社,1981,8-25.
[117]华东石油学院岩矿教研室.沉积岩石学(上册)[M].北京：石油工业出版社,1982,79-96.
[118]华东石油学院勘探系、基础地质、石油地质教研室.沉积岩[M].北京：石油化学工业出版社,1977,66-93.
[119]成都地质学院.沉积岩石学[M].北京：地质出版社,1980,307-320.
[120]Moldway L. On the governing Sedimentation from eolon suspension [J].Acta Universitatis Szogediensis.1962,14:75-109.
[121]Porter S.C.,An Z. S.Correlation between climate events in North Atlantic and China during the last glaciations [J].Nture,1995,375(25):305-308
[122]丁仲礼,孙继敏,朱日祥.黄土高原粘土成因及上新世北方干旱化问题[J].第四纪研究,1997,2：147-157.
[123]查小春,黄春长,庞奖励.关中东部缓坡地面全新世土壤侵蚀与沉积发展演变规律研究[J].生态环境,2005,14(1)：52-56.
[124]成都地质学院陕北队.沉积岩(物)粒度分析及应用[M].北京：地质出版社,1976，90-100.
[125]Gu Z.Y.,La I.D.,Liu T. S.,et al.Weatheringhistories of Chinese loess depostis based on uranium and thorium series nuclides and cosmogenici 10Be[J].Geochimica et Cosmochimica Acta,1997,61:5221-5231.
[126]文启忠,刁桂仪,余素华,等.黄河中游地区马兰黄土微量元素分布图[J].地球化学,1986,(4)：325-337.
[127]Pecsi M. Loess is not just the accumulation of the dust [J].Quaternary Intemational,1990,7(8):1-21.
[128]王云,魏复盛.土壤环境元素化学[M].北京：中国环境科学出版社,1995：362-379,75-86,180-192.
[129]叶玮,Yabuki S, Kanayama S.中国西风区黄土常量元素地球化学行为与古环境[J].干旱区地理,2003,26(1)：23-29.
[130]Johnson, D.L, Keller, E. A. Dynamic pedogenesis:new views on some key soil concepts, and a model for interpreting Quaternary soils [J].Quaternary Research, 1990,33,306-319.
[131]Kemp, R.A. Pedogenic modification of loess:significance for palaeoclimatic reconstructions[J].Earth-ScienceReviews,2001,54,145-156.
[132]Klokeadr S.Changing Metal Cycles and Human health. Berlin:Springerverlag, 1984,113-141.
[133]陈同斌,黄铭洪,黄焕忠,周海云.香港土壤中的重金属含量及其污染现状[J].地理学报,1997,52(3)：228-236.
[134]吴新民,李恋卿,潘根兴,等.南京市不同功能城区土壤中重金属Cu、Zn、Pb和Cd的污染特征[J].环境科学,2003,24(3)：105-111.
[135]孟可,张学林,秦建业,等.我国大城市环境铅污染影响因素分析[J].环境科学学报,1995,15(2)：135-147.
[136]施雅风,孔昭宸,王苏民,等.中国全新世大暖期的气候波动与重要事件[J].中国科学(B辑),1992,22：1300-1308.
[137]邢光熹,朱建国.土壤微量元素和稀土元素化学[M].北京：科学出版社,2003：30-31.
[138]Dasch.E. J.Strontium istopes in weathering profiles, deep sea sediments and sedimentary rocks [J].Geochim Cosmochimica Acta,1969,33:1521-1522.
[139]Gallet S,Jahn B, Torii M. Early Proterozoic climates and plate motions inferred from major element chemistry of lutites [J].Nature,1982,229:715-717.
[140]刁桂仪,文启忠.黄土风化成土过程中主要元素迁移序列[J].地质地球化学,1999,27(1)：21-26.
[141]Wedepohl K. H. Handbook of Geochemistry [M],Berlin, Springer,1969,248.
[142]冯连君,储雪蕾,张启锐,等.化学蚀变指数(CIA)及其在新元古代碎屑岩中的应用[J].地学前缘,2003,10(4)：539-544.
[143]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.
[144]McLennan S M. Weathering and global denudation [J].Journal of Geology,1993, 101:295-303.
[145]Nesbitt H W, Markovics G, Price R C.Chemical processes affecting alkalis and alkaline earths during continental weathering [J].Geochem Cosmochim Acta,1980,44(11):1659-1666.
[146]Chun Chang Huang, H. Su. Climate change and Zhou relocations in early Chinese history [J].Journal of Historical Geography,2008,1-14.
[147]C.C.Huang, S.C. Zhao, J.L. Pang, et,al.Climatic aridity and the relocations of the Zhou culture in the Southern Loess Plateau of China[J].Climatic Change,2003, 61:361-378.
[148]Y. Peng, J. Xiao, T. Nakamura, et al.Holocene East Asian monsoonal precipitation pattern revealed by grain-size distribution of core sediment of Daihai Lake in Inner Mongolia of north-central China [J].Earth and Planetary Science Letters,2005,233:467-479;
[149]竺可桢.中国五千年来的气候变迁研究[J].中国科学,1973,2：168-189.
[150]Huang C.C.,Pang, J.L.,Su, H.X.,et al.Climatic and anthropogenic impacts on soil formation in the semiarid loess table land in the middle reaches of the Yellow River, China[J].Journal of Arid Environments,2007,71:280-298.
[2]安芷生,符宗斌.全球变化科学的进展[J].地球科学进展,2001,16(5)：671-680.
[3]叶笃正,符宗斌.全球变化的主要科学问题[J].大气科学,1994,18(4)：498-512.
[4]刘东生.黄土与环境[M].北京：科学出版社,1985,191-302
[5]孙建中.黄土学[M].香港：香港考古学会出版,2005：1-25.
[6]赵景波.中国黄土地环境的研究进展[J].干旱区地理,2000,23(2)：186-190.
[7]丁仲礼,刘东生.1.80Ma以来黄土-深海古气候记录对比[J].科学通报,1991(15)：1401-1403.
[8]丁仲礼,任剑璋,刘东生,等.晚更新世季风-沙漠系统千年尺度的不规则变化及其机制问题[J].中国科学(D辑),1996：385-391.
[9]An Z. S.,Kutzbach J.E.,Poter S.C. Evolution of Asian monsoons and phased up lift of the Himalaya-Tibetan plateau since Late Miocene times [J].Nature,2001, 411:62-66.
[10]岳乐平,杨利荣,李智佩,等.西北地区干枯湖床沉积粒度组成与东亚沙尘天气[J].沉积学报,2004,22(2)：325-331.
[11]Pan B.T.,Burbank D., Wang Y.X.,et al. A 900 k.y record of strath terrance formation during glacial-interglacial transitions in northwest China [J].Geology, 2003,30(11):957-960.
[12]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,1999,17(2)：226-232.
[13]Rea D.K.,Snoeckx H.,Joseph L.H. Late Genozoic eolian deposition in the North Pacific:Aisan drying, Tibetan up lift, and cooling of the northern hemisphere [J]. Plaeoceanography,1998,13(3):215-224.
[14]Guo Z.T.,Ruddiman W.F., Hao Q.Z.,et al. Onset of Asian desertification by 22 M yr ago inferred from loess deposits in China [J].Nature,2002,416(14):159-163.
[15]Chen J.,An Z. S.,Head J. Variation of Rb/Sr ratios in the loess-paleosol sequences of Central China during the last 130,000 years and implication for monsoon paleoclimatology [J].Quaternary Research,1999,51:215-219.
[16]马峰,刘立,王安平,等.图门江下游沙丘粒度分布与石英表面结构研究[J]. 沉积学报,2004,22(2)：261-266.
[17]Zhou L.P., Oldfield F.,Wintle A.G,et al. Partly pedogenic origin of magnetic variation in Chinese loess [J].Nature,1990,346:1-3.
[18]Xiao J.L., Poter S.C.,An Z.S.,et al. Grain size of quartz as indicator of wintermonsoon strength on the loess plateau of Central China during the last 130,000 yr[J].Quaternary Research,1995,43:22-29.
[19]Ding Zhongli, Yu Zhiwei, Ruter N W, et al.Towards an orbital time scale for Chinese loess deposits [J].Quaternary Sciences Review,1994,13:39-70.
[20]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,1997,42(1)：66-69.
[21]鹿化煜,安芷生.黄土高原粒度组成的古气候意义[J].中国科学(D辑),1998,28(3)：278-283.
[22]赵景波.黄土的本质与形成模式[J].沉积学报,2003,21(2)：198-204.
[23]隋玉柱.黄土不同指标的古环境意义探讨[J].中国沙漠,2006,26(1)：14-19.
[24]徐建树,潘保田,李琼,等.陇西贫地末次冰期黄土粒度特征及其环境意义[J].沉积学报,2005,23(4)：702-708.
[25]丁仲礼,余志伟,刘东生.中国黄土研究新进展(三)：时间标尺[J].第四纪研究,1991,(4)：336-347.
[26]安芷生,吴锡浩,汪品先,等.最近130ka中国的古季风-Ⅰ.古季风记录[J].中国科学(B辑),1991,10：1076-1081.
[27]安芷生,吴锡浩,汪品先,等.最近130ka中国的古季风-Ⅱ.古季风变迁[J].中国科学(B辑),1991,11：1209-1215.
[28]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.
[29]Lu Huayu, LiLi, An Zhisheng, et al. EastAsiawintermonsoon oscillation and its correlation with the North Atlantic Heinrich events during the last glaciation [J]. Progress in Natural Science,1996,6(6):711-717.
[30]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,2000,18(3)：327-335.
[31]Heller F, Liu T S.Magnetostratigraphical dating of loess deposits in China [J]. Nature,1982,300:431-433.
[32]刘秀铭,许同春,刘东生.中国黄土磁化率各向异性及成因及其对第四纪研究的意义[J].中国科学(B辑),1989,(4)：441-448.
[33]李吉均.中国西北地区晚更新世以来环境变迁模式[J].第四纪研究,1990,(3)：197-204.
[34]陈发虎.兰州黄土记录与万年尺度气候变化周期[J].科学通报,1992,(24)：2263-2265.
[35]Heller F, Shen C D, Beer J, et al. Quantitative estimates and palaeoclimatic implications of pedogenic ferromagnetic mineral formation in Chinese loess [J]. Earth Sci lett,1993,114:385-390.
[36]吕厚远,韩家懋,吴乃琴,等.中国现代土壤磁化率分析及其古气候意义[J].中国科学(B辑),1994,24(12)：1290-1297.
[37]郭正堂,魏兰英,吕厚远.晚第四纪风尘物质成分的变化及其环境意义[J].第四纪研究,1999,(1)：41-48.
[38]刘东生.黄土的物质成分和结构[M].北京：科学出版社,1966,59-71.
[39]文启忠.中国黄土地球化学[M].北京：科学出版社,1989,115-145.
[40]顾兆炎.黄土-古土壤序列碳酸盐同位素组成与古气候变化[J].科学通报,1991,36：767-770.
[41]卢演铸.黄土地层中CaCO3含量变化与更新世气候旋回[J].地质科学,1981,(2)：122-125.
[42]管东红,奚晓霞,郝永萍,等.北源剖面碳酸钙记录的末次间冰期气候不稳定性[J].冰川冻土,1996,(2)：119-124
[43]Fang X.M.,Li J.J.Millennial-scale monsoonal climatic change from paleosol sequences on the Chinese Loess Plateau and Tibetan Plateau:A brief summary and review, China[J].Sci. Bull,1999,44(1):38-52.
[44]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),2000,31(3)：177-184.
[45]张虎才,史正涛,戴雪荣.深海氧同位素第5阶段的气候记录：武都黄土剖面与极地冰心／深海沉积同位素记录的对比[J].兰州大学学报(自然科学版),1997,33(4)：107-115.
[46]刁桂仪,文启忠.渭南黄土剖面碳酸盐和铁变化的古气候记录[J].地球化学,1995,24(增)：77-82.
[47]刘丛强,张劲,李春来.黄土中碳酸钙及其Sr同位素组成变化与古气候波动记录[J].科学通报,1999,44(10)：1088-1092.
[48]孙建中,赵景波.黄土高原第四纪[M].北京：科学出版社，1991,89-143.
[49]郝永萍,方小敏,李吉均,等.干旱-半湿润区土壤-气候转化函数的研究[J]. 地理科学,1998,18(3)：248-256.
[50]郝永萍,奚晓霞,方小敏等.西北干旱-半湿润区土壤与气候间转化函数的初步研究[J].土壤地质,1997,(4)：12-19.
[51]赵景波.淀积理论与黄土高原环境演变[M].北京：科学出版社,2002,17-44.
[52]Zheng S H, Wang Y, Chen C Y.Studies on the stable isotopes in carbonates in Luochuan loess section:Applicability of the Ca daduies as paleoclimate indicators. In:Liu T S ed. Aspects of Loess Research. Beijing:China Ocean Press,1987, 283-290.
[53]Hendy C H. The isotope geochemistry of speleothems-I. The calculation of effects of different modes of formation on isotopic composition of speleothems and their applicability as paleoclimatic indicators [J].Geochimica et Cosmochimica Acta,1971,35:801-824.
[54]Gu Z Y. The carbonate isotopic composition of the loess-paleosol sequence and its implication of paleoclimatic change [J].Chinese Science Bulletin,1991,36(20): 1979-1983
[55]Gu Z Y, Liu R M, Liu Y.Response of the table isotopic composition of loess-paleosol carbonate to paleoenvironmental changes. In:Liu T S ed. Loess, Environment and Global Change. Beijing:Science Press,1991.82-92.
[56]Lin B H, Liu R M, An Z S.Preliminary research on stable isotopic compositions of Chinese loess. In:Liu T S ed. Loess, Environment and Global Change. Beijing: Science Press,1991,124-131.
[57]韩家懋,姜文英,吴乃琴,等.黄土中钙结核的碳氧同位素研究(一)氧同位素及其古环境意义[J].第四纪研究,1995,(2)：130-137.
[58]韩家懋,姜文英,吕厚远,等.黄土中钙结核的碳氧同位素研究(二)碳同位素及其古环境意义[J].第四纪研究,1995,(4)：367-377.
[59]Han J M, Jiang W Y, Liu T Set al. Carbonate isotope records of paleoclimate changes in Chinese loess.Science in China(Series D),1996,39(5):460-467.
[60]Han J M, Keppens E, Liu T S.Stable isotope composition of the carbonate concretion in loess and climate change [J].Quaternary International,1997,37: 37-43.
[61]顾兆炎,韩家懋,刘东生.中国第四纪黄土地球化学研究进展[J].第四纪研究,2000,20(1)：41-55.
[62]陈骏,王洪涛,鹿化煜.陕西洛川黄土沉积物中稀土元素及其它微量元素的 化学淋滤研究[J].地质学报,1996,70：61-72
[63]陈骏,李峻峰,仇纲,等.陕西洛川黄土化学风化程度的地球化学研究[J].中国科学(D辑),1997,27(5)：531-536.
[64]陈骏,安芷生,汪永进,等.最近800ka洛川黄土剖面中Rb／Sr分布和古季风变迁[J].中国科学(D辑),1998,28(5)：498-504.
[65]陈骏,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,(4)：350-356.
[66]Gu Z Y, Lal D, Liu T Set al. Weathering histories of Chinese loess deposits based on uranium and thorium series nuclides and cosmogeniclOBe [J].Geochimica et Cosmochimica Acta,1997,61:5221-5231.
[67]Liu T S, Guo Z T, Liu J Qet al.Variation of eastern Asian monsoon over the last 140000 years [J].Bulletin Societ geologique France,1995,166:221-229.
[68]Guo Z T, Liu T S, Guiot Jet al.High frequency pulses of East Asianmonsoon climate in the last two glaciations:Link with the North Atlantic [J].Climate Dynamics,1996,12:701-709.
[69]刘连文,陈骏,陈肠,等.最近13ka以来黄土中Zr／Rb值变化及其对冬季风的指示意义[J],科学通报,2002,47(9)：702-706.
[70]李徐生,韩志勇,杨守业,等.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.
[71]吕厚远,王永吉.晚更新世以来洛川黑木沟黄土地层中植物硅酸体研究及古植被演替[J].第四纪研究,1991,(1)：72-84.
[72]吕厚远,吴乃琴,刘东生,等.最近15万年以来宝鸡黄土剖面植物硅酸体组合所反映的季节性气候变化[J].中国科学(D辑),1996,26：131-137.
[73]夏应菲,汪永进,陈骏.李家岗下蜀黄土剖面的反射光谱[J].土壤学报,2000,37(4)：443-448.
[74]陈焕伟.从古土壤看北京环境变迁[J].土壤学报,2000,37(3)：306-315.
[75]李叙勇,李保国,石元春.土壤发育指数及其在黄土-古土壤序列中的应用[J].土壤学报,2001,38(2)：153-159.
[76]张宗枯,魏明建.黄土中全氧化铁与气候指标的定量关系[J].科学通报,1995,40(13)：191-222.
[77]吴乃琴,吕厚远,孙湘君.植物硅酸体-气侯因子转换函数及其在渭南晚冰期以来古环境研究中的应用[J].第四纪研究,1994,3：270-279.
[78]夏敦胜,马玉贞,陈发虎,等.秦安大地湾高分辨率全新世植被演变与气候变 迁初步研究[J].兰州大学学报(自然科学版),1998,34(1)：119-127.
[79]Huang C.C., Zhou J, Pang J.L.,et, al. Aregional aridity Phase and its possible culture impact during the Holocene Megathermal in Guangzhong Basin [J].The Holocene,2000,10(1):135-143.
[80]Huang C.C.,Pang J.L.,Zhao J.B. Chinese loess and evolution of the East Asian monsoon [J].Progress in Physical Geography,2000,24 (1):75-96.
[81]黄春长,庞奖励,张占平.黄土高原环境恶化的自然背景研究[J].陕西师范大学学报(自然科学版),2000,28(3)：110-114.
[82]黄春长.渭河流域3100年前的资源退化与人地关系演变[J].地理科学,2001,21(1)：29-35.
[83]黄春长,庞奖励,陈宝群,等.渭河流域先周一西周时代环境和水土资源退化及其社会影响[J].第四纪研究,2003,4：404-414.
[84]Huang C.C, Pang J L, Su H X, et, al.The Ustic Isohumisol (Chernozem) distributed over the Chinese Loess Plateau:Modern soil or palaeosol [J]? Geoderma,2009,150:344-358.
[85]庞奖励,黄春长,张占平,等.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.
[86]庞奖励,黄春长,张占平,等.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.
[87]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,2007,3：357-364.
[88]Huang C.C, Pang J L, Chen S E. Charcoal records of the fire history in the Holocene loess-soil sequences over the southern Loess Plateau of China [J]. Palaeogeography Palaeoecology Palaeoclimatology.2006,239:28-44.
[89]Huang C.C, Pang J L, Zhou Q Y, et al. Holocene pedogenic change and the emergence and decline of rain-fed cereal agriculture on the Chinese Loess Plateau [J].Quaternary Science Reviews,2004,23:2529-2539.
[90]Huang C.C, Jia Y F, Pang J.L, et al. Holocene colluviation and its implications for tracing human-induced soil erosion and redeposition on the piedmont loess lands of the Qinling mountains, Northern China [J].Geoderma.2006,136:838-851.
[91]Huang C.C, Zhao S.C, Pang J.L.,et al.Climatic aridity and the relocations of the Zhou Culture in the Southern Loess Plateau of China[J].Climatic Change.2003, 61(3):361-378.
[92]Huang C.C, Pang J.L, Chen S.E, et al. Holocene dust accumulation and the formation of policyclic cinnamon soils in the Chinese Loess Plateau [J].Earth Surface Processes and Landforms.2003,28(12):1259-1270.
[93]王建,刘泽纯,姜文英,等.磁化率与粒度、矿物的关系及其古环境意义[J].地理学报,1996,51(2)：155-162.
[94]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(增刊),1992,12：279-285.
[95]Mather B.A.,Thompson R. Mineral magnetic record of the Chinese loess [J]. Geology,1991,19:3-6.
[96]彭先芝,贾蓉芬,李荣森,等.趋磁细菌及磁小体对黄土-古土壤序列磁化率贡献的模拟实验研究[J].第四纪研究,2002,22(2)：188-194.
[97]Kukla G.Loess stragtigraphy in cetral China [J].Quaternary Science Reserch, 1987,6:191-219.
[98]Kukla G J. Correlation of Chinese, European and America loess series with deep-sea sediments. Loess Research [D].Beijing:China Ocean Press.1987,27-38.
[99]Kukla G,An Z S.,Melice J.L., et, al. Magnetic susceptibility record of Chinese loess [J].Translation of the Royal Society of Edinburgh. Earth Science,1990, 81:263-288.
[100]安芷生,Kukla G,刘东生.洛川黄土地层学[J].第四纪研究,1989,2：155-168.
[101]强小科,安芷生,常宏.佳县红粘土堆积序列频率磁化率的古气候意义[J].海洋地质与第四纪地质,2003,23(3)：91-96.
[102]刘秀铭,刘东生,F Heller,等.黄土频率磁化率与古气候冷暖转换[J].第四纪研究,1990,(1)：42-49.
[103]谭红兵,马海州,张西营.碳酸盐研究与其记录的环境变化[J].盐湖研究,2003,11(4)：21-27.
[104]刘东生,丁仲礼.二百五十万年来季风环流与大陆冰量变化的阶段性耦合过程[J].第四纪研究,1992,(1)：12-23.
[105]陈忠,马海州,曹广超,等.黄土碳酸盐的研究[J].盐湖研究,2004,14(4)：66-72.
[106]朱宏,赵成义,李军,等.土壤CaCO3淀积对降水量及环境变化的指示[J].土壤通报,2001,38(4)：810-812.
[107]刘安娜.渭河流域全新世剖面元素地球化学特征与成壤环境变化研究[D]. 中国优秀博硕士学位论文全文数据库(硕士),2006,(10).
[108]石建省,石迎春,叶浩,等.黄土堆积序列“高温烧失量”指标对古气候演化的指示意义[J].地理学与国土研究,2002,8(4)：104-106.
[109]张佳华,孔昭衰,杜乃秋.烧失量数值波动对北京地区过去气候和环境的特征响应[J].生态学报,1998,18(4)：343-347.
[110]莱尔曼A.,王苏民,等译.湖泊的化学地质学和地理学[M].北京：地质出版社,1989：132-133.
[111]黄麒.柴达木盆地察尔汗湖区气候波动模式的初步研究[J].中国科学(B辑),1990：652-66.
[112]李新艳.淮河上游全新世黄土-土壤剖面高分辨率地球化学研究[D].中国优秀博硕士学位论文全文数据库(硕士),2006,(10).
[113]朱士光,王元林,呼林贵.历史时期关中地区气候变化的初步研究[J].第四纪研究,1998,(1)：2-10.
[114]刘孝义,依艳丽,张大庚.土壤水分与植物生长[M].辽宁科学技术出版社,2007,49-50.
[115](苏)罗戴,A.A.著,巴逢辰等译.土壤水[M].科学出版社,1964,300-340.
[116]任明达,王乃梁.现代沉积环境概论[M].北京：科学出版社,1981,8-25.
[117]华东石油学院岩矿教研室.沉积岩石学(上册)[M].北京：石油工业出版社,1982,79-96.
[118]华东石油学院勘探系、基础地质、石油地质教研室.沉积岩[M].北京：石油化学工业出版社,1977,66-93.
[119]成都地质学院.沉积岩石学[M].北京：地质出版社,1980,307-320.
[120]Moldway L. On the governing Sedimentation from eolon suspension [J].Acta Universitatis Szogediensis.1962,14:75-109.
[121]Porter S.C.,An Z. S.Correlation between climate events in North Atlantic and China during the last glaciations [J].Nture,1995,375(25):305-308
[122]丁仲礼,孙继敏,朱日祥.黄土高原粘土成因及上新世北方干旱化问题[J].第四纪研究,1997,2：147-157.
[123]查小春,黄春长,庞奖励.关中东部缓坡地面全新世土壤侵蚀与沉积发展演变规律研究[J].生态环境,2005,14(1)：52-56.
[124]成都地质学院陕北队.沉积岩(物)粒度分析及应用[M].北京：地质出版社,1976，90-100.
[125]Gu Z.Y.,La I.D.,Liu T. S.,et al.Weatheringhistories of Chinese loess depostis based on uranium and thorium series nuclides and cosmogenici 10Be[J].Geochimica et Cosmochimica Acta,1997,61:5221-5231.
[126]文启忠,刁桂仪,余素华,等.黄河中游地区马兰黄土微量元素分布图[J].地球化学,1986,(4)：325-337.
[127]Pecsi M. Loess is not just the accumulation of the dust [J].Quaternary Intemational,1990,7(8):1-21.
[128]王云,魏复盛.土壤环境元素化学[M].北京：中国环境科学出版社,1995：362-379,75-86,180-192.
[129]叶玮,Yabuki S, Kanayama S.中国西风区黄土常量元素地球化学行为与古环境[J].干旱区地理,2003,26(1)：23-29.
[130]Johnson, D.L, Keller, E. A. Dynamic pedogenesis:new views on some key soil concepts, and a model for interpreting Quaternary soils [J].Quaternary Research, 1990,33,306-319.
[131]Kemp, R.A. Pedogenic modification of loess:significance for palaeoclimatic reconstructions[J].Earth-ScienceReviews,2001,54,145-156.
[132]Klokeadr S.Changing Metal Cycles and Human health. Berlin:Springerverlag, 1984,113-141.
[133]陈同斌,黄铭洪,黄焕忠,周海云.香港土壤中的重金属含量及其污染现状[J].地理学报,1997,52(3)：228-236.
[134]吴新民,李恋卿,潘根兴,等.南京市不同功能城区土壤中重金属Cu、Zn、Pb和Cd的污染特征[J].环境科学,2003,24(3)：105-111.
[135]孟可,张学林,秦建业,等.我国大城市环境铅污染影响因素分析[J].环境科学学报,1995,15(2)：135-147.
[136]施雅风,孔昭宸,王苏民,等.中国全新世大暖期的气候波动与重要事件[J].中国科学(B辑),1992,22：1300-1308.
[137]邢光熹,朱建国.土壤微量元素和稀土元素化学[M].北京：科学出版社,2003：30-31.
[138]Dasch.E. J.Strontium istopes in weathering profiles, deep sea sediments and sedimentary rocks [J].Geochim Cosmochimica Acta,1969,33:1521-1522.
[139]Gallet S,Jahn B, Torii M. Early Proterozoic climates and plate motions inferred from major element chemistry of lutites [J].Nature,1982,229:715-717.
[140]刁桂仪,文启忠.黄土风化成土过程中主要元素迁移序列[J].地质地球化学,1999,27(1)：21-26.
[141]Wedepohl K. H. Handbook of Geochemistry [M],Berlin, Springer,1969,248.
[142]冯连君,储雪蕾,张启锐,等.化学蚀变指数(CIA)及其在新元古代碎屑岩中的应用[J].地学前缘,2003,10(4)：539-544.
[143]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.
[144]McLennan S M. Weathering and global denudation [J].Journal of Geology,1993, 101:295-303.
[145]Nesbitt H W, Markovics G, Price R C.Chemical processes affecting alkalis and alkaline earths during continental weathering [J].Geochem Cosmochim Acta,1980,44(11):1659-1666.
[146]Chun Chang Huang, H. Su. Climate change and Zhou relocations in early Chinese history [J].Journal of Historical Geography,2008,1-14.
[147]C.C.Huang, S.C. Zhao, J.L. Pang, et,al.Climatic aridity and the relocations of the Zhou culture in the Southern Loess Plateau of China[J].Climatic Change,2003, 61:361-378.
[148]Y. Peng, J. Xiao, T. Nakamura, et al.Holocene East Asian monsoonal precipitation pattern revealed by grain-size distribution of core sediment of Daihai Lake in Inner Mongolia of north-central China [J].Earth and Planetary Science Letters,2005,233:467-479;
[149]竺可桢.中国五千年来的气候变迁研究[J].中国科学,1973,2：168-189.
[150]Huang C.C.,Pang, J.L.,Su, H.X.,et al.Climatic and anthropogenic impacts on soil formation in the semiarid loess table land in the middle reaches of the Yellow River, China[J].Journal of Arid Environments,2007,71:280-298.