从彭阳剖面看黄土成壤模式及气候变化
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摘要
过去气候变化研究是今后气候动态预测的基础，变化指标和时间标尺的构建又是古气候研究的关键。作为第四纪古环境三大支柱记录之一的黄土在过去全球变化研究中占据着非常重要的地位。
针对黄土研究中出现的问题，本文制定的技术路线是：(1)在确认黄土也是土壤的前提下，通过国内外黄土土壤学系列研究成果的综合，构建黄土成壤模式；(2)通过土壤微形态学研究确定宁夏彭阳剖面各层古土壤的发育强度，并以此作为评价标准；(3)进行粒度、磁化率、化学成分、色度、CaCO_3、烧失量等多项指标的测试，并建立集定性、定量指标于一体的综合指标—土壤发育指数；(4)比较研究土壤发育指数及其它指标能否反映古土壤的发育强度；(5)以黄土成壤模式为依托，探讨各指标在反映成壤强度方面的差异性、矛盾性及其可能的原因，并筛选较优定量指标；(6)利用较优指标建立定年模型；(7)结合年代序列、成壤强度探讨黄土高原西北部重大气候事件及820ka气候变化。取得的主要新认识如下：
1．黄土成壤模式主要由母质的特异性(母质分布在上、下两个方向)，成壤、沉积的同步性，成壤的双向性(上、下)、速成性，土壤性状的均一性、叠加性、矛盾性(钙积与粘化同层)，成壤强度的特异性和成壤速率地表最大等要素构成。
2．运用本文初次建立的土壤指数定年模式证实，宁夏境内具有松山期的黄土层，B／M界线位于彭阳县城阳乡杨塬103m深的黄土中，其黄土年龄为0—828ka B.P.，这在既往研究中尚未报道。
3．与其它剖面相比，彭阳剖面粒度总体上要比东部的洛川、西安，甚至西部的兰州、新疆东湾要粗；CaCO_3平均含量不仅高于黄土高原中部，也高于高原西部，反映出本剖面富含碳酸盐的六盘山近源沉积起到了很重要的作用；易溶元素含量在剖面10m处快速升高，淀积特征明显，反映出黄土受现代淋溶成土作用影响较大，黄土直立、疏松、多孔特性和高温与多雨组合的气候特点，使得元素淋溶、淀积的强度和深度超出了传统的认识和判断；烧失量与其它指标相比，不仅能区分冰期、间冰期；而且能够区分出次一级的冰阶、间冰阶，有较高的分辨率；土壤发育指数、红度能够反映土壤强度差异，是反映气候波动的较好指标；然而，磁化率不能反映古土壤S_8的存在，且S_7的磁化率在全剖面中最高，这与大多剖面S_5磁化率最高的特点不一致。
4．在彭阳剖面成壤较弱的黄土层发现了黏粒胶膜，这在以往研究中很少报道，并且用传统土壤学难以解释，因为黄土成壤较弱，在碱性环境中难以形成胶膜。然而，此种“矛盾现象”恰能进一步证实上覆发育较强的土层已经产生了显著的粘粒移动，且迂出了土体，并在黄土中淀积。
5．500ka B.P.前后，本剖面出现了研究序列成壤最强的层段—S_5。经综合对比后确认，S_5发育时北亚热带可能波及到黄土高原西北部的六盘山北段，这又把前人研究的此时北亚热带向北推进了200km。土壤发育指数、红度、烧失量、CaCO_3形态和含量整体上反映出本区有逐渐变干的趋势。800ka B.P.以来，六盘山地区发生了796-792，766-756，730-722，510-504，350-336，100-88ka B.P.六次比较强的沙漠扩张。
Along with the warming and drying of modem climate, the evolution of arid and semiarid regions has become the focus in the research on climatic changes around the world. Studies of climatic variability in the past are essential for evaluating its evolution. Knowledge of the timing and extent of the growth and retreat of deserts is important for the prediction of future global changes and for understanding their mechanisms. Thick sequences of interstratified loess and paleosols from the Chinese Loess Plateau provide one of the most complete and most sensitive terrestrial records of environmental change for the past 2.5million years.
In the past climatic change research, the extraction and establishment of indexes are extremely important. In this paper, an attempt is made to integrate various physical and chemical proxies into a representative paleoclimate index, and verify mutually information from different proxies. The Pengyang section of the northwest Chinese Loess Plateau has been studied and a soil development index has been set up. Correspondingly, the paleoclimatic change patterns of this arid-semiarid region spanning the past 800,000 years have been developed.
The soil-forming mode of loess is mainly composed of the particularity of parent materials, synchronization of soil-forming and sediment, bi-directional weatherings, uniform and ambivalent properties and so on.
The defined B/M boundary is located in loess L8, in good agreement with that of the central loess plateau. Taking B/M boundary at 780 ka B. P., the average sedimentary rate in the Brunhes Chron is 13.21 cm.ka~(-1), therewith, the age of the section bottom is extrapolated to～828 ka B. P.
Compared with other loess section, the particle-size distribution of Pengyang section was coarser than that of luochuan, Xian, Lanzhou and Xinjiang Dongwan section. This is not surprising, given the closer proximity of Pengyang to the Asian inland dust sources; The average content of calcium carbonateis of Pengyang section is not only higher than that of central loess plateau, but also higher the west of Chinese Loess Plateau, which reflected Pengyang loess had been deposited by near Liupanshan's substances that contained more calcium carbonateis; The content of diffluent element of 10m depth in the section increased fast, which indicated that the modern eluviation and the leaching depth of loess may be stronger than our guess; The soil growth index can reflect the intensity of soil forming and the climatic changes; The "abrupt chang" of glacial and interglacial period was caused by strong soil-forming processes that enlarged the discrepancy of granularity between loess and paleosol. However, the magnetic susceptibility nearly cannot reflect the existence of S_8 and the magnetic susceptibility of S_7 is highest in the whole section, which is inconsistent with other studies that S_5 has the highest magnetic susceptibility.
Thin-section examination shows that the micro-texture of the soil layers is divided into both cementing texture in S_7, S_5 and S_1, and granular texture in all others. These paleosols exhibit both a Bt horizon and an argillic horizon with aped structure defined by slickensided clay skins and deeply penetrating sand-filled cracks and are similar to the most ancient known soil of well-drained forest ecosystems and S_5 (subtropical paleosol) of the Xian sequences. Because aeolian grains contain much calcium, pedogenesis must have been prolonged. Based on these facts together with the difference in particlesize distribution within loess, we prefer to consider the S_7, S_5 and S_1 (720-667ka, 513-412ka and 114-73 ka B. P.) as a kind of semitropical spectacle. Certainly, this needs be further validated.
The integrative analysis revealed that Qinling Mountains and Liupan Mountains were all in subtropics climate in 500,000 year before present, the soil growth index, red degree, the shape and the content of calcium carbonateis reflected that the climate of Liupan region had the dry tendency. The soil growth index has particular effects on reflecting climatic changes due to its generational mechanism. The paleoclimatic change patterns of arid-semiarid region spanning the past 800,000 years reveal that the desert expansion and approach in China happened in about 796-792, 766-756, 730-722, 510-504, 350-336, 100-88ka B. P..
针对黄土研究中出现的问题，本文制定的技术路线是：(1)在确认黄土也是土壤的前提下，通过国内外黄土土壤学系列研究成果的综合，构建黄土成壤模式；(2)通过土壤微形态学研究确定宁夏彭阳剖面各层古土壤的发育强度，并以此作为评价标准；(3)进行粒度、磁化率、化学成分、色度、CaCO_3、烧失量等多项指标的测试，并建立集定性、定量指标于一体的综合指标—土壤发育指数；(4)比较研究土壤发育指数及其它指标能否反映古土壤的发育强度；(5)以黄土成壤模式为依托，探讨各指标在反映成壤强度方面的差异性、矛盾性及其可能的原因，并筛选较优定量指标；(6)利用较优指标建立定年模型；(7)结合年代序列、成壤强度探讨黄土高原西北部重大气候事件及820ka气候变化。取得的主要新认识如下：
1．黄土成壤模式主要由母质的特异性(母质分布在上、下两个方向)，成壤、沉积的同步性，成壤的双向性(上、下)、速成性，土壤性状的均一性、叠加性、矛盾性(钙积与粘化同层)，成壤强度的特异性和成壤速率地表最大等要素构成。
2．运用本文初次建立的土壤指数定年模式证实，宁夏境内具有松山期的黄土层，B／M界线位于彭阳县城阳乡杨塬103m深的黄土中，其黄土年龄为0—828ka B.P.，这在既往研究中尚未报道。
3．与其它剖面相比，彭阳剖面粒度总体上要比东部的洛川、西安，甚至西部的兰州、新疆东湾要粗；CaCO_3平均含量不仅高于黄土高原中部，也高于高原西部，反映出本剖面富含碳酸盐的六盘山近源沉积起到了很重要的作用；易溶元素含量在剖面10m处快速升高，淀积特征明显，反映出黄土受现代淋溶成土作用影响较大，黄土直立、疏松、多孔特性和高温与多雨组合的气候特点，使得元素淋溶、淀积的强度和深度超出了传统的认识和判断；烧失量与其它指标相比，不仅能区分冰期、间冰期；而且能够区分出次一级的冰阶、间冰阶，有较高的分辨率；土壤发育指数、红度能够反映土壤强度差异，是反映气候波动的较好指标；然而，磁化率不能反映古土壤S_8的存在，且S_7的磁化率在全剖面中最高，这与大多剖面S_5磁化率最高的特点不一致。
4．在彭阳剖面成壤较弱的黄土层发现了黏粒胶膜，这在以往研究中很少报道，并且用传统土壤学难以解释，因为黄土成壤较弱，在碱性环境中难以形成胶膜。然而，此种“矛盾现象”恰能进一步证实上覆发育较强的土层已经产生了显著的粘粒移动，且迂出了土体，并在黄土中淀积。
5．500ka B.P.前后，本剖面出现了研究序列成壤最强的层段—S_5。经综合对比后确认，S_5发育时北亚热带可能波及到黄土高原西北部的六盘山北段，这又把前人研究的此时北亚热带向北推进了200km。土壤发育指数、红度、烧失量、CaCO_3形态和含量整体上反映出本区有逐渐变干的趋势。800ka B.P.以来，六盘山地区发生了796-792，766-756，730-722，510-504，350-336，100-88ka B.P.六次比较强的沙漠扩张。
Along with the warming and drying of modem climate, the evolution of arid and semiarid regions has become the focus in the research on climatic changes around the world. Studies of climatic variability in the past are essential for evaluating its evolution. Knowledge of the timing and extent of the growth and retreat of deserts is important for the prediction of future global changes and for understanding their mechanisms. Thick sequences of interstratified loess and paleosols from the Chinese Loess Plateau provide one of the most complete and most sensitive terrestrial records of environmental change for the past 2.5million years.
In the past climatic change research, the extraction and establishment of indexes are extremely important. In this paper, an attempt is made to integrate various physical and chemical proxies into a representative paleoclimate index, and verify mutually information from different proxies. The Pengyang section of the northwest Chinese Loess Plateau has been studied and a soil development index has been set up. Correspondingly, the paleoclimatic change patterns of this arid-semiarid region spanning the past 800,000 years have been developed.
The soil-forming mode of loess is mainly composed of the particularity of parent materials, synchronization of soil-forming and sediment, bi-directional weatherings, uniform and ambivalent properties and so on.
The defined B/M boundary is located in loess L8, in good agreement with that of the central loess plateau. Taking B/M boundary at 780 ka B. P., the average sedimentary rate in the Brunhes Chron is 13.21 cm.ka~(-1), therewith, the age of the section bottom is extrapolated to～828 ka B. P.
Compared with other loess section, the particle-size distribution of Pengyang section was coarser than that of luochuan, Xian, Lanzhou and Xinjiang Dongwan section. This is not surprising, given the closer proximity of Pengyang to the Asian inland dust sources; The average content of calcium carbonateis of Pengyang section is not only higher than that of central loess plateau, but also higher the west of Chinese Loess Plateau, which reflected Pengyang loess had been deposited by near Liupanshan's substances that contained more calcium carbonateis; The content of diffluent element of 10m depth in the section increased fast, which indicated that the modern eluviation and the leaching depth of loess may be stronger than our guess; The soil growth index can reflect the intensity of soil forming and the climatic changes; The "abrupt chang" of glacial and interglacial period was caused by strong soil-forming processes that enlarged the discrepancy of granularity between loess and paleosol. However, the magnetic susceptibility nearly cannot reflect the existence of S_8 and the magnetic susceptibility of S_7 is highest in the whole section, which is inconsistent with other studies that S_5 has the highest magnetic susceptibility.
Thin-section examination shows that the micro-texture of the soil layers is divided into both cementing texture in S_7, S_5 and S_1, and granular texture in all others. These paleosols exhibit both a Bt horizon and an argillic horizon with aped structure defined by slickensided clay skins and deeply penetrating sand-filled cracks and are similar to the most ancient known soil of well-drained forest ecosystems and S_5 (subtropical paleosol) of the Xian sequences. Because aeolian grains contain much calcium, pedogenesis must have been prolonged. Based on these facts together with the difference in particlesize distribution within loess, we prefer to consider the S_7, S_5 and S_1 (720-667ka, 513-412ka and 114-73 ka B. P.) as a kind of semitropical spectacle. Certainly, this needs be further validated.
The integrative analysis revealed that Qinling Mountains and Liupan Mountains were all in subtropics climate in 500,000 year before present, the soil growth index, red degree, the shape and the content of calcium carbonateis reflected that the climate of Liupan region had the dry tendency. The soil growth index has particular effects on reflecting climatic changes due to its generational mechanism. The paleoclimatic change patterns of arid-semiarid region spanning the past 800,000 years reveal that the desert expansion and approach in China happened in about 796-792, 766-756, 730-722, 510-504, 350-336, 100-88ka B. P..
引文
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2．安芷生，Porter S C，Chappell，等，1994，最近130Ka洛川黄土堆积序列与格陵兰冰芯记录对比，科学通报，39：2254-2256．
3．安芷生，刘晓东，2000，东亚季风气候的历史与变率，科学通报，45(3)：238-249．
4．安芷生，王苏民，吴锡浩等，1998，中国黄土高原的风尘证据：晚新生代北半球大冰期开始及青藏高原的隆升机制，中国科学(D)，28(6)：481-490．
5．安芷生、肖举乐，黄土高原风尘通量研究的一个实例．科学通报，1990，(3)：220～223．
6．安芷生、Porter S，Kukla G，等．最近13万年黄土高原季风变迁的磁化率证据[J]．科学通报，1990，35：529—532．
7．安芷生，吴锡浩，汪品先等，末次间冰期以来中国古季风气候与环境变迁，见：刘东生主编，黄土、第四纪地质、全球变化，第三集，科学出版社，14-30．
8．马溶之．对第四纪地层成因类型和中国第四纪古地理环境的几点意见[J]．中国第四纪研究，1958，(1)：70～73．
9．马溶之．中国黄土之生成．地质论评，1944，9：207～224．
10．曹继秀，徐齐治，张玉田等，1988，兰州九州台黄土—古土壤系列与环境演化研究．兰州大学学报，24：118～122．
11．陈发虎，李吉均，1995，末次间冰期陇西黄土记录的初步研究，见：青藏高原形成演化、环境变迁与生态系统研究学术论文年刊(1994)，北京：科学出版社，96～102
12．陈发虎，马玉贞，李吉均，1996，陇西黄土高原马兰黄土划分与末次冰期气候快速变化研究，冰川冻土，(2)：110～118
13．陈发虎，王建民，李吉均，1996，黄土高原西部地区马兰黄土记录及与GRIP冰心记录的可能对比．见：青藏高原形成演化、环境变迁与生态系统研究学术论文年刊 (1995)，北京：科学出版社，130～135
14．陈发虎等，1992，兰州黄土记录与万年尺度气候变化周期，科学通报，(24)2263-2265
15．陈骏，季峻峰，眭云霞等，1997，陕西洛川黄土中Mn~(2+)的电子顺磁共振特征与古季风变迁，科学通报，42(22)：2419-2421
16．陈旸，陈骏，季峻峰，等．陕西洛川黄土剖面的白度参数及其古气候意义[J]，地质论评，2002，48(1)：39-43．
17．陈旸，陈骏，刘连文．近13万年来黄土高原Rb／Sr记录与夏季风时空变迁[J]，中国科学[D]2003 33[6]513-519．
18．程鹏，高抒，李徐生．激光粒度仪测试结果及其与沉降法，筛选法的比较[J]，沉积学报，2001，19[3]：449-455．
19．丁仲礼，韩家懋，杨石岭等，2000，塔吉克斯坦南部黄土沉积．第四纪研究，20(2)：171-174
20．丁仲礼，刘东生，1998a，晚更新世东亚古季风变化动力机制的概念模型，科学通报，43(2)：122-132
21．丁仲礼，任剑璋，刘东生等，1996，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． 中国科学(D辑)，26：385～391
22．丁仲礼，孙继敏，刘东生，1999，联系沙漠-黄土演变过程中耦合关系的沉积学指标，中国科学，29(1)：84-87
23．丁仲礼，孙继敏，刘东生等，1999，上新世以来毛乌素沙地的阶段性扩张的黄土-红粘土证据，科学通报，44(3)：324-326
24．丁仲礼，孙继敏，杨石岭，等．灵台黄土红粘土序列的磁性地层及粒度记录[J]，第四纪研究，1998年2月，86-94．
25．丁仲礼，孙继敏，余志伟，刘东生，1998，黄土高原过去130ka来古气候事件年 表，科学通报，43(6)：567-574．
26．丁仲礼，余志伟，1995，第四纪时期东亚季风变化的动力机制，第四纪研究，(1)63-74
27．丁仲礼，余志伟，刘东生，1991，中国黄土研究新进展(三)：时间标尺，第四纪研究(4)：336-347．
28．马溶之．对第四纪的成因类型和中国古地理环境的几点意见．中国第四纪研究，1958，1(1)：70—73．
29．马溶之．中国黄土之生成．地质论评，1944，9：207～224．
30．孙继敏，刘东生．洛川黄土地层的再划分及其L9、L15古环境意义的新解释．第四纪研究，2002，22(5)：406-412．
31．董光荣，陈惠忠，王贵勇等，1995，15万年以来中国北方沙漠、沙地演化和气候变化，中国科学(B)，25(12)；1303-1312
32．董光荣，金炯，高尚玉等，1990．晚更新世以来我国北方沙漠地区的气候变化．第四纪研究，(3)：213～222
33．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年5月，158—167．
34．董光荣，王贵勇，李孝泽等，1996，末次间冰期以来我国东部沙区的古季风变迁，中国科学，(D)，26(5)：437-444．
35．胡双熙．陇东和陇中黑垆土的发生与演变．土壤学报，1994，31(3)：295～304．
36．伍光和，田连恕，胡双熙，王乃昂，2000．自然地理学(第3版)，高等教育出版社，北京．
37．方小敏，戴雪荣，李吉均等，1996．亚洲季风演化的突发性与不稳定性—以末次间冰期的土壤发生为例．中国科学，26(2)：339-345．
38．方小敏，李吉均，Banerjee S K等，1998，末次间冰期5e亚阶段夏季风快速变化的环境磁学研究．科学通报，43(21)：2330～2332．
39．方小敏，吕连清，扬胜利等，2000，昆仑山黄土与中国西部沙漠发育和高原隆升，中国科学(D)，31(3)，177-184．
40．方小敏，潘保田，管东红等，1999，兰州约60ka以来夏季风干年尺度不稳定性研究．科学通报，44(4)：535-5381．
41．冯兆东，陈发虎，张虎才等，2000，末次冰期-间冰期蒙古高原与黄土高原对全球变化的贡献，中国沙漠，20(2)：171-177．
42．葛同明，1984，洛川黄土沉积层的磁性地层学研究．海洋地质与第四纪地质，4(1)：37～44
43．顾兆炎、丁仲礼、熊尚发、刘东生．灵台红粘土和黄土—古土壤序列的地球化学演化第四纪研究1999年四期：357-365．
44．顾兆炎．黄土—古土壤序列破酸盐同位素组成与古气候变化[J]．科学通报，1991．36：767—770．
45．顾兆炎，韩家懋，刘东生．中国第四纪黄土地球化学研究进展．第四纪研究，第20卷第1期2000年1月 41-55．
46．管东红等，1996，北塬剖面碳酸钙记录的末次间冰期气候不稳定性，冰川冻土，(2)：119～124
47．郭斌，朱日祥，岳乐平等，1998，Cobb mountain极性事件在黄土中的记录．中国科学(D辑)，28(4)：327～333．
48．郭正堂，Fedoroff N，安芷生等，1993，约0.85Ma前后黄土高原区季风强度的变化，科学通报，38(2)：143～146
49．郭正堂，刘东生，安芷生．间冰期降尘与黄土中加积型古土壤．见：龚子同主编．土壤环境变化．北京：中国科学技术出版社，1992．25—30．
50．郭正堂，刘东生，安芷生．渭南黄土沉积中十五万年来的古土壤及其形成时的古环境[J]．第四纪研究，1994，[3]：256—269．
51．郭正堂，刘东生，吴乃琴等，1996，最后两个冰期黄土记录的Heinrich型气候 节拍．第四纪研究，(1)：21～30
52．郭正堂，刘东生．约0.85Ma前后黄土高原区季风强度的变化[J]．科学通报 1993 38 (2) 143-146
53．郭正堂，彭淑贞，郝清振等，1999，晚第三纪中国西北干旱化的发展及其与北极冰盖形成演化和青藏高原隆升的关系．第四纪研究，(6)：556～567
54．韩家懋，姜文英，刘东生等，1996，黄土碳酸盐中古气候变化的同位素记录．中国科学(D辑)，26：398～404
55．郝青振，郭正堂．1.2Ma以来黄土-古土壤序列风化成壤的定量化研究与东亚夏季风演化[J]，中国科学，2001，31[6]：520-528．
56．郝永萍，方小敏，李吉均，奚晓霞，胡双熙，1998，干旱-半湿润区土壤-气候转化函数的研究．地理科学，18(3)，248-256．
57．郝永萍，奚晓霞，方小敏等，1997，西北干旱-半湿润区土壤与气候间转化函数的初步研究．土壤地质(4)，中国农业出版社，12-19．
58．胡蒙育，B．Maher．中国黄土堆积的磁性记录与古降雨量重建[J]，地球科学进展，2002年6月，320-324．
59．黄成敏，龚子同．海南岛北部玄武岩上土壤发育过程的定量研究[J]，地理科学2000 20 (4)：337-342．
60．李吉均，1990，中国西北地区晚更新世以来环境变迁模式．第四纪研究，(3)：197～204
61．李吉均，方小敏，1998，青藏高原隆起与环境变化研究，科学通报，43(15)：1569～1574
62．李吉均，方小敏，潘宝田等，2001，新生代晚期青藏高原强烈隆升极其对周边环境的影响。第四纪研究，21(5)：381-391
63．李吉均．青藏高原的地貌演化与亚洲季风[J]，海洋地质与第四纪地质，1999年2月，1-10．
64．潘保田，王建民，1999，末次间冰期以来青藏高原东部季风演化的黄土沉积记录，第四纪研究，(3)：328-335
65．潘保田，邬光剑，王义祥．2000，祁连山东段沙沟河阶地的年代与成因．科学通报，45(24)：2669～2675
66．潘保田，王均平，高红山等，2005，从三门峡黄河阶地的年代看黄河何时东流入海．自然科学进展，15(6)：700-705．
67．李力，孙有斌，鹿化煜等，1998，末次间冰期黄土高原粉尘事件及其与北大西洋寒冷事件的对比．科学通报，43(1)：90～93
68．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年5月，153-159．
69．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．
70．刘东生，安芷生，陈明扬等，1996，最近0.6Ma南北半球古气候对比初探，中 国科学，26(2)：97-102
71．刘东生等，黄土与环境[M]，1985年，北京：科学出版社．
72．刘连文，陈骏，陈旸，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．
73．刘晓东，李力，安芷生，2001，青藏高原隆升与欧亚大陆及北非的干旱化，第四纪研究，21(2)：114-120
74．刘晓东，鹿化煜，安芷生，1999，利用黄土沉积速率与粒度的相关性建立黄土系列年龄的新方法，沉积学报，17(1)：145-148．
75．吴艳宏，李世杰．湖泊沉积物色度在短尺度古气候研究中的应用地球科学进展．2004，19(5)：789-792。
77．卢升高．亚热带土壤的磁性与氧化铁矿物学及其环境意义[D]．杭州：浙江大学，1998．
78．卢演俦，1987，黄土地层中CaCO_3含量变化与更新世气候旋回，地质科学，2，122～131
79．鹿化煜，安芷生，1997，前处理方法对黄土沉积物粒度测量影响的实验研究．科学通报，42：2535—2538
80．鹿化煜，安芷生，1998，黄土高原黄土粒度组成的古气候意义，中国科学(D辑)28(3)：278-283
81．鹿化煜，安芷生，J．Vandenberghe等，1997，洛川黄土地层定年的一个模式及其初步应用，沉积学报，15(3)：150-152
82．鹿化煜，马海洲，潭红兵等，2001，西宁黄土堆积记录的最近13万年高原季风气候变化，第四纪研究，21(5)：416-425
83．吕厚远，郭正堂，吴乃琴，1996，黄土高原和南海陆架古季风演变的生物记录与Heinrich事件．第四纪研究，(1)，11～20
84．吕厚远，韩家懋，吴乃琴等，1994，中国现代土壤磁化率分析极其古气候意义．中国科学(D辑)，24：1290～1297
85．吕厚远，刘东生．C3，C4植物及燃烧对土壤磁化率的影响[J]，中国科学，D辑，2001，31[1]：43-53．
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