贵州安顺三岔河土壤剖面地球化学特征反映的3000y来环境变化
|
摘要
一个地区植被覆盖情况不仅与区域气候变化息息相关,也与人类活动的影响密切相关。利用土壤剖面的地球化学信息获取有关气候变化的规律,能一定程度上了解岩溶地区石漠化形成和发展的过程。贵州位于全球最大的岩溶生态系统——中国西南岩溶生态系统的中心,脆弱的生态环境影响了当地经济的发展。了解贵州地区植被变化情况中的自然因素和人类施加的影响,有利于我们更好地认识区域脆弱生态系统的形成机理。
本文以贵州安顺三岔河土壤剖面为主要研究对象,探讨土壤中有机碳、氮的稳定同位素以及元素地球化学特征,以碳氮同位素研究为主,揭示土壤剖面反映的晚全新世以来的植被和气候的变化情况。经过初步研究得到了一下几点结论：
(1)Mg、Ca、Sr元素在土壤剖面中明显的淋溶和淀积作用反映了土壤剖面在淀积层(B层)基本没有受到外界的影响。土壤剖面中其他的元素较好的相关性,揭示各种元素的地球化学性质。土壤剖面中在距离顶部27cm处的重金属的富集点,反映了人类活动(开矿及耕作)对重金属富集与向下迁移现象的影响。
(2)结合土壤剖面中不同层次元素含量的变化,我们可以根据定年结果,建立比较可靠的年龄标尺。同时考虑到碳酸盐地区土壤在形成过程中,生物会吸收古老的碳酸盐溶解而来CO2合成有机物,而古老的碳酸盐中14C活度为0,这样使得有机碳定年结果偏老,为了建立可靠的年龄标尺,我们在考虑这一影响后,大致把土壤的年龄向年轻的方向校正400y。这样土壤剖面的沉积时段大约是从现今至3300 yr BP,形成于晚全新世。
(3)土壤剖面C／N比值说明了土壤中的有机物来源为陆相植物为主,土壤中的的δ13Corg指示了研究地区整个晚全新世的植被都以C3植物为主；剖面中22cm以上的δ15Norg值偏高反映了土壤上部受到了粪肥的影响,137cm以下的δ15Norg和δ13Corg值的不规律性反映了受到河流季节性涨水的影响,而这之间的δ15Norg值的范围基本反映了天然土壤的有机氮同位素特征,并且δ13Corg、δ15Norg变化趋势基本一致,说明δ13Corg、δ15Norg都来源于植被分解产生的有机物。
(4)δ13Corg、δ15Norg在3300 yr BP到2400 yr BP偏轻反映了研究地区植被以C3植物为主和中全新世温暖湿润的气候特点。δ13Corg、δ15Norg从2800 yr BP到2400 yr BP之间变化显示了研究区域从全新世中期向晚全新世过渡时期,夏季风逐渐减弱,气候逐渐变得干冷。从2400 yrBP到1500 yr BP,δ13Corg和δ15Norg变重也指示了晚全新世干冷的环境。
(5)1500 yr BP至今,δ13Corg和δ15Norg的逐渐迅速变重反映了人类活动和气候条件的综合影响。特别是在500 yr BP(公元1400)之后δ13Corg的偏高,是与历史上明朝云贵历史上大规模的移民活动有关,人口的大幅度增长造成对住所农田等方面的需求,从而对当地的植被造成一定的破坏。
(6)土壤剖面的δ13Corg记录能够可靠的反映研究地区晚全新世的植被和气候变化情况,与织金洞750 yr BP年后的洞穴沉积物中δ13C有较好的对比,这说明了土壤剖面中δ13Corg记录反映了人类活动的影响。而与董哥洞石笋中δ13C的对比说明了气候环境和人类活动的影响在贵州中部与南部存在差异。并且在研究中,除了考虑自然因素对区域植被、生态环境的影响外,我们必须考虑人类活动对区域环境变化的影响,这样才能为综合治理岩溶地区脆弱生态系统提出建议。
The vegetation coverage in Karst area can reflect the severity of karst rocky desertification and we can also understand the forming and developing process of rocky desertification in karst area. As the local vegetation coverage is closely related to the regional climate changes, the regular rules of these changes can be obtained. Guizhou is located in the center of Southwest China karst ecosystem, which is the world's largest karst ecosystem. The fragile eco-environment restricted the local economic development. Understanding the natural factors and artificial influence in the changes of vegetation coverage in Guizhou will help us realize the mechanism of fragile ecosystems.
The soil profiles of Sancha River in Anshun Guizhou are the main studying objects. We discussed their stable isotopes (δ13Corg、δ15Norg)and elemental geochemistry characteristics, in order to unveil vegetation and climate changes which are reflected by soil profile in the late Holocene. Then, we come up with the following conclusions:
(1)The leaching and deposition of Mg, Ca, Sr in the soil profile clearly reflected that the deposition layer (B layer) has not been influenced on the whole. The correlation of other elements in the soil profiles reflects the geochemical characteristics of various elements. This outstanding peak of high concentrations at a distance of 27cm from the top probably reflects a event caused by human activity and transfer of heavy metals in the area.
(2)Considering element changes in different levels of soil profiles, we can use dating results to establish a more reliable time scale. During the formation process of soil carbonates, organism would absorb CO2 from old carbonate dissolution to synthesize organic substance, while the 14C activity in ancient carbonate is 0, which makes organic carbon dating results ofδ13Corg older. In order to establish a reliable time scale, and considering this influence, we pushed forward the age of the soil about 400y. Then the deposition of soil profile is approximately from Oyr BP to 3300yr BP, formed in the late Holocene.
(3)The C/N ratio of soil profile illustrates the main sources of organic matter is terrestrial plant-based.δ13Corg values of the soil profile indicate that the C3 plant was the dominant vegetation during the late Holocene in the studied area. Theδ15N values of the part above the 22 cm line strongly reflect contamination of sewage fertilizer which had nitrogen isotopic enrichment, but the irregularity of theδ13Corg and 815NOrg values of the part below the 137 cm line may reflect the influence of seasonal swelling of the river. And theδ15Norg values of the part between 22 cm and 137 cm lines reflect that the soil profile is of natural soil.813Corg andδ15Norg values have similar variation trend, demonstrating thatδ13Corg andδ15Norg are all from the organic matters of decomposed plants.
(4)The value ofδ13Corg and 815Norg is lighter in 3300 yr BP to 2400 yr BP, which indicates that the C3 plant was dominant vegetation during that time in studied area. Theδ13Corg andδ15Norg values from 2800 yr BP to 2400 yr BP reflect that the monsoon weakened gradually and the climate turned cold and dry, which happened during the transition time from mid-Holocene to late Holocene. The heavier values ofδ13Corg andδ15Norg from 2400 yr BP to 1500 yr BP reflect the cold and dry environment in late Holocene.
(5) From 1500 yr BP to 0 yr BP, the values ofδ13Corg andδ15Norg increased gradually even faster, which reflect the dual effects of human activity and climatic conditions. Especially after 500 yr BP, the value ofδ13Corg gets much heavier because of the massive immigration in Ming dynasty in central-western Guizhou. And the greatly increasing population combined with the demands of house and farmland, led to the damage of local vegetation.
(6) The record ofδ13Corg can reliably reflect the vegetation and climate changes of late Holocene in the studied area. What's more, the good comparision with the value of theδ13C of the stalagmite records of Zhijin cave after 750 yr BP indicate the value ofδ13Corg reflects the impact of human activity. Compared with the stalagmite records of Dongge cave, the value ofδ13Corg in soil profile makes a good record of the changes in vegetation, climate and environment. The influence of human activities on the regional environmental changes must be considered, so as to give constructive advice about integrated management of karst region's fragile eco-system.
本文以贵州安顺三岔河土壤剖面为主要研究对象,探讨土壤中有机碳、氮的稳定同位素以及元素地球化学特征,以碳氮同位素研究为主,揭示土壤剖面反映的晚全新世以来的植被和气候的变化情况。经过初步研究得到了一下几点结论：
(1)Mg、Ca、Sr元素在土壤剖面中明显的淋溶和淀积作用反映了土壤剖面在淀积层(B层)基本没有受到外界的影响。土壤剖面中其他的元素较好的相关性,揭示各种元素的地球化学性质。土壤剖面中在距离顶部27cm处的重金属的富集点,反映了人类活动(开矿及耕作)对重金属富集与向下迁移现象的影响。
(2)结合土壤剖面中不同层次元素含量的变化,我们可以根据定年结果,建立比较可靠的年龄标尺。同时考虑到碳酸盐地区土壤在形成过程中,生物会吸收古老的碳酸盐溶解而来CO2合成有机物,而古老的碳酸盐中14C活度为0,这样使得有机碳定年结果偏老,为了建立可靠的年龄标尺,我们在考虑这一影响后,大致把土壤的年龄向年轻的方向校正400y。这样土壤剖面的沉积时段大约是从现今至3300 yr BP,形成于晚全新世。
(3)土壤剖面C／N比值说明了土壤中的有机物来源为陆相植物为主,土壤中的的δ13Corg指示了研究地区整个晚全新世的植被都以C3植物为主；剖面中22cm以上的δ15Norg值偏高反映了土壤上部受到了粪肥的影响,137cm以下的δ15Norg和δ13Corg值的不规律性反映了受到河流季节性涨水的影响,而这之间的δ15Norg值的范围基本反映了天然土壤的有机氮同位素特征,并且δ13Corg、δ15Norg变化趋势基本一致,说明δ13Corg、δ15Norg都来源于植被分解产生的有机物。
(4)δ13Corg、δ15Norg在3300 yr BP到2400 yr BP偏轻反映了研究地区植被以C3植物为主和中全新世温暖湿润的气候特点。δ13Corg、δ15Norg从2800 yr BP到2400 yr BP之间变化显示了研究区域从全新世中期向晚全新世过渡时期,夏季风逐渐减弱,气候逐渐变得干冷。从2400 yrBP到1500 yr BP,δ13Corg和δ15Norg变重也指示了晚全新世干冷的环境。
(5)1500 yr BP至今,δ13Corg和δ15Norg的逐渐迅速变重反映了人类活动和气候条件的综合影响。特别是在500 yr BP(公元1400)之后δ13Corg的偏高,是与历史上明朝云贵历史上大规模的移民活动有关,人口的大幅度增长造成对住所农田等方面的需求,从而对当地的植被造成一定的破坏。
(6)土壤剖面的δ13Corg记录能够可靠的反映研究地区晚全新世的植被和气候变化情况,与织金洞750 yr BP年后的洞穴沉积物中δ13C有较好的对比,这说明了土壤剖面中δ13Corg记录反映了人类活动的影响。而与董哥洞石笋中δ13C的对比说明了气候环境和人类活动的影响在贵州中部与南部存在差异。并且在研究中,除了考虑自然因素对区域植被、生态环境的影响外,我们必须考虑人类活动对区域环境变化的影响,这样才能为综合治理岩溶地区脆弱生态系统提出建议。
The vegetation coverage in Karst area can reflect the severity of karst rocky desertification and we can also understand the forming and developing process of rocky desertification in karst area. As the local vegetation coverage is closely related to the regional climate changes, the regular rules of these changes can be obtained. Guizhou is located in the center of Southwest China karst ecosystem, which is the world's largest karst ecosystem. The fragile eco-environment restricted the local economic development. Understanding the natural factors and artificial influence in the changes of vegetation coverage in Guizhou will help us realize the mechanism of fragile ecosystems.
The soil profiles of Sancha River in Anshun Guizhou are the main studying objects. We discussed their stable isotopes (δ13Corg、δ15Norg)and elemental geochemistry characteristics, in order to unveil vegetation and climate changes which are reflected by soil profile in the late Holocene. Then, we come up with the following conclusions:
(1)The leaching and deposition of Mg, Ca, Sr in the soil profile clearly reflected that the deposition layer (B layer) has not been influenced on the whole. The correlation of other elements in the soil profiles reflects the geochemical characteristics of various elements. This outstanding peak of high concentrations at a distance of 27cm from the top probably reflects a event caused by human activity and transfer of heavy metals in the area.
(2)Considering element changes in different levels of soil profiles, we can use dating results to establish a more reliable time scale. During the formation process of soil carbonates, organism would absorb CO2 from old carbonate dissolution to synthesize organic substance, while the 14C activity in ancient carbonate is 0, which makes organic carbon dating results ofδ13Corg older. In order to establish a reliable time scale, and considering this influence, we pushed forward the age of the soil about 400y. Then the deposition of soil profile is approximately from Oyr BP to 3300yr BP, formed in the late Holocene.
(3)The C/N ratio of soil profile illustrates the main sources of organic matter is terrestrial plant-based.δ13Corg values of the soil profile indicate that the C3 plant was the dominant vegetation during the late Holocene in the studied area. Theδ15N values of the part above the 22 cm line strongly reflect contamination of sewage fertilizer which had nitrogen isotopic enrichment, but the irregularity of theδ13Corg and 815NOrg values of the part below the 137 cm line may reflect the influence of seasonal swelling of the river. And theδ15Norg values of the part between 22 cm and 137 cm lines reflect that the soil profile is of natural soil.813Corg andδ15Norg values have similar variation trend, demonstrating thatδ13Corg andδ15Norg are all from the organic matters of decomposed plants.
(4)The value ofδ13Corg and 815Norg is lighter in 3300 yr BP to 2400 yr BP, which indicates that the C3 plant was dominant vegetation during that time in studied area. Theδ13Corg andδ15Norg values from 2800 yr BP to 2400 yr BP reflect that the monsoon weakened gradually and the climate turned cold and dry, which happened during the transition time from mid-Holocene to late Holocene. The heavier values ofδ13Corg andδ15Norg from 2400 yr BP to 1500 yr BP reflect the cold and dry environment in late Holocene.
(5) From 1500 yr BP to 0 yr BP, the values ofδ13Corg andδ15Norg increased gradually even faster, which reflect the dual effects of human activity and climatic conditions. Especially after 500 yr BP, the value ofδ13Corg gets much heavier because of the massive immigration in Ming dynasty in central-western Guizhou. And the greatly increasing population combined with the demands of house and farmland, led to the damage of local vegetation.
(6) The record ofδ13Corg can reliably reflect the vegetation and climate changes of late Holocene in the studied area. What's more, the good comparision with the value of theδ13C of the stalagmite records of Zhijin cave after 750 yr BP indicate the value ofδ13Corg reflects the impact of human activity. Compared with the stalagmite records of Dongge cave, the value ofδ13Corg in soil profile makes a good record of the changes in vegetation, climate and environment. The influence of human activities on the regional environmental changes must be considered, so as to give constructive advice about integrated management of karst region's fragile eco-system.
引文
Ambrose S H, Sikes N E. Soil carbon isotope evidence for Holocene habitat change in the Kenya rift valley [J].Science,1991,253:1402～1405.
An Zhisheng, Stephen C P, Zhou Weijian, et al.Episode of strengthened summer monsoon climate of Younger Dryas age on the Loess Plateau of Central China. Quaternary Research,1993,39(1):45～54
Arnold J R, Libby W F. Age determinations by radiocarbon content:Checks with samples of known age.Science.1949,110:678～680
Boutt TW. Stable Carbon Rations of Natural Materials.San Diego:Accdemic Press, 1991:173-185
Cao Yachen, Sun GuoQing, Xin GuanXi, Xu Hua. Natural abundance of15N in Main N-containing chemical fertilizers of China[J].Pedosphere,1991,1(4):377-382
Cerling T E, Quade J, Wang Y, et al.Carbon isotopes in soil and paleosols as ecologic and paleoecologic indicators. Nature,1989,341:138～139
Cinfuentes L A, Coffins R B, et al.Isotopic and elementalvartions of Carbon and nitrogen in amangrove estuary.Estuarine, Coastaland and Sceience,1996,43: 781～800
Ding Zhongli, Yu zhiwei, Rutter N W, et al. Towards an orbital time scale for Chinese loess deposits. Quaternary Sciences Review,1994,13:39～70
Genty D, Massault M, et al. Dead carbon in stalagmites:carbonate bedrock paleodissolution vs. ageing of soil organic matter.Implications for δ13C variations in speleothems. Geochimica et Cosmochimica Acta,2001,65(20):3443～3457
Gorlach U, Candelone J P, Boutron C, et al. Changes in heavy metal concent ration in Greenland snow during the past twenty three years. In:J G Farmer (ed.).Heavy metals in the environment. Vol 1 CEP Consultants,Edinburgh.1991.74～01
Michael Zech, Roland Zech, Bruno Glaser. A 240,000-year stable carbon and nitrogen isotope record from a loess-like palaeosol sequence in the Tumara Valley, Northeast Siberia. Chemical Geology,2007,242:307～318
Minagawa M, Wada E. Stepwise enrichment of 15N along food chains:further evidence and the relation between 815N and animal age. Geochim Cosmochim Acta,1984, 48:1135～1140
Kreitler, C.W. Nitrogen-isotope rations studies of soils and groundwater nitrate from alluvial fan aquifers in Texas. Jouranl of Hydrology,1979,(42):147-170
Ku, T L, Li, H C.Speleothems as high-resolution paleoenvironment Archives:Records from northeastern China. Proceedings of the Indian Academy of Sciences.Earth and Planetary Sciences.1998,(107):321～330
Levin I, Graul R, Trivett NBA. Long-term observations of at-mospheric CO2 and carbon isotopes at continental sites in Ger-many. Tellus,1995,47B:23～24
Robock A, Free M,The volcanic record in ice core for the past 2000 years. Climatic variation and forcing mechanism s of the last 2000years.New York. Springer-Verlag,1996:533～546
Stuiver M, Reimer P J, Bard E, et al.,Intca198 radiocarbon age alibration,24000-0 cal BP.Radiocarbon,1998,40(3):1041～1083
Yuan, D.,Cheng, H.,Edwards, R.L.,et al.,2004.Timing, duration, and transitions of the last interglacial Asian monsoon. Science 304,575-578.
H D 福斯.土壤科学原理[M].北京：农业出版社,1984.
安芷生,王俊达,李华梅.洛川黄土剖面的古地磁研究.地球化学,1977,(4)：239～249
安芷生,Porter S,Kukla G等.最近13万年黄土高原季风变化的磁化率证据.科学通报,1990,35(7)：529～532
安顺市志地方志编纂委员会.安顺市志.贵阳：贵州人民出版社,1995
陈祖拥,刘方等.贵州中部喀斯特森林退化过程中土壤酶活性的变化.贵州农业科学,2009.37(2)：47～50
蔡演军,彭子成,W.Beck等.洞穴次生碳酸盐中“死碳”对14C法测年的影响.科学通报,2005.50(5)：459～463
蔡演军,彭子成,安芷生等.贵州七星洞全新世石笋的氧同位素记录及其指示的季风气候变化.科学通报,2001.46(16)：1398～1402
丁仲礼,任剑璋.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),1996,26(5)：387～391
高强,中国南方喀斯特世界自然遗产地旅游环境承载力与可持续发展管理模式研究.贵阳师范大学硕士论文.2008
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,2000,20(1)：41～55
顾兆炎,刘强,许冰等.气候变化对黄土高原末次盛冰期以来的C3／C4植物相对丰度的控制.科学通报,2003,48(13)：1458～1464
胡超涌,黄俊华,方念乔,等.2002.湖北清江洞穴石笋双波长反射光谱特征及其古气候意义.第四纪研究,22：468-473
李春园,王先彬,文启彬,等.黄土沉积物中碳酸盐的碳、氧同位素组成特征与古气 候.中国科学(B辑),1995,25(30)：318～323
李红春,顾德隆,D. Paulsen,等.2000.陕南石笋稳定同位素的古气候和古季风信息.地震地质,22(增刊)：63-78
李红春,顾德隆,Lowell D Scott,等.北京石花洞石笋500年来的δ13C记录与古气候变化及大气CO2浓度变化的关系.中国岩溶,1997b.16(4)：285-295.
李红春,顾德隆,Lowell D Scott,等.高分辨率洞穴石笋稳定同位素应用之三-京津地区500 a来的气候变化-δ18O记录.中国科学(D辑),1998a.28(2)：181-186
李红春,顾德隆,陈文寄,等.利用洞穴石笋的δ18O和δ13C重建3000a以来北京地区古气候和古环境——石花洞研究系列之三.地震地质,1997a.19(1)：77-86
李红春,顾德隆,陈文寄,等.高分辨率洞穴石笋中稳定同位素应用——北京元大都建立后对森林资源的破坏-δ13C记录.地质论评,1998b.44(5)：456-463
李红春.全新世中期以来贵州生态环境及石漠化演变格局——石笋记录研究.国家自然科学基金项目申请书.2006
李亮亮,张大庚,依艳丽,等.葫芦岛市连山区龙港区土壤重金属垂直分布与迁移特征.安徽农业科学,2007,35(13)：3916～3918
李瑞玲,王世杰,张殿发,等.贵州喀斯特地区生态环境恶化的人为因素分析.矿物岩石地球化学通报,2002,21(1)；42～47
李阳兵,王世杰,李瑞玲,等.花江喀斯特峡谷地区石漠化成因初探.水文地质工程地质,2004b.(6)：37～42
李阳兵,王世杰,容丽.西南岩溶山地石漠化生态恢复研究展望.生态学杂志,2004a.23(6)：84～88
李俊云,李红春,刘子琦,等.贵州中西部洞穴水系与碳酸钙沉积物的Mg／Sr比值和地球化学特征.中国岩溶,2006.25(3)：177～186
林本海,刘荣谟.最近800 ka黄土高原夏季风变迁的稳定同位素证据.科学通报,1992,18：1691～1693
楼银林,张中俊,伍钢,等.镉在不同土壤和蔬菜中残留规律研究.环境科学学报,1990,10(2)：153-159
刘东生等.第四集环境,北京：科学出版社,1997
刘光锈,沈永平,王睿等.孢粉记录揭示的7万年以来若尔盖地区的气候变化.冰川冻土1995,17(2)：132-137
刘良梧,茅昂江.Radiocarbon Ages of Soils in China.土壤学报,2001,38(4)：506～513
刘秀铭,刘东生,John S.中国黄土磁性矿物特征及其古气候意义.第四纪研究,1993,(3)：282～287
刘卫国,宁有丰,安芷生等.黄土高原现代土壤和古土壤有机碳同位素对植被的响 应.中国科学D辑,2002,32(10)：830～836
刘子琦,李红春,徐晓梅,等.贵州中西部洞穴水系与碳酸钙的稳定同位素意义.地质论评,2007,53(2)：233～241
刘子琦.利用洞穴体系地球化学指标研究贵州中西部近现代石漠化成因及趋势.西南大学博士论文.2008
吕后远,吴乃琴,刘东生等.最近15万年来宝鸡剖面植物硅酸体组合反映的季节性气候变化.中国科学D辑,1996,26(2)：131～136
孙湘君,宋长青,王琒瑜等.黄土高原10万年以来的植被——陕西渭南黄土剖面的花粉记录.科学通报,1995,40(13)：1222～1224
史培军,宋长青,景贵飞等.加强我国土地利用覆盖变化及其对生态环境安全影响的研究——从荷兰“全球变化开放科学议”看人地系统动力学研究的发展趋势.地球科学进展,2002,17(2)：161-168.
沈承德,乔玉楼等.14C年龄测定方法的可靠性.第一次全国14C学术会议论文集.科学出版社,1984.
秦伯强,施雅风,于革.亚洲内陆湖泊在18kaBP和6kaBP的水位变化及其指示意义.科学通报,1997,42：2586～2596
施雅风,孔昭哀,王苏民等.中国全新世大暖期鼎盛阶段的气候与环境.中国科学(B),1993,865～873
屠玉麟.贵州岩溶地区森林资源现状及原因分析.人类活动与岩溶环境,北京：北京科学技术出版社.1994,40～46
万明.明代徽州汪公入黔考——兼论贵州屯堡移民社会的建构.《中国史研究》,2005,135～148
吴乃琴,D.D. Rousseau,刘东生等.110ka来洛川黄土地层中蜗牛化石记录与环境因子分析.中国科学D辑,1996,26(5)：405～410
吴旭东.重庆奉节地区古壤剖面反映的全新世以来的环境变化.西南大学硕士论文.2009
徐馨,沈志达.全新世环境.贵阳：贵州人民出版.1990,1～86
邢成起,吕德徽,董治平等.土壤年代学方法及其应用.西北地震学报,1997,19(3)：77～85
杨守业,李从先,李徐生等.长江下游下蜀黄土化学风化的地球化学研究.地球化学,2001,30(4)：402～406
杨琰,袁道先,程海,张美良等.末次冰消期亚洲季风突变事件的精确定年：以贵州衙门洞石笋为例.中国科学,2009,40(2)：199～210
肖进原.贵州岩溶植被类型的卫片影像特征及分布解译.贵州地质,1996,13(4)： 350～356
熊康宁,杜芳娟,廖婧琳,2005.喀斯特文化与生态建筑艺术.贵阳：贵州人民出版社,173.
熊康宁,黎平,周忠发等,2002.喀斯特石漠化的遥感——GIS典型研究.北京：地质出版社,1～183.
熊康宁,袁家榆,方伊,等.2007.贵州喀斯特石漠化综合防治图集.贵阳：贵州人民出版
杨明德,贵州高原喀斯特地貌结构及演化规律——喀斯特地貌与洞穴,北京：科学出版,1985
杨娟.贵州年降水量和年最大月降水量多年一遇的极值计算.贵州气象2008,32(6)：10～12
袁道先,刘再华,蒋忠诚,等.2003.碳循环与岩溶地质环境.北京：科学出版社.
袁道先,刘再华,林玉石,等.2002.中国岩溶动力系统.北京：地质出版社.
张振克,吴瑞金,王苏民,等.近8ka BP来云南洱海地区气候演化的有机碳稳定同位素记录.海洋地质与第四纪地质,1998.18(3)：23～28.
张美良,林玉石,覃嘉铭,等.黔南七星洞石笋古气候变化记录及末次间冰期终止点的确定.沉积学报,2003.21(3)：473～481.
张美良,林玉石,覃嘉铭,等.黔南洞穴石笋古气候变化记录及终止点Ⅱ的确定.中国科学,2002.32(11)：942～950.
张美良,程海,林玉石,等.贵州荔波1.5万年以来石笋高分辨率古气候环境记录.地球化学,2004,33(1)：65～77
张美良,朱晓燕,林玉石,洞穴石笋的δ13C记录研究.广西科学,2006,13(1)：48～51,57
张先恭,张富国,等.火山活动与我国旱涝、冷暖的关系.气象学报,1985,13(2)：196-207
竺可桢.中国近五千年来气候变迁的初步研究,考古学报,1972,(1)：15～38
朱照宇,王俊达,黄宝林等.红土·黄土·全球变化,第四纪研究,1995,(3)：267～277
周涛.贵州汛期河流面雨量的气候特征分析,贵州气象,2004,28(3)：14～18
周智,喻元秀,熊际翎,等.乌江流域水环境污染现状及容量与对策,贵州师范大学学报(自然科学版),2004,22(4)：42～45
织金县地方志编纂委员会.织金县志.贵阳：地方志出版社,1997
An Zhisheng, Stephen C P, Zhou Weijian, et al.Episode of strengthened summer monsoon climate of Younger Dryas age on the Loess Plateau of Central China. Quaternary Research,1993,39(1):45～54
Arnold J R, Libby W F. Age determinations by radiocarbon content:Checks with samples of known age.Science.1949,110:678～680
Boutt TW. Stable Carbon Rations of Natural Materials.San Diego:Accdemic Press, 1991:173-185
Cao Yachen, Sun GuoQing, Xin GuanXi, Xu Hua. Natural abundance of15N in Main N-containing chemical fertilizers of China[J].Pedosphere,1991,1(4):377-382
Cerling T E, Quade J, Wang Y, et al.Carbon isotopes in soil and paleosols as ecologic and paleoecologic indicators. Nature,1989,341:138～139
Cinfuentes L A, Coffins R B, et al.Isotopic and elementalvartions of Carbon and nitrogen in amangrove estuary.Estuarine, Coastaland and Sceience,1996,43: 781～800
Ding Zhongli, Yu zhiwei, Rutter N W, et al. Towards an orbital time scale for Chinese loess deposits. Quaternary Sciences Review,1994,13:39～70
Genty D, Massault M, et al. Dead carbon in stalagmites:carbonate bedrock paleodissolution vs. ageing of soil organic matter.Implications for δ13C variations in speleothems. Geochimica et Cosmochimica Acta,2001,65(20):3443～3457
Gorlach U, Candelone J P, Boutron C, et al. Changes in heavy metal concent ration in Greenland snow during the past twenty three years. In:J G Farmer (ed.).Heavy metals in the environment. Vol 1 CEP Consultants,Edinburgh.1991.74～01
Michael Zech, Roland Zech, Bruno Glaser. A 240,000-year stable carbon and nitrogen isotope record from a loess-like palaeosol sequence in the Tumara Valley, Northeast Siberia. Chemical Geology,2007,242:307～318
Minagawa M, Wada E. Stepwise enrichment of 15N along food chains:further evidence and the relation between 815N and animal age. Geochim Cosmochim Acta,1984, 48:1135～1140
Kreitler, C.W. Nitrogen-isotope rations studies of soils and groundwater nitrate from alluvial fan aquifers in Texas. Jouranl of Hydrology,1979,(42):147-170
Ku, T L, Li, H C.Speleothems as high-resolution paleoenvironment Archives:Records from northeastern China. Proceedings of the Indian Academy of Sciences.Earth and Planetary Sciences.1998,(107):321～330
Levin I, Graul R, Trivett NBA. Long-term observations of at-mospheric CO2 and carbon isotopes at continental sites in Ger-many. Tellus,1995,47B:23～24
Robock A, Free M,The volcanic record in ice core for the past 2000 years. Climatic variation and forcing mechanism s of the last 2000years.New York. Springer-Verlag,1996:533～546
Stuiver M, Reimer P J, Bard E, et al.,Intca198 radiocarbon age alibration,24000-0 cal BP.Radiocarbon,1998,40(3):1041～1083
Yuan, D.,Cheng, H.,Edwards, R.L.,et al.,2004.Timing, duration, and transitions of the last interglacial Asian monsoon. Science 304,575-578.
H D 福斯.土壤科学原理[M].北京：农业出版社,1984.
安芷生,王俊达,李华梅.洛川黄土剖面的古地磁研究.地球化学,1977,(4)：239～249
安芷生,Porter S,Kukla G等.最近13万年黄土高原季风变化的磁化率证据.科学通报,1990,35(7)：529～532
安顺市志地方志编纂委员会.安顺市志.贵阳：贵州人民出版社,1995
陈祖拥,刘方等.贵州中部喀斯特森林退化过程中土壤酶活性的变化.贵州农业科学,2009.37(2)：47～50
蔡演军,彭子成,W.Beck等.洞穴次生碳酸盐中“死碳”对14C法测年的影响.科学通报,2005.50(5)：459～463
蔡演军,彭子成,安芷生等.贵州七星洞全新世石笋的氧同位素记录及其指示的季风气候变化.科学通报,2001.46(16)：1398～1402
丁仲礼,任剑璋.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),1996,26(5)：387～391
高强,中国南方喀斯特世界自然遗产地旅游环境承载力与可持续发展管理模式研究.贵阳师范大学硕士论文.2008
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,2000,20(1)：41～55
顾兆炎,刘强,许冰等.气候变化对黄土高原末次盛冰期以来的C3／C4植物相对丰度的控制.科学通报,2003,48(13)：1458～1464
胡超涌,黄俊华,方念乔,等.2002.湖北清江洞穴石笋双波长反射光谱特征及其古气候意义.第四纪研究,22：468-473
李春园,王先彬,文启彬,等.黄土沉积物中碳酸盐的碳、氧同位素组成特征与古气 候.中国科学(B辑),1995,25(30)：318～323
李红春,顾德隆,D. Paulsen,等.2000.陕南石笋稳定同位素的古气候和古季风信息.地震地质,22(增刊)：63-78
李红春,顾德隆,Lowell D Scott,等.北京石花洞石笋500年来的δ13C记录与古气候变化及大气CO2浓度变化的关系.中国岩溶,1997b.16(4)：285-295.
李红春,顾德隆,Lowell D Scott,等.高分辨率洞穴石笋稳定同位素应用之三-京津地区500 a来的气候变化-δ18O记录.中国科学(D辑),1998a.28(2)：181-186
李红春,顾德隆,陈文寄,等.利用洞穴石笋的δ18O和δ13C重建3000a以来北京地区古气候和古环境——石花洞研究系列之三.地震地质,1997a.19(1)：77-86
李红春,顾德隆,陈文寄,等.高分辨率洞穴石笋中稳定同位素应用——北京元大都建立后对森林资源的破坏-δ13C记录.地质论评,1998b.44(5)：456-463
李红春.全新世中期以来贵州生态环境及石漠化演变格局——石笋记录研究.国家自然科学基金项目申请书.2006
李亮亮,张大庚,依艳丽,等.葫芦岛市连山区龙港区土壤重金属垂直分布与迁移特征.安徽农业科学,2007,35(13)：3916～3918
李瑞玲,王世杰,张殿发,等.贵州喀斯特地区生态环境恶化的人为因素分析.矿物岩石地球化学通报,2002,21(1)；42～47
李阳兵,王世杰,李瑞玲,等.花江喀斯特峡谷地区石漠化成因初探.水文地质工程地质,2004b.(6)：37～42
李阳兵,王世杰,容丽.西南岩溶山地石漠化生态恢复研究展望.生态学杂志,2004a.23(6)：84～88
李俊云,李红春,刘子琦,等.贵州中西部洞穴水系与碳酸钙沉积物的Mg／Sr比值和地球化学特征.中国岩溶,2006.25(3)：177～186
林本海,刘荣谟.最近800 ka黄土高原夏季风变迁的稳定同位素证据.科学通报,1992,18：1691～1693
楼银林,张中俊,伍钢,等.镉在不同土壤和蔬菜中残留规律研究.环境科学学报,1990,10(2)：153-159
刘东生等.第四集环境,北京：科学出版社,1997
刘光锈,沈永平,王睿等.孢粉记录揭示的7万年以来若尔盖地区的气候变化.冰川冻土1995,17(2)：132-137
刘良梧,茅昂江.Radiocarbon Ages of Soils in China.土壤学报,2001,38(4)：506～513
刘秀铭,刘东生,John S.中国黄土磁性矿物特征及其古气候意义.第四纪研究,1993,(3)：282～287
刘卫国,宁有丰,安芷生等.黄土高原现代土壤和古土壤有机碳同位素对植被的响 应.中国科学D辑,2002,32(10)：830～836
刘子琦,李红春,徐晓梅,等.贵州中西部洞穴水系与碳酸钙的稳定同位素意义.地质论评,2007,53(2)：233～241
刘子琦.利用洞穴体系地球化学指标研究贵州中西部近现代石漠化成因及趋势.西南大学博士论文.2008
吕后远,吴乃琴,刘东生等.最近15万年来宝鸡剖面植物硅酸体组合反映的季节性气候变化.中国科学D辑,1996,26(2)：131～136
孙湘君,宋长青,王琒瑜等.黄土高原10万年以来的植被——陕西渭南黄土剖面的花粉记录.科学通报,1995,40(13)：1222～1224
史培军,宋长青,景贵飞等.加强我国土地利用覆盖变化及其对生态环境安全影响的研究——从荷兰“全球变化开放科学议”看人地系统动力学研究的发展趋势.地球科学进展,2002,17(2)：161-168.
沈承德,乔玉楼等.14C年龄测定方法的可靠性.第一次全国14C学术会议论文集.科学出版社,1984.
秦伯强,施雅风,于革.亚洲内陆湖泊在18kaBP和6kaBP的水位变化及其指示意义.科学通报,1997,42：2586～2596
施雅风,孔昭哀,王苏民等.中国全新世大暖期鼎盛阶段的气候与环境.中国科学(B),1993,865～873
屠玉麟.贵州岩溶地区森林资源现状及原因分析.人类活动与岩溶环境,北京：北京科学技术出版社.1994,40～46
万明.明代徽州汪公入黔考——兼论贵州屯堡移民社会的建构.《中国史研究》,2005,135～148
吴乃琴,D.D. Rousseau,刘东生等.110ka来洛川黄土地层中蜗牛化石记录与环境因子分析.中国科学D辑,1996,26(5)：405～410
吴旭东.重庆奉节地区古壤剖面反映的全新世以来的环境变化.西南大学硕士论文.2009
徐馨,沈志达.全新世环境.贵阳：贵州人民出版.1990,1～86
邢成起,吕德徽,董治平等.土壤年代学方法及其应用.西北地震学报,1997,19(3)：77～85
杨守业,李从先,李徐生等.长江下游下蜀黄土化学风化的地球化学研究.地球化学,2001,30(4)：402～406
杨琰,袁道先,程海,张美良等.末次冰消期亚洲季风突变事件的精确定年：以贵州衙门洞石笋为例.中国科学,2009,40(2)：199～210
肖进原.贵州岩溶植被类型的卫片影像特征及分布解译.贵州地质,1996,13(4)： 350～356
熊康宁,杜芳娟,廖婧琳,2005.喀斯特文化与生态建筑艺术.贵阳：贵州人民出版社,173.
熊康宁,黎平,周忠发等,2002.喀斯特石漠化的遥感——GIS典型研究.北京：地质出版社,1～183.
熊康宁,袁家榆,方伊,等.2007.贵州喀斯特石漠化综合防治图集.贵阳：贵州人民出版
杨明德,贵州高原喀斯特地貌结构及演化规律——喀斯特地貌与洞穴,北京：科学出版,1985
杨娟.贵州年降水量和年最大月降水量多年一遇的极值计算.贵州气象2008,32(6)：10～12
袁道先,刘再华,蒋忠诚,等.2003.碳循环与岩溶地质环境.北京：科学出版社.
袁道先,刘再华,林玉石,等.2002.中国岩溶动力系统.北京：地质出版社.
张振克,吴瑞金,王苏民,等.近8ka BP来云南洱海地区气候演化的有机碳稳定同位素记录.海洋地质与第四纪地质,1998.18(3)：23～28.
张美良,林玉石,覃嘉铭,等.黔南七星洞石笋古气候变化记录及末次间冰期终止点的确定.沉积学报,2003.21(3)：473～481.
张美良,林玉石,覃嘉铭,等.黔南洞穴石笋古气候变化记录及终止点Ⅱ的确定.中国科学,2002.32(11)：942～950.
张美良,程海,林玉石,等.贵州荔波1.5万年以来石笋高分辨率古气候环境记录.地球化学,2004,33(1)：65～77
张美良,朱晓燕,林玉石,洞穴石笋的δ13C记录研究.广西科学,2006,13(1)：48～51,57
张先恭,张富国,等.火山活动与我国旱涝、冷暖的关系.气象学报,1985,13(2)：196-207
竺可桢.中国近五千年来气候变迁的初步研究,考古学报,1972,(1)：15～38
朱照宇,王俊达,黄宝林等.红土·黄土·全球变化,第四纪研究,1995,(3)：267～277
周涛.贵州汛期河流面雨量的气候特征分析,贵州气象,2004,28(3)：14～18
周智,喻元秀,熊际翎,等.乌江流域水环境污染现状及容量与对策,贵州师范大学学报(自然科学版),2004,22(4)：42～45
织金县地方志编纂委员会.织金县志.贵阳：地方志出版社,1997
© 2004-2018 中国地质图书馆版权所有 京ICP备05064691号 京公网安备11010802017129号 地址：北京市海淀区学院路29号 邮编：100083 电话：办公室：(+86 10)66554848；文献借阅、咨询服务、科技查新：66554700 |