岩溶洞穴系统稳定碳同位素演化的地球化学过程及其环境意义
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摘要
稳定碳同位素作为环境替代指标已经在不同的载体上得到了广泛运用，例如树轮、泥炭、碳酸盐岩等。目前岩溶学者也逐渐开始运用洞穴次生化学沉积物中的稳定碳同位素探讨古气候环境的变迁史，例如植被的更替、大气CO_2的浓度变化等。然而由于缺乏该指标在岩溶洞穴系统中形成机理的研究，使得该环境替代指标的运用非常有限。本论文在贵州岩溶地区选择了上覆植被分别为原始森林、灌丛草坡、草坡和石漠化的凉风洞、七星洞、犀牛洞、将军洞作为研究对象，对岩溶洞穴系统稳定碳同位素的时空演化规律进行了详细的分析，得出以下几点认识：
一．洞穴系统稳定碳同位素对地表气候环境的响应
通过对4个不同生境洞穴系统的研究，认为洞穴系统稳定碳同位素可以很好地将原始森林植被同其它植被类型区分开；但是不能很好地区分植被退化的过渡类型如灌丛、草坡以及石漠化等。表明石笋的δ~(13)C值在一定情况下可以用来探讨地表植被的变化。但要做更精确的反演需要在加深机理方面的研究。
通过同一洞穴不同滴水点的对比研究，发现不同滴水点沉积物的稳定碳同位素存在差异，并且差异还比较大，表明用石笋的δ~(13)C值对古气候环境进行重建时需要慎重考虑滴水点的详细情况。在这种情况下，应该对稳定碳同位素的地球化学过程进行详细研究，尤其应该结合水化学数据对水的运移途径进行深入研究，才能合理地运用稳定碳同位素对洞顶的植被情况进行正确的反演。
洞穴滴水和塘中水DIC δ~(13)C值和月累积降雨量成相反的变化趋势；地表泉水、土壤水DIC δ~(13)C值、土壤CO_2、土壤呼吸δ~(13)C值和月累积降雨量的变化在多数时候具有一致的变化趋势。
总体而言，洞穴系统水样DIC δ~(13)C值对月平均气温的响应不是很明显。只有洞穴塘中水DIC δ~(13)C值和月平均气温成相反的变化规律；土壤呼吸CO_2 δ~(13)C值对月均温响应较为明显：月平均温度越高，土壤呼吸CO_2 δ~(13)C值越偏轻，反映了温度较高的时候土壤层中的生物活动较强烈。
二． 岩溶洞穴系统稳定碳同位素的时间演化
犀牛洞、将军洞、七星洞10月份植被δ~(13)C值样品的δ~(13)C值比7月份样品
中国科学院研究生院博士学位论文
的6’3e值偏重。
犀牛洞和将军洞土壤空气co:的6‘3c值在8月份出现了一个峰值，以前在
清镇红枫湖生态站草地土壤剖面所作的工作8月份的值也同样偏重。在6月份时，
凉风洞和七星洞存在一个较为明显的低值，与微生物和植物的强烈呼吸作用有
关。土壤呼吸气coZ的6’3c值在6月份出现了明显的低值，和土壤co:的变化
趋势一致。
4个洞穴空气coZ的6‘3c值在8、9月份有一个低值口七星洞和外界的连通
性最好，其洞穴空气co:6‘3c值随时间的变化最不明显，而凉风洞与外界的连
通性最差，洞穴空气Co:6’3C值的变化幅度最大。
土壤水Dlc的6’3c值8月份存在一个峰值，在9月份的时候存在一个低值。
七星洞地表泉水Dlc的6 13c值自6月份开始有逐渐偏重的趋势，到8月份
达到一个不甚明显的峰，这个峰值在凉风洞的表层泉中也略有体现。和土壤水比
较，地表泉水的不同点在于低值不出现在9月份，而是出现在10月份，相对而
言滞后1个月。原因可能是表层泉水所到达的深度比土壤水深，土壤强烈呼吸作
用的响应要比土壤水慢。
各个洞穴的滴水Dlc6‘3c值随时间退推移出现了不同的变化规律，可能与
滴水的来源和途径不同有关。
4个洞穴塘中水Dlc的6’3c值统一在7月份达到了最低值，之后Dlc的6
，3c值逐渐偏重。
三.岩溶洞穴系统稳定碳同位素的空间演化
植被样不同部位的6’3c值总体上逐渐偏重的顺序是皮~叶一枝、根~干，
说明植物不同部位的稳定碳同位素存在差异。随着凉风洞~七星洞~犀牛洞~将
军洞的顺序，植被6‘’c值逐渐变重，反映了地表植被由C3植物向c3十C4植物的
过渡，指示了生态环境由原始森林~石漠化方向的退化。
土壤有机碳的6 13c值基本继承地表植物6 I3c值的特征。没有发生植被更
替土壤剖面上有机碳的6‘3c值随着深度的增加逐渐偏重;植被发生了变化的土
壤剖面则可能出现与正常规律相反的变化情况。
土壤剖面上co:的6 13c值自地表向下逐渐变轻，在一定深度后大致趋于稳
定;土壤呼吸co:6’3c值位于土壤co:6’3c值的变化范围;土壤呼吸co26’3c
岩溶洞穴系统稳定碳同位素演化的地球化学过程及其环境意义
值的变化规律和植被6’3C值的变化在空间上具有一致性。
土壤水Dle的6’3e值比土壤eoZ值偏重;泉水Dxe的6’3e值比土壤水oxe
的6’3C值偏重，原因是泉水可能已经渗入到基岩层之后再出露到地表，已经混
入了部分基岩无机碳的成分。
四个研究洞穴系统盖板基岩的6’3c值变化范围大约在2一3编之间。
凉风洞和犀牛洞不同滴水点滴水的6’七值相对比较稳定，七星洞和将军洞
的变化比较大。洞穴塘中水 Dlc的6‘3c值和洞穴滴水相比明显偏重，原因为洞
穴塘中水经历了强烈的蒸发作用;滴后水比滴前水整体偏重。
从洞口往内洞穴空气co:的6’3c值逐渐偏轻，并且洞穴空气co:6”c值
继承了洞穴水样Dlc6‘3c值的变化趋势。
洞穴化学次生沉积
As substitute index of environment, stable carbon isotope has been used broadly in different records, such as tree rings, peat and carbonate rock. Nowadays scholars have gradually used stable carbon isotope of speleothem in karst caves to discuss the changing history of palaeoclimate and palaeoenvironment, such as vegetation subrogation and the change of atmospheric CO2 concentration. However, the application of index is limited owning to lack of the study about formation mechanism in karst cave system. Taking cave systems under different vegetation in guizhou karst area as study objects, this paper analyzes the spatio-temporal evolution of stable carbon isotope in karst cave system. Vegetation of Liangfeng cave, Qixing cave, Xiniu cave and Jiangjun cave are respectively origin forest, bosk, grassplot and rocky desertification. Several results have been achieved as folio wings:
1.The response of stable carbon isotope in karst cave system to surface climate and environment.
This index can distinguish origin forest from other vegetation, but cannot distinguish transitional eco-environment such as bosk, grassplot and rocky desertification. It is showed that the 13C values of stalagmite can be used to discuss the changes of vegetation to some extent and more work should be done to the study of reconstruct-mechanism.
The 13C values of speleothem under different drip in same cave are different. It showed that the detail situation of drip water should be taken into account using the 13C values of stalagmite to reconstruct palaeoclimate and palaeoenvironment. In this condition, the geochemical process of stable carbon should be studied in detail especially combined the chemical data of water. Thus the vegetation above cave can be reconstructed correctly by stable carbon isotope.
The DIC 13C values of cave drip and pond become light with precipitation increasing. The 13C values of spring water, soil water, soil CO2 and soil respired CO2 become mostly heavy with precipitation increasing.
The 13C values of cave pond and soil respired CO2 become light with air temperature increasing, because organism activity is more intensive when temperature increase.
2. The temporal evolution of stable carbon isotope in karst cave system The 13C values of plants in October are heavier than those in July.
The 8 C values of soil CO2 in Xiniu cave system and Jiangjun cave system show a peak in August. In our previous study in grassland soil profiles of Qingzhen Hongfeng Lake karst ecotope experimental station, the values are also heavier in August. In June, it is obvious lighter than other month's results in Liangfeng cave and Qixing cave, the reason is that the respiration of microorganism and plant's root is most stronger. The values of soil respired CO2 in June are lower than other month's results due to strong respiration of microorganism and plant's root.
The 13C values of cave CO2 become low in August or September. The monthly change in Qixing cave is not obvious as other caves due to better connectivity with outside and the amplitude change is the largest in Liangfeng cave because of bad connectivity with outside.
The DIC 13C values of soil water in September are lighter than other month's results and there is a peak in August in Liangfeng cave and jiangjun cave systems.
The DIC 13C values of spring in Qixing cave have become gradually heavy from June, reach a peak in August and this peak also appears in Liangfeng cave in August. Compared with soil water, the light value of spring water does not appear in September but in October. The reason maybe is that spring water has already reached deep-level, its response to soil respiration is slower than soil water.
The DIC 13C values of cave drip in different cave show different changing patterns, might be relative to different sources and different routes of drip water.
The DIC 13C values of cave pond water reach minimum in July. Later the values gradually become heavy.
3.The spatial evolution of stable carbon isotope in karst cave system.
Different part of plants
一．洞穴系统稳定碳同位素对地表气候环境的响应
通过对4个不同生境洞穴系统的研究，认为洞穴系统稳定碳同位素可以很好地将原始森林植被同其它植被类型区分开；但是不能很好地区分植被退化的过渡类型如灌丛、草坡以及石漠化等。表明石笋的δ~(13)C值在一定情况下可以用来探讨地表植被的变化。但要做更精确的反演需要在加深机理方面的研究。
通过同一洞穴不同滴水点的对比研究，发现不同滴水点沉积物的稳定碳同位素存在差异，并且差异还比较大，表明用石笋的δ~(13)C值对古气候环境进行重建时需要慎重考虑滴水点的详细情况。在这种情况下，应该对稳定碳同位素的地球化学过程进行详细研究，尤其应该结合水化学数据对水的运移途径进行深入研究，才能合理地运用稳定碳同位素对洞顶的植被情况进行正确的反演。
洞穴滴水和塘中水DIC δ~(13)C值和月累积降雨量成相反的变化趋势；地表泉水、土壤水DIC δ~(13)C值、土壤CO_2、土壤呼吸δ~(13)C值和月累积降雨量的变化在多数时候具有一致的变化趋势。
总体而言，洞穴系统水样DIC δ~(13)C值对月平均气温的响应不是很明显。只有洞穴塘中水DIC δ~(13)C值和月平均气温成相反的变化规律；土壤呼吸CO_2 δ~(13)C值对月均温响应较为明显：月平均温度越高，土壤呼吸CO_2 δ~(13)C值越偏轻，反映了温度较高的时候土壤层中的生物活动较强烈。
二． 岩溶洞穴系统稳定碳同位素的时间演化
犀牛洞、将军洞、七星洞10月份植被δ~(13)C值样品的δ~(13)C值比7月份样品
中国科学院研究生院博士学位论文
的6’3e值偏重。
犀牛洞和将军洞土壤空气co:的6‘3c值在8月份出现了一个峰值，以前在
清镇红枫湖生态站草地土壤剖面所作的工作8月份的值也同样偏重。在6月份时，
凉风洞和七星洞存在一个较为明显的低值，与微生物和植物的强烈呼吸作用有
关。土壤呼吸气coZ的6’3c值在6月份出现了明显的低值，和土壤co:的变化
趋势一致。
4个洞穴空气coZ的6‘3c值在8、9月份有一个低值口七星洞和外界的连通
性最好，其洞穴空气co:6‘3c值随时间的变化最不明显，而凉风洞与外界的连
通性最差，洞穴空气Co:6’3C值的变化幅度最大。
土壤水Dlc的6’3c值8月份存在一个峰值，在9月份的时候存在一个低值。
七星洞地表泉水Dlc的6 13c值自6月份开始有逐渐偏重的趋势，到8月份
达到一个不甚明显的峰，这个峰值在凉风洞的表层泉中也略有体现。和土壤水比
较，地表泉水的不同点在于低值不出现在9月份，而是出现在10月份，相对而
言滞后1个月。原因可能是表层泉水所到达的深度比土壤水深，土壤强烈呼吸作
用的响应要比土壤水慢。
各个洞穴的滴水Dlc6‘3c值随时间退推移出现了不同的变化规律，可能与
滴水的来源和途径不同有关。
4个洞穴塘中水Dlc的6’3c值统一在7月份达到了最低值，之后Dlc的6
，3c值逐渐偏重。
三.岩溶洞穴系统稳定碳同位素的空间演化
植被样不同部位的6’3c值总体上逐渐偏重的顺序是皮~叶一枝、根~干，
说明植物不同部位的稳定碳同位素存在差异。随着凉风洞~七星洞~犀牛洞~将
军洞的顺序，植被6‘’c值逐渐变重，反映了地表植被由C3植物向c3十C4植物的
过渡，指示了生态环境由原始森林~石漠化方向的退化。
土壤有机碳的6 13c值基本继承地表植物6 I3c值的特征。没有发生植被更
替土壤剖面上有机碳的6‘3c值随着深度的增加逐渐偏重;植被发生了变化的土
壤剖面则可能出现与正常规律相反的变化情况。
土壤剖面上co:的6 13c值自地表向下逐渐变轻，在一定深度后大致趋于稳
定;土壤呼吸co:6’3c值位于土壤co:6’3c值的变化范围;土壤呼吸co26’3c
岩溶洞穴系统稳定碳同位素演化的地球化学过程及其环境意义
值的变化规律和植被6’3C值的变化在空间上具有一致性。
土壤水Dle的6’3e值比土壤eoZ值偏重;泉水Dxe的6’3e值比土壤水oxe
的6’3C值偏重，原因是泉水可能已经渗入到基岩层之后再出露到地表，已经混
入了部分基岩无机碳的成分。
四个研究洞穴系统盖板基岩的6’3c值变化范围大约在2一3编之间。
凉风洞和犀牛洞不同滴水点滴水的6’七值相对比较稳定，七星洞和将军洞
的变化比较大。洞穴塘中水 Dlc的6‘3c值和洞穴滴水相比明显偏重，原因为洞
穴塘中水经历了强烈的蒸发作用;滴后水比滴前水整体偏重。
从洞口往内洞穴空气co:的6’3c值逐渐偏轻，并且洞穴空气co:6”c值
继承了洞穴水样Dlc6‘3c值的变化趋势。
洞穴化学次生沉积
As substitute index of environment, stable carbon isotope has been used broadly in different records, such as tree rings, peat and carbonate rock. Nowadays scholars have gradually used stable carbon isotope of speleothem in karst caves to discuss the changing history of palaeoclimate and palaeoenvironment, such as vegetation subrogation and the change of atmospheric CO2 concentration. However, the application of index is limited owning to lack of the study about formation mechanism in karst cave system. Taking cave systems under different vegetation in guizhou karst area as study objects, this paper analyzes the spatio-temporal evolution of stable carbon isotope in karst cave system. Vegetation of Liangfeng cave, Qixing cave, Xiniu cave and Jiangjun cave are respectively origin forest, bosk, grassplot and rocky desertification. Several results have been achieved as folio wings:
1.The response of stable carbon isotope in karst cave system to surface climate and environment.
This index can distinguish origin forest from other vegetation, but cannot distinguish transitional eco-environment such as bosk, grassplot and rocky desertification. It is showed that the 13C values of stalagmite can be used to discuss the changes of vegetation to some extent and more work should be done to the study of reconstruct-mechanism.
The 13C values of speleothem under different drip in same cave are different. It showed that the detail situation of drip water should be taken into account using the 13C values of stalagmite to reconstruct palaeoclimate and palaeoenvironment. In this condition, the geochemical process of stable carbon should be studied in detail especially combined the chemical data of water. Thus the vegetation above cave can be reconstructed correctly by stable carbon isotope.
The DIC 13C values of cave drip and pond become light with precipitation increasing. The 13C values of spring water, soil water, soil CO2 and soil respired CO2 become mostly heavy with precipitation increasing.
The 13C values of cave pond and soil respired CO2 become light with air temperature increasing, because organism activity is more intensive when temperature increase.
2. The temporal evolution of stable carbon isotope in karst cave system The 13C values of plants in October are heavier than those in July.
The 8 C values of soil CO2 in Xiniu cave system and Jiangjun cave system show a peak in August. In our previous study in grassland soil profiles of Qingzhen Hongfeng Lake karst ecotope experimental station, the values are also heavier in August. In June, it is obvious lighter than other month's results in Liangfeng cave and Qixing cave, the reason is that the respiration of microorganism and plant's root is most stronger. The values of soil respired CO2 in June are lower than other month's results due to strong respiration of microorganism and plant's root.
The 13C values of cave CO2 become low in August or September. The monthly change in Qixing cave is not obvious as other caves due to better connectivity with outside and the amplitude change is the largest in Liangfeng cave because of bad connectivity with outside.
The DIC 13C values of soil water in September are lighter than other month's results and there is a peak in August in Liangfeng cave and jiangjun cave systems.
The DIC 13C values of spring in Qixing cave have become gradually heavy from June, reach a peak in August and this peak also appears in Liangfeng cave in August. Compared with soil water, the light value of spring water does not appear in September but in October. The reason maybe is that spring water has already reached deep-level, its response to soil respiration is slower than soil water.
The DIC 13C values of cave drip in different cave show different changing patterns, might be relative to different sources and different routes of drip water.
The DIC 13C values of cave pond water reach minimum in July. Later the values gradually become heavy.
3.The spatial evolution of stable carbon isotope in karst cave system.
Different part of plants
引文
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