潮田河流域（岩溶）地质碳汇过程及通量估算研究
摘要
全球气候变暖,极端气候等自然灾害频繁,已经引起世界各国的注意,影响着世界各国的经济。目前很多学者认为气候变化与温室气体(主要是C02)的变化有较大的关系。自有监测数据以来,全球CO2浓度在逐年的增加,人类生存环境变化巨大。
然根据全球碳平衡,目前碳还存一个差值,这个差值被叫做遗失碳汇(missing carbon)。该遗失碳汇随着大气CO2浓度逐年的增加而在逐渐增加。目前对于碳汇的研究主要分两大块,即陆地和海洋。在研究过程中,主要从碳元素影响因子与化学物质或化学元素之间的关系、碳元素与土壤及植被的关系、碳元素在湿地、河流及海洋特征等。但最终目的就是为了寻找遗失的碳汇。
一般认为,碳酸盐岩与CO2以及水作用,可以较快的吸收CO2,并产生了碳汇。因此短时间内岩溶区碳酸盐岩可较快的吸收大气中CO2；而长时间尺度内,主要认为是硅酸岩岩所产生的碳汇,并认为与碳酸盐岩对碳汇的效应约各占一半。
根据全球碳平衡,全球还存在着约2.8PgC的遗失碳汇,但多数从一个或几个方面的因素来研究碳汇。很少研究一个完整流域碳汇量,碳汇的影响因素等。本文以潮田河流域为例,通过对潮田河流域的地质背景的调查,选取24个不同地质背景下的研究点,通过野外与室内实验,得到水体中电导率(EC)、水温、PH值等参数,HCO3-、SO42-、K+、Na+、Ca2+、Mg2+等离子浓度,δD、8180、δ13CDIc等稳定同位素以及重金属元素Pb,Cr,Cd,Zn等的浓度。同时检测各岩性土壤中的重金属以及Ca、Mg元素的浓度。通过分析比较可得到一下结论：1、水类型主要决定于地层的岩性以及地层中所含有的矿物等。非岩溶区的主要有Mg·Ca-HCO3-SO4型水,Ca·Mg-HCO3型水；岩溶区的主要为Ca-HCO3型水,Mg·Ca-HCO3型水。然而,Mg·Ca-HCO3-SO4型水还受到混合、浓缩以及施肥等作用影响。在受人为因素影响较大的地方,Mg·Ca-HCO3-SO4型水也比较突出。
2、δ13在地下河与地表河的变化里相反的趋势。地表河中,8D由上游至下游在不断的变重,而地下河中的8D由上游至下游在不断的变轻；无论是地表河流还是地下河,氘氧同位素整体趋势从2011年8月至2011年11月较2011年12月至2012年7月轻,并且在一年之中成一定的变化趋势,主要原因可能是雨水和温度共同作用所致。该研究区域,δD与δ18O分别介于-45.7‰～-29.40‰之间与-7.50‰～-4.89‰之间,而这两个数值均重于高原中上的,说明季风气候因素影响了降雨中的δD与δ18O同位素。这也说明了潮田河流域的雨水主要来自季风作用,并受温度的影响。
3、δ13CDIC的变化范围在-18.00‰～-1.86‰,说明碳主要来自于大气,非岩溶区的碳来源受植被等生物作用影响明显,岩溶区主要受岩石的影响明显。随着季节性变化及降雨量的变化,δ13CDIC在一年当中呈周期性变化,在一年的2月份为最高,而到了一年的5-9月份(雨季)为最低,可能原因是植被的光合作用吸收了大量水中的碳源进而导致水中的无机碳(主要是HCO3-)变轻,而到了冬季,温度低,降雨少,植物作用相对较弱,使得δ13CDIC变得更重。
4、岩溶区与非岩溶区域在空间上水体中HCO3-浓度变化约10倍左右；时间上,沿着河流往下(非岩溶区水—外源水进入岩溶区),河流水体的HCO3-浓度在逐渐增大。HCO3-浓度在季节性变化中,旱季水中的HCO3-浓度略高于雨季,主要原因是水的稀释作用影响；而非岩溶地区,HCO3-浓度年变化不大。而同一天,水中植物丰富的地方,HCO3-浓度昼夜变化较明显。
5、水体中的PCO2有较明显的差异。岩溶区中的PCO2高于非岩溶区域；地下河中的PCO2高于地表河。
6、水体中的各种离子主要来自于岩石的风化作用。但碳的来源不同,非岩溶区水体中的碳主要来自于大气,岩溶区碳与岩石的来源在比例上将近一半,岩石来源占57.9%,而大气或土壤来源占42.1%。7、地质碳汇受多种因素的影响。地质背景直接影响土壤中的钙镁元素的量以及水中的Ca2+、Mg2+、HCO3-量,进而影响地质碳汇量,但地质碳汇量不仅仅只受地质背景影响；暴雨可以增加地质碳汇量,但此时水中的HCO3-的浓度低于非暴雨的时候；假设流量不变时,本文认为温度在20.2℃时为潮田河流域岩溶区产生碳汇量最大的时候,若低于20.2℃时,水可继续对碳酸盐岩进行溶解,若高于20.2℃温度时,水体可能将部分HC03-转化成C02和水,进而释放C02生物作用在整个地质碳汇作用中起到重要的作用,尤其是水体中的藻类等植物生长；含硫铅锌矿的开采,导致可被氧化的硫化物减少,水体中的SO42-离子减少,导致碳汇量的减少。一般认为岩溶区5O42-离子只是改变了碳循环的改变,并未增加碳汇,而非岩溶区硫化物的氧化可以增加碳汇量,或者说,非岩溶区由矿物氧化所得并进入水中SO42-离子含量的高低可以指示该区碳汇量的大小。故人类采矿(含硫铅锌矿)可能会导致地质碳汇成倍的较少。
8、在不考虑水体中的有机碳及悬浮颗粒碳的情况下,通过降雨量、径流深度、径流面积等计算可得：潮田河流域非岩溶区的年碳汇量为1586.9tc/a,岩溶区的碳汇量为4318.3tc/a,另外外源水流入到岩溶区后可以增加碳汇量为2818.8tc/a,故潮田河流域的年碳汇量为8724.0tc/a。故潮田河地质碳汇每平方千米的平均碳汇量分别是：非岩溶区地质碳汇量为5.2tc.a-1.km-2,岩溶区地质碳汇量为25.0tc.a-1.km-2,外源水可增加岩溶地质碳汇量为16.3tc.a-1.km-2,或者说潮田河流域外源水可使得该岩溶区地质碳汇增加到1.7倍。此时,包含水生生物光合作用产生23%的碳汇量以及地下潜流产生的33.8%的碳汇量。故潮田河流域碳汇量的计算需要考虑水生生物作用与潜流作用所产生的碳汇。
9、通过建立Ca2+、Mg2+与HCO3-关系模型可得：灰岩地区Ca2+就可以与HCO3-建立良好的关系模型,相关性较好,而白云岩区Ca2+、Mg2+与HCO3-的相关关系比Ca2+与HCO3-的相关关系好；Ca2+、Mg2+与HCO3-的关系模型可以间接说明碳汇主要影响因子：由Ca2+Mg2+与HCO3-的关系模型可得岩溶区地表明流段,水生生物的光合作用是碳汇主要影响因子,而地下河或泉水出口处,地质作用、CO2分压可能是碳汇的主要影响因子。
10、通过SWAT模型的模拟可知,潮田河流量除了受降雨作用的影响下,流域的渗透系数,水库的蓄水与排水直接影响到河流出口的流量,进而影响大潮田河流域的碳汇量；同时土壤的渗透系数变化与潮田河水的流量有直接的关系。经拟合,潮田河流域的流量与实际的流量基本一致。因此碳汇量也基本一致。并将潮田河流域的碳汇量表示为：F=42.43Q+13.98Q1(g)。
Natural disasters such as global climate warming, extreme climate events, is becoming more and more frequenct, which has attracted economy development all over the world. So it is focus on by many people or institutional framework. Some scholars believe that climate change have larger relationship with greenhouse gas (mainly CO2) at present. The atmospheric CO2concentration is increased and human survival environment is changed year by year since the monitored data.
According to the global carbon balance, the carbon has a difference which is called missing carbon. The missing carbon is increasing gradually as the atmospheric CO2concentration increases to this day. The missing carbon was studied in land carbon sink and sea carbon sink. Many scholars also studied the relationship of the carbon element and other elements, the carbon element and soil, the carbon element and vegetation, the carbon element and wetlands, rivers and oceans, etc. The aim is to find out the carbon sink.
Generally speaking, carbonate rock, the atmosphere CO2and water can rapidly alkaline reaction and produced carbon sinks. So carbonate rock can absort quickly CO2in the atmosphere in a short time, but in a long time scale, the carbonate-weathering-related carbon sink and silicate-weathering-related carbon sink are about the same.
According to the global carbon balance, there are about2.8PgC missing carbon now. The carbon sinks were studied in one or several aspects. For a comprehensive basin, few studies focus on the carbon sinks. Chaotian watershed, located on Guilin city, China, as a research site was choosed to study carbon sink.24points which come from different geological background were selected. And some water parameters such as electrical conductivity(EC), temperature, PH, HCO3-, SO42-, K+, Na+, Ca2+, Mg2+, stable isotope such as δD,δ18O,δ13CDIC, heavy metal elements such as Pb, Cr, Cd, Zn, were monitored. At the same time, the element Ca, Mg and some heavy metals which came from soil and rock were detected. All data were analyzed, and found that:
1, The type of water mainly depends on the formation of lithologic and the mineral. So the non-karst area water belongs to Mg·Ca-HCO3-SO4and Ca·Mg-HCO3mainly; The karst area water belongs to Ca-HCO3and Mg·Ca-HCO3mainly. However, Mg9Ca-HCO3-SO4water also affected by many factors,for example, mixing, enrichment, and fertilization etc. The water type of Mg·Ca-HCO3-SO4is influenced greatly by human activities.
2,8D isotope has an opposite trend to surface water and groundwater. When the process that flow from upstream to downstream,δD become heaverier in surface water and become lighter in groundwater; δD and δ18O also have an trend, from August2011to November2011,δD and δ18O are lighter than December2011to July2012, the reason may be that rainy and temperature. In study area,δD and δ18O are between-45.70%o～29.40%o and-7.50%o～4.89%o, respectively, and the value is hearvier than plateau. It shows that monsoon climate influence the rainfall. It also illustratesmost of the Chaotian watershed water comes from rain that is imported by monsoon climate.
3、The δ13CDIC ranges from-18.00‰to-1.86‰proves that carbon from the atmosphere, the carbon source in non-karst area affected obviously by vegetation, and karst area is mainly affected by rock. With the seasonal and precipitation changes,δ13CDIC present cyclical changes in a year, which reaches the heaviest point in February, while to the lightest point from May to September (rainy season). It possible results from vegetation photosynthesis absorbs a large number of carbon leading to lighten the DIC in water, especially inorganic carbon (HCO3-) lighter. Low temperature and little rainfall in the winter, and plant is relatively weak, makes δ13CDIC heavier.
4、The HC03-concentration in Karst water is about10times than non-karst area water. Along the river (non-karst area water (allogenic water) come into the karst area), the HCO3-concentration increases gradually. In seasonal changes, the HCO3-concentration in the dry season is slightly higher than the rainy season, mainly due to the dilution effects; Annual change of HCO3-concentration in non-karst area is small. But in the same day, HCO3-concentration diurnal variation is obvious in the rich aquatic plants.
5、PCO2in water have obviously differences which in Karst area is Higher than non-karst area; And the groundwater is higher than the surface water in Karst area.
6、Most of the ions in the water mainly come from the rocks weathering. And there is a different carbon source between karst and non-karst area. Most of Carbon source come from atomsphere in non-karst area, to the contrary, the carbon source is almost the same in karst area where are57.9%come from bedrock and42.1%.
7、There are many factors affecting geological carbon sink. Amount of calcium and magnesium elements in the soil and water are controled by the geological background directly, even though the amount of HCO3-. But the amount of geological carbon sinks are not just influenced by the geological background; heavy rain can increase the amount of geological carbon sinks, but the HCO3-concentration of water in rainstorm is lower than non rainstorm; Assume the flow is a constant, the largest carbon sinks occur at20.2℃in the Chaotian watershed karst area. If the tempreature is lower than20.2℃, the water can continue to dissolve carbonate rocks. To the contary, the tempreature is higher than20.2℃, parts of HCO3-converted into CO2and H2O, and then release the CO2; Also, biological action play an important role in the entire geological carbon sinks, especially the growth of algae and other plants in Water; The ore mining caused the geological carbon sinks to decrease, and the amount of geological carbon sinks reduce to half of the original. The reason is that the sulphur lead-zinc mining was ored, led to the oxidation of sulfide can be reduced, and the SO42-in water decreased. Also the SO42-in water can chang the carbon cycle in karst area, but the SO42-in water in non-karst area stand for the carbon sinks increased. So the sulphur lead-zinc mining can increased carbon sinks more quickly.
8、 Not consider the organic carbon and suspended particulate carbon of water, according to the rainfall, runoff depth, runoff area and available:the non-karst area in Chaotian watershed the amount of annual carbon sinks are1586.9tc/a, while in karst area the amount of carbon sinks are4318.3tc/a, allogenic water flow into the karst area can increase carbon sinks about2818.8tc/a. By all account, the amount of annual carbon sinks are about8724.0tc/a in Chaotian watershed. So the average geological carbon sinks per square kilometer in Chaotian watershed are:non-karst geological carbon sinks is5.2tc.a-1.km-2, karst geological carbon sinks is25.0tc.a-1.km-2, the allogenic water can increase the karst geological carbon sinks is16.3tc.a-1.km-2, that is to say extraterritorial source of water can make the karst geological carbon sinks increase to1.7times. Including23%of carbon sinks produced by aquatic photosynthesis and33.8%of carbon sinks generated by undercurrent. Therefore, the calculation of the amount of carbon sinks Chaotian watershed need to consider the the aquatic biological and undercurrents.
9, Through the establishment of Ca2+, Mg2+and HCO3-relationship model can obtained:Ca2+and HCO3-established a good model in limestone area, the correlation is well; While in dolomite zone, Ca2+, Mg2+and HCO3-1s relationship is better than the correlation of Ca2+and HCO3-. So Ca2+, Mg2+and HCO3-relationship model can indirectly illustrate the major impact factor of carbon sinks; From Ca2+, Mg2+and HCO3-relationship model, it can come to a conclusion that the stream segments, waterborn organisms photosynthesis is the major impact factors affect carbon sink in flow, but for the underground river or at the outlet of spring water geological processes, CO2partial pressure may be the main factors affecting carbon sinks.10、The SWAT model simulation shows Chaotian watershed flow not only affected by rainfall,
also the permeability coefficient, the storage and drainage of the reservoir affect the export flow of the river, thereby affect the amount of the carbon sinks in Chaotian watershed; There is a direct relationship between drainage of the reservoir, permeability coefficient and the Chaotian river's flow. The results show that the flow fitting curve and actual flow are basically the same in Chaotian watershed. So carbon sinks are basically the same. And the Chaotian watershed carbon sinks can be represented as:F=42.43Q+13.98Q1(g)
然根据全球碳平衡,目前碳还存一个差值,这个差值被叫做遗失碳汇(missing carbon)。该遗失碳汇随着大气CO2浓度逐年的增加而在逐渐增加。目前对于碳汇的研究主要分两大块,即陆地和海洋。在研究过程中,主要从碳元素影响因子与化学物质或化学元素之间的关系、碳元素与土壤及植被的关系、碳元素在湿地、河流及海洋特征等。但最终目的就是为了寻找遗失的碳汇。
一般认为,碳酸盐岩与CO2以及水作用,可以较快的吸收CO2,并产生了碳汇。因此短时间内岩溶区碳酸盐岩可较快的吸收大气中CO2；而长时间尺度内,主要认为是硅酸岩岩所产生的碳汇,并认为与碳酸盐岩对碳汇的效应约各占一半。
根据全球碳平衡,全球还存在着约2.8PgC的遗失碳汇,但多数从一个或几个方面的因素来研究碳汇。很少研究一个完整流域碳汇量,碳汇的影响因素等。本文以潮田河流域为例,通过对潮田河流域的地质背景的调查,选取24个不同地质背景下的研究点,通过野外与室内实验,得到水体中电导率(EC)、水温、PH值等参数,HCO3-、SO42-、K+、Na+、Ca2+、Mg2+等离子浓度,δD、8180、δ13CDIc等稳定同位素以及重金属元素Pb,Cr,Cd,Zn等的浓度。同时检测各岩性土壤中的重金属以及Ca、Mg元素的浓度。通过分析比较可得到一下结论：1、水类型主要决定于地层的岩性以及地层中所含有的矿物等。非岩溶区的主要有Mg·Ca-HCO3-SO4型水,Ca·Mg-HCO3型水；岩溶区的主要为Ca-HCO3型水,Mg·Ca-HCO3型水。然而,Mg·Ca-HCO3-SO4型水还受到混合、浓缩以及施肥等作用影响。在受人为因素影响较大的地方,Mg·Ca-HCO3-SO4型水也比较突出。
2、δ13在地下河与地表河的变化里相反的趋势。地表河中,8D由上游至下游在不断的变重,而地下河中的8D由上游至下游在不断的变轻；无论是地表河流还是地下河,氘氧同位素整体趋势从2011年8月至2011年11月较2011年12月至2012年7月轻,并且在一年之中成一定的变化趋势,主要原因可能是雨水和温度共同作用所致。该研究区域,δD与δ18O分别介于-45.7‰～-29.40‰之间与-7.50‰～-4.89‰之间,而这两个数值均重于高原中上的,说明季风气候因素影响了降雨中的δD与δ18O同位素。这也说明了潮田河流域的雨水主要来自季风作用,并受温度的影响。
3、δ13CDIC的变化范围在-18.00‰～-1.86‰,说明碳主要来自于大气,非岩溶区的碳来源受植被等生物作用影响明显,岩溶区主要受岩石的影响明显。随着季节性变化及降雨量的变化,δ13CDIC在一年当中呈周期性变化,在一年的2月份为最高,而到了一年的5-9月份(雨季)为最低,可能原因是植被的光合作用吸收了大量水中的碳源进而导致水中的无机碳(主要是HCO3-)变轻,而到了冬季,温度低,降雨少,植物作用相对较弱,使得δ13CDIC变得更重。
4、岩溶区与非岩溶区域在空间上水体中HCO3-浓度变化约10倍左右；时间上,沿着河流往下(非岩溶区水—外源水进入岩溶区),河流水体的HCO3-浓度在逐渐增大。HCO3-浓度在季节性变化中,旱季水中的HCO3-浓度略高于雨季,主要原因是水的稀释作用影响；而非岩溶地区,HCO3-浓度年变化不大。而同一天,水中植物丰富的地方,HCO3-浓度昼夜变化较明显。
5、水体中的PCO2有较明显的差异。岩溶区中的PCO2高于非岩溶区域；地下河中的PCO2高于地表河。
6、水体中的各种离子主要来自于岩石的风化作用。但碳的来源不同,非岩溶区水体中的碳主要来自于大气,岩溶区碳与岩石的来源在比例上将近一半,岩石来源占57.9%,而大气或土壤来源占42.1%。7、地质碳汇受多种因素的影响。地质背景直接影响土壤中的钙镁元素的量以及水中的Ca2+、Mg2+、HCO3-量,进而影响地质碳汇量,但地质碳汇量不仅仅只受地质背景影响；暴雨可以增加地质碳汇量,但此时水中的HCO3-的浓度低于非暴雨的时候；假设流量不变时,本文认为温度在20.2℃时为潮田河流域岩溶区产生碳汇量最大的时候,若低于20.2℃时,水可继续对碳酸盐岩进行溶解,若高于20.2℃温度时,水体可能将部分HC03-转化成C02和水,进而释放C02生物作用在整个地质碳汇作用中起到重要的作用,尤其是水体中的藻类等植物生长；含硫铅锌矿的开采,导致可被氧化的硫化物减少,水体中的SO42-离子减少,导致碳汇量的减少。一般认为岩溶区5O42-离子只是改变了碳循环的改变,并未增加碳汇,而非岩溶区硫化物的氧化可以增加碳汇量,或者说,非岩溶区由矿物氧化所得并进入水中SO42-离子含量的高低可以指示该区碳汇量的大小。故人类采矿(含硫铅锌矿)可能会导致地质碳汇成倍的较少。
8、在不考虑水体中的有机碳及悬浮颗粒碳的情况下,通过降雨量、径流深度、径流面积等计算可得：潮田河流域非岩溶区的年碳汇量为1586.9tc/a,岩溶区的碳汇量为4318.3tc/a,另外外源水流入到岩溶区后可以增加碳汇量为2818.8tc/a,故潮田河流域的年碳汇量为8724.0tc/a。故潮田河地质碳汇每平方千米的平均碳汇量分别是：非岩溶区地质碳汇量为5.2tc.a-1.km-2,岩溶区地质碳汇量为25.0tc.a-1.km-2,外源水可增加岩溶地质碳汇量为16.3tc.a-1.km-2,或者说潮田河流域外源水可使得该岩溶区地质碳汇增加到1.7倍。此时,包含水生生物光合作用产生23%的碳汇量以及地下潜流产生的33.8%的碳汇量。故潮田河流域碳汇量的计算需要考虑水生生物作用与潜流作用所产生的碳汇。
9、通过建立Ca2+、Mg2+与HCO3-关系模型可得：灰岩地区Ca2+就可以与HCO3-建立良好的关系模型,相关性较好,而白云岩区Ca2+、Mg2+与HCO3-的相关关系比Ca2+与HCO3-的相关关系好；Ca2+、Mg2+与HCO3-的关系模型可以间接说明碳汇主要影响因子：由Ca2+Mg2+与HCO3-的关系模型可得岩溶区地表明流段,水生生物的光合作用是碳汇主要影响因子,而地下河或泉水出口处,地质作用、CO2分压可能是碳汇的主要影响因子。
10、通过SWAT模型的模拟可知,潮田河流量除了受降雨作用的影响下,流域的渗透系数,水库的蓄水与排水直接影响到河流出口的流量,进而影响大潮田河流域的碳汇量；同时土壤的渗透系数变化与潮田河水的流量有直接的关系。经拟合,潮田河流域的流量与实际的流量基本一致。因此碳汇量也基本一致。并将潮田河流域的碳汇量表示为：F=42.43Q+13.98Q1(g)。
Natural disasters such as global climate warming, extreme climate events, is becoming more and more frequenct, which has attracted economy development all over the world. So it is focus on by many people or institutional framework. Some scholars believe that climate change have larger relationship with greenhouse gas (mainly CO2) at present. The atmospheric CO2concentration is increased and human survival environment is changed year by year since the monitored data.
According to the global carbon balance, the carbon has a difference which is called missing carbon. The missing carbon is increasing gradually as the atmospheric CO2concentration increases to this day. The missing carbon was studied in land carbon sink and sea carbon sink. Many scholars also studied the relationship of the carbon element and other elements, the carbon element and soil, the carbon element and vegetation, the carbon element and wetlands, rivers and oceans, etc. The aim is to find out the carbon sink.
Generally speaking, carbonate rock, the atmosphere CO2and water can rapidly alkaline reaction and produced carbon sinks. So carbonate rock can absort quickly CO2in the atmosphere in a short time, but in a long time scale, the carbonate-weathering-related carbon sink and silicate-weathering-related carbon sink are about the same.
According to the global carbon balance, there are about2.8PgC missing carbon now. The carbon sinks were studied in one or several aspects. For a comprehensive basin, few studies focus on the carbon sinks. Chaotian watershed, located on Guilin city, China, as a research site was choosed to study carbon sink.24points which come from different geological background were selected. And some water parameters such as electrical conductivity(EC), temperature, PH, HCO3-, SO42-, K+, Na+, Ca2+, Mg2+, stable isotope such as δD,δ18O,δ13CDIC, heavy metal elements such as Pb, Cr, Cd, Zn, were monitored. At the same time, the element Ca, Mg and some heavy metals which came from soil and rock were detected. All data were analyzed, and found that:
1, The type of water mainly depends on the formation of lithologic and the mineral. So the non-karst area water belongs to Mg·Ca-HCO3-SO4and Ca·Mg-HCO3mainly; The karst area water belongs to Ca-HCO3and Mg·Ca-HCO3mainly. However, Mg9Ca-HCO3-SO4water also affected by many factors,for example, mixing, enrichment, and fertilization etc. The water type of Mg·Ca-HCO3-SO4is influenced greatly by human activities.
2,8D isotope has an opposite trend to surface water and groundwater. When the process that flow from upstream to downstream,δD become heaverier in surface water and become lighter in groundwater; δD and δ18O also have an trend, from August2011to November2011,δD and δ18O are lighter than December2011to July2012, the reason may be that rainy and temperature. In study area,δD and δ18O are between-45.70%o～29.40%o and-7.50%o～4.89%o, respectively, and the value is hearvier than plateau. It shows that monsoon climate influence the rainfall. It also illustratesmost of the Chaotian watershed water comes from rain that is imported by monsoon climate.
3、The δ13CDIC ranges from-18.00‰to-1.86‰proves that carbon from the atmosphere, the carbon source in non-karst area affected obviously by vegetation, and karst area is mainly affected by rock. With the seasonal and precipitation changes,δ13CDIC present cyclical changes in a year, which reaches the heaviest point in February, while to the lightest point from May to September (rainy season). It possible results from vegetation photosynthesis absorbs a large number of carbon leading to lighten the DIC in water, especially inorganic carbon (HCO3-) lighter. Low temperature and little rainfall in the winter, and plant is relatively weak, makes δ13CDIC heavier.
4、The HC03-concentration in Karst water is about10times than non-karst area water. Along the river (non-karst area water (allogenic water) come into the karst area), the HCO3-concentration increases gradually. In seasonal changes, the HCO3-concentration in the dry season is slightly higher than the rainy season, mainly due to the dilution effects; Annual change of HCO3-concentration in non-karst area is small. But in the same day, HCO3-concentration diurnal variation is obvious in the rich aquatic plants.
5、PCO2in water have obviously differences which in Karst area is Higher than non-karst area; And the groundwater is higher than the surface water in Karst area.
6、Most of the ions in the water mainly come from the rocks weathering. And there is a different carbon source between karst and non-karst area. Most of Carbon source come from atomsphere in non-karst area, to the contrary, the carbon source is almost the same in karst area where are57.9%come from bedrock and42.1%.
7、There are many factors affecting geological carbon sink. Amount of calcium and magnesium elements in the soil and water are controled by the geological background directly, even though the amount of HCO3-. But the amount of geological carbon sinks are not just influenced by the geological background; heavy rain can increase the amount of geological carbon sinks, but the HCO3-concentration of water in rainstorm is lower than non rainstorm; Assume the flow is a constant, the largest carbon sinks occur at20.2℃in the Chaotian watershed karst area. If the tempreature is lower than20.2℃, the water can continue to dissolve carbonate rocks. To the contary, the tempreature is higher than20.2℃, parts of HCO3-converted into CO2and H2O, and then release the CO2; Also, biological action play an important role in the entire geological carbon sinks, especially the growth of algae and other plants in Water; The ore mining caused the geological carbon sinks to decrease, and the amount of geological carbon sinks reduce to half of the original. The reason is that the sulphur lead-zinc mining was ored, led to the oxidation of sulfide can be reduced, and the SO42-in water decreased. Also the SO42-in water can chang the carbon cycle in karst area, but the SO42-in water in non-karst area stand for the carbon sinks increased. So the sulphur lead-zinc mining can increased carbon sinks more quickly.
8、 Not consider the organic carbon and suspended particulate carbon of water, according to the rainfall, runoff depth, runoff area and available:the non-karst area in Chaotian watershed the amount of annual carbon sinks are1586.9tc/a, while in karst area the amount of carbon sinks are4318.3tc/a, allogenic water flow into the karst area can increase carbon sinks about2818.8tc/a. By all account, the amount of annual carbon sinks are about8724.0tc/a in Chaotian watershed. So the average geological carbon sinks per square kilometer in Chaotian watershed are:non-karst geological carbon sinks is5.2tc.a-1.km-2, karst geological carbon sinks is25.0tc.a-1.km-2, the allogenic water can increase the karst geological carbon sinks is16.3tc.a-1.km-2, that is to say extraterritorial source of water can make the karst geological carbon sinks increase to1.7times. Including23%of carbon sinks produced by aquatic photosynthesis and33.8%of carbon sinks generated by undercurrent. Therefore, the calculation of the amount of carbon sinks Chaotian watershed need to consider the the aquatic biological and undercurrents.
9, Through the establishment of Ca2+, Mg2+and HCO3-relationship model can obtained:Ca2+and HCO3-established a good model in limestone area, the correlation is well; While in dolomite zone, Ca2+, Mg2+and HCO3-1s relationship is better than the correlation of Ca2+and HCO3-. So Ca2+, Mg2+and HCO3-relationship model can indirectly illustrate the major impact factor of carbon sinks; From Ca2+, Mg2+and HCO3-relationship model, it can come to a conclusion that the stream segments, waterborn organisms photosynthesis is the major impact factors affect carbon sink in flow, but for the underground river or at the outlet of spring water geological processes, CO2partial pressure may be the main factors affecting carbon sinks.10、The SWAT model simulation shows Chaotian watershed flow not only affected by rainfall,
also the permeability coefficient, the storage and drainage of the reservoir affect the export flow of the river, thereby affect the amount of the carbon sinks in Chaotian watershed; There is a direct relationship between drainage of the reservoir, permeability coefficient and the Chaotian river's flow. The results show that the flow fitting curve and actual flow are basically the same in Chaotian watershed. So carbon sinks are basically the same. And the Chaotian watershed carbon sinks can be represented as:F=42.43Q+13.98Q1(g)
引文
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