Knowledge Resource Center for Ecological Environment in Arid Area
| 黑河流域典型景观植被带水热传输观测与模拟研究 | |
| 其他题名 | Measurement and simulation of heat and water transfer in typical vegetation landscape zone in Hei river basin |
| 宋克超 | |
| 出版年 | 2005 |
| 学位类型 | 博士 |
| 导师 | 康尔泗 |
| 学位授予单位 | 中国科学院寒区旱区环境与工程研究所 |
| 中文摘要 | 在内陆河流域典型景观植被带进行水热传输观测与模拟研究，对确定以植物耗水为主线的内陆河流域环境用水，对优化水资源限制条件下的流域植被种类与分布布局都有重大理论指导意义。本文以黑河流域三个典型景观植被带为研究对象，重点针对山区森林一草地植被带的水热过程进行观测与模拟，分析经典水热过程参数化方案在山区草地与林地的适用情况，分析这些参数化方案应该改进的方面。利用改进的SHAW／模型计算了青海云杉林系统的水热过程与水热分布格局。并设计两种小型蒸渗仪测算了林地地表与草地的蒸散发，评价了它们的适用性。定性分析了林地苔鲜对林地土壤水分、下渗、产流的影响。利用同步观测数据，分析了三个典型景观植被带的水热条件和环境要素差异。初步得到了以下研究结果。1．基于水汽密度差的方法，计算黑河流域山区草地的蒸散量偏大，使得进入土壤的下渗水量偏小。利用Penmon-Monteith或Shuttle-Wallace计算得到的蒸散量比较合理，一定程度上减小了土壤含水量预测偏低的问题。2．利用Ampt-Green降水下渗方案计算山区草地土壤水的分布，预测结果比实测含水量偏小。利用大孔隙优先流参数化方案代替Ampt-Green下渗方案，初步的结果表明，土壤含水量预测没有明显的改进。对内陆河山区植被带产流和下渗研究来说，大孔隙优先流是值得进一步深入研究的问题。3．利用SHAW模型预测的草地在夏季的土壤温度比较合理，偏差在3.5℃以内，冬季预测的地温偏高，预测的积雪厚度、积雪存留时间都偏小，而冻深偏小约40cm。积雪和冻土的参数化方案仍需进一步探讨。4．试验点处的青海云杉林，在5-11月的水份收入基本上用于蒸发，土壤水份储存仅占同期降水量的8.5％，蒸腾占总蒸发的49％，降水截留占总蒸发的18.5％，林内地表蒸发占总蒸发的32.5％。模拟得到林地地表日均蒸发为0.62mm，云杉日均蒸腾在1.0mm左右。5.Penman-Monteith、ASCE-Penman-Monteith和Priestley-Taylor三种方法对比计算草地蒸发，结果表明，Penman-Monteith精度最好，Priestlcy-Tayfor次之，然后是ASCE-Penman-Monteith方法。1黑河流域典型景观植被带水热传输观测与模拟研究6．大口径环刀式蒸渗仪不适宜测算黑河山区草地与林地的蒸散发，而桶式蒸渗仪适用性比较好。测算得到苔鲜覆盖的林地蒸发与枯枝落叶覆盖的林地日均蒸发分别为0.61mm与0.83mm；林地的降水下渗滞后于草地1-3天，苔鲜覆盖的林地降水下渗滞后于枯枝落叶下渗约1天。7．云杉密林内，林地苔鲜厚度大、盖度大，苔鲜层下的腐殖质厚，这使得下渗水富集在林地土壤表层，土壤深层下渗水少，限制了水分的侧向迁移和壤中产流，而云杉疏林则与以上情形相反；林地苔鲜利于在土内形成不连续的冰冻隔水层，对壤中融水径流形成有明显的促进作用。8．在黑河流域上游山区森林草地植被带、山前中游人工绿洲植被带和下游天然荒漠绿洲带，对同步环境观测要素分析表明，山区森林一草地复合生态区陆面是冷性湿润的下垫面，中游绿州一荒漠接触带是干性、较湿润的下垫面，下游荒漠河岸林景观带是干热性的下垫面，正是水热条件差异和冠层结构差异、土壤属性差异使得典型植被景观的水热过程和生态过程表现不一致。 |
| 英文摘要 | Land surface evapotranspiration and soil water infiltration in three typical vegetation landscape zones are mainly studied in this thesis. The simultaneous heat and water (SHAW) model was modified and adjusted based on evapotranspiration error analysis and soil water content error from the trial simulation which carried on a mountain grassland. The modified SHAW model was mainly used to simulate the Picea crassifolia forest ecosystem evapotranspiration and water transfer in soil, as well as the mountain grassland. Using two kinds of micro-lysimeter, we measured the actual evaporation of forest floor and grassland. Penman-Monteith equation, ASCE-Penman-Monteith method and Priestley-Taylor method were used to calculate the grassland evapotranspiration for evaluation of the two kinds of micro-lysimeter applicability in mountain region of Hei River. The effect of kind of grass and grassland coverage on evapotranspiration was analyzed. Based on the qualitative analysis and field measurements, we analyzed the hydrological and ecological function of forest floor moss layer. The environmental factors of three vegetation landscape zone were figured for their discrepancy in the aspect of water and heat conditions. It is unsuitable for SHAW model calculating evapotranspiration of the typical vegetation landscape zones in Heihe river based on water vapor density difference between ground surface and reference surface. The grassland evapotranspiration and intercepted rainfall by plant simulated by SHAW model are overestimated, these errors render the predicted water content underestimated; While using the Penman-Monteith or Shuttle-Wallace, the calculating evapotranspiration is more accurately than simulated by SHAW model. The underestimated soil water content may also be attributed to ignoring macropore preferential flow in soil, the typical Ampt-Green infiltration method adopted by SHAW model was limited by macropore soil. In summer, the predicted ground temperature compared well with the measurements; but in winter, the predicted ground temperature is overestimated, and the snow depth and resident time is underestimated, so did frozen depth, in the aspect of snowmelt, frozen soil process, much more work should be done The rainfall in Picea crassifolia forest was almost used in the aspect of evapotranspiration during May to November, the storage soil water is only 8.5 percentage of total rainfall, the transpiration by Picea crassifolia is about 49 percentage of total forest evapotranspiration, intercepted rainfall is about 18.5 percentage of total forest evapotranspiration, the forest floor evaporation is about 32.5 percentage of total forest evapotranspiration, the net radiation entering the forest floor is only about 19.5 percentage of about of forest canopy, the input energy are mainly used by forest canopy evaporation and heat exchange; the heat input to forest floor, 67 percentage are used by soil evaporation, the daily forest floor evaporation is only 0.62mm. The grassland evapotranspiration calculated by Penman-Monteith equation is more precisely than that produced by Priestley-Taylor method, and the evapotranspiration simulated by ASCE-Penman-Monteith equation have larger error. The designed larger diameter cutting ring micro-lysimeter is unsuitable for measuring evaporation, but the bucket- microlysimeter is suitable for measuring the evaporation from grassland and forest floor. The coverage of grassland has no obvious influence on evapotranspiration; the discrepancy in grass coverage can lead to the distribution difference between soil evaporation and grass transpiration, the total grass evapotranspiration is almost the same. The forest floor covered by moss layer has 0.83mm average daily evaporation, The forest floor covered by litter has 0.61mm average daily evaporation, the infiltration in forest floor is lagged for about 1-3 days compared with the grassland, the infiltration in forest floor covered by moss layer is lagged for about 1 day compared with the floor covered by litter. The forest density is larger, the forest moss layer thickness and coverage is larger, as well as the humus thickness, this render infiltration water enriching in shallow soil profile, less water infiltration into depth soil, this limited the lateral water transfer in forest soil and the subsurface flow in soil. In sparse forest, the moss layer is thin, it may be have positive effect to depth infiltration; the water holding capacity of moss-litter compound layer is larger than single moss layer or single litter layer; forest moss layer is facilitate to form the discontinuous frozen layer, have prominent positive effect on subsurface melt runoff. The comparison of environmental factors of three vegetation landscape zone showed that the mountain forest-grassland-shrub surface is cold and moisture, the transition zone between desert and oasis is drier and moisture landsurface, the desert riparian forest is drier and hot land surface. The water and heat conditions among these vegetation landscape zone, render the water and energy processes, and ecological process is differential. |
| 中文关键词 | 黑河流域 ; 典型景观植被带 ; 土壤-植被-大气连续体系 ; 水热传输 ; 观测与模拟 |
| 英文关键词 | Hei River basin Typical vegetation landscape zone Soil-vegetation-Plant continuum Water and heat transfer Measurement and simulation |
| 语种 | 中文 |
| 国家 | 中国 |
| 来源机构 | 中国科学院西北生态环境资源研究院 |
| 资源类型 | 学位论文 |
| 条目标识符 | http://119.78.100.177/qdio/handle/2XILL650/286416 |
| 推荐引用方式 GB/T 7714 | 宋克超. 黑河流域典型景观植被带水热传输观测与模拟研究[D]. 中国科学院寒区旱区环境与工程研究所,2005. |
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