利用模拟淋溶实验、质量平衡法、PROFILE模型、MAGIC模型以及两种经验方法对中国十几种主要土壤类型的风化速率进行了研究。研究表明，中国南方富铝土区域（包括砖红壤带、赤红壤带、红壤黄壤带和黄棕壤带）以及东北的硅铝土区域（包括暗棕壤黑土带和漂灰土带） 的风化速率普遍较低（通常低于1.0 keq•ha-1•a-1），土壤缓冲酸沉降的能力较弱。

以土壤类型、土地利用和湿度为生态因子，评价中国土壤对酸沉降的相对敏感性，并利用地理信息系统的工具绘制了相对敏感性区划图。在评价土壤的缓冲能力时，除了以土壤的化学性质为指标外，还综合考虑了土壤质地和温度这2个重要因素，使得评价方法更适合我国土壤理化性质差异大和南北温差大的特点。区划的结果表明，我国对酸沉降最敏感的地区主要分布在东北的大兴安岭地区、云南的南部和华南沿海地区，其次是东北地区、长江以南和青藏高原西部的广大地区，而我国的绝大多数地区，包括西北和华北地区，对酸沉降较不敏感。

在进行中国酸沉降临界负荷区划时，通常以1°×1°（经纬度）的网格为单位进行计算，难以反映网格内不同生态系统对酸沉降敏感性的差异。为了便于决策者根据临界负荷确定酸沉降控制对策，也为了使1°×1°的结果更具代表性和实用性，本研究确定了011°×011°网格为单位计算的中国酸沉降临界负荷，并在此基础上通过引入保证率的概念，得到了一系列与一定的经济技术水平相适应的、允许有一定损失的1°×1°的中国酸沉降临界负荷图。利用累积分布函数，本研究还确定了不同保证率下的中国酸沉降超临界负荷分布和各省、市、自治区的酸沉降临界负荷。

研究了酸沉降对中国南方地表水体的影响。应用动态酸化模型MA GIC，计算了中国南方80个地表水体的酸沉降临界负荷。结果表明：大部分水体的酸沉降临界负荷较高，大于2 kmo lõhm-2õa-1，呈现地带性分布。西南地区的地表水酸沉降临界负荷高于华东和华南地区，这主要是因为南方土壤的酸化敏感性由东南向西北减弱。临界负荷较高，表明这些水体对酸化不敏感。地表水酸化不太可能成为中国严重的区域环境问题。但是少数山地水体的酸化趋势值得关注。

研究了两种确定硫沉降目标负荷的方法——最小超临界负荷法和等比例降低超临界负荷法，介绍了其原理和相应的数学模型并分析了用这两种方法确定的硫沉降目标负荷及相应的超临界负荷分布。和等比例削减SO2方案比较，采用上述两种方法，中国超临界负荷总量会明显降低，而最小超临界负荷法可以使超临界负荷的区域面积比2000年无控方案减小约12%。综合考虑技术、经济和区域公平性建议在确定中国硫沉降目标负荷时采用这两种方法。

Vegetation uptake of nitrogen and base cations may be an important source of soil acidity.In this study, the uptake rate of nitrogen and base cations was estimated for each major vegetation type in China.Although the uptake rates of most vegetation types are lower than 2.0 keq hay1 ay1, great variations exist because of the significant differences in net primary productivity and elemental composition.Uptake rates decreased gradually from southeast to northwest, except for the wide-distributed agricultural areas in the east of China, where the nitrogen and base cation uptake rates are near zero.It is evident that this pattern coincides well with the distribution of the annual mean precipitation. However, the geographical distribution of the base cation uptake rate is not entirely the same as that of nitrogen, which indicates the importance of soil conditions in determining the chemical component and hence the uptake rate of different vegetation.The acidity input caused by vegetation uptake is quite high ()0.5 keq hay1 ay1), and even higher than the current acid deposition and the alkalinity produced by soil weathering in some areas, which indicates that the growth of the plants may contribute significantly to the soil acidification problem in China.

盐基阳离子排放清单的建立，对于中国酸沉降控制有重要的意义，针对电力、建材和钢铁工业，基于颗粒物的排放量和化学组成，分别计算工业点源和工业面源的大气盐基阳离子排放量，并绘制中国盐基阳离子排放强度分布图， 结果表明，中国2000年工业源排放盐基阳离子总量为417.0万t，其中工业面源占81.0%，中国工业源盐基阳离子排放强度分布呈现东部高西部低的格局，最大值出现在河南省，达到了212.8kmol•2•a-1。

任何一个天然生态系统都是一个稳定系统。在一定酸沉降量的作用下，生态系统最终会平衡在一个新的稳定状态。动态模型可以模拟不同酸沉降量下生态系统化学状态的变化趋势。根据信号与系统理论，这种趋势可以用一阶指数衰减函数进行模拟，以得到系统达到稳定状态时的化学指标值。根据不同酸沉降量和所对应的稳态化学指标值之间的剂量2响应曲线，可以求出当系统稳态化学指标值达到临界化学值时的酸沉降量，即为系统的酸沉降临界负荷。应用这种方法，以MAGIC模型为例，计算了四川峨眉山顶水和重庆南山湖泊的硫沉降临界负荷，分别为1154和6151 keq•（hm2•a）-1。通过和MAGIC计算的目标负荷及SSWC方法计算的临界负荷相比较，认为用本文介绍的方法所计算的临界负荷值是合理可信的。

SO2排放对我国的森林生态系统造成了严重的损害，因而损失计算对于SO2控制具有重要意义，但是目前仍缺乏有效的方法计算不同排放水平下的森林损失。本研究以硫沉降超临界负荷作为计算森林损失的参数，推导了适用于我国硫沉降导致森林损失的剂量2响应函数，并以湖南省为例，以1995为基准年，计算了2000年～2020年高中低3种SO2排放方案下的森林损失。研究结果表明，随着今后湖南省经济和能源消费的增长，森林损失将继续增加。高排放方案下2020年SO2排放将增长112倍，但森林损失增长413倍，边际损失高于6000元/t。在当前排放水平下对SO2排放进行削减，边际效益达到1500元/t，因此控制SO2具有显著的经济效益。对湖南案例的不确定性分析显示，计算方法有较高的可靠性。研究结果为区域SO2控制策略的优化提供了支持。

As an important parameter for critical load calculation and soil acidification simulation, weathering rates of soils in China were studied using different methods of calculation. The approaches used were the mass balance approach, the soil mineralogical classification, the total analysis correlation, the PROFILE model, the MAGIC model and a simulated leaching experiment. Since chemical weathering of secondary minerals usually plays a much more important role in neutralizing the long-term acidification of soils in China than that of parent material, soil mineralogy rather than parent rock/material type, which is regarded as the most suitable factor representing weathering rates in Europe, should be adopted as the basis for soil classification. The weathering rate assigned to each soil should also be corrected when the effect of temperature is considered. Due to the variation in experimental conditions, the weathering rates of soils from laboratory experiment may be difficult to compare with field determined rates, and should be adjusted by pH and percolation rate. The comparison of various methods in this study shows that the weathering rates of soils estimated by the PROFILE model coincide well with those from other independent methods such as the dynamic modeling by MAGIC and the modified leaching experiment. The weathering rates were very low (usually lower than 1.0 kEq-ha-1-year-1) for Allites (including Latosol, Lateritic Red Earth, Red Earth, Yellow Earth and Yellow-Brown Earth) in south China and Silalsols (consisting of Dark Brown Forest Soil, Black Soil and Podzolic Soil) in northeast China, and very high for Alpine Soils, Desert Soils and Pedocals in west China. The content of weatherable minerals in soil is the most important factor in determining the spatial distribution of weathering rate in China, while the difference in temperature may be the reason why the weathering rate of soil in northeast China was lower than that in southeast China.