本研究針對Purdue Regional Model (PRM)進行地表過程模式的改進。Sun and Chern （2005）發表一個新的地表過程模式，可以精準的長時間模擬，Sleeper河谷地表溫度。這個新的地表過程模式，包括植物、覆雪及土壤三個部分，利用這個模式，精進PRM的地表過程。並針對1998年東亞夏季季風個案，進行評估比對。東亞夏季季風的主要特性，夏季梅雨鋒面的平均降雨位置、季風肇始時間、降雨帶隨季節北移及季內振盪等現象。模式的模擬，對這些現象的掌握具備相當水準。但是，在模式的表現中，地表溫度比實際偏高，以及太平洋高壓的勢力仍比實際觀測偏強，這個太平洋高壓的誤差與過去模擬相同。太平高壓偏強的誤差，導致南海與中南半島模擬雨量減少，東亞地區鋒面的北移，過於偏北。
在地表使用（land use）資料的使用上，本研究蒐集二種新的高解析的地表使用資料，分別為美國馬里蘭大學（UMD， University of Maryland）及法國國家氣象研究中心（CNRM, centre national de recherches meteologiques / METEO-France），解析度均為1km×km。在植物模組中，引進植物葉面積指數（LAI）的衛星觀測資料，進行植物分布的修正。在不同地表使用與植物衛星資料的靈敏度測試中，發現當使用法國氣象研究中心的地表資料，模擬1998年東亞夏季季風，結果較為理想。當加入衛星植物LAI，可以小幅修正模擬的結果。在這些靈敏度的測試模擬中，使用法國資料模擬的地表溫度比UMD模擬的結果低，較為接近觀測資料。此結果的改善，是透過地表過程改變，使其高低層季風環流發生變化，影響降雨分布。
地表過程與大氣之間的交互作用是非常的複雜，為了瞭解地表過程對季風的影響如何，在此設計了一組地表過程的靈敏度實驗，實驗中透過地表加熱過程的改變、地表覆蓋改變（裸土、闊葉林及農田）及土水改變進行。在上述的實驗中，針對模擬的東亞大陸全部進行改變，雖然各式的改變，熱能與水文的變化會同時發生，但是由於熱能改變海陸間對比所造成水氣通量的改變，遠遠大於當地因為熱能與水文改變，所釋放出的蒸發量。所有模擬中雨量的改變，都受其季風水氣傳送帶改變所主導。當地表過程呈現增溫時，季風環流將增強，水氣傳送的通量明顯增加，導致東亞地區雨量增加。但因為地表增溫，季風環流增強，使得太平洋高壓減弱東退。並在東海與日本附近海面上，激發增強一個氣旋式系統。次環流的增強使韓國及中國華北地區西南季風減弱，降雨減少，因此在東亞大陸上出現一個類似三明治的結構降雨變化。 在呈現降溫的模擬結果中，太平洋高壓明顯增強，並向西伸。使得季風水氣傳送帶，向西移動至高原邊緣，東亞地區的雨量明顯減少。
在東亞季風進入與通過東亞地區時，必經的二個區域分別為中南半島，及華南地區。在此希望瞭解局部區域地表覆蓋的改變，對東亞季風的影響。二地區利用與前面相同的地表覆蓋改變（裸土、闊葉林及農田），當地表改為裸土時，地表溫度呈現增溫，當改為闊葉林時，地表呈現降溫，農田部分則呈現溫度變化較不明顯。當模擬中呈現增溫的模擬中，因為地表溫度上升增加海陸溫差，使其季風環流增強，季風的水氣傳送通量進入東亞地區增多。模擬降溫者，其反應相反，季風環流減弱，進入東亞地區的水氣傳送通量減少。在地表改變時，粗糙度隨植物種類改變而改變，其中農田與裸土部分較為相近。比較二者模擬，可以瞭解因為海陸溫差所增加的季風環流與水氣傳送量。中南半島增溫與粗糙度降低，所造成季風環流增強的位置，大致相近，都由中南半島陸地相東北延伸至台灣日本附近。華南地區的增溫，則增加由南海到台灣東北海域一帶的水氣傳送通量。華南地區的粗糙度改變，增加由南海向北方陸地傳送的水氣量。二者降雨的改變，都與水氣傳送的改變有關。地表過程的改變，對東亞地區夏季季風環流與降雨分布的影響，相當顯著。

In this study, the land surface scheme of the Purdue Regional Model (PRM) was improved. Sun and Chern (2005) had created a new land surface model which had the ability of long term continue simulation to the Sleeper River region. In the new land surface model, including the vegetation, snow and soil parts. The land surface model was tried to improve the land surface process of the PRM. To evaluate the performance of the PRM was simulated to the 1998 East Asian summer monsoon case. The PRM can hold the well major features of the East Asian summer monsoon include the location of summer seasonal mean, the date of the summer onset, the northward propagation of the rain bands and ISOs. The simulated surface temperature is warmer than observed, and the Pacific subtropical high also is too strong. Due to the tropical high is too strong induce the precipitation is less in the south China and Indochina. The location of Mei-Yu front is more northward.
The UMD and CNRM land use datasets are more high resolution what datasets were collected. In the vegetation scheme, the LAI data is used to modify the vegetation fraction. In the 1998 summer case, there are better results by using the CNRM dataset and observed LAI.
The interaction process is complex between the land and atmosphere. For understand that the impact of land surface process, design some sensitivity test for land surface processes change, such as the warm and cold effect, different land cover and soil moisture cases. In these testes, the land sea heat contrast is more important than the local evaporation release to the influence of monsoon flow change. The precipitation is dominated by the monsoon flow. As the land surface temperature is warm, the monsoon flow is stronger than control run, induce the precipitation increase over East Asian. The monsoon flow is strong because is warm land case, induce the subtropical high decrease and withdraw eastward. One cyclone over Japan Sea is generated because monsoon flow is stronger. In the cold temperature case, the Pacific subtropical high increase and extend westward. The moisture flow of the summer monsoon moves westward, and induce the precipitation decrease over East Asia.

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