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完整後設資料紀錄
DC 欄位 | 值 | 語言 |
---|---|---|
dc.contributor.advisor | 吳健銘(Chien-Ming Wu) | |
dc.contributor.author | Po-Yen Chen | en |
dc.contributor.author | 陳柏言 | zh_TW |
dc.date.accessioned | 2021-05-12T09:36:09Z | - |
dc.date.available | 2018-02-26 | |
dc.date.available | 2021-05-12T09:36:09Z | - |
dc.date.copyright | 2018-02-26 | |
dc.date.issued | 2018 | |
dc.date.submitted | 2018-01-17 | |
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Arakawa, 2010: Inclusion of Surface Topography into the Vector Vorticity Equation Model (VVM), J. Adv. Model. Earth Syst., 3, M04002. Wu, C. and A. Arakawa, 2014: A Unified Representation of Deep Moist Convection in Numerical Modeling of the Atmosphere. Part II. J. Atmos. Sci., 71, 2089–2103. Wu, C.-M., M.-H. Lo, W.-T. Chen, and C.-T. Lu, 2015: The impacts of heterogeneous land surface fluxes on the diurnal cycle precipitation: A framework for improving the GCM representation of land-atmosphere interactions, J. Geophys. Res. Atmos., 120, 3714–3727. | |
dc.identifier.uri | http://tdr.lib.ntu.edu.tw/handle/123456789/1313 | - |
dc.description.abstract | 本研究透過三維渦度向量方程式的雲解析模式(VVM)耦合陸地模式(LSM),分別探討在都市、牧場和草地三種的理想熱帶島嶼上,有無直接陸地大氣交互作用時對於降水日變化強度的影響。我們設計了兩組實驗,第一組為有直接的陸地大氣交互作用(VVM耦合LSM);第二組為沒有直接陸地大氣交互作用的結果(只有VVM),利用第一組實驗中包含高時空頻率的地面通量和溫度等資訊做為大氣地表邊界變化。最後去看在不同蒸發比的陸面下,兩組實驗中日降水變化和對流系統在時空上的差距,作為有無直接陸地大氣交互作用的影響。
結果顯示在三種陸面環境下,有直接陸地大氣交互作用的降水日變化幅度與極端降水事件強度都高於沒有直接陸地大氣交互作用。另一部份則是在都市的實驗下,降水日變化幅度與極端降水強度差異明顯高於在牧場與草地的實驗,都市與草地的差異最高可達71%。 造成降水日變化幅度的差異的機制,主要是在都市的陸面實驗中,由於空間尺度較大(大約在熱塔尺度,半徑約10km)的對流核心雲產生較強的冷池,而在較強冷池的交互作用下有利於激發更強的對流核心雲,因此在有直接陸地大氣交互作用的實驗下冷池對於對流發展為一個正貢獻過程。但在都市陸面實驗中,沒有直接陸地大氣交互作用實驗下則因為前面實驗的強冷池對於地面冷卻效果明顯,使得在冷區上方有微弱的下沉運動並讓對流偏好在冷區邊緣發展。而在牧場與草地的實驗則因為冷池強度和冷區偏弱,因此抑制對流發展強度降低。此結果初步顯示在經歷都市化或砍伐森林過程的熱帶島嶼上,降水的日變化強度和極端降水事件對於陸地大氣交互作用的過程更加敏感。 | zh_TW |
dc.description.abstract | This study investigates the impact of land-atmosphere interactions (LAI) on the diurnal intensity of precipitation over a tropical island. Idealized simulations are performed with three different land surface conditions urban, pasture and grass using a three-dimensional Vector Vorticity equation cloud-resolving Model (VVM) coupled with the Noah Land Surface Model (LSM). Two sets of experiments are performed in this study. The first set considers direct LAI in which VVM is fully coupled with LSM. The second set of experiment eliminates direct LAI by prescribing surface fluxes in VVM, in which the high spatiotemporal variabilities are preserved from the fully coupled VVM/LSM. With this approach, the difference in temporal and spatial evolution of precipitation and convective systems can be interpreted as the impact of LAI.
The results show that the diurnal amplitude and extreme precipitation is stronger with direct LAI than without under all land surface conditions. The impact of LAI is profound on the diurnal amplitude with urban experiment, which is 71% larger compared with grass experiment. This is due to strong cold pool intensity by convective systems with large updraft core clouds in urban experiment. There is a positive contribution to convective updraft core cloud development by strong cold pool intensity. The surface cooling in the experiments without direct LAI, on the other hand, produces a weak divergence to suppress the convection development. The convective cells prefer to develop at the boundary of surface cold patch. In experiments over pasture and grass, the strength of surface cooling becomes weaker and hence weaker impact on the convection development. These findings imply that the diurnal intensity of precipitation as well as the extreme events can be more sensitive to LAI over tropical islands through processes such as urbanization or deforestation. | en |
dc.description.provenance | Made available in DSpace on 2021-05-12T09:36:09Z (GMT). No. of bitstreams: 1 ntu-107-R03229005-1.pdf: 3816404 bytes, checksum: 8d35a3260de9050ce8dc1111fb2d2a69 (MD5) Previous issue date: 2018 | en |
dc.description.tableofcontents | 目 錄
口試委員會審定書....................................................i 謝辭...............................................................ii 中文摘要..........................................................iii 英文摘要...........................................................iv 目錄...............................................................vi 圖表目錄..........................................................vii 第一章 前言.........................................................1 第二章 數值模式與理想化實驗設計.....................................5 2.1 數值模式 Vector Vorticity Equation Cloud-Resolving Model(VVM) .........5 2.2 數值模式 Noah Land Surface Model(LSM) ...........................6 2.3.理想化實驗設計................................................6 2.3.1 島嶼及陸面型態設定.......................................6 2.3.2 耦合陸地大氣交互作用.....................................7 第三章 實驗結果.....................................................9 3.1 降水與對流分布及強度之日變化與機制.............................9 3.2 有無直接陸地大氣交互作用(Coupled vs. Prescribed)之日變化幅度差異.....12 3.3 雲尺寸定量分析...............................................13 3.4 對流雲之降水貢獻.............................................14 3.5 有無直接陸地大氣交互作用之日變化幅度差異機制探討...............16 第四章 總結........................................................18 第五章 討論........................................................20 參考文獻...........................................................21 附錄...............................................................44 圖表目錄 表1 大氣模式設定...................................................26 表2 陸地模式設定...................................................26 圖2.1 大氣初始場之位溫與水氣混合比垂直分布。紅線為位溫(potential temperature (K))。藍線為水氣混合比(water vapor mixing ratio (g kg^(-1)))。.................................................27 圖 2.2.1 陸地總地面通量之空間上平均時間序列圖。實線為六個系集實驗時間序列平均,其中淺色區域為時間序列的範圍。.......................28 圖 2.2.2 陸地總地面通量之空間上平均時間序列圖。實線為空間平均,淺色區域為地面通量之空間標準差。....................................28 圖2.3 五組陸面環境下的蒸發比(evaporative fraction)時序圖。實線為六個系集實驗時間序列平均,其中淺色區域為時間序列的範圍。................29 圖3.1 在Coupled實驗下,都市島嶼的日變化之空間分布圖。圖中左上角為時間,黑底為陸地,藍底為海洋。Color shading為地面降水。Gray shading為雲頂溫度。箭頭為風速風向之Y方向平均後的近地面(0~300公尺高)水平風,紅色為西風,藍色為東風。.......................................30 圖3.2 各陸面下Coupled 實驗之(a)左側海風移入距離時序圖,海風鋒面移入距離只顯示到兩側海風鋒面輻合的時刻,在此定義為近地面(0~180公尺高)及Y方向平均東西向風在下午陸地上東側發生最大水平輻合的時刻。(b)節自Crosman and Horel, 2010,其中整理四篇模擬海風移入距離時序圖,其中(a)(b)中紅色虛線方框為相同時間和海風鋒面移入距離區間。(c)為海風鋒面移動速度時序圖,移入速度只定義到海風鋒面輻合的時刻。淺色區域為六個系集實驗結果的範圍。..................................31 圖3.3 在各陸面下,Coupled實驗的陸地平均降水時序圖。淺色區域為六個系集實驗結果的範圍。..............................................32 圖3.4 各陸面下,Coupled實驗的降水(color shading)、雲頂溫度(gray shading)與近地面(0~300公尺)平均水平風速。時間點分別為Initiation (早上11點)、Condensation(下午1點)、Merge(海風鋒面輻合)與Prec.(陸地平均最大降水時刻)。.......................................................33 圖3.5 各陸面的Coupled和Prescribed下,取Y方向平均的下午對流與海風鋒面輻合時的垂直結構差異。Gray shading及白色contour為雲水雲冰混合比,contour等值線量值分別為0.4,0.5 (gkg-1)。紅色打點為垂直速度超過0.5(ms-1)區域、紅色contour分別為垂直速度1,1.2 (ms-1)。藍橘色shading及黑色contour為X方向風速。藍色打點為冷池邊界(-0.003 ms-1),藍色contour為冷池強度,等值線量值分別為 -0.01,-0.02 (ms-1)。...........34 圖3.6 各陸面的Coupled實驗中,陸地上平均 (a)邊界層高度(Boundary Layer height, BL) (b)冷池強度(cold pool intensity) (邊界層高度、冷池強度定義詳見附錄) (c)近地面兩公里內平均濕靜能(moist static energy, MSE) (d)舉升凝結面高度(Lifted of condensation level, LCL)。在此使用氣塊法(air parcel theorem)並利用近地面(0~21公尺高)的平均溫度和水氣混合比作為氣塊在地面之溫度與水氣混合比計算。淺色區域為六個系集實驗結果的範圍。..........................................................35 圖3.7 各陸面下之陸地上平均日降水時序變化差值(Coupled減Prescribed)。 中心黑點為六個系集實驗最大差值的平均,error bar為系集實驗差值之標準差。........................................................36 圖3.8 下午兩點到六點之間在(a) U00 (b) P05 (c) G08 陸面環境的陸地降水強度機率分布圖。..................................................37 圖3.9 在 (a) U00, (b) P05, (c) G08陸面環境下Coupled和Prescribed之雲(雲水+雲冰混合比超過10-5 kgkg-1) 尺寸機率分布圖(Probability of cloud-size distribution)。(d)不同陸面環境下六個系集實驗的雲總個數平均。.......38 圖3.10 在 (a) U00, (b) P05, (c) G08陸面下Coupled和Prescribed實驗的對流核心雲(convective core cloud) (雲水+雲冰混合比超過10-5 kgkg-1且垂直速度超過0.5 ms-1))尺寸機率分布圖。(d) 不同陸面環境下六個系集實驗的對流核心雲大雲(尺寸 超過103 km3 ) 總個數平均。...............39 圖3.11 三種陸面型態下對流核心雲的下午兩點至六點之降水貢獻比例在Coupled和Prescribed實驗的差異(Coupled減Prescribed)。其中Large為對流核心雲(convective core cloud)尺寸超過103 km3,Small為尺寸小於103 km3。...................................................40 圖3.12 在各陸面下Coupled和Prescribed實驗發生最大平均降水時,冷池強度和地面溫度距平(地面溫度和陸地地面溫度平均之差值)。藍色shading為冷池強度,紅色shading為地面溫度距平。......................41 圖3.13 (a)在各陸面下Coupled和Prescribed實驗發生最大平均降水時冷池強度和地面溫度距平(和陸地地面溫度平均之差值)區域分離比例(0為完全重合、1為完全分離)。實心點為六個系集實驗之空間分離度平均,error bar為系集實驗之空間分離度平均的標準差。(b)為空間分離度定義的示意圖。藍色為冷池強度超過10 (ms-1),紅色為地面溫度距平低於 -5 (K)。平均空間分離比例的計算為只考慮有數字的區域(0,1)(即不考慮NaN區域)之下取平均。.............................................42 圖3.14 造成在陸面從偏乾轉變到偏濕時,Coupled和Prescribed實驗中對流集結過程差異的機制示意圖。水藍色區域為地面冷區(cold region)強度,藍色實線為冷池鋒面(cold pool front)垂直剖面,藍色虛線為冷區造成上方大氣沉降。................................................43 | |
dc.language.iso | zh-TW | |
dc.title | 陸地大氣交互作用對於熱帶島嶼日降水強度之影響 | zh_TW |
dc.title | The impact of land-atmosphere interactions on the diurnal intensity of precipitation over tropical islands | en |
dc.type | Thesis | |
dc.date.schoolyear | 106-1 | |
dc.description.degree | 碩士 | |
dc.contributor.oralexamcommittee | 陳維婷,羅敏輝,陳建河 | |
dc.subject.keyword | 午後熱對流,冷池,陸地大氣交互作用,熱帶島嶼,降雨日變化, | zh_TW |
dc.subject.keyword | afternoon thunderstorm,cold pool,land atmosphere interaction,tropical island,diurnal cycle of precipitation, | en |
dc.relation.page | 48 | |
dc.identifier.doi | 10.6342/NTU201800080 | |
dc.rights.note | 同意授權(全球公開) | |
dc.date.accepted | 2018-01-17 | |
dc.contributor.author-college | 理學院 | zh_TW |
dc.contributor.author-dept | 大氣科學研究所 | zh_TW |
顯示於系所單位: | 大氣科學系 |
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ntu-107-1.pdf | 3.73 MB | Adobe PDF | 檢視/開啟 |
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