本研究利用台灣地區1995 - 2005年6個GPS衛星追蹤站與台灣南部、蘭嶼、綠島與澎湖共261個內政部一、二等GPS衛星控制點重複觀測資料，進行資料解算。並進一步探討海岸山脈到中央山脈過度帶的地殼變形型態、中央山脈的應變機制與澎湖群島的構造撓曲形態。研究結果顯示，GPS水平速度值由海岸山脈到縱谷介於59.42 - 83.28 mm/yr之間，方位角落在280.00° - 323.30°。中央山脈南段到恆春半島GPS速度值介於25.37 – 61.80 mm/yr之間，方位角落在263.30° - 293.63°。利用速度場來估算平均主應變率，觀測資料應變分析結果顯示恆春半島到中央山脈南段測區應變率介於0.01 – 1.8 µstrain/yr。海岸山脈南段往北至海岸山脈中段測區應變率介於0.9 – 1.7 µstrain/yr。恆春半島到中央山脈南段，伸張應變型態由南向北呈現東北東-西南西方向、東-西方向、東北東-西南西方向。中央山脈南段從東至西，山脈東側、山脊至山脈西側，應變量依序為0.19 µstrain/yr、0.36 µstrain/yr、0.02 µstrain/yr。台灣海峽的應變率結果顯示，澎湖以東測網的主應變率介於0.018 µstrain/yr - 0.121 µstrain/yr，澎湖西測網的主應變率介於0.004 µstrain/yr - 0.009 µstrain/yr。澎湖群島外圍為伸張型應力系統。澎湖群島中心，由南向北從望安島、澎湖本島，呈現一擠壓應變型態。
北港基盤高區造成台灣南部速度場以台東為分界，台東以北順時針旋轉，台東以南產生逆時針旋轉趨勢。而南部地區因構造脫逸使得高屏地區的GPS速度量加速。中央山脈南段在東西方向(垂直山脈走向)由北向南呈現單軸伸張變化，此伸張變形的機制是由於菲律賓海板塊與歐亞板塊相互碰撞作用導致山脈快速抬升所造成的結果。中央山脈南段兩翼在東西方向應變量隨著山脈增高而伸張應變量增加，山脈最高處為伸張應變量值最大之處，此現象因在同碰撞時期山脈抬升作用（Exhumation）與山脈塌陷（mountain collapse）所造成的。台灣海峽仍然為一穩定的大陸邊緣板塊，位於前陸盆地撓曲凸處的澎湖群島，因受持續造山運動的重壓影響，使造山帶與穩定大陸間之地殼彎曲，造成澎湖群島周圍產生張裂現象。

261 campaign-mode GPS observations and 6 continuously recording GPS data collected from the southern Taiwan GPS Network between 1995 and 2005 were adopted to reveal the crustal deformation in the southern Taiwan. We discuss the crustal deformation from Coastal Range to the Central Range, the strain rate pattern of the Central Range and the curvature-induced flexural extension in the western Taiwan foreland basin. GPS velocity field was estimated relative to the continuous GPS station S01R on the Penghu islands. GPS velocities for the stations from Coastal Range to Longitudinal Valley varied from 59.42 mm/yr to 83.28 mm/yr in azimuths ranging from 280.00° to 323.30°. GPS velocities for the stations from south of the Central Range to Hengchun Peninsula varied from 25.37 mm/yr to 61.80 mm/yr in azimuths ranging from 263.30° to 293.63°. The Hengchun Peninsula to southern Central Range, strain rate estimated from GPS velocities, is 0.01 – 1.8 μstrain/yr. From south to middle Coastal Range, the strain rate is 0.9 – 1.7 μstrain/yr. On the Hengchun Peninsula and Central Range areas, strain rate field from south to north shows significant ENE-WSW, E-W and ENE-WSW extension. In the southern Central Range, strain rate field from east to west is 0.19 µstrain/yr, 0.36 µstrain/yr and 0.02 µstrain/yr, respectively. In the central part of Penghu islands, strain rate field from south to north shows significant NNE-SSW to ESE-WNW extension. In the western side of Taiwan Strait, the strain rate estimated from GPS velocities is 0.004 - 0.009 μstrain/yr. In the eastern side of Taiwan Strait, the strain rate is 0.018 - 0.121 μstrain/yr. In the central part of Penghu islands, strain rate field from south to north shows significant convergence.
The velocity field of southern Taiwan was divided by Peikang High where Taitung is the boundary. Clockwise and counterclockwise rotations appears in the north and south of Taitung, respectively. Due to the lateral extrusion of southern Taiwan, the GPS velocity tends to accelerate in Kaoshung-Pingtung area. The principal strain rates from southern to northern Central Range shows significant extension. The extensional mechanism is due to the rapid exhumation where resulted from the collision between Philippine Sea Plate and Eurasian Plate. Over the twin flanks of Central Range, the extensional strain rate in east-west direction increased with the height of the range, and the top of the mountain also has the maximum extensional strain rate. This appearance was produced by simultaneous exhumation and mountain collapse. Taiwan Strait is still in a stable tectonic environment and Penghu islands are currently experiencing curvature-induced flexural extension resulting from the loading of Taiwan orogen.

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