蓬萊運動的弧陸斜碰撞使得台灣造山帶的山脈呈現崩塌(北部)、均衡(中部)、成長(南部)等三個不同演育階段的地形。河流水力侵蝕模型與基岩河道的河流縱剖面擬合分析的結果顯示，台灣均衡山脈的範圍北界約在蘭陽溪(東部)與大安溪(西部)附近，南界約在樂樂溪(東部)與老濃溪(西部)附近，其S-A關係圖呈現直線關係，河流縱剖面的擬合主要以指數函數為主，而位於均衡山脈以北與以南的山脈地區，其S-A關係圖則分別呈現下凹與上凸關係，河流縱剖面的擬合則以對數函數為主。
面積高度積分值(HI)的分佈與台灣地體生成的時序相關，除了最晚生成的平原區是因其沖積平原的性質而造成HI值的升高外，整體趨勢是中央山脈地質區相對於其兩側的海岸山脈與西部麓山帶早生成，其HI值相對較高，而西部麓山帶北段的HI值又比南段的高，暗示西部麓山帶的北段比南段早生成。此外，HI值在台灣西部海岸平原的分佈形態顯示，北港高區的影響不僅造成台灣西部前陸褶皺逆衝帶的發展，也造成近期台灣西部海岸平原沉積物的變形。
集水盆地的面積高度曲線型態與高程頻率分佈圖可反應該集水盆地的演育期與其內所殘留的土地體積分佈狀態。台灣的平原地形區中，單純的沖積平原其面積高度曲線呈現S形，高程頻率分佈集中在中高程部分，而構造陷落盆地或平原則呈現凹形，高程頻率分佈集中在低高程部分；西部麓山帶的面積高度曲線大致呈現凹形，高程頻率分佈集中在低高程部分。由於持續受到抬升作用的影響，西部麓山帶未來面積高度積分會逐漸增加，曲線朝S形發展，高程頻率往中高程集中。而於近期內抬升量較大的地區如林口、后里、湖口、台南台地等，其曲線呈現凸形，符合Strahler的幼年期；中央山脈地區的高程頻率分佈為常態分佈，曲線呈現S形且離散程度小，顯示此區的抬升作用與剝蝕作用達到平衡；海岸山脈的面積高度積分值偏低，曲線呈現凹形，高程頻率分佈主要在低高程的部分，與西部麓山帶的丘陵區型態類似。此外，一些尺度較小且近期內才形成的局部背斜或向斜構造，亦會造成局部面積高度積分值偏高或偏低的現象，顯示面積高度積分可用來偵測局部的構造變化。
以變異曲線法計測地形面的碎形參數時，可得到碎形維度值(D)、縱座標軸截距值(γ)與地表面任兩點間距離為40m時的坡度期望值等三個重要的地形碎形參數。發育較久的台灣山地地形特徵為起伏度大(γ大)，地表粗糙度小(D小)，最大坡度期望值大，而較近期發育的平原地形特徵則為起伏度小(γ小)，地表粗糙度大(D大)，最大坡度期望值小。由於地形特徵乃地形在形成過程中侵蝕的粗糙化作用、堆積的大尺度平滑化作用和擴散的小尺度平滑化作用間均衡的結果，而擴散作用的程度和時間成正比，因此地表粗糙度與最大坡度期望值亦反應了地形的發育期。
台灣中、北部地區構造線附近的標準化河流坡降指標(SL/k)值相對於嘉南至南部地區而言較高且Hack剖面呈現上凸形態的結果顯示，中、北部地區的構造活動傾向將應變潛能持續累積在地層中，而嘉南至南部地區則傾向將應變潛能以較高再現頻率的中、小規模地震釋放出來。其中位於北港高區以北斜壓帶的中部地區，具有高抬升累積與低水平縮短的地殼變形特徵，而位於北港高區以南斜張帶的嘉南地區，則具有低抬升累積與高水平縮短的地殼變形特徵。此外，台灣各活動斷層附近的SL/k值分佈亦暗示了來自菲律賓海板塊的推擠應力是由東向西以及由北向南傳遞分配的趨勢。
在分析台灣山脈於各均衡狀態時的一維地形特性上，由於河流縱剖面擬合分析比河流坡降指標與Hack剖面形態分析更為適用，因此綜合面積高度積分、地形碎形參數與河流縱剖面擬合的結果，雪山山脈、脊樑山脈、阿里山脈等均衡山脈地形區，其具有發展到最高的S形平均面積高度曲線、最高的平均面積高度積分值、最大的坡度期望值、最低的地表碎形維度值以及河流縱剖面的擬合呈現指數函數等構造地形指標特性；大武山脈與恆春半島等成長山脈地形區，其具有最低的S形平均面積高度曲線、最低的平均面積高度積分值、最低的最大坡度期望值、最高的地表碎形維度值以及河流縱剖面的擬合呈現對數函數等構造地形指標特性；而屬於崩塌山脈地形的雪山北部，其構造地形指標特性則介於以上兩者之間。
由以上分析可知，S-A關係圖可直接反應山脈地形的均衡、成長或崩塌狀態，而河流縱剖面的擬合則只能反應山脈地形是否均衡的一維性質。同時綜合次集水盆地的面積高度積分值、面積高度曲線與高程頻率分佈等參數可反應山脈地形在各均衡狀態時的三維性質，而同時綜合D值、γ值與最大坡度期望值等三個地表碎形參數則能反應山脈地形在各均衡狀態時的二維性質。

Oblique arc-continent collision in the period of Penglai orogeny made the Taiwan mountain belt develop landscape of three evolution stages of post-steady-state (north Taiwan, collapsing range), steady-state (central Taiwan) and pre-steady-state (south Taiwan, growing range). Analysis of stream-power erosion model shows linear form in the S-A plot and fittings of bedrock profiles are mainly the exponential functions in the steady-state range. The north boundaries of the steady-state range are near the Lanyang river (east Taiwan) and Taan river (west Taiwan), and the south boundaries are near the Lele river (east Taiwan) and Laonung river (west Taiwan). Moreover, the S-A plots in the ranges of north and south Taiwan show concave and convex forms, respectively, and fittings of bedrock profiles are both logarithmic.
Distribution of hypsometric integral (HI) in Taiwan reflects the uplift sequence of the Taiwan orogenic belt. The Central Range with higher HI uplifted earlier than the Eastern Coastal Range and the Western Foothills. In the Western Foothills, higher HI in the north district once implies that the north district uplifted earlier than the south district. Due to aggradation process, the plain areas that uplifted most presently have high HI contrarily. Pattern of HI in the Western Coastal Plain also shows that the passive indentation of the Peikang High has exerted crustal deformation not only to the oblique propagating fold-and-thrust units in the Western Foothills but also to the recent sediments in the Coastal Plains.
The hypsometric curve and the altitude frequency distribution reflect the landscape evolution stages and the residual mass distribution of drainage basin, respectively. In the plain areas, the hypsometric curves of the alluvial plains are S-shaped and the altitude frequency distribution concentrate in median altitude, but the hypsometric curves of the structural subsidence basins or plains are concave and the altitude frequency distribution concentrate in low altitude. In the western foothills, the hypsometric curves are concave and the altitude frequency distribution concentrate in low altitude. Due to continuous uplift process, the HI of the western foothills will increase, the hypsometric curves will gradually develop to S-shaped, and the altitude frequency distribution will finally concentrate in median altitude. Moreover, hypsometric curves of some high uplift rate areas, such as Linkou, Houli, Huko and Tainan tablelands, are convex and quite similar to the young age of the Strahler model. In the central range, due to the balance of uplifting and erosion, the hypsometric curves are all S-shaped and the altitude frequency show normal distribution. In the eastern coastal range, the hypsometric curves are concave and the altitude frequency distribution concentrate in low altitude, and are very similar to the hill areas in the western foothills. Beside, increasing or decreasing of HI caused by some local but young anticline or syncline shows that HI could be a good tool for detecting local variations of subsurface structures.
The variogram method is adopted to estimate the fractal dimension (D), the ordinate-intercept (γ) and the maximum expected slope from data subsets of the DEM using a moving-window operation. The mountainous terrain is characterized by high relief (high γ), low roughness (low D) and high maximum expected slope in contrast to the plain areas where low relief (low γ), high roughness (high D) and low maximum expected slope are found. The landscape may involve the balance between erosional roughening at all scales and diffusive smoothing at short wavelengths plus depositional smoothing at long wavelengths. Because the diffusive process has a negative correlation with roughness, the roughness and the maximum expected slope can also reflect the evolution stages of landscape.
According to the higher SL/k and convex Hack profile in the north to central Taiwan than in the chianan to south Taiwan, structures in the north to central Taiwan tend to easier “lock” strain energy caused by tectonic activities but to the contrary, strain energy in the chianan to south Taiwan tend to be “released” by median to small magnitude earthquakes with higher reoccurrence frequency. Moreover, a high uplift but low shortening rate typifies the crustal deformation style in the transpressional regime north of the Peikang Basement High in central Taiwan. On the contrary, a low uplift but high shortening rate characterizes the crustal deformation style in the transtensional regime south of the Peikang Basement High in southwestern Taiwan. Distribution of SL/k near the active faults in Taiwan implies that collision stress caused by the Philippine Sea plate spreads not only form east to west but also from north to south.
Fitting of river longitudinal profile is a more suitable tool than the SL index and Hack profile when analyzing one-dimensional landform characteristics of Taiwan ranges. Thus, summarizing the results of hypsometric integral, fractal parameters and fitting of river longitudinal profile, we fould that the steady-state ranges, such as Hsueshan range, Back-bone range and Ali range, have the highest S-shaped hypsometric curves, the highest HI, the highest maximum expected slope, the lowest surface fractal dimension and the exponential fitting function. The growing ranges, such as Tawu range and Hengchun Peninsula, have the lowest S-shaped hypsometric curves, the lowest HI, the maximum expected slope, the highest surface fractal dimension and the logarithmic fitting function. And then the morphotectonic index features of the collapsing North-Hsueshan range are between the two types of ranges mentioned above.
Concluding all the results above, the S-A plot can directionly show us the evolution stages of ranges, and the fitting of river longitudinal profile can also tell us that if ranges reach steady-state or not. Summarizing the results of hypsometric curve, HI, and altitude frequency distribution can reflect the three-dimensional landform characteristics of the Taiwan ranges in all evolution stages. And summarizing the results of D, γ and the maximum expected slope can reflect the two-dimensional landform characteristics.

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