- Ground-motion model for shallow crustal earthquakes is:
where A is in cm∕s2, c

_{1}= 2.8096, c_{2}= 0.8993, c_{3}= 0.4381, c_{4}= 1.0954, c_{5}= 0.0079 and σ = 0.60.Ground-motion model for subduction earthquakes is:

where A is in cm∕s2, c′

_{1}= 4.7141, c′_{2}= 0.8468, c′_{3}= 0.17451, c′_{4}= 1.2972 and σ = 0.56. - Note that there is limited site information available for strong-motion stations in Taiwan so do not consider local site effects.
- Use strong-motion data from Central Weather Bureau from 1994 to 1998 because it is more numerous and of better quality than older data.
- Separate earthquakes into shallow crustal and subduction earthquakes because of different seismic attenuation and seismogenic situation for the two types of earthquake.
- Shallow crustal earthquakes are mostly due to continental deformation, shallow collision or back-arc
opening or are the uppermost interface earthquakes. Focal depths depth between 1.1 and 43.7km with
most shallower than 20km. Most records from earthquakes with 4.5 ≤ M
_{w}≤ 6.0. - Subduction earthquakes are located in the Wadati-Benioff zone or the deep lateral collision zone and are principally intraslab. Focal depth between 39.9 and 146.4km.
- Do not use records from earthquakes associated with coseismic rupture because they have complex near-field source effects.
- To avoid irregularly large amplitudes at great distances reject distant data predicted to be less than trigger
level plus 1 standard deviation using this threshold formula: aM
_{w}-blnD+c ≥ lnV , where V is geometric mean of PGA equal to threshold plus 1 standard deviation. For shallow crustal earthquakes: a = 0.64, b = 0.83, c = 2.56 and V = 6.93 and for subduction earthquakes: a = 0.76, b = 1.07, c = 3.13 and V = 6.79. - For shallow crustal earthquakes examine effect of focal depth on seismic attenuation by finding geometric
attenuation rate using epicentral distance, D
_{e}, for earthquakes with 5km depth intervals. Find that deeper earthquakes have slower attenuation than shallow earthquakes. Therefore assume ground motion, A, is product of f_{source}(source effects) and f_{geometrical-spreading}(geometrical spreading effects) where

f_{source}= C_{1}exp(c_{2}M)∕D_{p}^{-c3}and f_{geometrical-spreading}= D_{e}^{-(c4-c5Dp)}where D_{p}is focal depth. - For subduction earthquakes examine effect of focal depth in the same way as done for shallow crustal
earthquakes but find no effect of focal depth on attenuation rate. Therefore use f
_{geometrical-spreading}= D_{h}^{-c4}. - Plot residuals of both equations against distance and find no trend.
- Note that it is important to separate subduction and shallow crustal earthquakes because of the different role of focal depth and attenuation characteristics.
- Plot residual maps of ground motion for Taiwan and find significant features showing the important effect of local structures on ground motion.
- Cite various published models for Taiwan
^{14}.

^{14}These are not summarised here as they are in Chinese and are not easily available.