Based on the Modern-Era Retrospective analysis for Research and Applications reanalysis dataset, this study analyzes the classification of stratosphere final warming (FW) that takes both the stratosphere and the lower mesosphere into account. The results show that the seasonal transition of circumpolar zonal wind from westerly to easterly wind also exists in the lower mesosphere, which is similar to that in the stratosphere. In addition, the interannual variability of polar-mean air temperature and circumpolar zonal wind in spring in the lower mesosphere is as strong as that in the stratosphere. Thus it is suggested that FW events still appear in the lower mesosphere. The annual FW onset date at each pressure level is then determined. It is found that the average onset date of FW events varies from April 7th to 27th at different pressure levels with a standard deviation varying from 11.3 to 18.3 days. The latest onset occurs at 1 hPa and the minimum standard deviation occurs at 0.1 hPa. According to the characteristics of the vertical profile of FW onset date, this study classifies the FW events into three types. That is simultaneous type, successive type, and climatology-like type, respectively. The FW occurs almost simultaneously at the whole levels from the mid-stratosphere to lower mesosphere in the simultaneous type. Accompanying with the FW occurrence, there is a reversal of the sign of polar-mean geopotential height and temperature anomalies. Strong planetary wave activities dominate the onset process of this type. Although the onset process of the successive type is relatively similar to that of the simultaneous type, the planetary wave activities weaken greatly during the FW onset in this type. The non-adiabatic heating of solar radiation plays an important role in this type. In the climatology-like type, the occurrence of FW event at 10 hPa is dominated by dynamics. After the occurrence of FW event in the mid-stratosphere, the planetary wave activities are inhibited in the upper stratosphere which causes the occurrence of FW event mainly resulting from non-adiabatic heating in those pressure levels. There are two possible explanations for the FW onset at 0.1 hPa. On the one hand, the 0.1-hPa FW onset may be dominated by non-adiabatic heating. On the other hand, for some FW events, secondary planetary wave activities following FW onset in the stratosphere may lead to the onset of FW at 0.1 hPa.