Abstract: Based on the conventional meteorological observations, the National Centers for Environmental Prediction (NCEP) Final (FNL) reanalysis data, satellite and radar measurements, we compared the characteristics and causes of precipitation during two extreme rainstorm events in the Southeast Peninsula of Liaoning province caused by the Typhoon "Damrey" in 2012 (Process 1) and the Typhoon "Haitang" in 2017 (Process 2) in this study.The results indicated that the precipitation during the two processes shows different characteristics.The stable and persistent heavy precipitation (lasting for 30 h) occurs over large areas during Process 1, due to the train effect caused by the multiple mesoscale cloud clusters triggered by a typhoon inverted trough.Process 2 is characterized by higher hourly precipitation intensity (reaching 113 mm·h^-1) and obvious convective precipitation.During Process 2, small-scale cumulus continue to regenerate and pour into the mesoscale cloud clusters.The radar charts show backward propagation, with basic reflectivity of strong storms of 50-60 dBz.The mesoscale convergent winds expand up to 9 km, and convective clouds develop more vigorously.Process 1 develops within the typhoon inverted trough, and Process 2 is generated by the interaction between warm-humid air transported by the typhoon and dry-cold air in the troposphere.During the two processes, a water vapor conveyor belt spanning 10 latitudes is formed between the typhoon remnant vortex and the Subtropical High, with the water vapor flux at 850 hPa reaching 20-25 g^-1·cm^-1·hPa^-1·s^-1 and the values of specific humidity and water vapor flux divergence reaching the rainstorm forecast thresholds for the landing typhoon in Liaoning province.The long-distance typhoons play a key role in blocking the southward movement of the Subtropical High and establishing the guiding airflow for the typhoons' northward movement.Due to the residual vortex inverted trough of typhoon "Damrey", the convergence layer extends from the ground to the height of 500 hPa during Process 1, exhibiting stronger dynamic uplift conditions.During Process 2, the pseudo-equivalent temperature at 850 hPa reaches 354 K, and the potential instability is stronger.Due to the large-scale convergence and forced uplift of terrains, deeper convective clouds are formed and generates more distinct convective precipitation.