(1) From the ground to 3 kilometers (mainly from the friction layer of 500- 1000 meters), the low-level airflow flows into this layer, and the airflow has a significant radial component converging toward the center. Due to the geostrophic bias, the inward airflow rotates in the cyclone. The closer it is to the typhoon center, the shorter the rotation radius, the greater the curvature of the isobar and the corresponding increase in centrifugal force. Under the action of geostrophic bias and centrifugal force, the inward airflow can't reach the center of the typhoon, and it strongly hovers around the eye wall of the typhoon. This layer has a decisive influence on the occurrence, development and extinction of typhoons; (2) The middle transition layer is about 3-8 kilometers, and the meridional component of the airflow is already very small, mainly circling around the eye wall of the typhoon in the tangential direction, and the rising speed reaches the maximum between 700-300 mbar;
(3) From about 8km to the tropopause (about 12- 16km), it is the upper outer layer. The tangential wind speed of this layer of updraft is very high, and at the same time, a lot of latent heat is released during the ascending process, which causes the temperature in the middle of the typhoon to be higher than that around it, and the horizontal pressure gradient force in the typhoon gradually decreases with the increase of height. When the updraft reaches a certain height (about 10-), the air outflow is roughly equivalent to the inflow of the inflow layer.