Ye. Yu. Fedurin, N. A. Kalinin 

Perm State University, Perm, Russian Federation

Methods of estimation of the atmospheric boundary layer height according to the rawinsonde measurements are considered. Calculations based on the data obtained during observations from the Perm land-based rawinsonde station for the period 2018 to 2024. The atmospheric boundary layer height was estimated based on calculations of the bulk Richardson number and the vertical gradient of the virtual potential temperature. The critical value of the Richardson number indicates atmospheric stability and turbulence. The first point at which the value of bulk Richardson number first reached the critical value is taken as the atmospheric boundary layer height. In other words, the atmospheric boundary layer it is the most turbulent layer of the atmosphere. The article suggests using four critical values of the Richardson number Ri_BC = {0,1; 0,25; 0,5; 1,0}. The critical value of the Richardson number Ri_BC = 1,0 shows the most accurate values of the atmospheric boundary layer height. It was determined that the maximum thickness of the atmospheric boundary layer is observed during daytime in summer (1800 m), and the minimum at nighttime in summer (500 m). Moreover, during daytime there is a trend of increasing of the atmospheric boundary layer height from winter to summer, and at nighttime the atmospheric boundary layer height has maximum values in the spring and autumn. Virtual potential temperature profiles are nearly adiabatic in the atmospheric boundary layer. The first point at which the vertical gradient of the virtual potential temperature becomes non-adiabatic is taken as the height of the atmospheric boundary layer. The article shows that values of the atmospheric boundary layer height based on calculations of the vertical gradient of the virtual potential temperature are too large. The use of the considered methods allows to estimate the atmospheric boundary layer height based on the rawinsonde data without making additional measurements, and these methods can be used to study the atmospheric processes occurring in this layer.

Fedurin Yegor Yurievich, Postgraduate, Department of Meteorology and Atmosphere Protection Perm State University 15, Bukirev st., Perm, 614068, Russian Federation e-mail: egor.fedurin@gmail.com 

Kalinin Nikolay Aleksandrovich, Doctor of Sciences (Geography), Professor of the Department of Meteorology and Atmosphere Protection Perm State University 15, Bukirev st., Perm, 614068, Russian Federation e-mail: kalinin@psu.ru

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