By David H. Bromwich, Charles R. Stearns
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Published by means of the yankee Geophysical Union as a part of the Antarctic learn Series.
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Additional info for Antarctic Meteorology and Climatology: Studies Based on Automatic Weather Stations
Dep. , Univ. , Madison, 19850. Savage, M. , C. R. Stearns, and D. , Dep. , Univ. , Madison, 19856. Savage, M. , C. R. Stearns, and D. , Dep. , Univ. , Madison, 1985c. Savage, M. , C. R. Stearns, G. A. Weidner, and D. , Dep. , Univ. , Madison, 1985d. Savage, M. , C. R. Stearns, G. A. Weidner, and D. , Dep. , Univ. , Madison, 1985e. , The TIROS-N/NOAA A-G satellite series, NOAA Tech. Memo. S. Dep. , Washington, D. C , 1978. , G. A. Weidner, and C. R. , Dep. , Univ. , Madison, 1986. , G. A. Weidner, and C.
Profile m e a s u r e m e n t s allowed us to calculate t h e e d d y fluxes. In Figure 17 the diurnal variation of the sensible and latent h e a t flux are p r e s e n t e d . It can be seen that t h e t surface w a r m s the air for the average s u m m e r day (negative flux), while at night t h e flux is in t h e opposite direction. T h e average latent heat flux is mostly nega tive, with larger values during the day a n d slightly positive values a r o u n d midnight. T h e heat flux into or out of t h e s n o w w a s obtained from the t e m p e r a t u r e in t h e s n o w .
Profile of (a) temperature, (b) wind speed, and ( c ) wind direction through the boundary layer, summer, Adelie Coast. s u p p o r t e d b y t h e p r e s e n c e of an inversion layer over t h e sloping t e r r a i n , which generates katabatic wind. During daytime t h e surface geostrophic wind d u e to the m e s o s cale horizontal t e m p e r a t u r e gradient r e m a i n s and acts j u s t like t h e katabatic wind at night. 4. Blowing Snow Strong w i n d s o v e r a s n o w surface t r a n s p o r t s n o w .