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Download e-book for iPad: Boundary Layer Studies and Applications: A Special Issue of by John C. Wyngaard (auth.), R. E. Munn (eds.)

By John C. Wyngaard (auth.), R. E. Munn (eds.)

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Read or Download Boundary Layer Studies and Applications: A Special Issue of Boundary-Layer Meteorology in honor of Dr. Hans A. Panofsky (1917–1988) PDF

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Additional info for Boundary Layer Studies and Applications: A Special Issue of Boundary-Layer Meteorology in honor of Dr. Hans A. Panofsky (1917–1988)

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E uw/u. 86 VERTICAL VARIATION OF TURBULENCE QUANTITIES Studies of the stably stratified boundary layer over land show a systematic and well ordered decrease of turbulence quantities with height, when height and turbulence parameters are suitably normalised. , 1979). In the time-evolving boundary layer over land, normalised turbulence quantities are a function of z/ h and of time, but where the time evolution is small (as is usually the case well after sunset for example), z/ h becomes the dominant dependent variable.

I I ~ 1, /' ...... \ i !. ·.... 1'",. 1. \/ \. / · \ / I. I ! i 1 i . i '' J. , . i '- . I \1 i ' . 04L------'---~----'--_7~-L--'--------' -70 -35 o 35 70 SEPARA liON DISTANCE (m) Fig. 6. Composite kinematic fluxes of horizontal momentum and vertical heat flux across the divergent transition zone. Using this observation and the results above, an attempt is made to combine the composited features of the intense convergent and divergent zones into a conceptual model of one circulation system.

12a-c. The wavelength of the spectral maximum, normalised by the IBL depth h, as a function of z/h - data from Cases 3 and 4: (a) Potential temperature (0) and specific humidity (e); (b) u (e) and v (0) wind components; (c) w component, for Case 3 (0) and Case 4 (e). 4. 014 (Garratt, 1987 - his Figure to); the relation was at least valid for the ranges of parameter values as follows, x: 100-900 km U: 10-30 m S-1 AfJ: 5-16 K. THE STABLY STRATIFIED INTERNAL BOUNDARY LAYER 37 The numerical coefficient represented by a (see Appendix) actually depends on the 0 profile shape (through the quantity Ao), layer flux Richardson number (Rf ), geostrophic drag coefficient (Co) and {3, the angle the wind vector above the IBL makes with the coastline.

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