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• W290046383 abstract "Venkatesh and Csanady (1974) have proposed a simple and novel method of determining some of the important boundary-layer parameters by fitting the measured wind profile to their eddy-viscosity model and the layer averaged equations of mean momentum. Their application of this to unstable or convective conditions is to be questioned, however, because the eddy-viscosity concept becomes generally invalid under such conditions, since buoyancy can transfer considerable momentum even when the mean velocity gradient is close to zero or of wrong sign in the bulk of the mixed layer (see Deardorff, 1972; Pennell and LeMone, 1974; Wyngaard et al., 1974a). The authors have simply avoided the problem of infinite or negative eddy viscosity by a priori assuming the validity of their K-model and then determining K indirectly from their so-called Ekman-layer depth D or H=2.3D, defined as the layer ‘characterized by rapid velocity variations’. Since their other parameters, such as surface geostrophic and thermal winds, are also dependent on H, the question arises how good is H as a measure of boundary-layer height under unstable conditions? Turbulence generated by thermal convection and the resulting mixing of air extend right up to the level oi‘ first inversion base and one would expect its height zi to be the appropriate height of the unstable boundary layer (see Lenschow, 1970; Deardorff, 1972; Wyngaard et al., 1974b). Convective mixing also affects mean velocities in the sense that they become more nearly uniform, especially in the upper part of the mixed layer. Therefore the layer in which mean velocity varies rapidly is expected to be considerably shallower than zi. Table I, representing the Wangara day-time runs, shows that this is indeed so (here H is based on the values of D tabulated by Venkatesh and Csanady, and zi represents the mean height of the inversion base as indicated by the measured potential temperature profiles at 1200 and 1500 local time). Note that H can be considered close enough to zi for only about one third of the total number of days, all of which could be characterized by rather strong winds and weak convection. Determination of thermal winds and other parameters by the authors depends on their assumption that geostrophic balance exists for z> H. This becomes rather untenable when His considerably smaller than zi, because it ignores the fact that there are also significant momentum fluxes in the part of the mixed layer above H. Large values of momentum flux in the upper part of a convective boundary layer have been ob-" @default.
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• W290046383 date "1975-01-01" @default.
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• W290046383 title "COMMENTS ON 'A BAROCLINIC PLANETARY BOUNDARY-LAYER MODEL AND ITS APPLICATIONS TO THE WANGARA DATA' Correspondence" @default.
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