Passive scalar roughness lengths for atmospheric boundary layer flow over complex, fractal topographies

Abstract

When modeling atmospheric boundary layer flow over rough landscapes, surface fluxes of flow quantities (momentum, temperature, etc.) can be described with equilibrium logarithmic law expressions, all of which require specification of a roughness length that is, physically, the elevation at which the flow quantity equals its surface value. In high Reynolds number flows, such as the atmospheric boundary layer, inertial forces associated with turbulent eddy motions are responsible for surface momentum fluxes (form, or pressure drag). Surface scalar fluxes, on the other hand, occur exclusively via diffusion in the immediate vicinity of the topography—the interfacial region—before being advected by turbulent eddy motions into the bulk of the flow. Owing to this difference in surface transfer mechanism, the passive scalar roughness length, $$z_{0S}$$ , is known to be less than the momentum roughness length, $$z_0$$ . In this work, classical relations are used to specify $$z_{0S}$$ during large-eddy simulation of atmospheric boundary layer flow over aerodynamically rough, synthetic, fractal topographies which exhibit power-law height energy spectrum, $$E_h (k) \sim k^{\beta _s}$$ , where $$\beta _s$$ is a (predefined) spectral exponent. These topographies are convenient since they resemble natural landscapes and $$\beta _s$$ can be varied to change the topography’s aerodynamic roughness (the study considers a suite of topographies with $$-2.4 \le \beta _s \le -1.2$$ , where $$-2.4$$ and $$-1.2$$ are the “most smooth” and “most rough” cases, respectively, corresponding with roughness Reynolds number, $$Re_0 \approx 10$$ and $$300$$ ). It is often assumed that $$z_{0S}/z_{0} \approx 10^{-1}$$ for all $$Re_0$$ . But results from this work show that the roughness length ratio, $$z_{0S}/z_{0}$$ , depends strongly on $$Re_0$$ , ranging between $$10^{-3}$$ and $$10^{-1}$$ .