232314
20180317092444.0
0022-1120
10.1017/jfm.2017.372
doi
000411563700007
ISI
ARTICLE
Direct numberical simulation of turbulent slope flows up to Grash of number Gr=2.1 x 10(11)
New York
2017
Cambridge Univ Press
2017
32
Journal Articles
Stably stratified turbulent flows over an unbounded, smooth, planar sloping surface at high Grashof numbers are examined using direct numerical simulations ( DNS). Four sloping angles ( alpha = 15 degrees; 30 degrees; 60 degrees and 90 degrees) and three Grashof numbers (Gr = 5 X 10(10); 1 X 10(11) and 2 : 1 X 10(11)) are considered. Variations in mean flow, second- order statistics and budgets of mean- ( MKE) and turbulent- kinetic energy ( TKE) are evaluated as a function of ff and Gr at fixed molecular Prandtl number. Pr = 1 . Dynamic and energy identities are highlighted, which diagnose the convergence of the averaging operation applied to the DNS results. Turbulent anabatic ( upward moving warm fluid along the slope) and katabatic ( downward moving cold fluid along the slope) regimes are identical for the vertical wall set- up ( up to the sign of the along- slope velocity), but undergo a different transition in the mechanisms sustaining turbulence as the sloping angle decreases, resulting in stark differences at low ff. In addition, budget equations show how MKE is fed into the system through the imposed surface buoyancy, and turbulent fluctuations redistribute it from the low- level jet ( LLJ) nose towards the boundary and outer flow regions. Analysis of the TKE budget equation suggests a subdivision of the boundary layer of anabatic and katabatic flows into four distinct thermodynamical regions: ( i) an outer layer, corresponding approximately to the return flow region, where turbulent transport is the main source of TKE and balances dissipation; ( ii) an intermediate layer, bounded below by the LLJ and capped above by the outer layer, where the sum of shear and buoyant production overcomes dissipation, and where turbulent and pressure transport terms are a sink of TKE; ( iii) a buffer layer, located at 5 / z C / 30, where TKE is provided by turbulent and pressure transport terms, to balance viscous diffusion and dissipation; and ( iv) a laminar sublayer, corresponding to z C / 5, where the influence of viscosity is significant.. / C denotes a quantity rescaled in inner units. Interestingly, a zone of global backscatter ( energy transfer from the turbulent eddies to the mean flow) is consistently found in a thin layer below the LLJ in both anabatic and katabatic regimes.
atmospheric flows
boundary layer structure
meteorology
Giometto, M. G.
Univ British Columbia, Dept Civil Engn, Vancouver, BC V6T 1Z4, Canada
218957
246172
Katul, G. G.
Duke Univ, Nicholas Sch Environm, Durham, NC 27708 USA
Fang, J.
Ecole Polytech Fed Lausanne, Sch Architecture Civil & Environm Engn, CH-1015 Lausanne, VD, Switzerland
133327
240839
Parlange, M. B.
Univ British Columbia, Dept Civil Engn, Vancouver, BC V6T 1Z4, Canada
155043
242902
589-620
Journal Of Fluid Mechanics
829
oai:infoscience.tind.io:232314
article
EFLUM
252105
U11028
EPFL-ARTICLE-232314
EPFL
PUBLISHED
REVIEWED
ARTICLE