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RESEARCH PAPERS

Implicit Large-Eddy Simulation in Meteorology: From Boundary Layers to Climate

[+] Author and Article Information
Piotr K. Smolarkiewicz

 National Center for Atmospheric Research, Boulder, CO 80307smolar@ucar.edu

Len G. Margolin

 Los Alamos National Laboratory, MS F644, Los Alamos, NM 87545len@lanl.gov

Andrzej A. Wyszogrodzki

 National Center for Atmospheric Research, Boulder, CO 80307andii@ucar.edu

J. Fluids Eng 129(12), 1533-1539 (Jul 21, 2007) (7 pages) doi:10.1115/1.2801678 History: Received January 18, 2007; Revised July 21, 2007

The dynamics of the atmosphere and oceans pose a severe challenge to the numerical modeler, due in large part to the broad range of scales of length and time that are encompassed. Modern numerical methods based on nonoscillatory finite volume (NFV) approximations provide a simple and effective means for mitigating this challenge by reproducing the large scale behavior of turbulent flows with no need for explicit subgrid-scale models. In this paper, we describe the remarkable properties of a particular NFV model, multidimensional positive definite advection transport algorithm, and highlight its application to a variety of meteorological and turbulent flows.

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Copyright © 2007 by American Society of Mechanical Engineers
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Figures

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Figure 1

Turbulence modeling of the convective PBL. ILES (solid line) and LES (long dashes) versus Schmidt–Schumann LES benchmark results (short dashes) and data (circles).

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Figure 2

EULAG LES of a hypothetical flow and contaminant dispersion in downtown of Oklahoma City

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Figure 3

Time-averaged westerly wind component (lower left) and resolved Reynolds stress (lower right) at a street-canyon location (x,y)=(474,954)m of Fig. 2, indicated by H in the upper panel. Circles and crosses denote results from two alternate LES, whereas thin lines are for alternate ILES runs. All alternate runs explore different means of momentum distribution near frictional boundaries.

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Figure 4

Instantaneous solutions of the idealized climate problem after three years of simulation. Plates a′ and a show isentropes in the vertical equatorial plane and at the surface, respectively. Plates b′ and b display the zonal velocity contours with imposed flow vectors, respectively, in the equatorial plane and at the surface. Contour extrema and intervals are shown in the upper left corner of each plate (in plate a′, we used a variable contour to capture θ variability in the troposphere). Negative values are dashed. Maximum vector lengths are shown in the upper right corner of plates b′ and b.

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Figure 5

The zonally averaged three-year means of potential temperature (plate a) and zonal velocity (plate b) for the simulation highlighted in Fig. 4. Contouring convention is similar to that used in Fig. 4.

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