The Ocean-Land-Atmosphere Model (OLAM) Robert L. Walko Roni Avissar Rosenstiel School of Marine and Atmospheric Science University of Miami, Miami, FL Martin Otte U.S. Environmental Protection Agency Research Triangle Park, NC 27711 David Medvigy Department of Geosciences and Program in Atmospheric and Oceanic Sciences, Princeton University, Princeton, NJ Motivation for OLAM originated in our work with the Regional Atmospheric Modeling System (RAMS) RAMS, begun in 1986, is a limited-area model similar to WRF and MM5 Features include 2-way interactive grid nesting, microphysics and other physics parameterizations designed for mesoscale & microscale simulations But, there are significant disadvantages to limited-area models External GCM domain RAMS domain Numerical noise at lateral boundary Information flow OLAM global lower resolution domain OLAM local high resolution region Information flow Well behaved transition region So, OLAM was originally planned as a global version of RAMS. OLAM began with all of RAMS’ physics parameterizations in place. Global RAMS 1997: “Chimera Grid” approach Lateral boundary values interpolated from interior of opposite grid Not flux conservative OLAM dynamic core is a complete replacement from RAMS Based on icosahedral grid Seamless local mesh refinement OLAM: Relationship between triangular and hexagonal cells (either choice uses Arakawa-C grid stagger) OLAM: Hexagonal grid cells Downscaling Regional Climate Model Simulations to the Spatial Scale of the Observations Terrain-following coordinates used in most models OLAM uses cut cell method One reason to avoid terrain-following grids: Error in horizontal gradient computation (especially for pressure) P P V V P P Another reason: Anomalous vertical dispersion Wind Thin cloud layer Terrain-following coordinate levels Terrain Continuous equations in conservation form Vi viV p i 2 v i g i Fi t Momentum conservation (component i) V M t Total mass conservation ( ) V H t p d Rd v Rv CP CV 1 p0 ( s) s V Q t conservation Rd CV Equation of State Scalar conservation (e.g. sv v / ) d v c Total density V v Momentum density qlat 1 C max( T , 253 ) p = potential temperature = ice-liquid potential temperature Finite-volume formulation: Integrate over finite volumes and apply Gauss Divergence Theorem d d d Discretized equations: p Vi d viV d d 2 v t xi d V d Fm d t d V d F d t s d s V d Fs d t i d gi d Fi d Conservation equations in discretized finite-volume form (SGS = “subgrid-scale eddy correlation”) Vi p 1 vi j V j SGS{vi j ,V j } j 2 v i gi Fi t xi j cell volume 1 V j j t j cell face area d 1 jV j SGS{ j ,V j } j H t j s 1 s j V j SGS{s j ,V j } j Q t j p sd Rd sv Rv CP CV 1 p0 Rd CV Discretized momentum density is consistent between all conservation equations Grid cells A and B have reduced volume and surface area Fully-underground cells have zero surface area A B Land cells are defined such that each one interacts with only a single atmospheric level Land grid cells Cut cells vs. terrain-following coordinates High vertical resolution near ground Direction of atmospheric isolines C-staggered momentum advection method of Perot (JCP 2002) 3D wind vector diagnosed Normal wind prognosed Neighbors of W point on hexagonal mesh itab_w(iw)%im(1:7) itab_w(iw)%iv(1:7) itab_w(iw)%iw(1:7) iw5 iw4 iv5 im4 iw6 im5 iv4 iv6 im3 im6 iw im2 iv7 iw7 iv3 im7 im1 iv2 iv1 iw1 iw2 iw3 Neighbors of V point on hexagonal mesh iw4 iv10 itab_v(iv)%im(1:6) itab_v(iv)%iv(1:16) itab_v(iv)%iw(1:4) iv11 im6 im5 iv12 iv9 iv3 iv4 im2 iv15 iv16 iv iw1 iw2 iu iv14 im1 iv13 iv5 iv2 iv1 iv8 im4 im3 iv6 iw3 iv7 Neighbors of M point on hexagonal mesh iw2 iv3 iw1 im iv2 iv1 iw3 itab_m(im)%iv(1:3) itab_m(im)%iw(1:3) RAMS/OLAM Bulk Microphysics Parameterization • Physics based scheme – emphasizes individual microphysical processes rather than the statistical end result of atmospheric systems • Intended to apply universally to any atmospheric system (e.g., convective or stratiform clouds, tropical or arctic clouds, etc.) • Represents microphysical processes that are considered most important for most modeling applications • Designed to be computationally efficient Physical Processes Represented • • • • • • • • • • Cloud droplet nucleation Ice nucleation Vapor diffusional growth Evaporation/sublimation Heat diffusion Freezing/melting Shedding Sedimentation Collisions between hydrometeors Secondary ice production Hydrometeor Types C 1. Cloud droplets D 2. Drizzle R 3. Rain P 4. Pristine ice (crystals) S 5. Snow A 6. Aggregates G 7. Graupel H 8. Hail Stochastic Collection Equation drx N tx N tyF dt 4a 0 0 f f mDxDx Dy Vtx Dx Vty D y 2 f mgx Dx f mgy D y E x, y dDx dDy Table Lookup Form of Collection Equation rx N tx N tyF E x, y t 4a J x, y , Dnx , Dny A wca V fluxes water rvc C wvc hvc wvs V wgc hgc rgv G2 wgvc1 G1 hgg wgg LANDCELL 1 rav rsv has hca C hvs wsc hsc rsa S2 wss rga wgvc2 was wca wvc LEAF–4 sensible heat hav hca hvc longwave radiation wav wgs wgvc2 wgg wgvc1 S1 hss G2 hgs G1 hgg LANDCELL 2 Water flux between soil layers Fwgg y z wh z Hydraulic conductivity(m/s) h h s h s 2b 3 Soil water potential (m) b h s y y s ; h Ks = saturation hydraulic conductivity ys = saturation water potential w = density of water [h / hs ] = soil moisture fraction b = 4.05, 5.39, 11.4 for sand, loam, clay ys 0 How should models represent convection at different grid resolutions? Conventional thinking is to resolve convection where possible and to parameterize it otherwise. Deep Convection Shallow Convection resolve resolve 0.1 ? ? parameterize parameterize 1 10 Horizontal grid spacing (km) 100