H. Morrison, A. Gettelman (NCAR) , S. Ghan (PNL)

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Presentation transcript:

Two-moment Stratiform Cloud Microphysics & Cloud-aerosol Interactions in CAM H. Morrison, A. Gettelman (NCAR) , S. Ghan (PNL) Thanks to: P. Field, S. Massie (NCAR), R. Wood (UW-Seattle) Morrison/Gettelman AGU December 2006

Motivation Aerosol-cloud interactions Better treatment of ice Multi-scale modeling (unify treatments) Method: Extend bulk microphysics (Rasch & Kristjannson, 1998) to do number. New Scheme based on Morrison et al (2005) Morrison/Gettelman AGU December 2006

N = number concentration q, N Convective Detrainment Aerosol (CCN q = mixing ratio N = number concentration q, N Convective Detrainment Aerosol (CCN Number) Aerosol (IN Number) q, N Cloud Droplets (Prognostic) q, N Cloud Ice (Prognostic) Conversion Processes Evap/Cond Dep/Sub q Water Vapor (Prognostic) Evaporation Sublimation Riming q, N Rain (Diagnostic) q, N Snow (Diagnostic) Sedimentation Sedimentation Morrison/Gettelman AGU December 2006

Key features of the new scheme Two-moment – predicts number concentrations and mixing ratios of cloud water and ice. Liquid/ice fraction determined by microphysical processes (Bergeron, heterogeneous freezing) instead of simple function of temperature. Coupled with aerosol by treating droplet activation (Abdul-Razzak and Ghan 1998) and ice nucleation (Cooper 1986). Diagnostic treatment of rain and snow mixing ratio and number concentration. Self-consistent treatment of sub-grid cloud water distribution for all relevant microphysics processes – straightforward to couple with diagnostic cloud scheme. Flexibility to allow independent column approach. Morrison/Gettelman AGU December 2006

Mixed Phase Processes Observed Simulated (QJRMS, 2004) why there is a small amount of ice above +5 C and liquid below -40 C (homogeneous freezing threshold in the model). This is because the output temperature is not exactly the same temperature that the microphysics scheme sees - it is affected by other processes. So for example, if the temperature is some value when it is output, by the time the microphysics sees the temperature (and the microphysical variables are output) it may have shifted several degrees due especially to the long time step in CAM. Morrison/Gettelman AGU December 2006

Particle Sizes Morrison/Gettelman AGU December 2006

Droplet Number Morrison/Gettelman AGU December 2006

AVHRR Column Drop Number Lohmann et al, 1999 from Han et al 1998 Morrison/Gettelman AGU December 2006

Tests of Aerosol effects Test with observations: Massie et al 2006 Indian ocean case Test run with sulfur scaled to 30% present Approx value for pre-industrial Morrison/Gettelman AGU December 2006

Observed Aerosol effects CAM sensitivity to aerosols is larger than MODIS for this particular region - but this may not necessarily be true for other regions or globally. Also, since we are using diagnostic aerosol, all variability in CAM aerosol optical depth is due to spatial variability, in MODIS, the aerosol optical depth varies over space and time. So, it is possible that the CAM results may more strongly reflect spatial variability that is not due entirely to changes in aerosol, if there is cross correlation between the CAM aerosol optical depth and other features such as the dynamics. MODIS data: S. Massie, 2006 Morrison/Gettelman AGU December 2006

Observed Aerosol effects CAM sensitivity to aerosols is Larger than MODIS in this region CAM MODIS MODIS data: S. Massie, 2006 Morrison/Gettelman AGU December 2006

‘Indirect’ Effects Scale sulfate aerosols to 30% present day See differences in: Radiative Forcing Size and number Liquid water path Changes to Radiative forcing (Wm-2), using Ghan method: Size Number Total Direct Indirect Num Size -3.0 -0.7 -2.3 -1.0 -1.3 Pre-industrial Present Morrison/Gettelman AGU December 2006

+10% Change in Liquid water Present Day Liquid Water Largest changes in Storm Tracks where LWP large. Little change in In stratocumulus regions Preindustrial - Present most of the change in the mid-latitude storm tracks, which is not surprising given that the highest amounts of liquid water are located there. The fact that we are getting little impact in the deep tropics may reflect the fact that the aerosol doesn't impact droplet number from detrained convection. Interestingly, there seems to be almost no impact on the subtropical stratocumulus regions - this is a very interest result. Morrison/Gettelman AGU December 2006

Summary/Conclusions New scheme performs well Aerosols affect clouds Reasonable Re distribution Reasonable Number distribution Aerosols affect clouds Sizes, Number, Liquid water path & Radiation Model ‘indirect’ effects are too strong Likey due to fixed size of nucelating aerosols Need to look more at observations, different regions Next Steps Refine aerosol nucleation treatment Focus on ice phase Morrison/Gettelman AGU December 2006