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Lagrangian cloud model (LCM)

The LCM is based on the formulation of the LPM (Sect. lagrangian particle model). For the LCM, however, the Lagrangian particles are representing droplets and aerosols. The droplet advection and sedimentation is given by the Eqs. for du_p,i / dt and τ_p^-1 in Sect. formulation of the LPM with ρ_p,0 = ρ_l,0. At present it is computationally not feasible to simulate a realistic amount of particles. A single Lagrangian particle thus represents an ensemble of identical particles (i.e., same radius, velocity, mass of solute aerosol) and is referred to as "super-droplet". The number of particles in this ensemble is referred to as the "weighting factor". For example, q_l of a certain LES grid volume results from all Lagrangian particles located therein considering their individual weighting factor A_n:

with N_p being the number of particles inside the grid volume of size ΔV, and r_n being the radius of the particle. The concept of weighting factors and super-droplets in combination with LES has been also used similarly by Andrejczuk et al. (2208) and Shima et al. (2009) for warm clouds, as well as by Sölch and Kärcher (2010) for ice clouds.

Diffusional growth

The growth of a particle by diffusion of water vapor, i.e., condensation and evaporation, is described by

with the coefficients

depending primarily on the diffusion of water vapor in air and heat conductivity of air, respectively. f_v is the ventilation factor, which accounts for the increased diffusion of water vapor, particularly the accelerated evaporation of large drops precipitating from a cloud (e.g., Pruppacher and Klett, 1997, Chap. 13.2.3):

Here, Re_p is particle Reynolds number. The relative water supersaturation S is computed from the LES values of θ and q_v, tri-linearly interpolated to the particle's position. The equilibrium saturation term S_eq considers the impact of surface tension as well as the physical and chemical properties of the solute aerosol on the equilibrium saturation of the droplet. In order to take into account these effects, the optional activation model for fully soluble aerosols must be switched on:

with coefficients for surface tension

and physical and chemical properties

Here, ϑ is the temperature-dependent surface tension, and M_l = 18.01528 g mol^-1 the molecular mass of water. Depending on the simulation setup (e.g., continental or maritime conditions), the physical and chemical properties of the aerosol, its mass m_s, molecular mass M_s, and the van't Hoff factor F_vH, indicating the degree of the solute aerosol's dissociation, are prescribed. As discussed by Hoffmann et al. (2015), the aerosol mass (or equivalently aerosol radius) can be specified by an additional particle feature allowing the initialization of aerosol mass distributions, i.e., varying aerosol masses among the simulated particle ensemble.

In summary, diffusional growth is the major coupling between the LES and LCM model. The change of water vapor during one time step is considered in the prognostic equations for potential temperature (see Eq. three in Sect. governing equations) and specific humidity (see Eq. four in Sect. governing equations) by

Here, r_n and r_n^∗ are the radius of the nth droplet before and after diffusional growth, respectively. Since the diffusional growth (see first Eq. in Sect. diffusional growth) is a stiff differential equation, we use a 4th-order Rosenbrock-method (Press et al., 1996; Grabowski et al., 2011), adapting its internal time step for both a computationally efficient and numerically accurate solution.

Collision and coalescence

Recent applications

References

• Andrejczuk M, Reisner JM, Henson B, Dubey MK, Jeffery CA. 2008. The potential impacts of pollution on a nondrizzling stratus deck: Does aerosol number matter more than type?. J. Geophys. Res. 113: D19204. ​doi.

• Shima S-I, Kusano K, Kawano A, Sugiyama T, Kawahara S. 2009. The super-droplet method for the numerical simulation of clouds and precipitation: a particle-based and probabilistic microphysics model coupled with a non-hydrostatic model. Q. J. Roy. Meteor. Soc. 135: 1307–1320.

• Sölch I, Kärcher B. 2010. A large-eddy model for cirrus clouds with explicit aerosol and ice microphysics and Lagrangian ice particle tracking. Q. J. Roy. Meteor. Soc. 136: 2074–2093.

• Pruppacher HR, and Klett JD. 1997. Microphysics of Clouds and Precipitation. 2nd Edn. Kluwer Academic Publishers. Dordrecht.

• Hoffmann F, Raasch S, Noh Y. 2015. Entrainment of aerosols and their activation in a shallow cumulus cloud studied with a coupled LCM-LES approach. Atmos. Res. 156: 43–57. ​doi

• Press WH, Teukolsky SA, Vetterling WT, and Flannery BP. 1996. Numerical Recipes in Fortran 90: the Art of Parallel Scientific Computing. 2nd Edn. Cambridge University Press. Cambridge.

• Grabowski WM, Andrejczuk M, Wang L-P. 2011. Droplet growth in a bin warm-rain scheme with Twomey CCN activation. Atmos. Res. 99: 290–301.