Equilibrium

Equilibrium constant parameterized by Equation 5 of Fountoukis and Nenes (2007): log K(T) = log K(T0) + H_coeff*(T0/T - 1) + C_coeff*(1 + ln(T0/T) - T0/T), where T0 = 298.15 K. Migrated from Aerosol.jl@c8c640bb src/isorropia/equilibria.jl:5 (`EqConst` @component). Parameters logK0, H_coeff, and C_coeff are reaction-specific values from Table 2 of Fountoukis and Nenes (2007). T is an input (driven by parent EquilibriumConstants in the coupled system); logK_eq is an algebraically observed output.

Aggregated equilibrium constants for ISORROPIA II. Composes 27 EqConst sub-components (r1...r27) from Table 2 of Fountoukis and Nenes (2007). Each ri.logK_eq(T) = logK0_i + H_i*(T0/T-1) + C_i*(1+ln(T0/T)-T0/T). A single T is broadcast to all subsystems via coupling equations. Migrated from Aerosol.jl@c8c640bb src/isorropia/equilibria.jl:22 (esm-y4v).

Layer-averaged equilibrium volumetric water content (θ_E, Eq. 5.101) and equilibrium matric potential at the layer node (ψ_E, Eq. 5.106) for a single soil layer, following Oleson et al. (2010, CLM4 Tech Note Ch. 5, §5.3.2.1, Eqs. 5.98–5.106). θ_E is fully saturated (θ_sat) when the water table is above the layer (z_v < z_h_upper), otherwise is computed by integrating the hydrostatic-equilibrium Clapp-Hornberger profile across the layer, clamped to [0, θ_sat]. ψ_E is derived from the Brooks-Corey inverse relation with a 1% saturation floor and a hard lower bound at ψ_min = −10⁵ m to prevent numerical underflow. Migrated from UrbanCanopy.jl@9200edd4 src/hydrology.jl:509 (`SoilWaterEquilibrium` @component). Note: the migration-tracker row for this component carried the blocking_gap `other:discretization-plan` because the row description mentioned an in-file Richards-equation PDE at src/hydrology.jl:674. Inspection shows that PDESystem lives in a separate non-`@component` helper function (`RichardsEquation`) and is not part of `SoilWaterEquilibrium`, which is a plain two-equation algebraic `@component`. No discretization plan is needed.