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**Geoscientific Model Development**
An interactive open-access journal of the European Geosciences Union

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**Model description paper**
23 Mar 2020

**Model description paper** | 23 Mar 2020

Simulating coupled surface–subsurface flows with ParFlow v3.5.0: capabilities, applications, and ongoing development of an open-source, massively parallel, integrated hydrologic model

Simulating coupled surface–subsurface flows with ParFlow v3.5.0: capabilities, applications, and ongoing development of an open-source, massively parallel, integrated hydrologic model
Simulating coupled surface–subsurface flows with ParFlow v3.5.0: capabilities, applications,...
Benjamin N. O. Kuffour et al.

^{1}Civil and Environmental Engineering, Washington State University, Pullman, WA, USA^{2}Center for Applied Scientific Computing, Lawrence Livermore National Laboratory, Livermore, CA, USA^{3}Hydrology and Atmospheric Sciences, University of Arizona, Tucson, AZ, USA^{4}Institute for Bio- and Geosciences, Agrosphere (IBG-3), Research Centre Jülich, Geoverbund ABC/J, Jülich, Germany^{5}Centre for High-Performance Scientific Computing in Terrestrial Systems, Geoverbund ABC/J, Jülich, Germany^{6}Integrated GroundWater Modeling Center and Department of Geology and Geological Engineering, Colorado School of Mines, Golden, CO, USA

^{1}Civil and Environmental Engineering, Washington State University, Pullman, WA, USA^{2}Center for Applied Scientific Computing, Lawrence Livermore National Laboratory, Livermore, CA, USA^{3}Hydrology and Atmospheric Sciences, University of Arizona, Tucson, AZ, USA^{4}Institute for Bio- and Geosciences, Agrosphere (IBG-3), Research Centre Jülich, Geoverbund ABC/J, Jülich, Germany^{5}Centre for High-Performance Scientific Computing in Terrestrial Systems, Geoverbund ABC/J, Jülich, Germany^{6}Integrated GroundWater Modeling Center and Department of Geology and Geological Engineering, Colorado School of Mines, Golden, CO, USA

**Correspondence**: Benjamin N. O. Kuffour (b.kuffour@wsu.edu)

**Correspondence**: Benjamin N. O. Kuffour (b.kuffour@wsu.edu)

Abstract

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Surface flow and subsurface flow constitute a naturally linked hydrologic continuum that has not traditionally been simulated in an integrated fashion. Recognizing the interactions between these systems has encouraged the development of integrated hydrologic models (IHMs) capable of treating surface and subsurface systems as a single integrated resource. IHMs are dynamically evolving with improvements in technology, and the extent of their current capabilities are often only known to the developers and not general users. This article provides an overview of the core functionality, capability, applications, and ongoing development of one open-source IHM, ParFlow. ParFlow is a parallel, integrated, hydrologic model that simulates surface and subsurface flows. ParFlow solves the Richards equation for three-dimensional variably saturated groundwater flow and the two-dimensional kinematic wave approximation of the shallow water equations for overland flow. The model employs a conservative centered finite-difference scheme and a conservative finite-volume method for subsurface flow and transport, respectively. ParFlow uses multigrid-preconditioned Krylov and Newton–Krylov methods to solve the linear and nonlinear systems within each time step of the flow simulations. The code has demonstrated very efficient parallel solution capabilities. ParFlow has been coupled to geochemical reaction, land surface (e.g., the Common Land Model), and atmospheric models to study the interactions among the subsurface, land surface, and atmosphere systems across different spatial scales. This overview focuses on the current capabilities of the code, the core simulation engine, and the primary couplings of the subsurface model to other codes, taking a high-level perspective.

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Kuffour, B. N. O., Engdahl, N. B., Woodward, C. S., Condon, L. E., Kollet, S., and Maxwell, R. M.: Simulating coupled surface–subsurface flows with ParFlow v3.5.0: capabilities, applications, and ongoing development of an open-source, massively parallel, integrated hydrologic model, Geosci. Model Dev., 13, 1373–1397, https://doi.org/10.5194/gmd-13-1373-2020, 2020.

1 Introduction

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Surface water and subsurface (unsaturated and saturated zones) water are connected components of a hydrologic continuum (Kumar et al., 2009). The recognition that flow systems (i.e., surface and subsurface) are a single integrated resource has stimulated the development of integrated hydrologic models (IHMs), which include codes like ParFlow (Ashby and Falgout, 1996; Kollet and Maxwell, 2006), HydroGeoSphere (Therrien and Sudicky, 1996), PIHM (Kumar, 2009), and CATHY (Camporese et al., 2010). These codes explicitly simulate different hydrological processes such as feedbacks between processes that affect the timing and rates of evapotranspiration, vadose zone flow, surface runoff and groundwater interactions. That is, IHMs are designed specifically to include the interactions between traditionally incompatible flow domains (e.g., groundwater and land surface flow) (Engdahl and Maxwell, 2015). Most IHMs adopt a similar physically based approach to describe watershed dynamics, whereby the governing equations of three-dimensional variably saturated subsurface flow are coupled to shallow water equations for surface runoff. The advantage of the coupled approach is that it allows hydraulically connected groundwater–surface water systems to evolve dynamically and for natural feedbacks between the systems to develop (Sulis et al., 2010; Maxwell et al., 2011; Weill et al., 2011; Williams and Maxwell, 2011; Simmer et al., 2015). A large body of literature now exists presenting applications of the various IHMs to solve hydrologic questions. Each model has its own technical documentation, but the individual development, maintenance, and sustainability efforts differ between tools. Some IHMs represent commercial investments and others are community open-sourced projects, but all are dynamically evolving as technology improves and new features are added. Consequently, it can be difficult to answer the question “what exactly can this IHM do today?” without navigating dense user documentation. The purpose of this paper is to provide a current review of the functions, capabilities, and ongoing development of one of the open-source integrated models, ParFlow, in a format that is more accessible to a broad audience than a user manual or articles detailing specific applications of the model.

ParFlow is a parallel integrated hydrologic model that simulates surface, unsaturated, and groundwater flow (Maxwell et al., 2016). ParFlow computes fluxes through the subsurface, as well as interactions with aboveground or surface (overland) flow: all driven by gradients in hydraulic head. The Richards equation is employed to simulate variably saturated three-dimensional groundwater flow (Richards, 1931). Overland flow can be generated by saturation or infiltration excess using a free overland flow boundary condition combined with Manning's equation and the kinematic wave formulations of the dynamic wave equation (Kollet and Maxwell, 2006). ParFlow solves these governing equations by employing either a fully coupled or integrated approach, whereby surface and subsurface flows are solved simultaneously using the Richards equation in three-dimensional form (Gilbert and Maxwell, 2017), or an indirect approach whereby the different components can be partitioned and flows in only one of the systems (surface or subsurface flows) is solved. The integrated approach allows for dynamic evolution of the interconnectivity between the surface water and groundwater systems. This interconnection depends only on the properties of the physical system and governing equations. An indirect approach permits the partitioning of the flow components, i.e., water and mass fluxes between surface and subsurface systems. The flow components can be solved sequentially. For the groundwater flow solution, ParFlow makes use of an implicit backward Euler scheme in time and a cell-centered finite-difference scheme in space (Woodward, 1998). An upwind finite-volume scheme in space and an implicit backward Euler scheme in time are used for the overland flow component (Maxwell et al., 2007). ParFlow uses Krylov linear solvers with multigrid preconditioners for the flow equations along with a Newton method for the nonlinearities in the variably saturated flow system (Ashby and Falgout, 1996; Jones and Woodward, 2001). ParFlow's physically based approach requires a number of parameterizations, e.g., subsurface hydraulic properties, such as porosity, the saturated hydraulic conductivity, and the pressure–saturation relationship parameters (relative permeability) (Kollet and Maxwell, 2008a).

ParFlow is well documented and has been applied to surface and subsurface
flow problems, including simulating the dynamic nature of groundwater and
surface–subsurface interconnectivity in large domains (e.g., over 600 km^{2}) (Kollet
and Maxwell, 2008a; Ferguson and Maxwell, 2012; Condon et al., 2013; Condon
and Maxwell, 2014), small catchments (e.g., approximately 30 km^{2}) (Ashby et
al., 1994; Kollet and Maxwell, 2006; Engdahl et al., 2016), complex terrain
with highly heterogenous subsurface permeability such as the Rocky Mountain
National Park, Colorado, United States (Engdahl and Maxwell,
2015; Kollet et al., 2017), large watersheds (Abu-El-Sha'r and Rihani, 2007; Kollet
et al., 2010), continental-scale flows (Condon et al., 2015; Maxwell et al.,
2015), and even subsurface–surface and atmospheric coupling (Maxwell
et al., 2011; Williams and Maxwell, 2011; Williams et al., 2013; Gasper et
al., 2014; Shrestha et al., 2015). Evidence from these studies suggests that
ParFlow produces accurate results in simulating flows in surface–subsurface
systems in watersheds; i.e., the code possesses the capability to perform
simulations that accurately represent the behaviors of natural systems on
which models are based. The rest of the paper is organized as follows: we
provide a brief history of ParFlow's development in Sect. 1.1. In Sect. 2,
we describe the core functionality of the code, i.e., the primary functions,
the model equations, and grid type used by ParFlow. Section 3 covers
equation discretization and solvers (e.g., inexact Newton–Krylov, the ParFlow
Multigrid (PFMG) preconditioner, and the multigrid-preconditioned conjugate
gradient (MGCG) method) used in ParFlow. Examples of the parallel scaling and
performance efficiency of ParFlow are revisited in Sect. 4. The coupling
capabilities of ParFlow, with other atmospheric, land surface, and
subsurface models, are shown in Sect. 5. We provide a summary and discussion,
future directions to the development of ParFlow, and some concluding
remarks in Sect. 6.

ParFlow development commenced as part of an effort to develop an open-source, object-oriented, parallel watershed flow model initiated by scientists from the Center for Applied Scientific Computing (CASC), environmental programs, and the Environmental Protection Department at the Lawrence Livermore National Laboratory (LLNL) in the mid-1990s. ParFlow was born out of this effort to address the need for a code that combines fast, nonlinear solution schemes with massively parallel processing power, and its development continues today (e.g., Ashby et al., 1993; Smith et al., 1995; Woodward, 1998; Maxwell and Miller, 2005; Kollet and Maxwell, 2008b; Rihani et al., 2010; Simmer et al., 2015). ParFlow is now a collaborative effort between numerous institutions including the Colorado School of Mines, Research Center Jülich, University of Bonn, Washington State University, the University of Arizona, and Lawrence Livermore National Laboratory, and its working base and development community continue to expand.

ParFlow was originally developed for modeling saturated fluid flow and chemical transport in three-dimensional heterogeneous media. Over the past few decades, ParFlow underwent several modifications and expansions (i.e., additional features and capabilities have been implemented) and has seen an exponential growth in applications. For example, a two-dimensional distributed overland flow simulator (surface water component) was implemented into ParFlow (Kollet and Maxwell, 2006) to simulate interaction between surface and subsurface flows. Such additional implementations have resulted in improved numerical methods in the code. The code's applicability continues to evolve; for example, in recent times, ParFlow has been used in several coupling studies with subsurface, land surface, and atmospheric models to include physical processes at the land surface (Maxwell and Miller, 2005; Maxwell et al., 2007, 2011; Kollet, 2009; Williams and Maxwell, 2011; Valcke et al., 2012; Valcke, 2013; Shrestha et al., 2014; Beisman et al., 2015) across different spatial scales and resolutions (Kollet and Maxwell, 2008a; Condon and Maxwell, 2015; Maxwell et al., 2015). Also, a terrain-following mesh formulation has been implemented (Maxwell, 2013) that allows ParFlow to handle problems with fine space discretization near the ground surface that comes with variable vertical discretization flexibility, which offer modelers the advantage to increase the resolution of the shallow soil layers (these are discussed in detail below).

2 Core functionality of ParFlow

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The core functionality of the ParFlow model is the solution of three-dimensional variably saturated groundwater flow in heterogeneous porous media ranging from simple domains with minimal topography and/or heterogeneity to highly resolved continental-scale catchments (Jones and Woodward, 2001; Maxwell and Miller, 2005; Kollet and Maxwell, 2008a; Maxwell, 2013). Within this range of complexity, the ParFlow model can operate in three different modes: (1) variably saturated; (2) steady-state saturated; and (3) integrated watershed flows; however, all these modes share a common sparse coefficient matrix solution framework.

ParFlow can operate in variably saturated mode using the well-known mixed form of the Richards equation (Celia et al., 1990). The mixed form of the Richards equation implemented in ParFlow is

$$\begin{array}{}\text{(1)}& {\displaystyle}{S}_{\mathrm{s}}{S}_{\mathrm{w}}\left(p\right){\displaystyle \frac{\partial p}{\partial t}}+\mathit{\varphi}{\displaystyle \frac{\partial \left({S}_{\mathrm{w}}\right(p\left)\right)}{\partial t}}=\mathrm{\nabla}\mathit{q}+{q}_{\mathrm{s}}\text{(2)}& {\displaystyle}\mathit{q}=-{k}_{\mathrm{s}}{k}_{\mathrm{r}}\left(p\right)\mathrm{\nabla}\left(p-z\right),\end{array}$$

where *S*_{s} is the specific storage coefficient [L^{−1}], *S*_{w} is the relative saturation
[-] as a function of pressure head *p* of the fluid or water
[L], *t* is time [T], *ϕ* is the porosity of the medium [-],
** q** is the specific volumetric (Darcy) flux [LT

The most basic operational mode is the solution of the steady-state, fully saturated groundwater flow equation:

$$\begin{array}{}\text{(3)}& \mathrm{\nabla}\mathit{q}-{q}_{\mathrm{s}}=\mathrm{0},\end{array}$$

where *q*_{s} represents a general source or sink term, e.g., wells [T^{−1}], ** q** is the Darcy flux [LT

$$\begin{array}{}\text{(4)}& \mathit{q}=-{k}_{\mathrm{s}}\mathrm{\nabla}P,\end{array}$$

where *k*_{s} is the saturated hydraulic conductivity [LT^{−1}], and *P* represents the 3-D
hydraulic head-potential [L]. ParFlow does include a
direct solution option for the steady-state saturated flow that is distinct
from the transient solver. For example, ParFlow uses the solver “impes”
under the single-phase, fully saturated, steady-state condition relative to the
variably saturated, transient mode wherein the Richards equation solver is used (Maxwell et al., 2016).
When studying sophisticated or complex phenomena, e.g., simulating a fully
coupled system (i.e., surface and subsurface flow), an overland flow boundary
condition is employed.

Surface water systems are connected to the subsurface, and these interactions are particularly important for rivers. However, these connections have been historically difficult to explicitly represent in numerical simulations. A common approach has been to use river-routing codes, like Hydrologic Engineering Center (HEC) codes, as well as MODFLOW and its River Package to determine head in the river, which is then used as a boundary condition for the subsurface model. This approach prevents feedbacks between the two models, and a better representation of the physical processes in these kinds of problems is one of the motivations for IHMs. Overland flow is implemented in ParFlow as a two-dimensional kinematic wave equation approximation of the shallow water equations. The continuity equation for two-dimensional shallow overland flow is given as

$$\begin{array}{}\text{(5)}& {\displaystyle \frac{\partial {\mathit{\psi}}_{\mathrm{s}}}{\partial t}}=\mathrm{\nabla}\left(\mathit{\upsilon}{\mathit{\psi}}_{\mathrm{s}}\right)+{q}_{\mathrm{s}},\end{array}$$

where ** υ** is the depth-averaged velocity vector [LT

$$\begin{array}{}\text{(6)}& {S}_{\mathrm{f},i}={S}_{\mathrm{o},i},\end{array}$$

which is known as the kinematic wave approximation. The *S*_{f,i} and
*S*_{o,i} represent the friction [-] and bed slopes (gravity
forcing term) [-], respectively, where *i* indicates the *x* and
*y* directions (also shown in Eqs. 7 and 8) (Maxwell et al., 2015). Manning's
equation is used to generate a flow depth–discharge relationship:

$$\begin{array}{}\text{(7)}& {\displaystyle}{\mathit{\upsilon}}_{x}={\displaystyle \frac{\sqrt{{S}_{\mathrm{f},x}}}{n}}{\mathit{\psi}}_{\mathrm{s}}^{\mathrm{2}/\mathrm{3}}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{and}\text{(8)}& {\displaystyle}{\mathit{\upsilon}}_{y}={\displaystyle \frac{\sqrt{{S}_{\mathrm{f},y}}}{n}}{\mathit{\psi}}_{\mathrm{s}}^{\mathrm{2}/\mathrm{3}},\end{array}$$

where *n* is the Manning roughness coefficient $\left[{\mathrm{TL}}^{-\mathrm{1}/\mathrm{3}}\right]$. The flow of water out of an overland
flow simulation domain only occurs horizontally at an outlet
controlled by specifying a type of boundary condition at the edge of the
simulation domain. In a natural system, the outlet is usually taken as the
region where a river enters another water body such as a stream or lake.
ParFlow determines the overland flow direction through the D4 flow-routing
approach. In a simulation domain, the D4 flow-routing approach allows for
flow to be assigned from a focal cell to only one neighboring cell accessed
via the steepest or most vertical slope. The shallow overland flow
formulation (Eq. 9) assumes that the flow depth is averaged vertically
and neglects a vertical change in momentum in the column of surface water.
To account for vertical flow (from the surface to the subsurface or
subsurface to the surface), a formulation that couples the system of
equations through a boundary condition at the land surface becomes
necessary. Equation (5) can be modified to include an exchange rate with
the subsurface, *q*_{e}, as

$$\begin{array}{}\text{(9)}& {\displaystyle \frac{\partial {\mathit{\psi}}_{\mathrm{s}}}{\partial t}}=\mathrm{\nabla}\left(\mathit{\upsilon}{\mathit{\psi}}_{\mathrm{s}}\right)+{q}_{\mathrm{s}}+{q}_{\mathrm{e}},\end{array}$$

which is common in other IHMs. In ParFlow, the overland flow equations are
coupled directly to the Richards equation at the top boundary cell under
saturated conditions. Conditions of continuity of pressure (i.e., the
pressures of the subsurface and surface domains are equal right at the
ground surface) and flux at the top cell of the boundary between the
subsurface and surface systems are assigned. Fig. 1 demonstrates the
continuity of pressure at the ground surface for flow from the surface into
the subsurface. This assignment is done by setting pressure head in Eq. (1) equal to the vertically averaged surface pressure, *ψ*_{s},

$$\begin{array}{}\text{(10)}& p={\mathit{\psi}}_{\mathrm{s}}=\mathit{\psi},\end{array}$$

and the flux, *q*_{e}, equal to the specified boundary conditions (e.g.,
Neumann or Dirichlet type). For example, if Neumann-type boundary conditions
are specified, which are given as

$$\begin{array}{}\text{(11)}& {q}_{\mathrm{BC}}=-{k}_{\mathrm{s}}{k}_{\mathrm{r}}\mathrm{\nabla}(\mathit{\psi}-z),\end{array}$$

and one solves for the flux term in Eq. (10), the result is

$$\begin{array}{}\text{(12)}& {q}_{\mathrm{e}}={\displaystyle \frac{\partial \u2225\mathit{\psi},\mathrm{0}\u2225}{\partial t}}-\mathrm{\nabla}\mathit{\upsilon}\u2225\mathit{\psi},\mathrm{0}\u2225-{q}_{\mathrm{s}},\end{array}$$

where the ∥*ψ*,0∥ operator is defined as the greater of
the quantities, *ψ* and 0. Substituting Eq. (12) for the boundary
condition in Eq. (11), requiring the aforementioned flux continuity
*q*_{BC}=*q*_{e}, leads to

$$\begin{array}{}\text{(13)}& -{k}_{\mathrm{s}}{k}_{\mathrm{r}}\mathrm{\nabla}\left(\mathit{\psi}-z\right)={\displaystyle \frac{\partial \u2225\mathit{\psi},\mathrm{0}\u2225}{\partial t}}-\mathrm{\nabla}\cdot \left(\mathit{\upsilon}\u2225\mathit{\psi},\mathrm{0}\u2225\right)-{q}_{\mathrm{s}}.\end{array}$$

Equation (13) shows that the surface water equations are represented as a boundary condition to the Richards equation. That is, the boundary condition links flow processes in the subsurface with those at the land surface. This boundary condition eliminates the exchange flux and accounts for the movement of the free surface of ponded water at the land surface (Kollet and Maxwell, 2006; Williams and Maxwell, 2011).

Many IHMs couple subsurface and surface flows by making use of the exchange
flux, *q*_{e}, model. The exchange flux between the domains (the surface and
the subsurface) depends on hydraulic conductivity and the gradient across
some interface where indirect coupling is used (VanderKwaak, 1999; Panday and Huyakorn, 2004). The
exchange flux concept gives a general formulation of a single set of coupled
surface–subsurface equations. The exchange flux term, *q*_{e}, may be
included in the shallow overland flow continuity equation as the exchange
rate term with the subsurface (Eq. 9) in a coupled system (Kollet and Maxwell, 2006).

Most applications of the code have reflected ParFlow's core functionality as a single-phase flow solver, but there are also embedded capabilities for the multiphase flow of immiscible fluids and solute transport. Multiphase systems are distinguished from single-phase systems by the presence of one or more interfaces separating the phases, with moving boundaries between phases. The flow equations that are solved in multiphase systems in a porous medium comprise a set of mass balance and momentum equations. The equations are given by

$$\begin{array}{}\text{(14)}& {\displaystyle \frac{\partial}{\partial t}}\left(\mathit{\varphi}{\mathit{\rho}}_{i}{S}_{i}\right)+\mathrm{\nabla}\left(\mathit{\varphi}{\mathit{\rho}}_{i}{S}_{i}{\mathit{\upsilon}}_{i}\right)-{\mathit{\rho}}_{i}{Q}_{i}=\mathrm{0},\text{(15)}& {\displaystyle}\mathit{\varphi}{S}_{i}{\mathit{\upsilon}}_{i}+{\mathit{\lambda}}_{i}\left(\mathrm{\nabla}{p}_{i}-{\mathit{\rho}}_{i}\mathit{g}\right)=\mathrm{0},\end{array}$$

where $i=\mathrm{1},\mathrm{\dots},n$ denotes a given phase (such as air or
water). In these equations, *ϕ* is the porosity of the medium [-], which explains the fluid capacity of the porous medium, and for
each phase, *i*
*S*_{i}(*x**t*) is the relative saturation [-], which indicates the
content of phase *i* in the porous medium,
*υ*_{i}(*x**t*) represents the Darcy velocity vector [LT^{−1}],
*Q*_{i}(*x**t*) stands for the source or sink term [T^{−1}],
*p*_{i}(*x**t*) is the average pressure $\left[{\mathrm{ML}}^{-\mathrm{1}}{\mathrm{T}}^{-\mathrm{2}}\right]$, *ρ*_{i}(*x**t*) is the mass density [ML^{−3}], *λ*_{i} is the mobility [L^{3}TM^{−1}],
** g** is the gravity vector [LT

The transport equations included in the ParFlow package describe mass conservation in a convective flow (no diffusion) with degradation effects and adsorption included along with extraction and injection wells (Beisman et al., 2015; Maxwell et al., 2016). The transport equation is defined as follows:

$$\begin{array}{}\text{(16)}& \begin{array}{rl}\left({\displaystyle \frac{\partial}{\partial t}}\left(\mathit{\varphi}{c}_{i,j}\right)\right.& \left.+{\mathit{\lambda}}_{j}\mathit{\varphi}{c}_{i,j}\right)+\mathrm{\nabla}\left({c}_{i,j}\mathit{\upsilon}\right)=\\ & -\left({\displaystyle \frac{\partial}{\partial t}}\left(\left(\mathrm{1}-\mathit{\varphi}\right){\mathit{\rho}}_{\mathrm{s}}{F}_{i,j}\right)+{\mathit{\lambda}}_{i}\left(\mathrm{1}-\mathit{\varphi}\right){\mathit{\rho}}_{\mathrm{s}}{F}_{i,j}\right)\\ & +\sum _{k}^{{n}_{\mathrm{I}}}{\mathit{\gamma}}_{k}^{\mathrm{I};i}\mathit{\chi}{\mathrm{\Omega}}_{k}^{\mathrm{I}}\left({c}_{i,j}-{c}_{i,j}^{-k}\right)-\sum _{k}^{{n}_{\mathrm{E}}}{\mathit{\gamma}}_{k}^{\mathrm{E};i}\\ & \mathit{\chi}{\mathrm{\Omega}}_{k}^{\mathrm{E}}{c}_{i,j},\end{array}\end{array}$$

where
*c*_{i,j}(*x**t*) represents the concentration fraction of contaminant [-], *λ*_{i} is degradation rate [T^{−1}],
*F*_{i}(*x**t*) is the mass concentration [L^{3}M^{−1}], *ρ*_{s}(** x**) is the density of the solid mass [ML

$$\begin{array}{}\text{(17)}& {F}_{i,j}={K}_{d;j}{c}_{i,j},\end{array}$$

where *K*_{d;j} is the distribution coefficient of the component [L^{3}M^{−1}]. The
transport–advection equation or convective flow calculation performed by
ParFlow offers a choice of a first-order explicit upwind scheme or a
second-order explicit Godunov scheme. The advection calculations are
discretized as boundary value problems for each primary dimension over each
compute cell. The discretization is a fully explicit, forward Euler,
first-order accurate in time approach. The implementation of a second-order
explicit Godunov scheme (second-order advection scheme) minimizes numerical
dispersion and presents a more accurate computational process at these timescales
than either an implicit or lower-order explicit scheme. The stability issue here
is that the simulation time step is restricted via the
Courant–Friedrichs–Lewy (CFL) condition, which demands that time steps are
chosen as small enough to ensure that mass is not transported more than one
grid cell in a single time step in order to maintain stability
(Beisman, 2007).

An accurate numerical approximation of a set of partial differential equations is strongly dependent on the simulation grid. Integrated hydrologic models can use unstructured or structured meshes for the discretization of the governing equations. The choice of grid type to adopt is problem-specific and often a subjective choice since the same domain can be represented in many ways, but there are some clear trade-offs. For example, structured grid models, such as ParFlow, may be preferred to unstructured grid models because structured grids provide significant advantages in computational simplicity and speed, and they are amenable to efficient parallelization (Durbin, 2002; Kumar et al., 2009; Osei-Kuffuor et al., 2014). ParFlow adopts a regular, structured grid specifically for its parallel performance. There are currently two regular grid formulations included in ParFlow, an orthogonal grid and a terrain-following formulation (TFG); both allow for variable vertical discretization (thickness over an entire layer) over the domain.

Orthogonal grids have many advantages, and many approaches are available to transform an irregular grid into an orthogonal grid such as conformal mapping. This mapping defines a transformed set of partial differential equations using an elliptical system with “control functions” determined in such a way that the generated grid would be either orthogonal or nearly orthogonal. However, conformal mapping may not allow flexibility in the control of the grid node distribution, which diminishes its usefulness with complex geometries (Mobley and Stewart, 1980; Haussling and Coleman, 1981; Visbal and Knight, 1982; Ryskin and Leal, 1983; Allievi and Calisal, 1992; Eca, 1996).

A Cartesian, regular, orthogonal grid formulation is implemented by default in ParFlow, though some adaptive meshing capabilities are still included in the source code. For example, layers within a simulation domain can be made to have varying thickness. Figure 2a shows the standard way that topography or any other non-rectangular domain boundaries are represented in ParFlow. The domain limits, and any other internal boundaries, can be defined using grid-independent triangulated irregular network (TIN) files that define a geometry, or a gridded indicator file can be used to define geometric elements. ParFlow uses an octree space-partitioning algorithm (a grid-based algorithm or mesh generators filled with structured grids) (Maxwell, 2013) to depict complex structure and land surface representations (e.g., topography, watershed boundaries, and different hydrologic facies) in three-dimensional space (Kollet et al., 2010). These land surface features are mapped onto the orthogonal grid, and looping structures that encompass these irregular shapes are constructed (Ashby et al., 1997). The grid cells above the ground surface are inactive (shown in Fig. 2a) and are stored in the solution vector but not included in the solution.

The inactive portion of a watershed defined with an orthogonal grid can be
quite large in complex watersheds with high relief. In these cases, it is
advantageous to use a grid that allows these regions to be omitted.
ParFlow's structured grid conforms to the topography via transformation by
the terrain-following grid formulation. This transform alters the form of
Darcy's law to incorporate a topographic slope component. For example,
subsurface fluxes are computed separately in both the *x* and *y* directions
by making use of the terrain-following grid transform as

$$\begin{array}{}\text{(18)}& \begin{array}{r}{q}_{x}=K\mathrm{sin}\left({\mathit{\theta}}_{x}\right)+K{\displaystyle \frac{\partial p}{\partial x}}\mathrm{cos}\left({\mathit{\theta}}_{x}\right),\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{and}\\ {q}_{y}=K\mathrm{sin}\left({\mathit{\theta}}_{y}\right)+K{\displaystyle \frac{\partial p}{\partial y}}\mathrm{cos}\left({\mathit{\theta}}_{y}\right),\end{array}\end{array}$$

where *q*_{x} and *q*_{y} represent source or sink terms, such as fluxes, that
include potential recharge flux at the ground surface [LT^{−1}], *p* is the pressure head [L], *K* is the saturated hydraulic conductivity tensor,
[LT^{−1}], *θ* is the local angle
[-] of topographic slope, and *S*_{x} and *S*_{y} in the *x* and
*y* directions may be presented as ${\mathit{\theta}}_{x}={\mathrm{tan}}^{-\mathrm{1}}{S}_{x}$ and
${\mathit{\theta}}_{y}={\mathrm{tan}}^{-\mathrm{1}}{S}_{y}$, respectively (Weill et al., 2009). The
terrain-following grid formulation comes in handy when solving coupled surface
and subsurface flows (Maxwell, 2013). The terrain-following grid formulation uses the same surface slopes specified for
overland flow to transform the grid, whereas the slopes specified in the
orthogonal grid are only used for 2-D overland flow routing and do not
impact the subsurface formulation (see Fig. 2). Note that TIN files can
still be used to deactivate portions of the transformed domain.

3 Equation discretization and solvers

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The core of the ParFlow code is its library of numerical solvers. As noted above, in most cases, the temporal discretization of the governing equations uses an implicit (backward Euler) scheme with cell-centered finite differences in spatial dimensions. Different components of this solution framework have been developed for the various operational modes of ParFlow including an inexact Newton–Krylov nonlinear solver (Sect. 3.1), a multigrid algorithm (Sect. 3.2), and a multigrid-preconditioned conjugate gradient (MGCG) solver in (Sect. 3.3). The conditions, requirements, and constraints on the solvers depend on the specifics of the problem being solved, and some solvers tend to be more efficient (faster overall convergence) than others for a given problem. The core structure of these solvers and some of their implementation details are given below, with an emphasis on the main concepts behind each solver.

The cell-centered fully implicit discretization scheme applied to the Richards equation leads to a set of coupled discrete nonlinear equations that need to be solved at each time step, and, for variably saturated subsurface flow, ParFlow does this with the inexact Newton–Krylov method implemented in the KINSOL package (Hindmarsh et al., 2005; Collier et al., 2015). Newton–Krylov methods were initially utilized in the context of partial differential equations by Brown and Saad (1990). In the approach, a coupled nonlinear system as a result of discretization of the partial differential equation is solved iteratively. Within each iteration, the nonlinear system is linearized via a Taylor expansion. After linearization, an iterative Krylov method is used to solve the resulting linear Jacobian system (Woodward, 1998; Osei-Kuffuor et al., 2014). For variably saturated subsurface flow, ParFlow uses the GMRES Krylov method (Saad and Schultz, 1986). Figure 3 is a flowchart of the solution technique ParFlow uses to provide approximate solutions to systems of nonlinear equations.

The benefit of this Newton–Krylov method is that the Krylov linear solver requires only matrix–vector products. Because the system matrix is the Jacobian of the nonlinear function, these matrix–vector products may be approximated by taking directional derivatives of the nonlinear function in the direction of the vector to be multiplied. This approximation is the main advantage of the Newton–Krylov approach as it removes the requirement for matrix entries in the linear solver. An inexact Newton method is derived from a Newton method by using an approximate linear solver at each nonlinear iteration, as is done in the Newton–Krylov method (Dembo and Eisenstat, 1982; Dennis Jr. and Schabel, 1996). This approach takes advantage of the fact that when the nonlinear system is far from converged, the linear model used to update the solution is a poor approximation. Thus, the convergence criteria for an early linear system solver are relaxed. The tolerance required for the solution of the linear system is decreased as the nonlinear function residuals approach zero. The convergence rate of the resulting nonlinear solver can be linear or quadratic, depending on the algorithm used. Through the KINSOL package, ParFlow can either use a constant tolerance factor or ones from Eisenstat and Walker (1996). Krylov methods can be very robust, but they can be slow to converge. As a result, it is often necessary to implement a preconditioner, or accelerator, for these solvers.

Multigrid (MG) methods constitute a class of techniques or algorithms for solving differential equations (system of equations) using a hierarchy of discretization (Briggs et al., 2000). Multigrid algorithms are applied primarily to solve linear and nonlinear boundary value problems and can be used as either preconditioners or solvers. The most efficient method for preconditioning linear systems in ParFlow is the ParFlow Multigrid (PFMG) algorithm (Ashby and Falgout, 1996; Jones and Woodward, 2001). Multigrid algorithms arise from the discretization of elliptic partial differential equations (Briggs et al., 2000) and, in ideal cases, have convergence rates that do not depend on the problem size. In these cases, the number of iterations remains constant even as problem sizes grow large. Thus, the algorithm is algorithmically scalable. However, it may take longer to evaluate each iteration as problem sizes increase. As a result, ParFlow utilizes the highly efficient implementation of the PFMG in the hypre library (Falgout and Yang, 2002).

For variably saturated subsurface flow, ParFlow uses the Newton–Krylov
method coupled with a multigrid preconditioner to accurately solve for the
water pressure (hydraulic head) in the subsurface and diagnoses the
saturation field (which is used in determining the water table) (Woodward, 1998;
Jones and Woodward, 2000, 2001; Kollet et al., 2010). The water table is
calculated for computational cells having hydraulic heads above the bottom
of the cells. Generally, a cell is saturated if the hydraulic head in the
cell is above the node elevation (cell center), or the cell is unsaturated if
the hydraulic head in the cell is below the node elevation. For saturated
flow, ParFlow uses the conjugate gradient method also coupled with a
multigrid method. It is important to note that subsurface flow systems are
usually much larger radially than they are thick, so it is common for
computational grids to have highly anisotropic cell aspect ratios to balance
the lateral and vertical discretization. Combined with anisotropy in the
permeability field, these high aspect ratios produce numerical anisotropy in
the problem, which can cause the multigrid algorithms to converge slowly (Jones and Woodward, 2001). To correct
this problem, a semi-coarsening strategy or algorithm is employed, whereby the
grid is coarsened in one direction at a time. The direction chosen is the
one with the smallest grid spacing, i.e., the tightest coupling. In an
instance in which more than one direction has the same minimum spacing, then
the algorithm chooses the direction in the order of *x*, followed by *y*,
and then in *z*. To decide on how and when to terminate the coarsening
algorithm, Ashby and Falgout (1996) determined that a
semi-coarsening down to a $(\mathrm{1}\times \mathrm{1}\times \mathrm{1})$ grid is ideal for groundwater
problems.

ParFlow uses the multigrid-preconditioned conjugate gradient (CG) solver to solve the groundwater equations under steady-state and fully saturated flow conditions (Ashby and Falgout, 1996). These problems are symmetric and positive definite, two properties the CG method was designed to target. While CG lends itself to efficient implementations, the number of iterations required to solve a system that results from the discretization of the saturated flow equation increases as the problem size grows. The PFMG algorithm is used as a preconditioner to combat this growth and results in an algorithm for which the number of iterations required to solve the system grows only minimally. See Ashby and Falgout (1996) for a detailed description of these solvers and the parallel implementation of the multigrid-preconditioned CG method in ParFlow (Gasper et al., 2014; Osei-Kuffuor et al., 2014).

As discussed above, coupling between subsurface and surface or overland flow in ParFlow is activated by specifying an overland boundary condition at the top surface of the computational domain, but this mode of coupling allows for activation and deactivation of the overland boundary condition during simulations in which ponding or drying occurs. Thus, surface–subsurface coupling can occur anywhere in the domain during a simulation, and it can change dynamically during the simulation. Overland flow may occur by the Dunne or Horton mechanism depending on local dynamics. Overland flow routing is enabled when the subsurface cells are fully saturated. In ParFlow the coupling between the subsurface and surface flows is handled implicitly. ParFlow solves this implicit system with the inexact Newton–Krylov method described above. However, in this case, the preconditioning matrix is adjusted to include terms from the surface coupling. In the standard saturated or variably saturated case, the multigrid method is given the linear system matrix, or a symmetric version, resulting from the discretization of the subsurface model. Because ParFlow uses a structured mesh, these matrices have a defined structure, making their evaluation and the application of a multigrid straightforward. Due to varying topographic height of the surface boundary, where the surface coupling is enforced, the surface effects add nonstructured entries in the linear system matrices. These entries increase the complexity of the matrix entry evaluations and reduce the effectiveness of the multigrid preconditioner. In this case, the matrix–vector products are most effectively performed through the computation of the linear system entries rather than the finite-difference approximation to the directional derivative. For the preconditioning, surface couplings are only included if they model flow between cells at the same vertical height, i.e., in situations in which overland flow boundary conditions are imposed or activated. This restriction maintains the structured property of the preconditioning matrix while still including much of the surface coupling in the preconditioner. Both these adjustments led to considerable speedup in coupled simulations (Osei-Kuffuor et al., 2014).

4 Parallel performance efficiency

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Scaling efficiency metrics offer a quantitative method for evaluating the performance of any parallel model. Good scaling generally means that the efficiency of the code is maintained as the solution of the system of equations is distributed onto more processors or as the problem resolution is refined and processing resources are added. Scalability can depend on the problem size, the processor number, the computing environment, and the inherent capabilities of the computational platform used, e.g., the choice of a solver. The performance of ParFlow (or any parallel code) is typically determined through weak and strong scaling (Gustafson, 1988). Weak scaling involves the measurement of the code's efficiency in solving problems of increasing size (i.e., it describes how the solution time changes with a change in the number of processors for a fixed problem size per processor). In weak scaling, the simulation time should remain constant, as the size of the problem and number of processing elements grow such that the same amount of work is conducted on each processing element. Following Gustafson (1988), scaled parallel efficiency is given by

$$\begin{array}{}\text{(19)}& E\left(n,p\right)={\displaystyle \frac{T(n,\mathrm{1})}{T(pn,p)}},\end{array}$$

where *E*(*n**p*) denotes parallel efficiency, and *T* represents the runtime as a
function of the problem size *n*, which is spread across several
processors, *p*. Parallel code is said to be perfectly efficient if
$E\left(n,p\right)=\mathrm{1}$, and the efficiency decreases as *E*(*n**p*) approaches
0. Generally, parallel efficiency decreases with increasing processor number
as communication overhead between nodes and/or processors becomes the limiting
factor.

Strong scaling describes the measurement of how much the simulation or
solution time changes with the number of processors for a given problem of
fixed total size (Amdahl, 1967). In strong scaling, a fixed size
task is solved on a growing number of processors, and the associated time
needed for the model to compute the solution is determined (Woodward,
1998; Jones and Woodward, 2000). If the computational time decreases
linearly with the processor number, a perfect parallel efficiency, (*E*=1),
results. The value of *E* is determined using Eq. (19). ParFlow has been
shown to have excellent parallel performance efficiency, even for large
problem sizes and processor counts (see Table 1) (Ashby
and Falgout, 1996; Kollet and Maxwell, 2006). In situations in which ParFlow
works in conjunction with or coupled to other subsurface, land surface, or
atmospheric models (see Sect. 5), i.e., increased computational complexity by
adding different components or processes, improved computational time may
not only depend on ParFlow. The computational cost of such an integrated
model is extremely difficult to predict because of the nonlinear nature of
the system. The solution time may depend on a number of factors including the
number of degrees of freedom, the heterogeneity of the parameters, and which
processes are active (e.g., snow accumulation compared to nonlinear snowmelt
processes in a land surface model or the switching on or off of the overland
flow routing in ParFlow). The only way to know how fast a specific problem
will run is to try that problem. Many of the studies presented in Table 1
include computational times for problems with different complexities when
ParFlow was used. In a scaling study with ParFlow, Maxwell (2013) examined the relative performance
of preconditioning the coupled variably saturated subsurface and surface
flow system with the symmetric portion or full matrix for the system. Both
options use ParFlow's multigrid preconditioner. Solver performance was
demonstrated by combining the analytical Jacobian and the nonsymmetric
linear preconditioner. The study showed that the nonsymmetric linear
preconditioner presents faster computational times and efficient scaling. A
section of the study results is reproduced in Table 1, in addition to other
scaling studies demonstrating ParFlow's parallel efficiency. This trade-off
was also examined in Jones and Woodward (2000).

It is worth noting that large and/or complex problem sizes (e.g., simulating a large heterogenous domain size with over 8.1 billion unknowns) will always take time to solve directly, but the approach for setting up a problem depends on the specific problem being modeled. Even for one specific kind of model there may be multiple workflows, and how to model such complexity becomes the sole responsibility of the modeler. The studies involving ParFlow outlined in Table 1 provide a wealth of knowledge regarding domain setup for problems of different complexities. Since these are all specific applications, the information will likely be very useful to modelers trying to build a new domain during the setup and planning phases.

5 Coupling

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Different integrated models, including atmospheric or weather prediction models (e.g., Weather Research Forecasting model, Advanced Regional Prediction System, Consortium for Small-Scale Modeling), land surface models (e.g., Common Land Model, Noah Land Surface Model), and a subsurface model (e.g., CrunchFlow), have been coupled with ParFlow to simulate a variety of coupled earth system effects (see Fig. 4a). Coupling between ParFlow and other integrated models was performed to better understand the physical processes that occur at the interfaces between the deeper subsurface and ground surface, as well as between the ground surface and the atmosphere. None of the individual models can achieve this on their own because ParFlow cannot account for land surface processes (e.g., evaporation), and atmospheric and land surface models generally do not simulate deeper subsurface flows (Ren and Xue, 2004; Chow et al., 2006; Beisman, 2007; Maxwell et al., 2007; Shi et al., 2014). Model coupling can be achieved either via “offline coupling”, whereby models involved in the coupling process are run sequentially and interactions between them are one-way (i.e., information is only transmitted from one model to the other), or “online” whereby they interact and feedback mechanisms among components are represented (Meehl et al., 2005; Valcke et al., 2009). Each of the coupled models uses its own solver for the physical system it is solving, and then information is passed between the models. As long as each model exhibits good parallel performance, this approach still allows for simulations at very high resolution, with a large number of processes (Beven, 2004; Ferguson and Maxwell, 2010; Shen and Phanikumar, 2010; Shi et al., 2014). This section focuses on the major couplings between ParFlow and other codes. We point out specific functions of the individual models as stand-alone codes that are relevant to the coupling process. In addition, information about the role or contribution of each model at the coupling interface (see Fig. 4b) that connects with ParFlow is presented (Fig. 5 shows the communication network of the coupled models). We discuss couplings between ParFlow and its land surface model (a modified version of the original Common Land Model introduced by Dai et al. 2003), the Consortium for Small-Scale Modeling (COSMO), the Weather Research Forecasting model, the Advanced Regional Prediction System, and CrunchFlow in Sect. 5.1, 5.2, 5.3, 5.4, and 5.5, respectively.

The Common Land Model (CLM) is a land surface model designed to complete
land–water–energy balance at the land surface (Dai et al., 2003). CLM parameterizes
the moisture, energy, and momentum balances at the land surface and includes
a variety of customizable land surface characteristics and modules,
including land surface type (land cover type, soil texture, and soil color),
vegetation and soil properties (e.g., canopy roughness, zero-plane
displacement, leaf dimension, rooting depths, specific heat capacity of dry
soil, thermal conductivity of dry soil, porosity), optical properties (e.g., albedos of thick canopy), and physiological properties related to the
functioning of the photosynthesis–conductance model (e.g., green leaf area,
dead leaf, and stem area indices). A combination of numerical schemes is
employed to solve the governing equations. CLM uses a time integration
scheme that proceeds through a split-hybrid approach, in which the solution
procedure is split into “energy balance” and “water balance” phases in a
very modularized structure (Mikkelson
et al., 2013; Steiner et al., 2005, 2009). The CLM described here and as
incorporated in ParFlow is a modified version of the original CLM introduced
by Dai et al. (2003), though the
original version was coupled to ParFlow in previous model applications (e.g.,
Maxwell and Miller, 2005). The current coupled model, PF.CLM, consists of
ParFlow incorporated with a land surface model (Jefferson
et al., 2015, 2017; Jefferson and Maxwell, 2015). The modified CLM
is composed of a series of land surface modules that are called as a
subroutine within ParFlow to compute energy and water fluxes (e.g., evaporation and transpiration) to and out of the soil. For example, the
modified CLM computes the bare ground surface evaporative flux, *E*_{gr}, as

$$\begin{array}{}\text{(20)}& {E}_{\mathrm{gr}}=-\mathit{\beta}{\mathit{\rho}}_{\mathrm{a}}{u}_{\ast}{q}_{\ast},\end{array}$$

where *β* (dimensionless) denotes the soil resistance factor, *ρ*_{a}
represents air density [ML^{−3}],
*u*_{∗} represents friction velocity [LT^{−1}], and *q*_{∗} (dimensionless) stands for the humidity scaling
parameter (Jefferson and Maxwell, 2015).
Evapotranspiration for vegetated land surface, *E*_{veg}, is computed as

$$\begin{array}{}\text{(21)}& {E}_{\mathrm{veg}}=\left[{R}_{\mathrm{pp},\mathrm{dry}}+{L}_{\mathrm{w}}\right]{L}_{\mathrm{SAI}}\left[{\displaystyle \frac{{\mathit{\rho}}_{\mathrm{a}}}{{r}_{\mathrm{b}}}}\left({q}_{\mathrm{sat}}-{q}_{\mathrm{af}}\right)\right],\end{array}$$

where *r*_{b} is the air density boundary resistance factor [LT^{−1}], *q*_{sat} (dimensionless) is saturated
humidity at the land surface, and *q*_{af} (dimensionless) is the canopy
humidity. The combination of *q*_{sat} and *q*_{af} forms the potential
evapotranspiration. The potential evapotranspiration is divided into
transpiration *R*_{pp,dry} (dimensionless), which depends on the dry fraction
of the canopy, and evaporation from foliage covered by water *L*_{w}
(dimensionless). *L*_{SAI} (dimensionless) is the summation of the leaf and stem
area indices that estimates the total surface from which evaporation can
occur. A detailed description of the equations PF.CLM uses can be
found in Jefferson
et al. (2015, 2017) and Jefferson and Maxwell (2015).

PF.CLM simulates variably saturated subsurface flow, surface or overland flow, and aboveground processes. PF.CLM was developed prior to the current Community Land Model (see Sect. 5.2), and the module structure of the current and early versions are different. PF.CLM has been updated over the years to improve its capabilities. PF.CLM was first done in the early 2000s as an undiversified, a column proof-of-concept model, whereby data or a message was transmitted between the coupled models via input/output files (Maxwell and Miller, 2005). Later, PF.CLM was presented in a distributed or diversified approach with a parallel input/output file structure wherein CLM is called as a set sequence of steps within ParFlow (Kollet and Maxwell, 2008a). These modifications, for example, were done to incorporate subsurface pressure values from ParFlow into chosen computations (Jefferson and Maxwell, 2015). These, to some extent, differentiate the modified version (PF.CLM) from the original CLM by Dai et al. (2003). Within the coupled PF.CLM, ParFlow solves the governing equations for overland and subsurface flow systems, and the CLM modules add the energy balance and mass fluxes from the soil, canopy, and root zone that can occur (i.e., interception, evapotranspiration, etc.) (Jefferson and Maxwell, 2015).

At the coupling interface where the models overlap and undergo online communication (Fig. 4b), ParFlow calculates and passes soil moisture and pressure heads of the subsurface to CLM, and CLM calculates and transmits transpiration from plants, canopy and ground surface evaporation, snow accumulation and melt, and infiltration from precipitation to ParFlow (Ferguson et al., 2016). In short, CLM does all canopy water balances and snow, but once the water through falls to the ground or snow melts, ParFlow takes over and estimates the water balances via the nonlinear Richards equation. The coupled model, PF.CLM, has been shown to more accurately predict root-depth soil moisture compared to the uncoupled model, i.e., the stand-alone land surface model (CLM), with capability to compute near-surface soil moisture. This increased accuracy results from the coupling of soil saturations determined by ParFlow and their impacts on other processes including runoff and infiltration (Kollet, 2009; Shrestha et al., 2014; Gebler et al., 2015; Gilbert and Maxwell, 2017). For example, Maxwell and Miller (2005) found that simulations of deeper soil saturation (more than 40 cm) vary between PF.CLM and uncoupled models, with PF.CLM simulations closely matching the observed data. Table 2 contains summaries of studies conducted with ParFlow coupled to either the original version of CLM by Dai et al. (2003) or the modified CLM (ParFlow with a land surface model).

“CLM” indicates that coupling with ParFlow was by the original Common Land
Model or Community Land Model. “CLM (modified)” indicates that the modified
version of

the Common Land Model by Dai et al. (2003) was a module for ParFlow.

It is well established that ParFlow in conjunction with CLM performs well in estimating all canopy water and subsurface water balances (Maxwell and Miller, 2005; Mikkelson et al., 2013; Ferguson et al., 2016). ParFlow, as a component of the coupled model, has been modified into a new parallel numerical model, ParFlowE, to incorporate the more complete heat equation coupled to variably saturated flow. ParFlowE simulates the coupling of terrestrial hydrologic and energy cycles, i.e., coupled moisture, heat, and vapor transport in the subsurface. ParFlowE is based on the original version of ParFlow, having identical solution schemes and a coupling approach as CLM. A coupled three-dimensional subsurface heat transport equation is implemented in ParFlowE using a cell-centered finite-difference scheme in space and an implicit backward Euler differencing scheme in time. However, the solution algorithm employed in ParFlow is fully exploited in ParFlowE wherein the solution vector of the Newton–Krylov method was extended to two dimensions (Kollet et al., 2009). In some integrated and climate models, the convection term of subsurface heat flux and the effect of soil moisture on energy transport is neglected due to simplified parameterizations and computational limitations. However, both convection and conduction terms are considered in ParFlowE (Khorsandi et al., 2014). In ParFlowE, functional relationships (i.e., equations of state) are performed to relate density and viscosity to temperature and pressure, as well as thermal conductivity to saturation. That is, modeling thermal flows by relating these parameterizations in simulating heat flow is an essential component of ParFlowE. In coupling between ParFlowE and CLM, ParFlowE[CLM], the one-dimensional subsurface heat transport in the CLM, is replaced by the three-dimensional heat transport equation including the process of convection of ParFlowE. CLM computes the mass and energy balances at the ground surface that lead to moisture fluxes and passes these fluxes to the subsurface moisture algorithm of ParFlowE[CLM]. These fluxes are used to compute subsurface moisture and temperature fields, which are then passed back to the CLM.

ParFlow is part of the Terrestrial System Modeling Platform TerrSysMP, which
comprises the nonhydrostatic fully compressible limited-area atmospheric
prediction model, COSMO, designed for both operational numerical weather
prediction and various scientific applications on the meso-*β*
(horizontal scales of 20–200 km) and meso-*γ* (horizontal scales of
2–20 km) (Duniec
and Mazur, 2011; Levis and Jaeger, 2011; Bettems et al., 2015), and the
Community Land Model version 3.5 (CLM3.5). Currently, it is used in direct
simulations of severe weather events triggered by deep moist convection,
including intense mesoscale convective complexes, prefrontal squall-line
storms, supercell thunderstorms, and heavy snowfall from wintertime
mesocyclones. COSMO solves nonhydrostatic, fully compressible
hydro-thermodynamical equations in advection form using the traditional
finite-difference method (Vogel
et al., 2009; Mironov et al., 2010; Baldauf et al., 2011; Wagner et al., 2016).

An online coupling between ParFlow and the COSMO model is performed via CLM3.5 (Gasper et al., 2014; Shrestha et al., 2014; Keune et al., 2016). Similar to the Common Land Model (by Dai et al., 2003), the CLM3.5 module accounts for surface moisture, carbon, and energy fluxes between the shallow or near-surface soil (discretized or specified top soil layer), snow, and the atmosphere (Oleson et al., 2008). The model components of a fully coupled system consisting of COSMO, CLM3.5, and ParFlow are assembled by making use of the multiple–executable approach (e.g., with the OASIS3–MCT model coupler). The OASIS3–MCT coupler employs communication strategies based on the message passing interface standards MPI1/MPI2 and the Project for Integrated Earth System Modeling, PRISM, Model Interface Library (PSMILe) for parallel communication of two-dimensional arrays between the OASIS3–MCT coupler and the coupling models (Valcke et al., 2012; Valcke, 2013). The OASIS3–MCT specifies the series of coupling, frequency of the couplings, the coupling fields, the spatial grid of the coupling fields, the transformation type of the (two-dimensional) coupled fields, and simulation time management and integration.

At the coupling interface, the OASIS3–MCT interface interchanges the atmospheric forcing terms and the surface fluxes in serial mode. The lowest level and current time step of the atmospheric state of COSMO is used as the forcing term for CLM3.5. CLM3.5 then computes and returns the surface energy and momentum fluxes, outgoing longwave radiation, and albedo to COSMO (Baldauf et al., 2011). The air temperature, wind speed, specific humidity, convective and grid-scale precipitation, pressure, incoming shortwave (direct and diffuse) and longwave radiation, and measurement height are sent from COSMO to CLM3.5. In CLM3.5, a mosaic tiling approach may be used to represent the subgrid-scale variability of land surface characteristics, which considers a certain number of patches or tiles within a grid cell. The surface fluxes and surface state variables are first calculated for each tile and then spatially averaged over the whole grid cell (Shrestha et al., 2014). As with PF.CLM3.5, the one-dimensional soil column moisture predicted by CLM3.5 gets replaced by ParFlow's variably saturated flow solver, so ParFlow is responsible for all calculations relating to soil moisture redistribution and groundwater flow. Within the OASIS3–MCT ParFlow sends the calculated pressure and relative saturation for the coupled region soil layers to CLM3.5. CLM3.5 also transmits depth-differentiated source and sink terms for soil moisture including soil moisture flux, e.g., precipitation, and soil evapotranspiration for the coupled region soil layers to ParFlow. Applications of TerrSysMP in fully coupled mode from saturated subsurface across the ground surface into the atmosphere include a study on the impact of groundwater on the European heat wave of 2003 and the influence of anthropogenic water use on the robustness of the continental sink for atmospheric moisture content (Keune et al., 2016).

The Weather Research and Forecasting (WRF) model is a mesoscale numerical weather prediction system designed to be flexible and efficient in a massively parallel computing architecture. WRF is a widely used model that provides a common framework for idealized dynamical studies, full-physics numerical weather prediction, air-quality simulations, and regional climate simulations (Michalakes et al., 1999, 2001; Skamarock et al., 2005). The model contains numerous mesoscale physics options such as microphysics parameterizations (including explicitly resolved water vapor, cloud, and precipitation processes), surface layer physics, shortwave radiation, longwave radiation, land surface, planetary boundary layer, data assimilation, and other physics and dynamics alternatives suitable for both large-eddy and global-scale simulations. Similar to COSMO, the WRF model is a fully compressible, conservative-form, nonhydrostatic atmospheric model that uses time-splitting integration techniques (discussed below) to efficiently integrate the Euler equations (Skamarock and Klemp, 2007).

The online ParFlow WRF coupling (PF.WRF) extends the WRF platform down to the bedrock by including highly resolved three-dimensional groundwater and variably saturated shallow or deep vadose zone flows, as well as a fully integrated lateral flow above the ground surface (Molders and Ruhaak, 2002; Seuffert et al., 2002; Anyah et al., 2008; Maxwell et al., 2011). The land surface model portion that links ParFlow to WRF is supplied by WRF through its land surface component, the Noah Land Surface Model (Ek et al., 2003); the stand-alone version of WRF has no explicit model of subsurface flow. Energy and moisture fluxes from the land surface are transmitted between the two models via the Noah LSM that accounts for the coupling interface and is conceptually identical to the coupling in PF–COSMO. The three-dimensional variably saturated subsurface and two-dimensional overland flow equations, and the three-dimensional atmospheric equations given by ParFlow and WRF, are simultaneously solved by the individual model solvers. Land surface processes, such as evapotranspiration, are determined in the Noah LSM as a function of potential evaporation and vegetation fraction. This effect is calculated with the formulation

$$\begin{array}{}\text{(22)}& E\left(x\right)=\phantom{\rule{0.125em}{0ex}}{F}^{fx}(\mathrm{1}-{f}_{\mathrm{avg}}){E}_{\mathrm{pot}},\end{array}$$

where *E*(*x*) stands for the rate of soil evapotranspiration (length per unit
time), *f**x* represents empirical coefficient, *f*_{avg} denotes vegetation
fraction, and *E*_{pot} is potential evaporation, determined depending on
atmospheric conditions from the WRF boundary layer parameterization (Ek et al., 2003). The vegetation fraction is zero over
bare soils (i.e., only soil evaporation), so Eq. (22) becomes

$$\begin{array}{}\text{(23)}& E\left(x\right)=\phantom{\rule{0.125em}{0ex}}{F}^{fx}{E}_{\mathrm{pot}}.\end{array}$$

The quantity *F* is parameterized as follows:

$$\begin{array}{}\text{(24)}& F=\phantom{\rule{0.125em}{0ex}}{\displaystyle \frac{\mathit{\varphi}{S}_{\mathrm{w}}-\mathit{\varphi}{S}_{\mathrm{res}}}{\mathit{\varphi}-\mathit{\varphi}{S}_{\mathrm{res}}}},\end{array}$$

where *ϕ* is the porosity of the medium, and *S*_{w} and *S*_{res} are
relative saturation and residual saturation, respectively, from the van Genuchten
relationships (van Genuchten, 1980; Williams and
Maxwell, 2011). Basically, *F* refers to the parameterization of the
interrelationship between evaporation and near-ground soil water content and
provides one of the connections between Noah LSM, ParFlow, and thus WRF.

In the presence of a vegetation layer, plant transpiration (length per unit time) is determined as follows:

$$\begin{array}{}\text{(25)}& T=G\left(z\right){C}_{\mathrm{plant}}{f}_{\mathrm{veg}}{E}_{\mathrm{pot}},\end{array}$$

where *C*_{plant}(−) represents a constant coefficient between 0 and 1,
which depends on vegetation species, and the *G*(z) function
represents soil moisture, which provides other connections between the coupled
models (i.e., ParFlow, Noah, and WRF). The solution procedure of PF.WRF uses
an operator-splitting approach in which both model components use the same
time step. WRF soil moisture information, including runoff, surface ponding
effects, and unsaturated and saturated flow, which includes an explicitly
resolved water table, is calculated and sent directly to the Noah LSM within
WRF by ParFlow and utilized by the Noah LSM in the next time step. WRF
supplies ParFlow with evapotranspiration rates and precipitation via the
Noah LSM (Jiang et al., 2009). The
interdependence between the energy and land balance of the subsurface, ground
surface, and lower atmosphere can fully be studied with this coupling
approach. The coupled PF.WRF via the Noah LSM has been used to simulate
explicit water storage and precipitation within basins, surface
runoff, and the land–atmosphere feedbacks and wind patterns as a
result of subsurface heterogeneity (Maxwell et al.,
2011; Williams and Maxwell, 2011). Studies with the coupled model PF.WRF are
highlighted in Table 2.

The Advanced Regional Prediction System (ARPS) is composed of a parallel
mesoscale atmospheric model created to explicitly predict convective storms
and weather systems. The ARPS platform aids in effectively investigating the
changes and predictability of storm-scale weather in both idealized and more
realistic settings. The model deals with the three-dimensional, fully
compressible, nonhydrostatic, spatially filtered Navier–Stokes equations
(Rihani et al., 2015). The governing equations include the
conservation of momentum, mass, water, heat or thermodynamics, turbulent
kinetic energy, and the equation of state of moist air by making use of a
terrain-following curvilinear coordinate system (Xue et al., 2000). The governing
equations presented in a coordinate system with *z* as the vertical coordinate
are given as follows.

$$\begin{array}{}\text{(26)}& {\displaystyle \frac{\mathrm{d}\mathit{v}}{\mathrm{d}t}}=-\mathrm{2}\mathrm{\Omega}\times \mathit{v}-{\displaystyle \frac{\mathrm{1}}{\mathit{\rho}}}\mathrm{\nabla}P+g+F\text{(27)}& {\displaystyle \frac{\mathrm{d}\mathit{\rho}}{\mathrm{d}t}}=-\mathit{\rho}\mathrm{\nabla}v\text{(28)}& {\displaystyle \frac{\mathrm{d}T}{\mathrm{d}t}}=-{\displaystyle \frac{\mathrm{RT}}{{C}_{\mathit{\upsilon}}}}\mathrm{\nabla}\mathit{v}+{\displaystyle \frac{Q}{{C}_{\mathit{\upsilon}}}}\text{(29)}& {\displaystyle}P=\mathit{\rho}\mathrm{RT}\end{array}$$

Equations (26) to (29) are momentum, continuity, thermodynamics, and
the equation of state, respectively. The material (total) derivative *d*∕d*t* is defined as

$$\begin{array}{}\text{(30)}& {\displaystyle \frac{d}{\mathrm{d}t}}={\displaystyle \frac{\partial}{\partial t}}+\mathrm{\nabla}\cdot \mathit{v}.\end{array}$$

The variables ** v**,

The PF.ARPS forms a fully coupled model that simulates spatial variations in aboveground processes and feedbacks, forced by physical processes in the atmosphere and below the ground surface. In the online coupling process, the ARPS land surface model forms the interface between ParFlow and ARPS to transmit information (i.e., surface moisture fluxes) between the coupled models. ParFlow, as a component of the coupled model, replaces the subsurface hydrology in the ARPS land surface model. Thus, ARPS is integrated into ParFlow as a subroutine to create a numerical overlay at the coupling interphase (specified layers of soil within the land surface model in ARPS) with the same number of soil layers at the ground surface within ParFlow. The solution approach employed is an operator splitting that allows ParFlow to match the ARPS internal time steps. ParFlow calculates the subsurface moisture field at each time step of a simulation and passes the information to the ARPS land surface model, which is used in each subsequent time step. At the beginning of each time step, the surface fluxes from ARPS that are important to ParFlow include the evapotranspiration rate and spatially variable precipitation (Maxwell et al., 2007). PF.ARPS has been applied to investigate the effects of soil moisture heterogeneity on atmospheric boundary layer processes. PF.ARPS keeps a realistic soil moisture that is topographically driven and shows a spatiotemporal relationship between water depth, land surface, and lower atmospheric variables (Maxwell et al., 2007; Rihani et al., 2015). A summary of current studies involving PF.ARPS is included in Table 2.

CrunchFlow is a software package developed to simulate multicomponent multidimensional reactive flow and transport in porous and/or fluid media (Steefel, 2009). Systems of chemical reactions that can be solved by the code include kinetically controlled homogenous and heterogeneous mineral dissolution reactions, equilibrium-controlled homogeneous reactions, thermodynamically controlled reactions, and biologically mediated reactions (Steefel and Lasaga, 1994; Steefel and Yabusaki, 1996). In CrunchFlow, discretization of the governing coupled partial differential equations that connect subsurface kinetic reactions and multicomponent equilibrium, flow, and solute transport is based on finite volume (Li et al., 2007, 2010). The coupling of reactions and transport in CrunchFlow that are available at runtimes is performed using two approaches. These are briefly discussed below.

The first is a global implicit or one-step method approach based on a backwards Euler time discretization, with a global solution of the coupled reactive transport equations using Newton's method. This global implicit scheme solves the transport and reaction terms simultaneously (up to two-dimensional) (Kirkner and Reeves, 1988; Steefel, 2009). The second is a time or operator splitting of the reaction and transport terms, which is based on an explicit forward Euler method: the sequential noniterative approach, SNIA (in which the transport and reaction terms are solved) (Steefel and Van Cappellen, 1990; Navarre-Sitchler et al., 2011). The stability criterion associated with the explicit approach is that the simulation time step is restricted via the Courant–Friedrichs–Lewy (CFL) condition, under the circumstance that the transportation of mass does not occur over multiple grid cells, but a single grid cell in a time step. Thus, a small time step must be used to ensure this condition holds. This small step size may lead to simulations that will demand much more time to solve Beisman (2007), so more processors are used in order to decrease the processor workload and decrease the solution time of the simulation. The coupling of fully saturated flow to the reactive transport calculations and coupling between a partially saturated flow and transport (flow and diffusion) can be done successively. However, these simulations require calculations of the flow and liquid saturation fields with a different model.

ParCrunchFlow is a parallel reactive transport model developed by combining ParFlow with CrunchFlow. ParCrunchFlow was designed to only be applicable for subsurface simulation. The coupled model relies on ParFlow's robustness ability to efficiently represent heterogeneous domains and simulate complex flow to provide a more realistic representation of the interactions between biogeochemical processes and nonuniform flow fields in the subsurface than the uncoupled model. ParFlow provides a solution of the Richards equation to ParCrunchFlow, which is not present in the biogeochemical code CrunchFlow. ParCrunchFlow employs an operator-splitting method for reactive transport, in which the transport and reaction terms are decoupled and calculated independently. Online coupling between the models is achieved through a sequential noniterative approach, whereby the reaction terms in CrunchFlow's operator-splitting solver get connected to ParFlow's advection terms. ParCrunchFlow takes advantage of the multidimensional advection capability of ParFlow instead of CrunchFlow's advective–dispersive transport capabilities (up to two-dimensional). A steady-state governing differential equation for reaction and advection (with no dispersion and diffusion terms) in a single-phase system is given by

$$\begin{array}{}\text{(31)}& {\displaystyle \frac{\partial {C}_{i}}{\partial t}}+\mathrm{\nabla}\left(\mathit{v}{C}_{i}\right)-{R}_{i}=\mathrm{0},\left(i=\mathrm{1},{N}_{\mathrm{tot}}\right),\end{array}$$

where *C*_{i} is the concentration of species *i*, ** v** represents the velocity
of flow,

6 Discussion and summary

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IHMs constitute classes of simulation tools ranging from simple lumped
parameter models to comprehensive deterministic, distributed, and physically
based modeling systems for the simulation of multiple hydrological processes (LaBolle
et al., 2003; Castronova et al., 2013). They are indispensable in studying
the interactions between surface and subsurface systems. IHMs that calculate
surface and subsurface flow equations in a single matrix (Maxwell et al., 2015), scaling from the beginning parts to the
mouth of continental river basins at high resolutions, are essential (Wood, 2009) in understanding and modeling surface–subsurface
systems. IHMs have been used to address surface and subsurface science and
applied questions. This includes, for example, evaluating the effects of groundwater
pumping on streamflow and groundwater resources (Markstrom et al., 2008),
evaluating relationships between topography and groundwater (Condon and Maxwell, 2015), coupling water flow
and transport (Sudicky et
al., 2008; Weill et al., 2011), assessing the resilience of water
resources to human stressors or interventions, and related variations
(Maxwell et al., 2015) over large spatial extents at high
resolution. Modeling and simulations at large spatial extents, e.g., regional
and continental scales with resolutions of 1 km^{2} (Fig. 6) or even
small spatial scales (Fig. 7), come with the associated computational load,
even on massively parallel computing architectures. IHMs, such as ParFlow,
have overcome the computational burden of simulating or resolving questions
(e.g., involving approximating variably saturated and overland flow
equations) beyond such levels of higher spatial scales and resolutions. This
capability may not be associated with more conceptually based models, which,
for example, may not simulate lateral groundwater flow or resolve surface
and subsurface flow by specifying zones of a groundwater network of streams
before performing a simulation (Maxwell et al., 2015). For
cross-comparison of ParFlow with other contemporary IHMs, more
comprehensive model testing and analyses have recently been done, and readers
can access these resources in Maxwell et al. (2014), Koch et al. (2016), and Kollet et al. (2017).

ParFlow is based on efficient parallelism (high performance efficiency) and robust hydrologic capabilities. The model solvers and numerical methods used are powerful, fast, robust, and stable, which has contributed to the code's excellent parallel efficiency. As stated earlier, ParFlow is very capable of simulating flows under saturated and variably saturated conditions, i.e., surface, vadose, and groundwater flows, even in highly heterogeneous environments. For example, in simulations of surface flows (i.e., solving the kinematic wave overland flow equations), ParFlow possess the ability to accurately solve streamflow (channelized flow) by using parameterized river-routing subroutines (Maxwell and Miller, 2005; Maxwell et al., 2007, 2011). ParFlow includes coupling capabilities with a flexible coupling interface that has been utilized extensively in resolving many hydrologic problems. The interface-based and process-level coupling used by ParFlow is an example for enabling high-resolution, realistic modeling. However, based on the applications, it would be worthwhile to create one, or several, generic coupling interfaces within ParFlow to make it easier to use its surface–subsurface capabilities in other simulations. Nonetheless, ParFlow has been used in coupling studies to simulate different processes and/or systems, including simulating energy and water budgets of the surface and subsurface (Rihani et al., 2010; Mikkelson et al., 2013), surface water and groundwater flows and transport (Kollet and Maxwell, 2006; Beisman, 2007; Beisman et al., 2015; Maxwell et al., 2015), and subsurface, surface, and atmospheric mass and energy balance (Maxwell and Miller, 2005; Maxwell et al., 2011; Shrestha et al., 2014; Sulis et al., 2017). Undoubtedly, such coupled model simulations come with computational burden, and ParFlow performs well in overcoming such problems, even at high spatial scales and resolutions. This capability of ParFlow (coupling with other models) is continuously being exploited by hydrologic modelers, and new couplings are consistently being established. For example, via model coupling, the entire transpiration process could be investigated, i.e., from carbon dioxide sequestration from the atmosphere by plants, to subsurface moisture dynamics and impacts, to oxygen production by plants. Likewise, land cover change effects on mountain pine beetles may be investigated via the coupling of integrated models. But these projected research advances can only be achieved if the scientific community keeps advancing code performance by developing, revising, updating, and rigorously testing these model capabilities.

Presently, ParFlow's open-source model and open developer community is fully transparent, and this openness is a major difference between it and other models that has enabled ParFlow to continue evolving. The user community is growing daily across the globe. Code developers have made available, aside from the ParFlow working manual, an active and frequently updated blog (current blog: http://parflow.blogspot.com/, last access: 13 July 2019) and other sources including https://www.parflow.org (last access: 13 July 2019) and https://github.com/parflow (last access: 13 July 2019), where code developers and experienced users provide great information and suggestions that help fix bugs and ease the frustrations of other users. Over the years, these easily accessible resources have proven to be helpful. The code is constantly updated through the release of new versions with modifications designed to meet varying hydrologic challenges and directions for applications across different scales and fields. Each ParFlow package (version) comes with verified simulation test cases with directions that simulate different real systems and idealized cases. These serve as a great resource wherein additional code modifications have been tested in every release of the code. ParFlow has a clear, rigorous verification procedure to make sure that any changes checked in do not “break” previous developments. This ensures numerical accuracy and backwards compatibility. Moreover, the full suite of test cases is automatically rerun before any submitted change can even be considered for merging with the master branch of the code. The number of branches and/or forks cannot be controlled in any open-source (or community) code, but any contributions to the master branch are exhaustively vetted before being pushed out to users. Further, there is a software development and sustainability plan to improve the capabilities of ParFlow, such as the incorporation of new formulations of both kinematic and diffusive wave approximations and advanced parallelization support (GPUs and heterogeneous compute architectures). ParFlow works very well on different computing architectures and operating systems from “laptops to supercomputers” (single CPU, Linux clusters, highly scalable systems including IBM Blue Gene) with the same source code and input on all platforms. The code can use significant computational power and runs efficiently on supercomputing environments (e.g., Edison, Cori, JUQUEEN, and Yellowstone). Through ParFlow hydrologic modelers have available a very efficient yet still growing integrated hydrologic model to simulate and understand surface–subsurface flows.

Code availability

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Code availability.

ParFlow is an open-source, object-oriented, parallel watershed flow model developed by the community of scientists from the Environmental Protection Department at the Lawrence Livermore National Laboratory (LLNL), Colorado School of Mines, and FZ Jülich, along with supporting scientists from several other institutions. The current version of ParFlow is available at https://github.com/parflow/parflow/releases/tag/v3.6.0 (last access: 4 September 2019; Smith, 2019). The version of ParFlow described in this paper is archived on Zenodo: https://doi.org/10.5281/zenodo.3555297 (Kuffour, 2019).

Author contributions

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Author contributions.

Section 3 of the paper was written by CSW. BNOK and NBE wrote the other sections, and the entire paper was edited by LEC, SK, and RMM.

Competing interests

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Competing interests.

The authors declare that they have no conflict of interest.

Acknowledgements

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Acknowledgements.

We kindly acknowledge funding of the project by the U.S. Department of Energy, Office of Science (Subsurface Biogeochemical Research), award number DE-SC0019123.

Financial support

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Financial support.

This research has been supported by the U.S. Department of Energy, Office of Science (Subsurface Biogeochemical Research) (grant no. DE-SC0019123).

Review statement

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Review statement.

This paper was edited by Jeffrey Neal and reviewed by two anonymous referees.

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Short summary

Integrated hydrologic models (IHMs) were developed in order to allow for more accurate simulations of real-world ecohydrologic conditions. Many IHMs exist, and the literature can be dense, so it is often difficult to understand what a specific model can and cannot do. We provide a review of the current core capabilities, solution techniques, communication structure with other models, some limitations, and potential future improvements of one such open-source integrated model called ParFlow.

Integrated hydrologic models (IHMs) were developed in order to allow for more accurate...

Geoscientific Model Development

An interactive open-access journal of the European Geosciences Union