# Mode: `REACTIVE TRANSPORT`

(Keyword `CHEMISTRY`

)¶

The governing mass conservation equations for the geochemical transport mode for a multiphase system written in terms of a set of independent aqueous primary or basis species with the form

and

for minerals with molar volume \(\overline{V}_m\), mineral reaction rate \(I_m\) and mineral volume fraction \(\varphi_m\) referenced to an REV. Sums over \({{\alpha}}\) in Eqn. (1) are over all fluid phases in the system. The quantity \(\Psi_j^{{\alpha}}\) denotes the total concentration of the \(j\)th primary species \({{\mathcal A}}_j^{\rm pri}\) in the \({{\alpha}}\)th fluid phase defined by

In this equation the subscript \(l\) represents the aqueous electrolyte phase from which the primary species are chosen. The secondary species concentrations \(C_i^{{\alpha}}\) are obtained from mass action equations corresponding to equilibrium conditions of the reactions

yielding the mass action equations

with equilibrium constant \(K_i^{{\alpha}}\), and activity coefficients \(\gamma_k^{{\alpha}}\). For the molality of the \(k\)th aqueous species, the Debye-Hückel activity coefficient algorithm is given by

and the Davies algorithm by the expression

with valence \(z_k\), Debye-Hückel parameters \(A\), \(B\), and ionic radius \(\stackrel{\circ}{a}_k\), and ionic strength \(I\) defined as

for molality \(m_j\) and \(m_i\) of primary and secondary species, respectively (note: \(C_i^l = \rho_l y_w^l m_i \simeq \rho_l m_i\), \(\rho_l\) = fluid density, \(y_w^l\) = mass fraction of \(\mathrm{H_2O}\)). For high-ionic strength solutions (approximately above 0.1 M) the Pitzer model should be used. Currently, however, only the Debye-Hückel algorithm is implemented in PFLOTRAN.

The total flux \({\boldsymbol{\Omega}}_j^{{\alpha}}\) for species-independent diffusion is given by

The diffusion/dispersion tensor \({\boldsymbol{D}}_{\alpha}\) may be different for different phases, e.g. an aqueous electrolyte solution or gas phase, but is assumed to be species independent. Dispersivity currently must be described through a diagonal dispersion tensor.

The Darcy velocity \({\boldsymbol{q}}_{{\alpha}}\) for phase \({{\alpha}}\) is given by

with bulk permeability of the porous medium \(k\) and relative permeability \(k_{{\alpha}}\), fluid viscosity \(\mu_{{\alpha}}\), pressure \(p_{{\alpha}}\), density \(\rho_{{\alpha}}\), and acceleration of gravity \(g\). The diffusivity/dispersivity tensor \({\boldsymbol{D}}_{{\alpha}}\) is the sum of contributions from molecular diffusion and dispersion which for an isotropic medium has the form

with longitudinal and transverse dispersivity coefficients \(a_L\), \(a_T\), respectively, \(\tau\) refers to tortuosity, and \(D_m\) to the molecular diffusion coefficient. Currently, only a diagonal dispersion tensor with principal axes aligned with the grid for longitudinal and transverse dispersion is implemented in PFLOTRAN.

The porosity may be calculated from the mineral volume fractions according to the relation

The temperature dependence of the diffusion coefficient is defined through the relation

with diffusion activation energy \(A_D\) in kJ/mol. The quantity \(D_m^\circ\) denotes the diffusion coefficient at the reference temperature \(T_0\) taken as 25\(^\circ\)C and the quantity \(R\) denotes the gas constant (\(8.317\times 10^{-3}\) kJ/mol/K). The temperature \(T\) is in Kelvin.

The quantity \(Q_j\) denotes a source/sink term

where \(q_M\) denotes a mass rate in units of kg/s, \(\rho\) denotes the fluid density in kg/m\(^3\), and \({\boldsymbol{r}}_{n}\) refers to the location of the \(n\)th source/sink. The quantity \(S_j\) represents the sorbed concentration of the \(j\)th primary species considered in more detail in the next section.

Molality \(m_i\) and molarity \(C_i\) are related by the density of water \(\rho_w\) according to

The activity of water is calculated from the approximate relation

## Mineral Precipitation and Dissolution¶

The reaction rate \(I_m\) is based on transition state theory taken as positive for precipitation and negative for dissolution, with the form

where the sum over \(l\) represents contributions from parallel reaction mechanisms such as pH dependence etc., and where \(K_m\) denotes the equilibrium constant, \(\sigma_m\) refers to Temkin’s constant which is defined as the average stoichiometric coefficient of the overall reaction (Lichtner, 1996b; see also Section [thermo:database]), \(\beta_m\) denotes the affinity power, \(a_m\) refers to the specific mineral surface area, and the ion activity product \(Q_m\) is defined as

with molality \(m_j\) of the \(j\)th primary species. The rate constant \(k_{ml}\) is a function of temperature given by the Arrhenius relation

where \(k_{ml}^0\) refers to the rate constant at the reference temperature \(T_0\) taken as 25\(^\circ\)C, with \(T\) in units of Kelvin, \(E_{ml}\) denotes the activation energy (kJ/mol), and the quantity \({{{\mathcal P}}}_{ml}\) denotes the prefactor for the \(l\)th parallel reaction with the form

where the product index \(i\) generally runs over both primary and secondary species, the quantities \(\alpha_{il}^m\) and \(\beta_{il}^m\) refer to prefactor coefficients, and \(K_{ml}\) is an attenuation factor. The quantity \(R\) denotes the gas constant (\(8.317 \times 10^{-3}\) kJ/mol/K).

### Rate Limiter¶

A rate-limited form of the mineral kinetic rate law can be devised according to the expression

with rate-limiter \(r_{\rm lim}\). In the limit \(K_mQ_m\rightarrow\infty\), the rate becomes

Defining the affinity factor

or

the rate may be expressed alternatively as

### Changes in Material Properties¶

Porosity, permeability, tortuosity and mineral surface area may be updated optionally due to mineral precipitation and dissolution reactions according to the relations

with

and

where the super/subscript 0 denotes initial values, with a typical value for \(n\) of \(2/3\) reflecting the surface to volume ratio. Note that this relation only applies to primary minerals \((\varphi_m^0\ne 0)\). The quantity \(\varphi_c\) refers to a critical porosity below which the permeability is assumed to be constant with scale factor \(f_{\rm min}\).

In PFLOTRAN the solid is represented as an aggregate of minerals described quantitatively by specifying its porosity \(\varphi\) and the volume fraction \(\varphi_m\) of each primary mineral. It is not necessary that Eqn. (26) relating porosity and mineral volume fractions holds. Typically, however, the solid composition is specified by giving the mass fraction \(y_m\) of each of the primary minerals making up the solid phase. The volume fraction is related to mole \(x_m\) and mass \(y_m\) fractions by the expressions

with inverse relation

and similarly for the mass fraction, where

and the solid molar density \(\eta_s\) is given by

In these relations \(W_m\) refers to the formula weight and \(\overline{V_m}\) the molar volume of the \(m\)th mineral. The solid molar density is related to the mass density \(\rho_s\) by

with the mean molecular weight \(W_s\) of the solid phase equal to

Mass and mole fractions are related by the expression

### Affinity Threshold¶

An affinity threshold \(f\) for precipitation may be introduced which only allows precipitation to occur if \(K_m Q_m > f > 1\).

### Surface Armoring¶

Surface armoring occurs when one mineral precipitates on top of another mineral, blocking that mineral from reacting. Thus suppose mineral \({{\mathcal M}}_m\) is being replaced by the secondary mineral \({{\mathcal M}}_{m'}\). Blocking may be described phenomenologically by the surface area relation

for \(\varphi_{m'} < \varphi_{m'}^c\), and

if \(\varphi_{m'}(t) \geq \varphi_{m'}^c\), where \(\varphi_{m'}^c\) represents the critical volume fraction necessary for complete blocking of the reaction of mineral \({{\mathcal M}}_m\).

## Sorption¶

Sorption reactions incorporated into PFLOTRAN consist of ion exchange and surface complexation reactions for both equilibrium and multirate formulations.

### Ion Exchange¶

Ion exchange reactions may be represented either in terms of bulk- or mineral-specific rock properties. Changes in bulk sorption properties can be expected as a result of mineral reactions. However, only the mineral-based formulation enables these effects to be captured in the model. The bulk rock sorption site concentration \(\omega_{{\alpha}}\), in units of moles of sites per bulk sediment volume (mol/dm:math:^3), is related to the bulk cation exchange capacity \(Q_{{\alpha}}\) (mol/kg) by the expression

with solid density \(\rho_s\) and porosity \(\varphi\). The cation exchange capacity associated with the \(m\)th mineral is defined on a molar basis as

The site concentration \(\omega_{{\alpha}}\) is related to the sorbed concentrations \(S_k^{{\alpha}}\) by the expression

In PFLOTRAN ion exchange reactions are expressed in the form with the reference cation denoted by \({{\mathcal A}}_j^{z_j+}\) on the right-hand side of the reaction

with valencies \(z_j\), \(z_i\) of cations \({\mathcal A}_j^{z_j+}\) and \({\mathcal A}_i^{z_i+}\), respectively, and exchange site \(\chi_{{\alpha}}^-\) on the solid surface. The cations \({{\mathcal A}}_i^{z_i+}, \,i\ne j\) represents all other cations besides the reference cation. The corresponding mass action equation is given by

with selectivity coefficient \(K_{ij}^{{\alpha}}\), solid phase activity coefficients \(\lambda_l^{{\alpha}}\) (taken as unity in what follows), and mole fraction \(X_l^{{\alpha}}\) of the \(l\)th cation of site \({{\alpha}}\). For \(N_c\) cations participating in exchange reactions, there are \(N_c-1\) independent reactions and thus \(N_c-1\) independent selectivity coefficients.

The exchange reactions may also be expressed as half reactions in the form

with corresponding selectivity coefficient \(k_j^{{\alpha}}\). The half-reaction selectivity coefficients are related to the \(K_{ij}^{{\alpha}}\) by

or

This relation is obtained by multiplying the half reaction for cation \({{\mathcal A}}_j\) by the valence \(z_i\) and subtracting from the half reaction for \({{\mathcal A}}_i\) multiplied by \(z_j\), resulting in cancelation of the empty site \(X^{{\alpha}}\), to obtain the complete exchange reaction (44). It should be noted that the coefficients \(k_l^{{\alpha}}\) are not unique since, although there are \(N_c\) coefficients in number, only \(N_c-1\) are independent and one may be chosen arbitrarily, usually taken as unity. Thus for \(k_j^{{\alpha}}=1\), Eqn. (48) yields

An alternative form of reactions (44) often found in the literature is

obtained by dividing reaction (44) through by the product \(z_i z_j\). The mass action equations corresponding to reactions (50) have the form

The selectivity coefficients corresponding to the two forms are related by the expression

and similarly for \(k_i^{{\alpha}}\), \(k_j^{{\alpha}}\). When comparing with other formulations it is important that the user determine which form of the ion exchange reactions are being used and make the appropriate transformations.

The selectivity coefficients satisfy the relations

and from the identity

the following relation is obtained

To see how the selectivity coefficients change when changing the reference cation from \({{\mathcal A}}_j^{z_j+}\) to \({{\mathcal A}}_k^{z_k+}\) note that

and

This latter relation follows from adding the two reactions

to give

with \({{\mathcal A}}_k^{z_k+}\) as reference species.

In terms of the selectivity coefficients \(K_{ij}^{{\alpha}}\) it follows that

or

In terms of the coefficients \(k_i^{{\alpha}}\) and \(\overline k_i^{{\alpha}}\) corresponding to reference cation \({{\mathcal A}}_k\) the transformation becomes

In terms of the coefficients \(k_l^{{\alpha}}\) the sorbed concentration for the \(i\)th cation can be expressed as a function of the reference cation from the mass action equations according to

For a given reference species \({{\mathcal A}}_{J_0}\) the coefficients \(K_{iJ_0}\) are uniquely determined. For some other choice of reference species, say \({{\mathcal A}}_{I_0}\), the coefficients \(K_{iI_0}\) are related to the original coefficients by the expressions

Taking the reference cation as \({{\mathcal A}}_j\) then \(k_i^{{\alpha}}\) is given by

As an example consider the ion-exchange reactions with Ca\(^{2+}\) as reference species

with selectivity coefficients \(K_{\rm NaCa}\) and \(K_{\rm MgCa}\). Alternatively, using Na\(^+\) as reference cation gives

with selectivity coefficients \(K_{\rm CaNa}\) and \(K_{\rm MgNa}\). The selectivity coefficients are related by the equations

Using the Gaines-Thomas convention, the equivalent fractions \(X_k^{{\alpha}}\) are defined by

with

For equivalent exchange \((z_j=z_i=z)\), an explicit expression exists for the sorbed concentrations given by

where \(m_k\) denotes the \(k\)th cation molality. This expression follows directly from the mass action equations for the sorbed cations and conservation of exchange sites.

In the more general case \((z_i\ne z_j)\) it is necessary to solve the nonlinear equation

for the reference cation mole fraction \(X_j\). From the mass action equation Eqn. (45) it follows that

Defining the function

its derivative is given by

The reference mole fraction is then obtained by Newton-Raphson iteration

The sorbed concentration for the \(j\)th cation appearing in the accumulation term is given by

with the derivatives for \(j\ne l\)

and for \(j=l\)

### Surface Complexation¶

Surface complexation reactions are assumed to have the form

for the \(i\)th surface complex \(>{{\mathcal S}}_{i{{\alpha}}}\) on site \({{\alpha}}\) and empty site \(>\chi_{{\alpha}}\). As follows from the corresponding mass action equation the equilibrium sorption concentration \(S_{i{{\alpha}}}^{\rm eq}\) is given by

and the empty site concentration by

where the ion activity product \(Q_i\) is defined by

The site concentration \(\omega_{{\alpha}}\) satisfies the relation

and is constant. The equilibrium sorbed concentration \(S_{j{{\alpha}}}^{\rm eq}\) is defined as

### Multirate Sorption¶

In the multirate model the rates of sorption reactions are described through a kinetic relation given by

for surface complexes, and

for empty sites, where \(S_{{\alpha}}^{\rm eq}\) denotes the equilibrium sorbed concentration. For simplicity, in what follows it is assumed that \(\nu_{{\alpha}}=1\). With each site \({{\alpha}}\) is associated a rate constant \(k_{{\alpha}}\) and site concentration \(\omega_{{\alpha}}\). These quantities are defined through a given distribution of sites \(\wp({{\alpha}})\), such that

The fraction of sites \(f_{{\alpha}}\) belonging to site \({{\alpha}}\) is determined from the relation

with the property that

Given that the total site concentration is \(\omega\), then the site concentration \(\omega_{{\alpha}}\) associated with site \({{\alpha}}\) is equal to

An alternative form of these equations is obtained by introducing the total sorbed concentration for the \(j\)th primary species for each site defined as

Then the transport equations become

The total sorbed concentrations are obtained from the equations

## Sorption Isotherm <Under Revision>¶

The distribution coefficient \(\widetilde K_j^D\) [m:math:^3 kg\(^{-1}\)] is customarily defined as the ratio of sorbed to aqueous concentrations with the sorbed concentration referenced to the mass of solid as given by

where \(M_j^s = W_j N_j^s\), \(M_j^{\rm aq}=W_j N_j^{\rm aq}\), refers to the mass and number of moles of sorbed and aqueous solute related by the formula weight \(W_j\) of the \(j\)th species, \(M_s\) refers to the mass of the solid, \(V_l\) denotes the aqueous volume, \(\widetilde S_j=N_j^s/M_s\) [mol kg\(^{-1}\)] represents the sorbed concentration referenced to the mass of solid, \(C_j=N_j^{\rm aq}/V_l\) denotes molarity, and \(m_j=C_j/\rho_w\) represents molality, where \(\rho_w\) is the density of pure water.

The distribution coefficient \(\widetilde K_j^D\) may be related to its dimensionless counterpart \(K_j^D\) [—] defined by

by writing

with grain density \(\rho_s=M_s/V_s\), bulk density \(\rho_b=(1-\varphi)\rho_s\), porosity \(\varphi=V_p/V\), and saturation \(s_l=V_l/V_p\).

An alternative definition of the distribution coefficient denoted by \(\widehat K_j^D\) [kg m\(^{-3}\)] is obtained by using molality to define the solute concentration and referencing the sorbed concentration to the bulk volume \(V\)

A sorption isotherm \(S_j\) may be specified for any primary species \({{\mathcal A}}_j\) resulting in the transport equation

for a partially saturated medium. Substituting \(S_j=\varphi s_l K_j^D C_j\) from Eqn. (96) and introducing the retardation \({{{\mathcal R}}}_j\) gives

with the retardation given by the alternative forms

Three distinct models are available for the sorption isotherm \(S_j\) in PFLOTRAN:

linear \(K_D\) model:

(102)\[S_j = \varphi s_l K_j^D C_j = \widehat K_j^D m_j,\]with distribution coefficient \(\widehat K_j^D\),

Langmuir isotherm:

(103)\[S_j= \frac{K_j^L b_j^L C_j/ \rho_w}{1+K_j^L C_j/ \rho_w} = \frac{K_j^L b_j^L m_j}{1+K_j^L m_j},\]with Langmuir coefficients \(K_j^L\) and \(b_j^L\), and

Freundlich isotherm:

(104)\[S_j = K_j^F \left(\frac{C_j}{\rho_w}\right)^{(1/n_j^F)} = K_j^F \big(m_j\big)^{(1/n_j^F)},\]with coefficients \(K_j^F\) and \(n_j^F\).

## Colloid-Facilitated Transport¶

Colloid-facilitated transport is implemented into PFLOTRAN based on surface complexation reactions. Competition between mobile and immobile colloids and stationary mineral surfaces is taken into account. Colloid filtration processes are not currently implemented into PFLOTRAN. A colloid is treated as a solid particle suspended in solution or attached to a mineral surface. Colloids may be generated through nucleation of minerals in solution, although this effect is not included currently in the code.

Three separate reactions may take place involving competition between mobile and immobile colloids and mineral surfaces

with corresponding reaction rates \(I_k^{{\rm m}}\), \(I_k^{{\rm im}}\), and \(I_k^s\), where the superscripts \(s\), \(m\), and \(im\) denote mineral surfaces, and mobile and immobile colloids, respectively. In addition, reaction with minerals \({{\mathcal M}}_s\) may occur according to the reaction

The transport equations for primary species, mobile and immobile colloids, read

where \({\boldsymbol{q}}_c\) denotes the colloid Darcy velocity which may be greater than the fluid velocity \({\boldsymbol{q}}\). For conditions of local equilibrium the sorption reaction rates may be eliminated and replaced by algebraic sorption isotherms to yield

In the kinetic case either form of the primary species transport equations given by Eqn. (107) or (111) can be used provided it is coupled with the appropriate kinetic equations Eqns. (108) – (110). The mobile case leads to additional equations that must be solved simultaneously with the primary species equations. A typical expression for \(I_k^m\) might be

with rate constant \(k_k\) and where \(S_{km}^{\rm eq}\) is a known function of the solute concentrations. In this case, Eqn. (108) must be added to the primary species transport equations. Further reduction of the transport equations for the case where a flux term is present in the kinetic equation is not possible in general for complex flux terms.

## Tracer Mean Age¶

PFLOTRAN implements the Eulerian formulation of solute age for a nonreactive tracer following Goode (1996). PFLOTRAN solves the advection-diffusion/dispersion equation for the mean age given by

where \(A\) denotes the mean age of the tracer with concentration \(C\). Other quantities appearing in the age equation are identical to the tracer transport equation for a partially saturated porous medium with saturation state \(s\). The age and tracer transport equations are solved simultaneously for the age-concentration \(\alpha = A C\) and tracer concentration \(C\). The age-concentration \({{\alpha}}\) satisfies the usual advection-diffusion-dispersion equation with a source term on the right-hand side.

The mean tracer age is calculated in PFLOTRAN by adding the species
`Tracer_Age`

together with `Tracer`

to the list of primary species

```
PRIMARY_SPECIES
Tracer
Tracer_Age
/
```

including sorption through a constant \(K_d\) model if desired

```
SORPTION
ISOTHERM_REACTIONS
Tracer
TYPE LINEAR
DISTRIBUTION_COEFFICIENT 500. ! kg water/m^3 bulk
/
Tracer_Age
TYPE LINEAR
DISTRIBUTION_COEFFICIENT 500. ! kg water/m^3 bulk
/
/
/
```

and specifying these species in the initial and boundary `CONSTRAINT`

condition as e.g.:

```
CONSTRAINT initial
CONCENTRATIONS
Tracer 1.e-8 F
Tracer_Age 1.e-16 F
/
/
```

Output is given in terms of \(\alpha\) and \(C\) from which the mean age \(A\) can be obtained as \(A= \alpha/C\).

## Thermodynamic Database¶

PFLOTRAN reads thermodynamic data from a database that may be customized
by the user. Reactions included in the database consist of aqueous
complexation, mineral precipitation and dissolution, gaseous reactions,
and surface complexation. Ion exchange reactions and their selectivity
coefficients are entered directly from the input file. A standard
database supplied with the code is referred to as `hanford.dat`

and is
found in the `./database`

directory in the PFLOTRAN Git
repository. This database is an ascii text file that can be edited by
any editor and is equivalent to the EQ3/6 database:

```
data0.com.V8.R6
CII: GEMBOCHS.V2-EQ8-data0.com.V8.R6
THERMODYNAMIC DATABASE
generated by GEMBOCHS.V2-Jewel.src.R5 03-dec-1996 14:19:25
```

The database provides equilibrium constants in the form of log \(K\) values at a specified set of temperatures listed in the top line of the database. A least squares fit is used to interpolate the log \(K\) values between the database temperatures using a Maier-Kelly expansion of the form

with fit coefficients \(c_i\). The thermodynamic database stores all
chemical reaction properties (equilibrium constant \(\log K_r\),
reaction stoichiometry \(\nu_{ir}\), species valence \(z_i\),
Debye parameter \(a_i\), mineral molar volume \(\overline V_m\),
and formula weight \(w_i\)) used in PFLOTRAN. The database is
divided into 5 blocks as listed in Table [tdatabase], consisting of
database primary species, aqueous complex reactions, gaseous reactions,
mineral reactions, and surface complexation reactions. Each block is
terminated by a line beginning with `’null’`

. The quantity
\(N_{\rm temp}\) refers to the number of temperatures at which log
\(K\) values are stored in the database. In the `hanford.dat`

database \(N_{\rm temp}=8\) with equilibrium constants stored at the
temperatures: 0, 25, 60, 100, 150, 200, 250, and 300\(^\circ\)C.
The pressure is assumed to lie along the saturation curve of pure water
for temperatures above 25\(^\circ\)C and is equal to 1 bar at
lower temperatures. Reactions in the database are assumed to be written
in the canonical form

for species \({{\mathcal A}}_r\), where `nspec`

refers to the
number of aqueous or gaseous species \({{\mathcal A}}_i\) on the
right-hand side of the reaction. Redox reactions in the standard
database `hanford.dat`

are usually written in terms of
O\(_{2(g)}\). Complexation reactions involving redox sensitive
species are written in such a manner as to preserve the redox state.

Primary Species: | name, \(a_0\), \(z\), \(w\) |

Secondary Species: | name, nspec, (\(\nu\)(n), name(\(n\)), \(n\)=1, nspec), log\(K\)(1:\(N_{\rm temp}\)), \(a_0\), \(z\), \(w\) |

Gaseous Species: | name, \(\overline V\), nspec, (\(\nu\)(n), name(\(n\)), \(n\)=1, nspec), log\(K\)(1:\(N_{\rm temp}\)), \(w\) |

Minerals: | name, \(\overline V\), nspec, (\(\nu\)(n), name(\(n\)), \(n\)=1, nspec), log\(K\)(1:\(N_{\rm temp}\)), \(w\) |

Surface Complexes: | \(>\)name, nspec, \(\nu\), \(>\)site, (\(\nu\)(n), name(\(n\)), \(n\)=1, nspec-1), log\(K\)(1:\(N_{\rm temp}\)), \(z\), \(w\) |

Note that chemical reactions are not unique. For example, given a particular mineral reaction

and equally acceptable reaction is the scaled reaction

with scale factor \(\lambda_m\) corresponding to a different choice of formula unit. A different scale factor may be used for each mineral. The scaled reaction corresponds to

with \({\mathcal M}_m' = \lambda_m{\mathcal M}_m\), \(\nu_{jm}' = \lambda_m\nu_{jm}\). In addition, the mineral molar volume \(\overline V_m\), formula weight \(W_m\), and equilibrium constant \(K_m\) are scaled according to

The saturation index \({\rm SI}_m\) transforms according to

Consequently, equilibrium is not affected as is to be expected. However, a more general form for the reaction rate is needed involving Temkin’s constant [see Eqn. (17)], in order to ensure that the identical solution to the reactive transport equations is obtained using the scaled reaction (Lichtner, 2016). Thus it is necessary that the following conditions hold

This requires that the reaction rate \(I_m\) transform as

which guarantees that mineral volume fractions and solute concentrations are identical to that obtained from solving the reactive transport equations using the unscaled reaction.

From the above relations it is found that the reaction rate transforms according to

where the last result is obtained by scaling Temkin’s constant according to

It should be noted that the mineral concentration \((C_m' =({\overline V}_m^{-1})^{'} \phi_m = \lambda_m^{-1} C_m)\), differs in the two formulations; however, mass density \((\rho_m = W_m \overline V_m^{-1})\) is an invariant, unlike molar density \((\eta_m=\overline V_m^{-1})\). The scaling factor \(\lambda_m\) can be found under MINERAL_KINETICS with the option MINERAL_SCALE_FACTOR.

## Eh, pe¶

Output for Eh and pe is calculated from the half-cell reaction

with the corresponding equilibrium constant fit to the Maier-Kelly expansion Eqn. (114). The fit coefficients are listed in Table below.

coefficient | value |
---|---|

\(c_{-1}\) | 6.745529048 |

\(c_0\) | -48.295936593 |

\(c_1\) | -0.000557816 |

\(c_2\) | 27780.749538022 |

\(c_3\) | 4027.337694858 |

Table: Fit coefficients for log \(K\) of reaction (125).