one d diff transport
DESCRIPTION
ÂTRANSCRIPT
One dimensional dissolution diffusion transport for quartz
vein formation
The porosity of the host rock is , the silica concentration is m in units mol m-3
, the
supersaturation of the host rock prior to fracturing is m2, and D is the diffusion coefficient
D in units m2 s
-1 . m2 is related to pressure solution
The left hand side of Eq. (1) is a diffusion equation and the right hand side is a source
term when m<m2. The dissolution process is represented by a source term that is
proportional to both a reaction rate kd (in units mol m-3
s-1
) and the concentration
difference m - m2. Source term may represent other dissolution process as well
One boundary condition could be
m (x=) = m2 (concentration in the host rock far away from fracture)
The second boundary condition is at x=0 (on the fracture) is essentially a mass
conservation equation i.e., mass of silica input to the fracture by diffusion equals the
mass deposited on the fracture
(2)
Precipitation of quartz in the fracture is controlled by the reaction rate kp (units mol m
-2 s
-
1), the effective surface area for precipitation per unit area fracture wall a1 (units m
2/m
2)
and the difference m - m1 between the concentration of silica in the fracture fluid, m, and
the equilibrium concentration of silica in the racture, m1.
Precipitation process is fully reversible i.e. net of the forward (dissolution) and backward
(precipitation) - dissolution has a different rate than precipitation since precipitation
depends on surface area.
Conversion of the equation to dimensionless form (characteristic length l0 and
characteristic time
Concentration m can be represented by unit concentration
Concentration c=0 corresponds to m=m1 and c=1 to m=m2
With the imposed boundary condition the equation can be written as
(dimensionless equation) (3)
C=1 at x (cap) =
Where dimensionless distance x(cap) and are given by x(cap) = x/l0 and
= t/t0
td and tp are the characteristic time for the dissolution and precipitation and
are given by
The ratios t0/td and t0/tp are the only parameters in the model they are the Damkohler
numbers
…. (4)
These numbers measure the characteristic time for the diffusion process relative to the
characteristic time for the dissolution process and the precipitation process respectively.
The dimensionless equation has time dependent general solution but taking a stationary
state (time much longer than the characteristic time of any of the process) where the c/t
= 0 the equation reduces to
(the last two are the boundary condition where ld and lp are the characteristic lengths of
dissolution-transport and precipitation respectively and given by)
ld is the length scale into the host rock where there is a concentration difference because
of the cementation process.
The inverse length scale 1/lp can be interpreted as a characteristic concentration gradient
into the fracture.
By letting l0 = ld be the characteristic length of the system, we see that Nd = 1 and Np =
ld/lp. The number Np is therefore the relevant parameter for the cementation process over
long time spans where the silica concentration is almost stationary. This parameter (Np)
is now denoted Da and it can be written
…(5)
The solution for the stationary equation becomes
…(6)
The concentration of silica on the fracture cf and mf are given by
Da-number defines two different regimes in terms of the silica concentration in the
fractures, depending on whether Da is much less than 1 or much larger than 1. cf = 0 if
Da>> 1 and cf= 1 if Da <<1 – the latter is precipitation dominated regime and the former
is dissolution transport dominated regime
The stationary solution to the concentration difference between the host rock and fracture
has the characteristic length l0.
The concentration difference between the fracture (mf) and deep into the host rock (m2) is
reduced to the half at the distance x = ln2l0. It is seen from Nd=1 that the characteristic
time for diffusion and dissolution are equal for the characteristic length l0.
The Damkohler number
The rate kd is now replaced by the Da-number and the quartz cementation process is
studied in terms of the Da-number. The Da-number allows for a study of the vein
cementation process without going into details of the dissolution process. The quartz
cementation process can be studied using the following Da-numbers 0.01, 0.1, 1 and 10,
100 and 1000 where the precipitation limited regime is represented by Da = 0.01 and 0.1,
and
the diffusion limited regime is represented by Da = 10, 100 and 1000, and where Da = 1
is an intermediate regime. The characteristic time and length can be represented as
follows using the Da-number
…(7)
Numbers for the parameters D, m1, m2, kp and a1 are needed before the characteristic
time, length and cementation rates can be calculated. A simplified system where quartz is
the dominant mineral is assumed,
H2O + SiO2 = H4SiO4
for which you can calculate the K
very simplistically, you can assume activities of water and silica to be unity and also the
solution to be sufficiently diluted for taking activity coeff. of SiO2 = 1, then the
equilibrium conc. of vein fluid (m1) can be taken as equal to K for which the temperature
dependence is known
kp can be expanded by the Arrhenius law as
problem with the laboratory data for quartz kinetics applied to sandstones could be that
simple geometrical models for the pore space over-estimates the effective surface area for
quartz precipitation
D- is also a difficult parameter to estimate
Rate of Fracture Cementation
The rate at which the fracture is filled is given by
…..(8)
Where vq is the molar volume of quartz (multiplication by 2 is because
fracture is filled bothways from the fracture centre)
Using the previous solution (stationary condition)( eq 6)
For Da<<1
Characteristic time for dissolution and transport process in the host rock is much longer
than the characteristic time for precipitation in the fracture when Da>>1. The
cementation rate in this regime taking Da+1=Da
Using the definition of Da (lp/ld) as previously given,
We can also find out the dissolution rate for values of Da with D and kp known by using
the equation previously derived (eq 5).