unit 07 : advanced hydrogeology solute transport
TRANSCRIPT
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Unit 07 : Advanced Hydrogeology
Solute Transport
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Mass Transport Processes
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Advection
• Advection is mass transport due simply to the flow of the water in which the mass is carried.
• The direction and rate of transport coincide with that of the groundwater flow.
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Diffusion
• Diffusion is the process of mixing that occurs as a result of concentration gradients in porous media.
• Diffusion can occur when there is no hydraulic gradient driving flow and the pore water is static.
• Diffusion in groundwater systems is a very slow process.
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Dispersion
• Dispersion is the process of mechanical mixing that takes place in porous media as a result of the movement of fluids through the pore space.
• Hydrodynamic dispersion is a term used to include both diffusion and dispersion.
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Pure Advection
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Advection in Stream Tube
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Linear Advective Velocity
From Darcy’s Law:
v = q / ne = - (K / ne).dh/dx
where ne is the effective (or connected) porosity
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Fractured Rocks and Clays
• In fractured rocks, the effective porosity (ne) can be very small implying relatively high advective velocities.
• In clays and shales, effective porosity can also be very low and high advective velocities might be expected but there are other factors at work.
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Deviations from Advective Velocity
• Electrical charges on clay mineral surfaces can force anions to the centre of pores where velocities are highest.
• Anions can then travel faster than the advective velocity.
• Cations are attracted by the clay mineral surface charge and can be retarded (travel slower than the advective velocity).
• Bi-polar water molecules can similarly be retarded giving rise to osmotic and membrane filtration effects.
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Electrokinetic Effects
Distance AA’
Vel
oci
ty
A
A’
PoreClay
Clay
Clay Surface
Clay Surface
-
--- -
- - -
-
-
--- -
- - -
-
Pore
--
-
--
+
++
+
+
-
+Anion
Cation
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Dispersion Concepts
• Mechanical dispersion spreads mass within a porous medium in two ways:– Velocity differences
within pores on a microscopic scale.
– Path differences due to the tortuosity of the pore network.
Position in Pore
Ve
loci
ty
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Macroscopic Dispersion
• Random variations in velocity and tortuous paths through flow systems are created on a larger scale by lithological heterogeneity.
• Heterogeneity is responsible for macroscopic dispersion in flow systems
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Experimental Continuous Tracer
Time
C/C
o
0
1
Start
Time
C/C
o
0
1
Start
INFLOW A OUTFLOW B
A B
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Continuous Tracer Test
• First tracer C/Co > 0.0 arrives faster than advective velocity.
• Mean tracer arrival time C/Co = 0.5 corresponds to advective velocity.
• Last tracer C/Co = 1.0 travels slower than advective velocity.
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Continuous Tracer Transient
t = t1
t = t2
t = t3
C/Co = 0C/Co = 1
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Experimental Pulse Tracer
Time
C/C
o
0
1
Start
Time
C/C
o
0
1
Start
INFLOW A OUTFLOW B
A B
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Pulse Tracer Test
• The “box function” of the source is both delayed and attenuated by dispersion.
• The pulse peak arrival time corresponds to the advective velocity.
• The peak concentration C/Co is less than 1.0
• The breadth and height of the peak characterize the dispersivity of the porous medium.
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Pulse Tracer Transient
t = t1
t = t2
t = t3
C/Co = 0 C/Co = 0
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Pulse Zone of Dispersion
• The zone of dispersion broadens and the peak concentration C/Co reduces as it moves through the porous medium.
• Ahead of the zone C/Co = 0
• Behind the zone C/Co =0
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Transverse and Longitudinal Dispersion
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Diffusion Law
• Darcy’s law for relates fluid flux to hydraulic gradient:
q = -K.grad(h)
• For mass transport, there is a similar law (Fick’s law) relating solute flux to concentration gradient in a pure liquid:
J = -Dd.grad(C)where J is the chemical mass flux [moles. L-2T-1] C is concentration [moles.L-3]
Dd is the diffusion coefficient [L2T-1]
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Molecular Diffusion
• Molecular diffusion is mixing caused by random motion of solute molecules as a result of thermal kinetic energy.
• The diffusion coefficient in a porous medium is less than that in pure liquids because of collisions with the pore walls.
J = -Dd.[grad(nC) + / V] where V is a chemical averaging volume [moles-1L3], n is porosity and is the tortuosity of the porous medium.
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Fick’s Law for Sediments• This theoretical function, for practical
applications, has been simplified to :J = -D*d.n.grad(C)
where D*d is a bulk diffusion coefficient accounting for tortuosity
• This form of the function is known as Fick’s law for diffusion in sediments often written as:
J = -D’d.grad(C) = - u.n.Dd.grad(C)
where D’d is an effective diffusion coefficient , Dd is the self diffusion coefficient of the solute ion, n is porosity and u is a dimensionless factor < unity.
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Estimating D’d
• The factor u depends on the tortuosity of the medium and empirical values (Hellferich, 1966) lie between 0.25 and 0.50
• Bear (1972) suggest values between 0.56 and 0.80 based on a theoretical evaluation of granular media.
• Whatever the factor used, D’d increases with increasing porosity and decreases with increasing tortuosity = Le/L
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Dd for Common Ions
Cation Dd (10-10 m2/s) Anion Dd (10-10 m2/s)
H+ 93.1 OH- 52.7
K+ 19.6 Cl- 20.3
Na+ 13.3 HS- 17.3
HCO3- 11.8
Ca2+ 7.93 SO42- 10.7
Fe2+ 7.19 CO32- 9.55
Mg2+ 7.05
Fe3+ 6.07Typical factors to calculate D’d are 0.10 to 0.20 for granular materials
Notice that diffusion coefficients are smaller the higher the charge on the ion
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Mechanical Dispersion
• Mechanical dispersion is caused by local variations in the velocity field on scales ranging from microscopic through macroscopic to megascopic.
• Variations in hydraulic conductivity due to lithological heterogeneities are the main sources of velocity variations.
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Dispersion Coefficient
• The hydrodynamic dispersion coefficient (D) is a combination of mechanical dispersion (D’) and bulk diffusion (D’d):
D = D’ + D’d• The advective flow velocity (v) and mean grain
diameter (dm) have been shown to be the main controls on longitudinal dispersion (DL) parallel to the flow direction.
• Transverse dispersion (DT) also takes place normal to the flow direction.
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Peclet Number
• D/Dd is a convenient ratio that normalizes dispersion coefficients by dividing by the diffusion coefficient.
• v.dm /Dd is called the Peclet Number (NPE) a dimensionless number that expresses the advective to diffusive transport ratio.
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Empirical Data on Dispersion
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Transport Regimes
• For NPE < 0.02
diffusion dominates• For 0.02 > NPE < 8
diffusion and mechanical dispersion• For NPE > 8
mechanical dispersion dominates
Some authors place the boundaries at 0.01 and 4 rather than 0.02 and 8
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Velocity Proportionality
• For values of NPE > 8 the longitudinal (and transverse) dispersion coefficient (DL) is proportional to the advective velocity (v).
• This result has been generalized to describe dispersion both on microscopic and megascopic scales.
• Tranverse dispersion coefficients (DT) are typically around 0.1DL for NPE > 100 although values as low as 0.0 1DL have been reported.
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Dispersivity
• Dispersion coefficients may be written:
DL = L.v and DT = T.v
where L and T are called the dispersivities.
• Dispersivities have units of length and are characteristic properties of porous media.
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Dispersion and Scale• Most knowledge of dispersion has been gleaned
from experimental work at the microscopic scale.• A review of many dispersivity measurements
(Gelhar et al, 1992) gave values for L spanning almost six orders of magnitude.
• Microscopic scale dispersivities as a result of velocity changes on the pore scale are about two orders of magnitude smaller than macroscopic dispersivities arising from heterogeneity in hydraulic conductivity.
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Fickian Model
• Hydrodynamic dispersion occurs due to a combination of molecular diffusion and mechanical dispersion.
• A Fickian dispersion model implies that mass transport is proportional to the concentration gradient and in the direction of the concentration gradient (just like Fick’s law for diffusion).
• Using such a model, we treat dispersion in a way fully analogous to diffusion (even though the processes of diffusion and dispersion are quite different).
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Quantifying Dispersion
Recall that concentration (C) against position (x) after time (t) for a pulse source resembles the Gaussian distribution function.
For the Gaussian (normal) distribution is the standard deviation and measures the spread about the mean value.
About 95.4% of the area under the concentration graph (mass) lies between –2L and +2L.
To complete the analogy with dispersion, we find that L = (2DLt)1/2
-3 -2 -1 0 1 2 3 x/
C
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One-Dimensional Pulse
• The peak concentration for a pulse source travels at the advection velocity v = x / t.
DL = L2 / 2t = L
2.v / 2x
where v is the advective velocity and x is the distance travelled by the peak at time t.
• This provides a means to estimate DL from field or laboratory measurements of concentration (C) with position (x).
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Two-Dimensional Pulse
• Two-dimensional spread of a pulse tracer in a unidirectional flow field results in an elliptically shaped concentration plume with a Gaussian mass distribution.
C/C
o
to t2t1
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Three-Dimensional Pulse• 3D plumes are generally “cigar-shaped”• Typically, vertical transverse dispersion is
small and plumes have a “surfboard” shape• Pulse source plumes are symmetric about the
centroid.
• Continuous source plumes are assymmetric, broadening in direction of flow.
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Breakthrough Curvet = (t84 – t16) / 2
The value t2 is a temporal
variance measured in c-t space for the breakthrough curve. Previously we recognized L
2 as a spatial variance measure in c-x space.
Fortunately the two variances are simply related by the advective velocity: L
2 = v2 t2
DL = L2 / 2t = v2 t
2 / 2t
0.16
0.50
0.84
C /
Cm
ax
t16 t50 t84
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Spatial PlumeL = (x84 – x16) / 2
This may be a difficult to measure so the width of the peak at C / Cmax = 0.5 denoted by can be used.
L = / 1.665 (1D case)
For the 2D case, the peak width is divided by sqrt(2) so the standard deviation is given by:
L = / 2.345 (2D case)
(See Robbins, 1983)
0.16
0.50
0.84
C /
Cm
ax
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Fractured Media
• Assumptions:– Advection and
dispersion only occurs in the fracture network
– Diffusion from fractures to the matrix is possible
Matrix
Matrix
AdvectionDispersion
FractureDiffusion
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Mixing Processes in Fractures
• Mechanical mixing due to velocity variations within rough fractures
• Mixing at fracture intersections• Velocity variations between different fracture
sets• Diffusion between fractures and matrix may
be important because fractures localize mass and concentration gradients may be high
• Interactions of various processes can be complex
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Geostatistics
• Geostatistics allow spatial variability to be included in the analysis of flow and transport in porous media
• Important because heterogeneity is the at the root of macroscopic dispersion
• We use three statistical parameters: mean, variance and correlation length
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Geostatistical Parameters
• Mean (ym) measures central value:
y = yi / n
• Variance (2y) measures spread or scatter:
2y = (yi - y)2 / n
• Correlation length (y) measures spatial persistence:
y(b) = f(-|b| / y) = exp(-|b| / y)
where b is a distance sampling interval parameter called the lag
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Spatial Data
-3
0
3
0 50
-3
0
3
0 50
Stationary data series : mean independent of position
Data series with trend: mean changes with position
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Autocorrelated DataStationary autocorrelated data series
Autocorrelated data series with trend
-3
0
3
0 50
-3
0
3
0 50
The distance between peaks is the correlation length
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Correlogram
• When a data series is correlated with itself for various lags, the autocorrelation eventually approaches zero after a number of lags corresponding to
• The chart plotting correlation coefficient against lag is called a correlogram.
Lag
Co
rrel
atio
n 1
0
-1
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Variogram
• Geostatistical theory does not use the autocorrelation, but instead uses a related property called the semi-variance.
• The semi-variance is simply half the variance of the differences between all possible points spaced a constant distance apart.
• For a lag of zero, the semi-variance is thus zero.
• For large lags, the semi-variance approaches half the variance of the spatial dataset.
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Variogram TerminologyAt lags where spatial correlations exist, the data values are similar and the semivariance is low.
A variogram is like an upside down correlogram. Special terms describe the function:• sill corresponds to the semivariance of the dataset• range is a distance parameter similar to correlation length• nugget is the projected intercept on the semivariance axis for experimental data
Sem
ivar
ian
ce
Lag
Sill
Nugget
Range
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Hydraulic Conductivity Fields
• Many hydrogeologic parameters, particularly hydraulic conductivity, have spatial structure
• Procedures are available for generating spatial data with a particular , and
• These measures of heterogeneity can be used to predict dispersivity
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Geostatistical Estimation• Gelhar and Axness (1983) suggested:
AL = 2y / 2
where AL is called the asymptotic longitudinal dispersivity and y = ln(K) where K is hydraulic conductivity and is a flow factor (taken to be unity).
• AL accounts in a quantitative fashion for heterogeneity in the hydraulic conductivity field
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Geostatistical Model of Dispersion
Dispersivity is conceptually believed to have three components: diffusive mixing, pore scale mixing and mixing through spatial heterogeneities:
AL* = AL + L + Dd
* / v
This leads to an expression for hydrodynamic dispersion coefficient with the form:
DL = (AL + L).v + Dd*