summerschool modelling of mass and energy transport
TRANSCRIPT
Summerschool
Modelling of Mass and Energy Transport
Black Box Analogy
)(teRidt
diL
i: current, e(t): input voltage.
Characteristic Volume
Material Mix
Storage Capacity - Porosity
Grainsize, Ordering, Secundary Processes
Internal Structure
Anisotropy + Secondary Pathways
Mass and Energy Transport
ExerciseGiven a flux vector approaching an oblique oriented surface element (line) of your choice. Separate it graphically into the flux components
parallel and oblique to the surface
Normal Vector and FluxesThe normal is perpendicular to the surface.
The normal vector points to the outside of the closed are.The closed area is always surrounded anticlockwise.
)1,0(),1,0(),0,1(),0,1( in
),0(),,0(),0,(),0,( aaaavi The fluxes for the left case are
iiiWithin Lnvchange
S
Within dsnvchang
or
Fluxes Derived from a Potential
0
0
0
0
gradj
gradv
change = iii Lngrad
)( iii Lngrad
)(=
change= S
dsngrad
)( = S
dsngrad
)(
.
Gauss Theorem
SV
dsnvdVv
Green‘s Formulae,,, vuorHWGVFU
HGF ,,,
G G S
dsnvvdgdgv )(are functions of (x,y,z),
In case the vector v(F,G,H) is the gradient of a scalar field
vdsndgdg
G G S
*)()()(2 .constc
G S
dsndg *)(2
.
Mass and Energy Balance Continued
V S
dsnvudVdt
d
V S
dsnvdVt
u
0))((
dVvdivt
u
V
In this case there is no gain or loss within the control volume
Gain or loss within the control volume
VV V
dVvdivQdVdVt
u)(
0))((
dVQvdivt
u
V
Key QuestionUnder which conditions will the equality in the equations
0))((
dVvdivt
u
V
and
0))((
dVQvdivt
u
V
hold, independent of the size of the control volume?
Remark
V S
dsnvdVQt
u )(
The equation
where Q may be zero, provides a weak formulation of the problem to solve transport processes. For that purpose subdivide the area under consideration into aerial subsets, by example triangles as illustrated in the sketch
Then we can evaluate the volume integral by using the Gauss theorem and we can formally evaluate the fluxes through the bounding lines or surfaces:
FV-Method
The Differential Equation
If the flux is derived from a potential
0)(
Qvdivt
u 0 Qvut
or
0)(
Qgraddivt
uor 02 Qut
Without temporal change within the black box
02
Boundary and Initial Conditions
1st kind or DIRICHLET’s condition: Find a harmonic solution for the interior of the considered area so that the solution ),,( zyx
)(sf
2nd kind or NEUMANN’s condition: Find a harmonic solution for the interior of the considered area so that the solution ),,( zyx
satisfies given values of the normal derivative )(sfn
3rd kind or mixed condition: Find a solution for the interior of the considered area so that the solution ),,( zyxsatisfies the equation
)(sfn
and
)0,,( 22 const
satisfies given values of
Exercises
1)Find (qualitatively) the solution for the 1-D problem 0
2
2
x
u
with u=a at x=0 and u=b at x=1.
2) What would be the solution over a square with values of u given at the four corner points?
3) How can the boundary condition 0n
u be interpreted (2 possibilities).
4) Consider a well located within a homogeneous aquifer with free surface. The well has diameter r and you are pumping continuously Q [m3 ] water. The free water surface within the well than will have dropped to height H. Through the surface area of the well water will flow v [m/s]which is proportional
to the slope of the free water surface or x
yKv
with y the height of the free water surface. At the boundary of the wellthe water level in the aquifer will be equal to the free water level within the well. Derive the differential equation, the required boundaryconditions and the solution. Sketch the solution.
Solution Exercise 4
Through any cylindrical surface area xy2
surrounding the well we have the flux sec]/[mv
and the total flux becomes xyvQ 2
.
By experience, the flux is dxcdyv /
We find the differential equation '2 cxyyQ
With the boundary conditions y=H for x=r
Solution: ))(/()/ln( 22 HyQcrx
'2 cxyyQ Differential equation:
For rx and Hy for rx
Fick‘s 1st law
CDjc
D is mostly given as the diffusion coefficent in pure water. Provide an estimate for porous media.
The flux is related to the temporal change by
)( CDt
C
Or if chemical reactions are involved within the porous medium
)( CDQt
C
Heat conductionTjT
The change of energy within the control volume becomes
)( Tt
Tc
Or if sources or sinks are vailable (chemical reactions, radioactive heat production)
)( TQt
Tc
Observe that )(Tcc and )(T
,
and that the specific volume
will also depend on the temperature. In detail the size of the control volume changes
[J/s]
Exercises
1) Linearize the equation )( Tt
Tc
by partially differentiating the time derivative with respect to the parameters, observing that c=c(T) and )(T
.
2) Consider the heat flow from the interior of the earth which mostly is considered stationary, i.e. it is governed by the equation 0)( T QT )(
At the surface an average thermal gradient of 30°C is observed. At about 100 km depth the boundary between the lithosphere and the astenosphere is reached, the latter behaves like a fluid due to seismological data, the temperature at this boundary is approximately 1300°C, due to experiments.
a) Compute the expected temperature at the base of the lithosphere based on the average surface gradient.
b) Compute the expected temperature gradient throughout the lithosphere, based on a surface temperature of 0°C.
c) Discuss for a layered crust qualitatively how the thermal conductivity should vary with depth.
d) Determine for a homogenous lithosphere the heat production required to fit the boundary conditions
or
Darcy‘s Law
)(
gpk
qM
[kg m/s]
)( zgpKqD
[m/s]
)(* hKqh
or
l
hKqh
*
or´ )/( zpKqD
[m/s]
))((
gpk
Qt
))(( hg
k
t
hS
Coupled equations
0)())((
CQqCCD
t
C
0)())((
Tff
bb QqTcTt
Tc
0
f
f Qqt
)(
gpk
q
),,( cQTp
D=D(T)
),,( cbb QTpcc
),,( cff QTpcc
),,( fff QTp
),,,( cfbb QQTp
)(T
).,( iQTpk
Mathematical formulation of the thermohaline flow problem in FEFLOW
0 BoussinesqS +div( )t
Q
q
0
0
( ) f f
f
q K grad
+div div ( ) C
CC C Q
t
q Dgrad
(1 ) +div( ) div ( ) Tf f s s f fc c T c T T Q
t
q λgrad
0
( , )f
f
g
C T
k
Κ
0 0 0 00
1 ( , )( ) ( , )( ) ( )f f
sat
T p T T T p p p C CC C
f
ffsat
0
0
Stability criteria
TdK
RaT
Solutal Rayleigh number
Thermal Rayleigh number
d
sats D
CdKCC
Ra
0
The solutal and thermal Rayleigh numbers are related by
Ts RaLeNRa
Buoyancy ratio (Turner) T
CCC
N sat
0
Lewis number dD
Le
24 sTC RaRaRa
CRa
• The monotonic instability (or stationary convection) boundary is a • straight line defined by
is the critical Rayleigh number.
.
The region delimited by 24 sT RaRa
is a stable regime characterized by pure conduction and no convection.
In a range between 3002404 2 sT RaRasteady state convective cells develop
For 2csT RaRaRa the convection regime is unstable
Cross section through the Büsum diapir and adjacent rim synclines with temperature isolines (left) and vitrinite reflectance isolines (right)
Type of large-scale gw flow
Type of thermohaline flow
Thermally induced brine plumes developping on a deep salt sheet
Brine lenses, gravitational convection from a shallow salt sheet
Dasehd lines: isotherms (°C)
Thermohaline flow in the NE German BasinStratigraphic units
Thermohaline flow: Zoom salt dome
Mixed convection in the NE German Basin
Bold vectors represent the topography-driven flow (i.e. regional flow)
Thermal convection in a shallow salt dome
Thermohaline flow in a shallow salt dome
Dashed lines: isotherms (°C)