thermodynamics of glaciers 1 / 34...thermodynamics of glaciers mccarthy summer school, june 2010...
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Thermodynamics of GlaciersMcCarthy Summer School, June 2010
Andy Aschwanden
Arctic Region Supercomputing CenterUniversity of Alaska Fairbanks, USA
McCarthy Summer School, June 2010
1 / 34
On Notation
I (hopefully) consistent with Continuum Mechanics (Truffer)I with lots of input from Luethi & Funk: Physics of Glaciers I lecture at
ETHI notation following Greve & Blatter: Dynamics of Ice Sheets and Ice
Sheets
Introduction 3 / 34
Types of Glaciers
cold glacierice below pressure melting point, no liquid water
temperate glacierice at pressure melting point, contains liquid water in theice matrix
polythermal glaciercold and temperate parts
Introduction 5 / 34
Why we care
The knowledge of the distribution of temperature in glaciers and ice sheetsis of high practical interest
I A temperature profile from a cold glacier contains information on pastclimate conditions.
I Ice deformation is strongly dependent on temperature (temperaturedependence of the rate factor A in Glen’s flow law);
I The routing of meltwater through a glacier is affected by icetemperature. Cold ice is essentially impermeable, except for discretecracks and channels.
I If the temperature at the ice-bed contact is at the pressure meltingtemperature the glacier can slide over the base.
I Wave velocities of radio and seismic signals are temperaturedependent. This affects the interpretation of ice depth soundings.
Introduction 6 / 34
Energy balance: depicted
QE QH
R
Qgeo
P
surface energy balance
strain heating
fricitional heating
geothermal heatfirn + near surface layer
latent heat sources/sinks
Energy balance 8 / 34
Energy balance: equation
ρ
(∂u∂t + v · ∇u
)= −∇ · q + Q
ρ ice densityu internal energyv velocityq heat fluxQ dissipation power
(strain heating)Noteworthy
I strictly speaking, internal energy is not a conserved quantityI only the sum of internal energy and kinetic energy is a conserved
quantity
Energy balance 9 / 34
Temperature equation
Temperature equation
I ice is cold if a change in heat content leads to a change intemperature alone
I independent variable: temperature T = c(T )−1u
ρc(T )
(∂T∂t + v · ∇T
)= −∇ · q + Q
Fourier-type sensible heat flux
q = qs = −k(T )∇T
c(T ) heat capacityk(T ) thermal conductivity
Cold Ice Equation 11 / 34
Thermal properties
−50 −40 −30 −20 −10 0
1800
1900
2000
2100
temperature θ [° C]
c [J
kg−
1 K−
1 ]
heat capacity is amonotonically-increasingfunction of temperature
−50 −40 −30 −20 −10 0
2.2
2.4
2.6
temperature θ [° C]
k [W
m−
1 K−
1 ]
thermal conductivity is amonotonically-decreasing function oftemperature
Cold Ice Thermal properties 12 / 34
Flow law
Viscosity η is a function of effective strain rate de andtemperature T
η = η(T , de) = 1/2B(T )d (1−n)/ne
where B = A(T )−1/n depends exponentially on T
Cold Ice Flow law 13 / 34
Ice temperatures close to the glacier surface
Assumptions
I only the top-most 15m experience seasonal changesI heat diffusion is dominant
We then get∂T∂t = κ
∂2T∂h2
where h is depth below the surface, and κ = k/(ρc) is thethermal diffusivity of ice
Cold Ice Examples 14 / 34
Ice temperatures close to the glacier surface
Boundary Conditions
T (0, t) = T0 + ∆T0 · sin(ωt) ,
T (∞, t) = T0 .
T0 mean surface temperature∆T0 amplitude2π/ω frequency
Cold Ice Examples 15 / 34
Ice temperatures close to the glacier surface
h
0
T0
t
T
ΔT0
φ(h)
Cold Ice Examples 16 / 34
Ice temperatures close to the glacier surface
Analytical Solution
T (h, t) = T0 + ∆T0 exp(−h√ω
2κ
)
︸ ︷︷ ︸∆T (h)
sin(ωt − h
√ω
2κ︸ ︷︷ ︸ϕ(h)
).
∆T (h) amplitude variation with depth
Cold Ice Examples 17 / 34
Ice temperatures close to ice divides
Assumptions
I only vertical advection and diffusionWe then get
κ∂2T∂z2 = w(z)
∂T∂z
where w is the vertical velocity
Analytical solution
I can be obtained
Cold Ice Examples 18 / 34
Cold Glaciers
I Dry Valleys, AntarcticaI (very) high altitudes at lower latitudes
Cold Ice Examples 19 / 34
Water content equation
Water content equation
I Ice is temperate if a change in heat content leads to achange in water content alone
I independent variable: water content (aka moisturecontent, liquid water fraction) ω = L−1u
ρL(∂ω
∂t + v · ∇ω)
= −∇ · q + Q
⇒ in temperate ice, water content plays the role of temperature
Temperate Ice Equation 21 / 34
Flow law
Flow LawViscosity η is a function of effective strain rate de and watercontent ω
η = η(ω, de) = 1/2B(ω)d (1−n)/ne
where B depends linearly on ωI but only very few studies (e.g. from Lliboutry and Duval)
Latent heat flux
q = ql =
{Fick-typeDarcy-type
⇒ leads to different mixture theories (Class I, Class II, Class III)
Temperate Ice Flow law 22 / 34
Sources for liquid water in temperate Ice
. .. .. .. .. .. .. . .. .. .. . ... . . . ...
bedrocktemperate ice
firncold ice
. ... . mWS microscoptic water systemMWS macroscoptic water system
mWS
waterinclusionb
temperate ice
cold-dry icecWS
C SMT
a
1. water trapped in the ice as water-filled pores2. water entering the glacier through cracks and crevasses at the ice surface in
the ablation area3. changes in the pressure melting point due to changes in lithostatic pressure4. melting due energy dissipation by internal friction (strain heating)
Temperate Ice Flow law 23 / 34
Temperature and water content of temperate ice
Temperature
Tm = Ttp − γ (p − ptp) , (1)
I Ttp = 273.16K triple point temperature of waterI ptp = 611.73Pa triple point pressure of waterI Temperature follows the pressure field
Water contentI generally between 0 and 3%
I water contents up to 9% found
Temperate Ice Flow law 24 / 34
Temperate Glaciers
Temperate glaciers are widespread, e.g.:I Alps, Andes, Alaska,I Rocky Mountains, tropical glaciers, Himalaya
Temperate Ice Flow law 25 / 34
Polythermal glaciers
temperate cold
a) b)
I contains both cold and temperate iceI separated by the cold-temperate transition surface (CTS)I CTS is an internal free surface of discontinuity where
phase changes may occurI polythermal glaciers, but not polythermal ice
Polythermal Glaciers 27 / 34
Scandinavian-type thermal structure
temperate cold
a) b)
I ScandinaviaI SvalbardI Rocky MountainsI AlaskaI Antarctic Peninsula
Polythermal Glaciers Thermal Structures 28 / 34
Scandinavian-type thermal structure
Why is the surface layer in the ablation area cold? Isn’t thiscounter-intuitive?
temperate cold firn meltwater
Polythermal Glaciers Thermal Structures 29 / 34
Canadian-type thermal structure
temperate cold
a) b)
I high Arctic latitudes in CanadaI AlaskaI both ice sheets Greenland and Antartica
Polythermal Glaciers Thermal Structures 30 / 34
Thermodyamics in ice sheet models
I only few glaciers are completely coldI most ice sheet models are so-called cold-ice method modelsI so far two polythermal ice sheet models
ρc(T )
(∂T∂t + v · ∇T
)= ∇ · k∇T + Q
ρ L(∂ω
∂t + v · ∇ω)
= Q
or
ρ
(∂E∂t + v · ∇E
)= ∇ · ν∇E + Q
Ice Sheet Models 32 / 34
Thermodyamics in ice sheet models
Cold vs Polythermal for Greenland
I thinner temperate layerI but difference in total ice volume for steady-state run is < 1% (Greve,
1995)I SO WHAT?I better conservation of energyI temperate basal ice means ice is sliding at the baseI new areas may become temperate
Ice Sheet Models 33 / 34