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VISCOUS HEATING in the Earth‘s Mantle Induced by Glacial Loading

VISCOUS HEATING in the Earth‘s Mantle Induced by Glacial Loading.

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VISCOUS HEATING in the Earth‘s Mantle Induced by Glacial Loading

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  1. VISCOUS HEATINGin the Earth‘s MantleInduced by Glacial Loading L. Hanyk1, C. Matyska1, D. A. Yuen2 and B. J. Kadlec21Department of Geophysics, Faculty of Mathematics and Physics, Charles University in Prague, Czech Republic2Department of Geology and Geophysics, University of Minnesota, Minneapolis, USA

  2. IDEAHow efficient can be the shear heating in the Earth’s mantle due to glacial forcing, i.e., internal energy source with exogenic origin?(“energy pumping into the Earth’s mantle”)APPROACH• to evaluate viscous heating in the mantle during a glacial cycle by Maxwell viscoelastic modeling • to compare this heating with background radiogenic heating• to make a guess on the magnitude of surface heat flow below the areas of glaciation

  3. PHYSICAL MODEL• a prestressed selfgravitating spherically symmetric Earth• Maxwell viscoelastic rheology• arbitrarily stratified density, elastic parameters and viscosity• both compressible and incompressible models• cyclic loading and unloading

  4. MATHEMATICAL MODEL• momentum equation & Poisson equation• Maxwell constitutive relation• boundary and interface conditions • formulation in the time domain (not in the Laplace domain)• spherical harmonic decomposition• a set of partial differential equations in time and radial direction• discretization in the radial direction • a set of ordinary differential equations in time• initial value problem

  5. NUMERICAL IMPLEMENTATION• method of lines (discretization of PDEs in spatial directions)• high-order pseudospectral discretization• staggered Chebyshev grids• multidomain discretization• ‘almost block diagonal’ (ABD) matrices (solvers in NAG)• numerically stiff initial value problem (Rosenbrock-Runge-Kutta scheme in Numerical Recipes)

  6. DISSIPATIVE HEATING φ(r ) In calculating viscous dissipation, we are not interested in the volumetric deformations as they are purely elastic in our models and no heat is thus dissipated during volumetric changes. Therefore we have focussed only on the shear deformations. The Maxwellian constitutive relation (Peltier, 1974) rearranged for the shear deformations takes the form ∂ τS / ∂ t = 2 μ ∂ eS / ∂ t – μ / ητS , τS = τ – K div uI , eS = e – ⅓ div uI , where τ, e and Iare the stress, deformation and identity tensors, respectively, and u is the displacement vector. This equation can be rewritten as the sum of elastic and viscous contributions to the total deformation, ∂ eS / ∂ t = 1 / (2 μ)∂ τS / ∂ t + τS / (2η) = ∂ eSel / ∂ t + ∂ eSvis / ∂ t . The rate of mechanical energy dissipation φ (cf. Joseph, 1990, p. 50) is then φ = τS : ∂ eSvis / ∂ t = (τS : τS) / (2η) .

  7. EARTH MODELS M1 . . . . . . . . PREM isoviscous mantle elastic lithosphere M2 . . . . . . . . PREM LM viscosity hill elastic lithosphere M3 . . . . . . . . PREM LM viscosity hill low-viscosity zone elastic lithosphere

  8. SHAPE OF THE LOAD parabolic cross-sections radius 15 max. height 3500 m

  9. LOADING HISTORIES L1 . . . . . . . . . . . . . glacial cycle 100 kyr linear unloading 100 yr L2 . . . . . . . . . . . . . glacial cycle 100 kyr linear unloading 1 kyr L3 . . . . . . . . . . . . . glacial cycle 100 kyr linear unloading 10 kyr

  10. DISSIPATIVE HEATING φ(r ) Earth model M1 (isoviscous) Loading History L1 (100 yr) L2 (1 kyr) L3 (10 kyr)

  11. DISSIPATIVE HEATING φ(r ) Earth Model M1 Loading History L1

  12. DISSIPATIVE HEATING φ(r ) Earth model M2 (LM viscosity hill) Loading History L1 (100 yr) L2 (1 kyr) L3 (10 kyr)

  13. DISSIPATIVE HEATING φ(r ) Earth Model M2 Loading History L1

  14. DISSIPATIVE HEATING φ(r ) Earth model M3 (LM viscosity hill & LVZ) Loading History L1 (100 yr) L2 (1 kyr) L3 (10 kyr)

  15. DISSIPATIVE HEATING φ(r ) Earth Model M3 Loading History L1

  16. TIME EVOLUTION OF MAX LOCAL HEATING maxrφ(t) normalized by the chondritic radiogenic heating of 3x10-9 W/m3 M1 ► Earth Model M2 ► Loading histories L1 ... solid lines L2 ... dashed lines L3 ... dotted lines M3 ►

  17. EQUIVALENT MANTLE HEAT FLOW qm(θ) peak values time averages [mW/m2] [mW/m2] M1 ► Earth Model M2 ► Loading histories L1 ... solid lines L2 ... dashed lines L3 ... dotted lines M3 ►

  18. CONCLUSIONS• explored (for the first time ever) the magnitude of viscous dissipation in the mantle induced by glacial forcing• peak values 10-100 higher than chondritic radiogenic heating (below the center and/or edges of the glacier of 15 radius)• focusing of energy into the low-viscosity zone, if present• magnitude of the equivalent mantle heat flow at the surface up to mW/m2 after averaging over the glacial cycle • extreme sensitivity to the choice of the time-forcing function (equivalent mantle heat flow more than 10 times higher)

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