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VISCOUS HEATING in the Earths Mantle Induced by Glacial Loading L. Hanyk 1, C. Matyska 1, D. A. Yuen 2 and B. J. Kadlec 2 1 Department of Geophysics, Faculty of Mathematics and Physics, Charles University in Prague, Czech Republic 2 Department of Geology and Geophysics, University of Minnesota, Minneapolis, USA

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IDEA How efficient can be the shear heating in the Earths mantle due to glacial forcing, i.e., internal energy source with exogenic origin? (energy pumping into the Earths 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

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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

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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

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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)

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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 τ S / t = 2 μ e S / t – μ / η τ S, τ S = τ – K div u I, e S = e – div u I, where τ, e and I are 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, e S / t = 1 / (2 μ) τ S / t + τ S / (2 η) = e S el / t + e S vis / t. The rate of mechanical energy dissipation φ (cf. Joseph, 1990, p. 50) is then φ = τ S : e S vis / t = (τ S : τ S ) / (2 η).

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EARTH MODELS M PREM isoviscous mantle elastic lithosphere M PREM LM viscosity hill elastic lithosphere M PREM LM viscosity hill low-viscosity zone elastic lithosphere

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SHAPE OF THE LOAD parabolic cross-sections radius15 max. height3500 m

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LOADING HISTORIES L glacial cycle 100 kyr linear unloading 100 yr L glacial cycle 100 kyr linear unloading 1 kyr L glacial cycle 100 kyr linear unloading 10 kyr

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

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Earth Model M1 Loading History L1

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

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

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

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

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

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EQUIVALENT MANTLE HEAT FLOW q m ( θ ) Loading histories L1...solid lines L2...dashed lines L3...dotted lines peak values time averages [mW/m 2 ] [mW/m 2 ] Earth Model M2 M3 M1

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CONCLUSIONS explored (for the first time ever) the magnitude of viscous dissipation in the mantle induced by glacial forcing peak values 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/m 2 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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