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Dynamic topography, phase boundary topography and latent-heat release Bernhard Steinberger Center for Geodynamics, NGU, Trondheim, Norway

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Prediction of surface uplift and subsidence over time on a large scale is one of the most important outcomes of mantle flow models

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Dynamic topography influences which regions are below sea level, and at what depth, and therefore where sediments and related natural resources may form Before attempting to compute uplift and subsidence in the geologic past, we must first understand present-day dynamic topography Present-day topography

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Dynamic topography influences which regions are below sea level, and at what depth, and therefore where sediments and related natural resources may form Before attempting to compute uplift and subsidence in the geologic past, we must first understand present-day dynamic topography Present-day topography m

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Dynamic topography influences which regions are below sea level, and at what depth, and therefore where sediments and related natural resources may form Before attempting to compute uplift and subsidence in the geologic past, we must first understand present-day dynamic topography Present-day topography minus 200 m

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Actual topography Spherical harmonic expansion of observed topography to degree 31 What to compare computations to for present-day

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Actual topography MINUS Isostatic topography Computed based on densities and thicknesses of crustal layers in CRUST 2.0 model (Laske, Masters and Reif)

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Actual topography MINUS Isostatic topography Non-isostatic topography =

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MINUS Thermal topography Computed from the age_2.0 ocean floor age grid (Müller, Gaina, Sdrolias and Heine, 2005) for ages < 100 Ma

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Non-isostatic topography residual topography MINUS Thermal topography =

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residual topography, l=1-31

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Values above sea level multiplied with factor 1.45, because dynamic topography is computed for global seawater coverage

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residual topography, l=1-12, above sea level mulitiplied with 1.45 residual topography, l=1-31 Above sea level multiplied with 1.45

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residual topography, l=1-12 RMS amplitude 0.52 km

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residual topography, l=1-12, our model RMS amplitude 0.52 km Model by Panasyuk and Hager (2000) RMS amplitude 0.52 km Correlation coefficient 0.74

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residual topography, l=1-12, our model RMS amplitude 0.52 km Model by Kaban et al. (2003) RMS amplitude 0.64 km Correlation coefficient 0.86

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Positive Clapeyron slope

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Radial stress kernels K r,l (z) describe how much a density anomaly lm at a depth z contributes to dynamic topography: Computed for global water coverage: s = 2280 kg/m 3 Figure from Steinberger, Marquart and Schmeling (2001) l=2 l=31 l=2 l=31 l=2 l=31 l=2 l=31 K r,l (z)

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Densities inferred from S-wave tomography -- here: model S20RTS (Ritsema et al., 2000) Conversion factor ~ 0.25 (Steinberger and Calderwood, 2006) – 4 % velocity variation ~ ~ 1 % density variation Depth 300 km

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Densities inferred from S-wave tomography -- here: model S20RTS (Ritsema et al., 2000) Disregard velocity anomalies above 220 km depth Depth 200 km

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Dynamic topography Spectral method (Hager and O’Connell, 1979,1981) for computation of flow and stresses NUVEL plate motions for surface boundary condition (results remain similar with free-slip and no-slip surface) Radial viscosity variation only RMS amplitude 1.07 km With other tomography models: 0.63 km [Grand] to 1.47 km [SB4L18, Masters et al., 2000] Viscosity profile from Steinberger and Calderwood (2006)

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Dynamic topography RMS amplitude 1.07 km With other tomography models: 0.63 to 1.47 km Correlation 0.33 With other tomography models: 0.30 to 0.53 Residual topography RMS amplitude 0.52 km Other models: 0.47 to 0.64 km

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Predicted “410” topography Thermal effect only RMS amplitude 4.81 km With other tomography models: 2.85 to 7.43 km

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Predicted “410” topography Thermal effect only RMS amplitude 4.81 km With other tomography models: 2.85 to 7.43 km Observed “410” topography Gu, Dziewonski, Ekström (2003) RMS amplitude 5.24 km Other models: 3.90 to 5.24 km Correlation between different ”observed” models 0.10 to 0.44 Correlation 0.37 With computation based on other tomography models: 0.27 to 0.42

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Predicted “660” topography Thermal effect only RMS amplitude 4.57 km With other tomography models: 2.69 to 5.59 km Observed “660” topography Gu, Dziewonski, Ekstrøm (2003) RMS amplitude 7.31 km Other models: 6.98 to 7.31 km Correlation between different “ observed” models 0.33 to 0.50 Correlation 0.35 With computation based on other tomography models: 0.06 to 0.35 Correlation with “410”: (-0.21 to with other models) Correlation with “410”: 0.24 (0.24 to 0.49 with other models)

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Predicted TZ thickness variation Thermal effect only RMS amplitude 8.89 km With other tomography models: 5.05 to km Observed TZ thickness variation Gu, Dziewonski, Ekstrøm (2003) RMS amplitude 7.92 km Other models: 6.52 to 7.92 km Correlation between different “observed” models 0.30 to 0.41 Correlation 0.51 With computation based on other tomography models: 0.36 to 0.51

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Dynamic topography – correlation with predicted TZ thickness variation –0.77 With other tomography models: to –0.89 Residual topography - correlation with observed TZ thickness variation –0.17 Other models: to 0.02

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Summary of results with thermal effect only:

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Predicted dynamic topography bigger than observed

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Summary of results with thermal effect only: Predicted dynamic topography bigger than observed Predicted topography “660” smaller than observed

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Summary of results with thermal effect only: Predicted dynamic topography bigger than observed Predicted topography “660” smaller than observed “410” and “660” topography correlation predicted negative, observed positive

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Summary of results with thermal effect only: Predicted dynamic topography bigger than observed Predicted topography “660” smaller than observed “410” and “660” topography correlation predicted negative, observed positive TZ thickness and dyn. topography correlation predicted negative, obs. ~ zero

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Summary of results with thermal effect only: Predicted dynamic topography bigger than observed Predicted topography “660” smaller than observed “410” and “660” topography correlation predicted negative, observed positive TZ thickness and dyn. topography correlation predicted negative, obs. ~ zero Correlations between predicted and observed models not too good

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410 km: Phase boundary with positive Clapeyron slope Latent heat causes HIGHER temperature BELOW Phase boundary topography by latent heat effects (Christensen, 1998, EPSL) 660 km: Phase boundary with negative Clapeyron slope Latent heat causes LOWER temperature BELOW In both cases: Temperature gradient on upstream side Constant temperature on downstream side Boundary displaced in direction of flow

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410 km: Phase boundary with positive Clapeyron slope Latent heat causes HIGHER temperature BELOW 660 km: Phase boundary with negative Clapeyron slope Latent heat causes LOWER temperature BELOW In both cases: Temperature gradient on upstream side Constant temperature on downstream side Boundary displaced in direction of flow Phase boundary topography by latent heat effects (Christensen, 1998, EPSL) L Q = g c p ) = 3.8 km c p = specific heat capacity L Q = 4.4 km

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For divariant phase change, amount of displacement depends on flow speed 410 km 660 km

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For divariant phase change, amount of displacement depends on flow speed 410 km 660 km V= Z=

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Computed flow speed – Depth 410 km Computed flow speed – Depth 660 km Density model inferred from S20RTS (Ritsema et al., 2000)

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depth 660 km Phase boundary displacement due to latent heat– depth 410 km

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“660” phase boundary displacement Thermal effect Latent heat effect Predicted topography “660” smaller than observed Increases by including latent heat effect (but not enough – note different scale!)

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depth 660 km Phase boundary displacement due to latent heat– depth 410 km “410” and “660” topography correlation predicted negative, observed positive Latent heat effect displaces phase boundaries in same direction and hence contributes towards less negative correlation (but not enough – note different scale!)

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depth 660 km Phase boundary displacement due to latent heat – depth 410 km Effect of latent heat effect on dynamic topography

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Dynamic topography with thermal effect only Computed dynamic topography bigger than observed Including latent heat effect reduces dynamic topography (note opposite sense of color scale! - but not enough – note different scale)

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Residual topography RMS 0.52 km Computed dynamic topography bigger than observed Including latent heat effect reduces dynamic topography Including latent heat effect generally somewhat increases correlations (but not by much) Correlation 0.34 Dynamic topography with computed phase boundaries RMS 1.02 km

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Residual topography -- RMS 0.52 km Including latent heat effect generally somewhat increases correlations (but not by much) Replacing computed by observed phase boundary topography in the calculation of dynamic topography generally does not improve results Correlation 0.34 Dynamic topography with computed phase boundaries -- RMS 1.02 km Dynamic topography with observed phase boundaries -- RMS 0.98 km Correlation 0.26

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Combine dynamic topography with sea level curve to compute inundation

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Heine et al., in preparation Present-day

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64 Ma

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41 Ma

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31 Ma

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13 Ma

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8 Ma

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3 Ma

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Dynamic topography on New Jersey Margin

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Outlook: Understanding of present-day dynamic topography A multi-disciplinary approach is required, including, but not limited to the following aspects Improving both seismic and geodynamic models of phase boundary topography Improving mantle density models, in particular in the lithosphere More realistic and laterally variable rheology, in particular in the lithosphere Regional computations

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Outlook II: Time-dependent dynamic topography and plate motions Past mantle structure cannot be fully recovered by simple backward- advection A global mantle reference frame through geologic times is required to relate computed uplift and subsidence to geological observations

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