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GRACE constraints on Earth rheology of the Barents Sea and Fennoscandia
Rovira-Navarro, M.; van der Wal, W.; Barletta, V.R.; Root, B.C.; Sandberg Sørensen, L. (2020). GRACE constraints on Earth rheology of the Barents Sea and Fennoscandia. Solid Earth 11(2): 379-395. https://dx.doi.org/10.5194/se-11-379-2020

Bijhorende info:
In: Solid Earth. COPERNICUS GESELLSCHAFT MBH: Gottingen. ISSN 1869-9510; e-ISSN 1869-9529, meer
Peer reviewed article  

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  • Rovira-Navarro, M., meer
  • van der Wal, W.
  • Barletta, V.R.
  • Root, B.C.
  • Sandberg Sørensen, L.

Abstract
    The Barents Sea is situated on a continental margin and was home to a large ice sheet at the Last Glacial Maximum. Studying the solid Earth response to the removal of this ice sheet (glacial isostatic adjustment; GIA) can give insight into the subsurface rheology of this region. However, because the region is currently covered by ocean, uplift measurements from the center of the former ice sheet are not available. The Gravity Recovery and Climate Experiment (GRACE) gravity data have been shown to be able to constrain GIA. Here we analyze GRACE data for the period 2003–2015 in the Barents Sea and use the data to constrain GIA models for the region. We study the effect of uncertainty in non-tidal ocean mass models that are used to correct GRACE data and find that it should be taken into account when studying solid Earth signals in oceanic areas from GRACE. We compare GRACE-derived gravity disturbance rates with GIA model predictions for different ice deglaciation chronologies of the last glacial cycle and find that best-fitting models have an upper mantle viscosity equal or higher than 3×1020 Pa s. Following a similar procedure for Fennoscandia we find that the preferred upper mantle viscosity there is a factor 2 larger than in the Barents Sea for a range of lithospheric thickness values. This factor is shown to be consistent with the ratio of viscosities derived for both regions from global seismic models. The viscosity difference can serve as constraint for geodynamic models of the area.

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