LDR   03650nam^^22004453a^4500
001        FI15062163_00001
005        20150731113408.0
006        m^^^^^o^^d^^^^^^^^
007        cr^^n^---ma^mp
008        150731n^^^^^^^^xx^||||^o^^^^^|||^u^eng^d
245 00 |a Geodetic measurements of vertical crustal velocity in West Antarctica and the implications for ice mass balance |h [electronic resource] |y English.
260        |a [S.l.] : |b American Geophysical Union, |c 2009.
490        |a Geochemistry Geophysics Geosystems Volume 10 Number 10.
506        |a Please contact the owning institution for licensing and permissions. It is the user's responsibility to ensure use does not violate any third party rights.
520 3    |a The GRACE satellite mission, which measures temporal changes in Earth’s gravity field, can infer near-surface mass changes with unprecedented precision, but in Antarctica (as in Greenland) these estimates are unusually ambiguous, because GRACE cannot distinguish between changes in ice mass and nearby changes in rock mass associated with postglacial rebound (PGR) [Le Meur and Huybrechts, 2001; Velicogna and Wahr, 2002]. Therefore, numerical models of PGR are used during or after the analysis of GRACE observations to account for the viscous influx of rock mass into the study area, and thereby isolate the changes in ice mass [Velicogna and Wahr, 2006; Chen et al., 2006; Ramillien et al., 2006, Sasgen et al., 2007a]. Over much of Antarctica, this ‘‘PGR correction’’ is larger than the resulting estimate of ice mass change, sometimes much larger [Velicogna and Wahr, 2006]. This vulnerability is worrying because there are many disparate predictions for contemporary uplift rates in Antarctica, and little really firm basis for choosing between them. For example, we contrast the predictions of PGR models ICE-5G (VM2) [Peltier, 2004] and IJ05 (6A) [Ivins and James, 2005, see Figure 6A] in Figure 1. These disagreements are not surprising, since PGR models are based on (1) an ice history model and (2) a geomechanical model (parameterized in terms of the thickness of the lithosphere, the underlying mantle viscosity structure, etc.), neither of which are strongly constrained by observations. Indeed, because PGR beneath and adjacent to an actively evolving ice sheet is sensitive to the details of crustal and mantle rheology, and these details are not known with the necessary level of accuracy, many theorists produce suites of PGR predictions by combining a single ice history model with a set of geomechanical scenarios [Ivins and James, 2005; Wang et al., 2008]. Predictions of PGR can be improved by reducing the underlying uncertainties in rock rheology (e.g., using seismology) and ice history (e.g., using glacial geomorphology and stratigraphy). They can also be tested and improved by utilizing geodetic observations of crustal motion [Milne et al., 2004], which is our approach.
533        |a Electronic reproduction. |c Florida International University, |d 2015. |f (dpSobek) |n Mode of access: World Wide Web. |n System requirements: Internet connectivity; Web browser software.
650    0 |a Climate Change.
650    0 |a Ice Sheets.
650    0 |a Geodesy.
651    0 |a Antarctica.
700 1    |a Bevis, Michael.
700 1    |a Kendrick, Eric.
700 1    |a Smalley, Robert Jr..
700 1    |a Dalziel, Ian.
700 1    |a Caccamise, Dana.
700 1    |a Sasgen, Ingo.
700 1    |a Helsen, Michiel.
700 1    |a Taylor, F.W..
700 1    |a Zhou, Hao.
700 1    |a Brown, Abel.
700 1    |a Raleigh, David.
700 1    |a Willis, Michael.
700 1    |a Wilson, Terry.
700 1    |a Konfal, Stephanie.
830    0 |a dpSobek.
830    0 |a Sea Level Rise.
852        |a dpSobek |c Sea Level Rise
856 40 |u http://dpanther.fiu.edu/dpService/dpPurlService/purl/FI15062163/00001 |y Click here for full text
992 04 |a http://dpanther.fiu.edu/sobek/content/FI/15/06/21/63/00001/FI15062163_thm.jpg
997        |a Sea Level Rise


The record above was auto-generated from the METS file.