and direction, as well as air temperature, from the IMO operational surface station net-
work. Most anemometers are installed at 10 m above ground level (mAGL). However, at some
stations, surface winds are measured at different heights, h, varying between 4.0 and 18.3 m.
3This is done using a GRIB-API command on Parameter 141 (snow depth) in the earliest boundary
data file: grib_set -f -d 0.0 -w
/media/vedurstofan/utgafa/skyrslur/2014/VI_2014_005.pdf
in
Norway was provided by the Norwegian Water Resources and Energy Directorate (NVE).
TóJ 12 5.12.2009
Memo
References
Bahr, D. B., M. F. Meier and S. D. Peckham. 1997. The physical basis of glacier volume–area
scaling. J. Geophys. Res., 102(B9), 20,355–20,362.
Björnsson, H., and F. Pálsson. 2008. Icelandic glaciers. Jökull, 58, 365–386.
Fenger, J. (Ed.). 2007. Impacts of Climate Change on Renewable
/media/ces/ces-glacier-scaling-memo2009-01.pdf
and candidate situations is evaluated with
the Teweles-Wobus (S1) skill score (Wilks, 1995). The S1 score compares the shape of two fields
by considering their gradient at each grid point of the analogy domain:
S1(u) = 100
n 1
i=1
m
j=1
jDAi DFij+
n
i=1
m 1
j=1
jDA j DFjj
n 1i=1
m
j=1 Gi +
n
i=1
m 1
j=1 G j
(3)
with
DAi = A(i+1; j;u) A(i; j;u) (4)
DFi = F(i+1; j; t) F(i; j; t) (5)
DA j
/media/vedurstofan/utgafa/skyrslur/2014/VI_2014_006.pdf
Th. Árnadóttir, C. Völksen, W. Jiang, E. Sturkell, T. Villemin, P. Einarsson,
F. Sigmundsson, and R. Stefánsson (2006). Current plate movements across the Mid-
Atlantic Ridge determined from 5 years of continuous GPS measurements in Iceland. J.
Geophys. Res., 111, B09407, doi:10.1029/2005JB003717.
Guðmundsson, Á., S. Brynjólfsson (1993). Overlapping rift zone segments and the
evolution
/media/vedurstofan/utgafa/skyrslur/2009/VI_2009_013.pdf
longwave radiation and latent
heat losses, and small downward sensible heat fluxes. This excess energy then becomes available
for melting of surface snow.
The energy needed to melt a given mass of snow, ms, is given by
E = ms L f ; (1)
where L f = 334;000 J kg 1 is the latent heat of fusion. With an hourly change in snow water
equivalent due to melting, dDmelt, the amount of energy absorbed
/media/vedurstofan/utgafa/skyrslur/2015/VI_2015_006.pdf
& Ólafsson, H. (2010). Validation of numerical simulations of precipitation in complex terrain at high temporal resolution. Hydrology Research, 41 (3-4), 164-170.
Christensen, J.H., Boberg, F., Christensen, O.B. & Lucas-Picher, P. (2008), On the need for bias correction of regional climate change projections of temperature and precipitation, Geophys. Res. Lett., 35, L20709, doi:10.1029/2008GL035694
/ces/publications/nr/1680
elevation of 1423 m (F. Pálsson, personal
communication, 2004) was the highest attained
since the enormous jökulhlaup of November
1996. Under these conditions, drainage of the
lake by a jökulhlaup could trigger an eruption.
Inferred signs of increasing geothermal activ-
ity in the caldera were recorded at SIL station
GRF (Figure 1b) during August–October 2004,
initially as occasional ~25-min-long
/media/jar/myndsafn/2005EO260001.pdf
Reykjavík, 209 s.
Ogilvie, A. E. J. 1991. Climatic changes in Iceland A. D. c. 865 to 1598. Í: The Norse of the North Atlantic (Presented by G. F. Bigelow). Acta Archaeologica 61(1990), 233-251.
Ogilvie, A. E. J. 1992. Documentary evidence for changes in the climate of Iceland, A. D. 1500 to 1800. Í R.S. Bradley and P. D. Jones. Climate Since A.D. 1500. Routledge. London and New York, 92-117
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