of Icelandic glaciers 1992–1997). Rep.
OS-98082 (in Icelandic), National Energy Authority, Reykjavík.
Sigurðsson, O., Thorsteinsson Th., Ágústsson S. M. and Einarsson B. 2004.
Afkoma Hofsjökuls 1997–2004. (Mass balance of Hofsjökull 1997–2004.) Rep.
OS-2004/029, National Energy Authority, Reykjavík.
Uppala, S.M., and 45 co-authors 2005. The ERA-40 re-analysis. Q. J. R. Mete-
orol. Soc., 131, 2961
/media/ces/Paper-Olafur-Rognvaldsson_91.pdf
performance of the
model.
REFERENCES
Førland, E. J., Allerup P., Dahlström B., Elomaa E., Jónsson T., Madsen H.,
Perälä J., Rissanen P., Vedin H. and Vejen F. 1996. Manual for operational cor-
rection of Nordic precipitation data. DNMI Report No. 24/96 Klima, 66 pp.
Benoit, R., Pellerin P., Kouwen N., Ritchie H., Donaldson N., Joe P. and Soulis
E. D. 2000. Toward the use of coupled atmospheric
/media/ces/Paper-Olafur-Rognvaldsson_92.pdf
properly even if the
sample size is increased and systematic biases may be expected.
2.2.3 Predictors
Mean sea level pressure (MSLP), geopotential height (Z), specific humidity (q) and tempera-
ture (T) at different pressure levels are considered in this study to describe the meteorological
situations at the synoptic scale and to identify weather analogues. The MSLP and geopotential
height (Z) describe
/media/vedurstofan/utgafa/skyrslur/2014/VI_2014_006.pdf
236
1992 09 167 124 167 98
1995 07 1994 1759 599 368
1995 10 96 62 73 37
1997 07 921 728 330 184
2000 08 1240 1083 365 221
2002 09 689 582 267 160
2003 11 241 207 139 98
2006 04 1370 1340 300 270
2008 10 1350 1290 300 265
The origin of the 1957, 1960, 1964 and 1966 jökulhlaups is not certain but is most likely the eastern cauldron. The discharge
and volume for the 1995 jökulhlaup are a sum from
/media/vedurstofan/utgafa/skyrslur/2009/VI_2009_006_tt.pdf
: 3601/B2007.EEA53004 and 3601/RO/CLC/
B2007.EEA52971, Landmælingar Íslands, Reykjavik, Iceland.
Bechtold, P., Köhler, M., Jung, T., Doblas-Reyes, F., Leutbecher, M., Rodwell, M. J., Vitart, F.,
and Balsamo, G. (2008). Advances in simulating atmospheric variability with the ECMWF
model: from synoptic to decadal time-scales. Q. J. R. Meterol. Soc., 134:1337–1351.
Brousseau, P., Berre, L., Bouttier
/media/vedurstofan/utgafa/skyrslur/2014/VI_2014_005.pdf
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/media/loftslag/Outline_for_the_case_Road_maintenance_in_a_changing_climate.pdf
Q. J. R. Meteorol.
Soc., 137, 409-422.
Giesen, R. H., Andreassen, L. M., Oerlemans, J., & van den Broeke, M. R. (2014). Surface
energy balance in the ablation zone of Langfjordjøkelen, an arctic, maritime glacier in
northern Norway. J. Glaciol., 60(219), 57-70.
Seity, Y., Brousseau, P., Malardel, S., Hello, G., Bénard, P., Bouttier, F., . . . Masson, V. (2011).
The AROME-France convective-scale
/media/vedurstofan/utgafa/skyrslur/2015/VI_2015_006.pdf
time-series.
For wind energy assessments, the main emphasis is on an accurate determination of average wind
power density. As discussed in previous sections, average power density is approximately propor-
tional to the mean cube of wind speed. Rescaling factors for modelled wind speed time-series,
interpolated to station locations, are therefore defined here as 3
q
S3o=S3m. Aside from
/media/vedurstofan/utgafa/skyrslur/2013/2013_001_Nawri_et_al.pdf