-
lations for regional climate downscaling. Mon. Wea. Rev., 131, 2857–2874.
Rögnvaldsson, Ó., Jónsdóttir J. F. and Ólafsson H. 2007. Numerical simulations
of precipitation in the complex terrain of Iceland—Comparison with glaciolog-
ical and hydrological data. Meteorol. Z., 16(1), 71–85.
Sigurðsson, O., and Sigurðsson Ó. J. 1998. Afkoma nokkurra jökla á Íslandi
1992–1997 (Mass balance of a number
/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
water.
Since, in this study, the focus is on large-scale storm systems, persisting for at least one day,
variability on shorter time-scales (mainly the diurnal cycle and atmospheric tides) is eliminated
by calculating averages from the four 6-hourly reanalysis fields of each day (6-hourly precip-
8
Figure 1. Top: Average fields of 500 hPa geopotential height in winter (DJF 1989-90)
and summer (JJA
/media/vedurstofan/utgafa/skyrslur/2015/VI_2015_005.pdf
was therefore formed
by ice lifting and deformation induced by subglacial water pressures higher than ice
overburden pressure.
The discharge data and the derived size of the subglacial flood path, as indicated
by the volume of water stored subglacially, indicates a development towards more
efficient subglacial flow over the course of the jökulhlaup. Thus, a discharge in the
iii
range 80–90 m3 s 1
/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
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/media/loftslag/Outline_for_the_case_Road_maintenance_in_a_changing_climate.pdf
horizontal displacement of the most active part of Þófi since the start of
the measurements is mostly in the range 10–35 cm (maximum 69 cm), whereas the movement
in Neðri-Botnar is slower, with the more active points having total displacement mostly in the
range 5–10 cm (maximum 46 cm). The maximum measured velocity of the horizontal movement
in the Þófi area was 92 cm/a over a two-month period in late
/media/vedurstofan-utgafa-2016/VI_2016_006_rs.pdf
contours). Bottom panel: manned and automated surface
observations over Iceland.
13
Figure 4. Hourly rainfall during 3 September 2012, based on HARMONIE model simula-
tions. Times are in UTC (local time).
14
Figure 5. Distribution of low- (red crosses), medium- (green vertical lines), and high-
level (blue horizontal lines) cloud cover of at least 90%, based on HARMONIE model
simulations. Terrain
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approximately centred around Iceland: the outer domain with
43 42 grid points spaced at 27 km (1134 1107 km), the intermediate domain with 95 90 grid
points spaced at 9 km, and the inner domain with 196 148 grid points spaced at 3 km. The
northwest corner of the outer domain covers a part of the southeast coastal region of Greenland.
Otherwise, the only landmass included in the model domain
/media/vedurstofan/utgafa/skyrslur/2013/2013_001_Nawri_et_al.pdf