in an overall
cold bias, compared with station measurements. To test, whether this is due to the HARMONIE
model core or the external surface scheme, biases of 2-m temperature from SURFEX are com-
pared with biases of temperature projected from the lowest two model levels to 2 mAGL. It is
found that the negative temperature biases are due to shallow inversion layers near the ground,
which are introduced
/media/vedurstofan/utgafa/skyrslur/2014/VI_2014_005.pdf
improving
management policies and practices by learning from the
outcomes of implemented management strategies. Partici-
patory integrated assessment is here a form of problem
structuring for identification of gaps, ambiguity and
multiple frames, confrontation, and integration of the
most divergent views with respect to a given problem
situation.
Additional methods and tools that AM require com/media/loftslag/Henriksen_Barlebo-2008-AWM_BBN-Journ_Env_Management.pdf
J A
0 100 200 30020
0
60
0
100
0
Days since Sept. 1st
Q
(m
^3
/s)
Obs
Pred−nearest
Pred−weight
Method 4 T+2: RMSE−nearest= 69.6 RMSE−weight= 44.5
S O N D J F M A M J J A
Figure 7. Observed and predicted daily discharges at vhm 64 for a forecast range (T) of 2 days
and water-year 2004–2005, using methods 1 to 4 with rescaling. The 80%, 90% and 95% pre-
diction intervals are represented by grey
/media/vedurstofan/utgafa/skyrslur/2013/VI_2013_008.pdf
when the spring floods decreased and autumn
and winter floods increased.
The differences between the scenarios were estimated by com-
paring the average changes of the scenarios (marked with dia-
monds in Fig. 5). The differences between different emission
scenarios with the same GCM were rather small; the average
changes in floods differed on average by 1.7% units in 2070–
2099. The B1 scenario
/media/ces/Journal_of_Hydrology_Veijalainen_etal.pdf
) and are
Global Navigation Satellite System (GNSS) data providers (SONEL, n.d.).
The North Sea is home to one of the most dense tide gauge networks in the world, with over 15 tide
gauge series that span at least 100 years along its coastline (Quante and Colijn, 2016). In Denmark,
17
the national tide gauge network consists of 90 automatic stations run in cooperation of the Danish
Meteorological
/media/vedurstofan-utgafa-2020/VI_2020_005.pdf
the com-
plexity of the hydrological processes through modelling, but its application is usually limited to
the short-range. Although the results demonstrated a great potential for this method, its success-
ful application in real-time will strongly depend on the quality and availability of streamflow
observations, which can be poor or simply missing during periods of variable durations, e.g
/media/vedurstofan/utgafa/skyrslur/2014/VI_2014_006.pdf
of the glaciers. An up to 8 m thick winter snow layer
was measured in the accumulation area (∼4 m w.e.). Ice melt
of up 10 m w.e. was measured in the lowest part of the ab-
lation zone in summer, and 2 m w.e. was melted during win-
ter. Taking into account ∼2 m of annual rainfall, the runoff
from this part of the glacier was estimated as ∼14 m w.e. per
year; a surprisingly high value (Ahlmann, 1939
/media/ces/Adalgeirsdottir-etal-tc-5-961-2011.pdf
andEnergy Directorate (NVE), Oslo, Norway2Department of Geosciences, University of Oslo, Norway3Institute for Marine and Atmospheric Research, Utrecht University, Utrecht, the Netherlands
Andreassen, L. and Oerlemans, J., 2009: Modelling long-term
summer and winter balances and the climate sensitivity of Stor-breen, Norway. Geogr. Ann. 91 A (4): 233–251.
ABSTRACT. Measurements of winter balance (bw
/media/ces/GA_2009_91A_4_Andreassen.pdf
farvegarins undir jöklinum út frá rúmmáli vatns
sem þar hefur safnast fyrir benda til þess að viðnám gegn vatnsrennsli við jökul-
botn minnki eftir því sem líður á hlaupið. Undir lok hlaupsins runnu á bilinu 80–
90 m3 s 1 um farveg sem var einungis einn þriðji hluti af rúmmáli farvegar sem flutti
svipað vatnsmagn á fyrsta eða öðrum degi eftir að hlaupið hófst við jökuljaðar. Þessi
niðurstaða er
/media/vedurstofan/utgafa/skyrslur/2009/VI_2009_006_tt.pdf