the validity of the ideal gas law, hydrostatic
balance, a piecewise linear vertical gradient of air temperature, and neglecting the effects of water
vapour. Pressure, p, as a function of height can then be derived through vertical integration of the
hydrostatic balance equation, and is given by
p(h(x;y);z) = p0 exp
g
R
Z h(x;y)+z
0
dx
T (x )
; (5)
where p0 is pressure at mean sea level, T/media/vedurstofan/utgafa/skyrslur/2013/2013_001_Nawri_et_al.pdf
Arason T., Geirsson H., Karlsdóttir S., Hjaltadóttir S., Ólafsdóttir U., Thorbjarnardóttir B., Skaftadóttir T., Sturkell E., Jónasdóttir E.B., Hafsteinsson G., Sveinbjörnsson H., Stefánsson R., and Jónsson T.V., 2005, Forecasting and Monitoring a Subglacial Eruption in Iceland, Eos, Vol. 86, No. 26, p. 245-252, 28 June 2005.
Location
Location of the weather radar at Keflavik airport
/earthquakes-and-volcanism/articles/nr/2072
the contiguous USA. 30th Annual Applied Geography Conference, Indianapolis, October 2007. 10 pp.
Clausen, N.-E., Lundsager, P., Barthelmie, R., Holttinen, H., Laakso, T. & Pryor, S.C. (2007). Wind Power. In: J. Fenger (Ed.) Impacts of Climate Change on Renewable Energy Sources: Their role in the Nordic energy system, Nord 2007:003, 105-128.
Clausen N.E., Pryor S.C., Larsén X.G., Hyvönen R
/ces/publications/nr/1944
variability
Models
Emission scenarios
2000 2100
LEVEL OF
UNCERTAINTY
Near future End of the
century
Natural climate variability + +
Climate model sensitivity (+) ++
Emission scenarios ++
Source: J. Räisänen (Univ. of Helsinki)
Probabilistic forecasts
of temperature change
in southern Finland
(1971-2000 barb2right 2011-2020)
Temperature change (ºC)
P
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b
a
b
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1
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/media/loftslag/Case_B___Road_transport_operation_and_infrastructure_planning.pdf
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20
40
60
80
100
120
140
jan feb mar apr mai jun jul aug sep okt nov des
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m
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m
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60
80
100
120
140
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Ensemble approach for probabilistic
hydrological projections
Catchment
/media/ces/Lawrence_Deborah_CES_2010.pdf
(To) and Tindfjallajo¨kull (Ti) ice caps, estimated as the mean difference
between available elevation maps for time period 1 and 2. (b, c) Corresponding temperature (T) and precipitation (P) at the Vı´k and Hveravellir weather
stations averaged over all the seasons covered by the differential digital elevation maps. The cold and dry years from 1979 to 1984 are included in the
mass balance calculation for Torfajo
/media/ces/Gudmundsson-etal-2011-PR-7282-26519-1-PB.pdf
by
the modal occurrences shown in Figure 9, is equal to the seasonal mean field.
The eight modal mean MSLP fields, together with the corresponding average centred temporal
tendencies of the MSLP field (d p=d tjt0 = (p(t0 + d t) p(t0 d t))=2d t, with d t = 2 days) in
winter are shown in Figure 10. In summer, the spatial patterns of mean MSLP fields are similar
but less distinct, with weaker pressure
/media/vedurstofan/utgafa/skyrslur/2015/VI_2015_005.pdf