L. Michaelis, S. Mori, T. Morita, W.Pepper,
H. Pitcher, L. Price, K. Raihi, A. Roehrl, H.-H. Rogner, A. Sankovski, M.Schlesinger,
P.Shukla, S. Smith, R. Swart, S. van Rooijen, N. Victor, Z. Dadi, 2000: IPCC Special Report
on Emission Scenarios. Cambridge University Press, United Kingdom and New York, NY,
USA.
a)
b)
c)
Fig.1 Change of annual extreme temperature range
/media/ces/CES_D2.4_VMGO.pdf
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
on the quantity at hand (strengths and weaknesses in
Box 1. The error propagation equation
The error propagation equations for the most common
operators are (s is the standard deviation):
Addition and Subtraction: z ¼ x þ yþ/ or z ¼
x y/
sz ¼
ffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffiffi
s2x
þ
s2y
þ/
r
Multiplication by an exact number: z/media/loftslag/Refsgaard_etal-2007-Uncertainty-EMS.pdf
” The latter is in our case
a policy decision represented by point z in Fig. 1. In
European water management, typical policy
decisions that involve participation include water
management plans.
Leading up to the policy decision is the participation
process, represented by the space between points y
and z, in which stakeholders interact with each other
but also with the agency responsible
/media/loftslag/vonKorff_etal-2010.pdf
) is considered as a sequence of steps
corresponding to n individual glaciers of different sizes (with volumes vi and areas si for i = 1
to n), or using
V (v) =
Z v
0
1
g
dS
ds
dx ; (7)
where the slope of the area distribution function, dS=ds, is considered as a function of ice vol-
TóJ 5 5.12.2009
Memo
0 50 100 150 200
0
5
10
15
20
25
Cumulative area (km2)
Area
(km
2 )
0 5 10 15
0.
0
0.
5
1.
0
1.
5
2.
0
2.
5
/media/ces/ces-glacier-scaling-memo2009-01.pdf
et
al
.(
200
4)
21
.Explici
tconsideratio
n
o
funcertaint
y
(relate
dt
o
CC
impacts
)
Uncertaintie
s
ar
e
no
t
glosse
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ove
r
bu
tcommunicate
d
(in
fina
lreports
,orally
)
Diet
z
et
al
.(
200
3),
Brugnac
h
et
al
.(
200
8)
Researcher
s
ar
e
willin
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to
tal
k
wit
h
stakeholder
s
abou
tuncertaintie
s
Diet
z
et
al
.(
200
3),
Brugnac
h
et
al
.(
200
8)
22
.Broa
d
communicatio
n
(on
CC
impacts
/media/loftslag/Huntjens_etal-2010-Climate-change-adaptation-Reg_Env_Change.pdf
) of the forthcoming changes are
uncertain. This uncertainty comes from three basic sources:
z Scenario uncertainty: future changes in the atmospheric composition, and thus the
external forcing of the climate system, depend on the magnitude of future anthropogenic
emissions of greenhouse gases and other radiatively active substances such as aerosol
particles and their precursor gases.
z Modelling
/media/ces/D2.3_CES_Prob_fcsts_GCMs_and_RCMs.pdf
&
4
Y
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/media/loftslag/programme2---PhD-Workshop-preceding-Adaptation-Research-Conference.pdf
Numerical simulations
of precipitation in the complex terrain of Iceland—Comparison with glaciolog-
ical and hydrological data. Meteorol. Z., 16(1), 71–85.
Rögnvaldsson, Ó. and Ólafsson H. 2008. Dynamical downscaling of precipi-
tation – Part I: Comparison with glaciological data. Proceedings of the XXV
Nordic Hydrological Conference, Reykjavík, Iceland.
Tómasson, H. 1982. Vattenkraft i Island och dess
/media/ces/Paper-Olafur-Rognvaldsson_92.pdf