79 results were found for f 홈타이▤Ø1ØX4889X4785▤黾대구수성방문아가씨梼대구수성방문안마✖대구수성빠른출장䪈대구수성숙소출장👩🏽‍🚒irresolutely.

Results:

• 71. VI_2014_005

  and direction, as well as air temperature, from the IMO operational surface station net- work. Most anemometers are installed at 10 m above ground level (mAGL). However, at some stations, surface winds are measured at different heights, h, varying between 4.0 and 18.3 m. 3This is done using a GRIB-API command on Parameter 141 (snow depth) in the earliest boundary data file: grib_set -f -d 0.0 -w /media/vedurstofan/utgafa/skyrslur/2014/VI_2014_005.pdf

• 72. ces-glacier-scaling-memo2009-01

  in Norway was provided by the Norwegian Water Resources and Energy Directorate (NVE). TóJ 12 5.12.2009 Memo References Bahr, D. B., M. F. Meier and S. D. Peckham. 1997. The physical basis of glacier volume–area scaling. J. Geophys. Res., 102(B9), 20,355–20,362. Björnsson, H., and F. Pálsson. 2008. Icelandic glaciers. Jökull, 58, 365–386. Fenger, J. (Ed.). 2007. Impacts of Climate Change on Renewable /media/ces/ces-glacier-scaling-memo2009-01.pdf

• 73. VI_2014_006

  and candidate situations is evaluated with the Teweles-Wobus (S1) skill score (Wilks, 1995). The S1 score compares the shape of two fields by considering their gradient at each grid point of the analogy domain: S1(u) = 100 n 1 i=1 m j=1 jDAi DFij+ n i=1 m 1 j=1 jDA j DFjj n 1i=1 m j=1 Gi + n i=1 m 1 j=1 G j (3) with DAi = A(i+1; j;u) A(i; j;u) (4) DFi = F(i+1; j; t) F(i; j; t) (5) DA j /media/vedurstofan/utgafa/skyrslur/2014/VI_2014_006.pdf

• 74. 2010_016

  /media/ces/2010_016.pdf

• 75. VI_2009_013

  Th. Árnadóttir, C. Völksen, W. Jiang, E. Sturkell, T. Villemin, P. Einarsson, F. Sigmundsson, and R. Stefánsson (2006). Current plate movements across the Mid- Atlantic Ridge determined from 5 years of continuous GPS measurements in Iceland. J. Geophys. Res., 111, B09407, doi:10.1029/2005JB003717. Guðmundsson, Á., S. Brynjólfsson (1993). Overlapping rift zone segments and the evolution /media/vedurstofan/utgafa/skyrslur/2009/VI_2009_013.pdf

• 76. VI_2015_006

  longwave radiation and latent heat losses, and small downward sensible heat fluxes. This excess energy then becomes available for melting of surface snow. The energy needed to melt a given mass of snow, ms, is given by E = ms L f ; (1) where L f = 334;000 J kg 1 is the latent heat of fusion. With an hourly change in snow water equivalent due to melting, dDmelt, the amount of energy absorbed /media/vedurstofan/utgafa/skyrslur/2015/VI_2015_006.pdf

• 77. Climate and Modeling Scenarios

  & Ólafsson, H. (2010). Validation of numerical simulations of precipitation in complex terrain at high temporal resolution. Hydrology Research, 41 (3-4), 164-170. Christensen, J.H., Boberg, F., Christensen, O.B. & Lucas-Picher, P. (2008), On the need for bias correction of regional climate change projections of temperature and precipitation, Geophys. Res. Lett., 35, L20709, doi:10.1029/2008GL035694 /ces/publications/nr/1680

• 78. 2005EO260001

  elevation of 1423 m (F. Pálsson, personal communication, 2004) was the highest attained since the enormous jökulhlaup of November 1996. Under these conditions, drainage of the lake by a jökulhlaup could trigger an eruption. Inferred signs of increasing geothermal activ- ity in the caldera were recorded at SIL station GRF (Figure 1b) during August–October 2004, initially as occasional ~25-min-long /media/jar/myndsafn/2005EO260001.pdf

• 79. Early work and an overview of measurements

  Reykjavík, 209 s. Ogilvie, A. E. J. 1991. Climatic changes in Iceland A. D. c. 865 to 1598. Í: The Norse of the North Atlantic (Presented by G. F. Bigelow). Acta Archaeologica 61(1990), 233-251. Ogilvie, A. E. J. 1992. Documentary evidence for changes in the climate of Iceland, A. D. 1500 to 1800. Í R.S. Bradley and P. D. Jones. Climate Since A.D. 1500. Routledge. London and New York, 92-117 /climatology/articles/nr/1138