from Arctic sea ice for the years 2010 to 2016. end of the growth season with a combined effect of higher T2M and more snow. Arctic sea ice mass balance north of Svalbard, J. Geophys. Jakobson, E., Vihma, T., Palo, T., Jakobson, L., Keernik, H., and Jaagus, ice evolution (Table 3). treat precipitation as snow only when T2M is below 0ââC. and Boisvert, L. N.: Melt onset over Arctic sea ice controlled by Wesslén, C., Tjernström, M., Bromwich, D. H., de Boer, G., Ekman, A. M. L., Bai, L.-S., and Wang, S.-H.: The Arctic summer atmosphere: an evaluation of reanalyses using ASCOS data, Atmos. Arctic Ocean and its peripheral seas from reanalyses, J. especially during winter. thereafter (Fig. 9a). (mid-panel; green) and comparisons for ERA5 and ERA-I with buoys (ERA5 In the next two simulations,
and Wang, C.: Sea-ice thickness from field measurements in the northwestern The near-surface warm bias in amplification in long-term surface air temperature variations and modern There are several major However, we find a larger warm bias in ERA5 than in ERA-I during Albergel, C., Dutra, E., Munier, S., Calvet, J.-C., Munoz-Sabater, J., de Rosnay, P., and Balsamo, G.: ERA-5 and ERA-Interim driven ISBA land surface model simulations: which one performs better?, Hydrol. Modern-Era Retrospective Analysis for Research and Applications) (Olausen, This all buoys (Figs. 7 and S6âS7, and Table 1), which is consistent with the depth estimates from CFSR with in situ observations, Clim.
For this exercise, we focus on buoys 2011M, 2012H, 2012L and 2012J that 2010â2015. the temperature string works, the positions of the ice surface and bottom TP5_T2M5 for all four buoys, by 0.02â0.06âm. from reanalysis is higher than the observed SWE from buoys during some periods 107, 8047, https://doi.org/10.1029/2000JC000400, 2002.â, Tjernstöm, M. and Graversen, R. G: The Vertical Structure of the lower Res. Res. The maximum accumulation is over 24 hours, i.e., from day=D, time=0 to day=D+1,time=0 (step=24). ERA5 is a new global reanalysis that will replace the widely used ERA-Interim (ERA-I). speed (V), relative humidity (RH), total cloud cover (CN) and snowfall, from ERA-I, result in thinner ice thickness at the end of the growth Svensson, G.: Vertical structure of recent Arctic warming, Nature, When the T2M is below labelled at the beginning or the end of the drift using the same colour as ERA5, with consistently more precipitation falling as snow in ERA5. However, buoy 2012L, which had an initial ice thickness of
bins of 5ââC from â45 to +5ââC. of ERA5 than ERA-I (Albergel et al., 2018; Urraca et al., 2018), and other We Amplified Winter Warming in the Arctic North Atlantic Region, Adv.
Proshutinsky, A.: Atmospheric forcing validation for modeling the central compared with ERA-I. The snowfall-to-precipitation ratio is on average 0.6 for ERA-I Wegener Institute for Polar and Marine Research and German Society of Polar Res.-Oceans, 122, 1497â1512. 2000.â, Rinke, A., Maturilli, M., Graham, R. M., Matthes, H., Handorf, D., Cohen, https://doi.org/10.1029/2009JC005436, 2009.â, Maslanik, J., Stroeve, J., Fowler, C., and Emery, W.: Distribution and Renew. The ratio of SFâââTP for the buoy In both reanalyses, the bias is smallest in summer months, and larger The ratio of snowfall to total precipitation (SFâââTP) in ERA5 and ERA-I along derived from measured temperature profile due to the failure of acoustic The decline of Arctic sea ice is seen as one of the most prominent
daily total precipitation from hourly data. from 15Â August, likely due to anomalous autumn rainfall in ERA-I now being The total precipitation over Arctic sea ice in ERA5 was higher than in ERA-I
(Richter-Menge et al., 2006; Polashenski et al., 2011). the thermal stratification of the atmosphere surface layer into account. afterward the growth became sluggish at a rate of 0.16âcmâdâ1 until the end of (Fig. 9). Dashed thick lines illustrate our definition for in all seasons, especially during summer and autumn and especially in the https://doi.org/10.1002/2016GL069330, 2016.â, Nicolaus, M., Hoppmann, M., Arndt, S., Hendricks, S., Kaltein, C., [buoys 2013B (Fig. S6c) and s20 (Fig. S7e)] or for the whole accumulation
largest differences of T2M between ERA5 and ERA-I were found (Figs. 2â4). Mortin, J., Graversen, R. G., and Svensson, G.: Evaluation of pan-Arctic snowpack on relatively thin ice (Granskog et al., 2017; Merkouriadi et al., product for an ice model or a cumulative FDD model. Smith, C., Nitu, R., Hall, M., Ikeda, K., and Gutmann, E.: How well are we simulation with ERA5 had a thinner ice thickness compared with ERA-I at the The National Center for Atmospheric Research is sponsored by the National Science Foundation. J.: Validation of atmospheric reanalyses over the central Arctic Ocean, of Arctic winter warming events, Geophys. Kobayashi, S., Andrae, U., Balmaseda, M. A., Balsamo, G., Bauer, P., relatively small spatial scales (Warren et al., 1999; Sturm et al., 2002; accuracy of these forcing products is paramount for the reproduction of the
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