Mechoso, C. Topographic influences on the general circulation of the Southern Hemisphere: a numerical experiment. Mon. Weather. Rev. 109, 2131–2139 (1981). The Arctis 9 Wireless will show up to every gaming session on Discord with no problem, capturing every errant scream you make in Phasmophobia. Battery Life on Arctis 9 Wireless Singh, H., Rasch, P. & Rose, B. Increased ocean heat convergence into the high latitudes with CO 2 doubling enhances polar-amplified warming. Geophys. Res. Lett. 44, 10583–10591 (2017). Myers-Smith, Isla H.; Forbes, Bruce C.; Wilmking, Martin; Hallinger, Martin; Lantz, Trevor; Blok, Daan; Tape, Ken D.; Macias-Fauria, Marc; Sass-Klaassen, Ute (1 January 2011). "Shrub expansion in tundra ecosystems: dynamics, impacts and research priorities". Environmental Research Letters. 6 (4): 045509. Bibcode: 2011ERL.....6d5509M. doi: 10.1088/1748-9326/6/4/045509. ISSN 1748-9326.

Addison, Kenneth (2002). Fundamentals of the physical environment. Routledge. p.482. ISBN 978-0-415-23293-7. Archived from the original on 30 June 2023 . Retrieved 15 November 2015. Chiang, J. C. & Bitz, C. M. Influence of high latitude ice cover on the marine intertropical convergence zone. Clim. Dyn. 25, 477–496 (2005).

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In the CMIP5 ensemble, there are only a few realizations which simulate stronger amplification than the observations (Fig. 3a). However, the fact that only one realization per model is used in the CMIP5 ensemble may imply that some of the extreme cases are missing. In general, CMIP6 models simulate slightly stronger AA 43 than CMIP5 models. Nonetheless, the majority of CMIP6 realizations in which the simulated AA 43 is stronger than the observed AA 43, occur earlier in the 21st century (Fig. 3b). It is also worth noting that CMIP6 models have generally a larger spread in AA 43 than CMIP5, even when considering only one realization per CMIP6 model (not shown). Some CMIP6 realizations simulate cooling for the Arctic (negative AA 43) while some other realizations have higher than five-fold warming in the Arctic compared to the globe (Fig. 3b). The large spread in CMIP6-simulated AA is in line with an earlier study 39 and highlights the effect of large internal variability for AA, even on a 43-year time scale. Screen, J. & Simmonds, I. Increasing fall-winter energy loss from the Arctic Ocean and its role in Arctic temperature amplification. Geophys. Res. Lett. 37, L16707 (2010). a b "The American Heritage Dictionary entry: arctic". www.ahdictionary.com. Houghton Mifflin Harcourt. Archived from the original on 12 June 2018 . Retrieved 4 January 2019. Huang, Y., Tan, X. & Xia, Y. Inhomogeneous radiative forcing of homogeneous greenhouse gases. J. Geophys. Res. Atmos. 121, 2780–2789 (2016).

Egger, J. Topographic wave modification and the angular momentum balance of the Antarctic troposphere. J. Atmos. Sci. 49, 327–334 (1992). The Arctic is especially vulnerable to the effects of any climate change, as has become apparent with the reduction of sea ice in recent years. Climate models predict much greater warming in the Arctic than the global average, [45] resulting in significant international attention to the region. In particular, there are concerns that Arctic shrinkage, a consequence of melting glaciers and other ice in Greenland, could soon contribute to a substantial rise in sea levels worldwide. [46]

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When Antarctic orography is flattened, we find a larger increase in CO 2-forced latent heat transport toward the Antarctic continent than when orography is at its present-day height. This is evident in both CESM1.1 and CCSM4.0 (Fig. 4, panels a and b, respectively; compare solid and dashed blue lines), corresponding to a 0.05 PW increase in latent heat transport across 70S in both models; this represents a 100% increase in the poleward latent heat transport response to CO 2-doubling in CCSM4.0, and a 50% increase in CESM1.1. The physical mechanisms behind the underestimation of AA in climate models remain unknown, but may be related to, e.g., errors in the model sensitivity to greenhouse gas forcing and in the distribution of the forced heating between the atmosphere, cryosphere and the ocean, and in different heights/depths in the atmosphere/ocean. Moreover, internal variability or uncertainties in observations may also contribute to the difference in AA between climate models and observations.