Arctis 9 Wireless Headphones with Microphone 61484

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Pauluis, O., Czaja, A. & Korty, R. The global atmospheric circulation in moist isentropic coordinates. J. Clim. 23, 3077–3093 (2010). Arctic life is characterized by adaptation to short growing seasons with long periods of sunlight, and cold, dark, snow-covered winter conditions.

Bailey, A., Singh, H. K. & Nusbaumer, J. Evaluating a moist isentropic framework for poleward moisture transport: implications for water isotopes over Antarctica. Geophys. Res. Lett. 46, 7819–7827 (2019).Seviour, W. et al. The Southern Ocean sea surface temperature response to ozone depletion: a multimodel comparison. J. Clim. 32, 5107–5121 (2019).

Hurrell, J. et al. The Community Earth System Model: a framework for collaborative research. Bull. Am. Meteorol. Soc. 94, 1339–1360 (2013). Main article: Arctic cooperation and politics Polar bears on the sea ice of the Arctic Ocean, near the North Pole. USS Honolulu pictured. As of 2012, the Kingdom of Denmark is claiming the continental shelf based on the Lomonosov Ridge between Greenland and over the North Pole to the northern limit of the Russian EEZ. [34]

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On 2 August 2007, two Russian bathyscaphes, MIR-1 and MIR-2, for the first time in history descended to the Arctic seabed beneath the North Pole and placed there a Russian flag made of rust-proof titanium alloy. The flag-placing during Arktika 2007 generated commentary on and concern for a race for control of the Arctic's vast hydrocarbon resources. [30] Map of the Arctic region showing the Northeast Passage, the Northern Sea Route within it, and the Northwest Passage.

In this study, we have used two state-of-the-art GCMs to show that Antarctic ice sheet orography robustly decreases climate sensitivity over the Antarctic continent, and that a flattened Antarctic ice sheet would experience significantly greater surface warming than the present-day Antarctic ice sheet. When CO 2 is doubled, we have shown that both moist and dry dynamic processes are more efficient at warming a flattened Antarctic continent. These dynamic processes differ from those that occur when Antarctica is at its present-day elevation because the presence of Antarctic orography significantly alters the atmospheric circulation at high Southern latitudes (see, e.g., 14, 15, 16); differences in the unperturbed circulation due to differences in orography result in different (moist and dry transport) responses to CO 2-doubling. In addition to the three purely observational datasets, we used ERA5 reanalysis 66, which has been produced by the European Centre for Medium-Range Weather Forecasts. We used monthly mean 2-m temperature fields in the native, 0.25 ∘ horizontal resolution. The first release of ERA5 covers the years from 1979 to the present, but a preliminary extension for 1950–1978 was recently released 43. We used the whole time series, from 1950 to 2021. All the observational temperature datasets used are listed in Table S 1.Main articles: Climate of the Arctic and Global warming in the Arctic A snowy landscape of Inari located in Lapland ( Finland) The earliest inhabitants of North America's central and eastern Arctic are referred to as the Arctic small tool tradition (AST) and existed c. 2500 BCE. AST consisted of several Paleo-Eskimo cultures, including the Independence cultures and Pre-Dorset culture. [17] [18] The Dorset culture ( Inuktitut: Tuniit or Tunit) refers to the next inhabitants of central and eastern Arctic. The Dorset culture evolved because of technological and economic changes during the period of 1050–550 BCE. With the exception of the Quebec/ Labrador peninsula, the Dorset culture vanished around 1500 CE. [19] Supported by genetic testing, evidence shows that descendants of the Dorset culture, known as the Sadlermiut, survived in Aivilik, Southampton and Coats Islands, until the beginning of the 20th century. [20] Egger, J. Antarctic slope winds and the polar stratospheric vortex. J. Atmos. Terr. Phys. 56, 1067–1072 (1994). Landrum, L. L., Holland, M. M., Raphael, M. N. & Polvani, L. M. Stratospheric ozone depletion: an unlikely driver of the regional trends in Antarctic sea ice in Austral fall in the late twentieth century. Geophys. Res. Lett. 44, 11–062 (2017). Meehl, G. A. et al. Climate change projections in CESM1 (CAM5) compared to CCSM4. J. Clim. 26, 6287–6308 (2013).

In this study, we’ve identified Antarctic orography as one of (likely) several factors that reduces the magnitude of CO 2-forced warming over the Antarctic continent. Further factors may also be responsible for a weak climate change signal over the Antarctic continent, including heat uptake by the Southern Ocean 37 and the meagre decline of Antarctic sea ice (in both observations and future GCM projections; see refs. 12, 38). More research is necessary to identify the extent to which warming or cooling over the open Southern Ocean and sea ice zones impacts surface temperatures over high-elevation regions of the Antarctic ice sheet, as the dynamics of the extratropical atmosphere suggests that these regions should be relatively isolated from adjacent low-elevation regions 28, 39, 40. Our experiments, for example, show that differences in sea ice loss and warming over the marginal ice zone are not primarily responsible for greater warming over the flattened Antarctic continent. In fact, CESM1.1 simulates less Antarctic sea ice retreat with CO 2-doubling when Antarctica is flattened whereas CCSM4.0 simulates more Antarctic sea ice retreat (see Supplementary Fig. 5), even though both models simulate greater warming over the continent (recall Figs. 2 and 3).

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Holland, M. M. & Bitz, C. M. Polar amplification of climate change in coupled models. Clim. Dyn. 21, 221–232 (2003). To assess the accuracy of the four datasets applied in our study (GISTEMP, BEST, HadCRUT5, ERA5) in the Arctic, we conducted a validation against the Global Historical Climatology Network monthly (GHCN-M) station data 67. We used the station data which was bias-adjusted for non-climatic effects (indicated by the suffix “.qcf” in the GHCN-M database). We selected all the stations located north of 66.5 ∘N that had at least 39 years of data over the 43-year period of 1979–2021. In total, these criteria resulted in 87 stations. We calculated the temperature trends for each station, and compared them with the average across the four gridded datasets. These results are shown in Fig. S 1. The median difference between the trends estimated from the gridded data and the 87 station observations (gridded minus stations) is −0.019 ∘C decade −1. Therefore, we conclude that the average of the four gridded temperature datasets generally captures well the temporal trends of the near-surface mean temperature in the Arctic, which makes it suitable to be used as a basis of our study. Climate model data