Spatial Impacts of Climate Change. Denis Mercier

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content (OHC) in the upper water section above 2,000 m from 1955 to 2019. For a color version of this figure, see www.iste.co.uk/mercier/climate.zip

      COMMENT ON FIGURE 1.3.- The histogram represents annual anomalies (ZJ: Zetta Joules, where 1 ZJ = 1021 Joules) where positive anomalies relative to a mean calculated between 1981 and 2010 are shown as red bars and negative anomalies are shown in blue. The two dashed black lines represent linear trends for the periods 1955-1986 and 1987-2019 (source: Cheng et al. 2020).

      Figure 1.4. Vertical cross-section of ocean temperature trends from 1960 to 2019 from the sea surface to 2,000 m (60-year ordinary least squares linear trend). For a color version of this figure, see www.iste.co.uk/mercier/climate.zip

      COMMENT ON FIGURE 1.4.- The zonal mid-sections of each ocean basin are organized around the Southern Ocean (south of 60° S) in the center. The black outlines show the associated mean temperature with 2°C intervals (in the Southern Ocean, 1°C intervals are shown as dashed lines) (source: Cheng et al. 2020).

      This increase in global ocean surface temperatures leads, through thermal expansion, to a rise in sea level, as an increase in air temperature contributes to the melting of the Earth's cryosphere and thus to the increase in the amount of water in the global ocean (see Chapter 2 on melting of the cryosphere). Similarly, rising ocean temperatures reduce dissolved oxygen in the ocean and significantly affect marine life, especially corals and other organisms sensitive to temperature and water chemistry (IPCC 2019; see Chapter 4 on coasts). Increasing ocean surface water temperature promotes evaporation over the oceans and moisture in the atmosphere, which logically can promote heavy rainfall, and can be associated with more frequent and/or more intense cyclones, and can, depending on the case, lead to flooding (IPCC 2019). The consequence of this change in ocean temperatures is prolonged contemporary warming simply because of the thermal inertia of these gigantic ocean masses.

      (source: AMAP 2017). For a color version of this figure, see www.iste.co.uk/mercier/climate.zip

Graph depicts the temporal distribution of air temperature warming at Longyearbyen, 78° 25' N, 15° 47' E, capital of the Svalbard archipelago, for the period 1898–2019.

      Figure 1.6. Temporal distribution of air temperature warming at Longyearbyen, 78° 25' N, 15° 47' E, capital of the Svalbard archipelago, for the period 1898-2019 at different time scales, annual in black, summer (June, July, August) in red, autumn (September, October, November) in purple, winter (December, January, February) in blue, spring (March, April, May) in green. For a color version of this figure, see www.iste.co.uk/mercier/climate.zip

      COMMENT ON FIGURE 1.6.- The baseline average is calculated for the period 1961-1990. Change in mean annual precipitation with a five-year sliding average (in pink) (source: based on data from the Norwegian Meteorological Institute3).

Graph depicts the annual mean precipitation and annual mean temperatures from 1969 to 2016 at the Ny-Ålesund weather station (north-western Spitsbergen, Svalbard).

      Figure 1.7. Annual mean precipitation and annual mean temperatures from 1969 to 2016 at the Ny-Alesund weather station (northwestern Spitsbergen, Svalbard)

      (source: Bourriquen et al. 2018, based on data from the Norwegian Meteorological Institute). For a color version of this figure, see www.iste.co.uk/mercier/climate.zip

      Thus, whatever the spatial scales used here, contemporary climate change is illustrated by an increase in temperatures and an associated increase in precipitation.

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