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Climate change

Global warming until now

Recent accelerated global warming

In 2024, Earth’s average temperature climbed to more than 1.5°C above pre-industrial levels. This was the first time since the pre-industrial times of the late 19th century and in fact the first time in the Holocene. This threshold has a special significance: the Paris Climate Agreement stipulates that we should strive to keep warming below 1.5°C compared to pre-industrial levels.

June 2024 was the twelfth month in a row with global mean surface temperatures at least 1.5 °C above pre-industrial conditions (269).


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Responsibilities for global warming until now

Some countries are hardly responsible for climate change but will face the consequences much more than others. These countries are often relatively poor. The high-income countries have made their fortune by emitting greenhouse gases into the atmosphere for more than 150 years. In a sense, the consequences of their economic development are passed on to low-income countries.


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Global warming in the 21st century

At the moment, according to experts, plausible scenarios for emissions during the 2005–2050 period project between 2°C and 3°C of global warming by 2100, with a median of 2.2°C. These scenarios also indicate that the world is still off track from limiting 21st-century warming to 1.5°C or below 2°C (the targets of the Paris Agreement) (242).

IPCC 5th Assessment Report

For the Fifth Assessment Report of the IPCC a different type of climate change scenarios has been defined than for the previous IPCC reports: the so-called Representative Concentration Pathways (RCPs) (73). More information on these scenarios is presented below under the heading 'Climate change scenarios'. Scenarios that are often used for climate projections are the low RCP2.6, the moderate RCP4.5 and the high-end RCP8.5 scenario.


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Projected change in annual global mean surface air temperature (°C) by the mid- and end of the 21st century relative to present day (1986–2005) for RCP2.6 (32 models), RCP4.5 (42 models) and RCP8.5 (39 models) as well as the 5% - 95 % ranges from the models’ distribution (numbers between brackets) according to the IPCC 5th Assessment Report (105).
Period RCP2.6 RCP4.5 RCP8.5
2046 - 2065 1.0 (0.4 - 1.6) 1.4 (0.9 - 2.0) 2.0 (1.4 - 2.6)
2081 - 2100 1.0 (0.3 - 1.7) 1.8 (1.1 - 2.6) 3.7 (2.6 - 4.8)

In a special report in 2019, the IPCC has presented updates of the projections of global warming, and used different time slices and a different reference (the period 1850-1900) (213):

Projected global mean surface temperature change relative to 1980 - 1900 for two time periods under four RCPs.
Period RCP2.6 RCP4.5 RCP6.0 RCP8.5
mean (likely range) mean (likely range) mean (likely range) mean (likely range)
2031 - 2050 1.6 (1.1 - 2.0) 1.7 (1.3 - 2.2) 1.6 (1.2 - 2.0) 2.0 (1.5 - 2.4)
2081 - 2100 1.6 (0.9 - 2.4) 2.5 (1.7 - 3.3) 2.9 (2.0 - 3.8) 4.3 (3.2 - 5.4)

Several studies have projected climate change beyond 2100 based on the so-called extended concentration pathways (ECPs). The central estimates for global mean temperature increase by 2200, relative to pre-industrial levels, are between 1.3°C for ECP2.6 and 7.1°C for ECP8.5 (131). 

IPCC 4th Assessment Report

In the previous Fourth Assessment Report somewhat different results on projected global warming were reporting. One of the reasons for these different results when compared with the more recent Fifth Assessment Report is the fact that different climate change scenarios were used.  

According to the Fourth Assessment Report the projected increase in this century globally is between 1.8 and 4.0°C (best estimate), and is considered likely (66% probability) to be between 1.1 and 6.4°C for the six IPCC climate change (SRES) scenarios and multiple climate models, comparing the 2080–2100 average with the 1980–1999 average. These scenarios assume that no additional policies to limit greenhouse gas emissions are implemented (2). The range results from the uncertainties in future socio‑economic development and in climate models.

Global heat wave changes in the 21st century

When will hot summers be so widespread that half of the population regularly experiences summers that are hotter than any summer of the past? Much sooner than most people probably expect, according to a recent study (114). Under an intermediate (RCP4.5) scenario of climate change, more than half of the world’s population is projected to experience a summer that’s hotter than any summer of the past in 1 out of 2 years within 20 years, and nearly the entire world population just after 2050. In fact, in just over a decade such a hot summer in 1 out of 2 years may already be a fact for half of the world’s population under a high-end scenario (RCP8.5) of climate change (114). These results were obtained from a probabilistic approach that combines information from observations on temperatures in the past (the period 1950 - 2012) and future climate model projections for the period 2013 - 2069. For this study global land surface was divided into 26 regions.


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Global heat waves and the Paris agreement (2015)

According to the Paris agreement of 2015, global warming should be kept below 2 °C above pre-industrial levels, and preferably be limited to 1.5 °C. What if we do succeed in reaching these goals, what would future heat waves look like? This was studied with a very high-resolution global model. The model results were used to calculate an index for wave magnitude that takes into account both heat wave duration and intensity. The higher this index, the more extreme the heat wave. Three types of heat waves were distinguished: severe, extreme and exceptional heat waves. These heat wave types more ore less agree with the heat waves of the Balkans (2007), France (2003) and Russia (2010), respectively.


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Air temperature changes in Europe until now

Between 2006 and 2015, the average annual temperature over the European land area increased by 1.45°C to 1.59°C, relative to the pre-industrial period. This increase is larger than that for global average temperature and makes it the warmest decade on record (125). Moreover, 2014 and 2015 were the joint warmest years in Europe since instrumental records began. Anthropogenic climate change made these temperature records 35-80 times more likely (126). Moreover, climate reconstructions show that summer temperatures in Europe in recent decades are the warmest in at least 2000 years and that they lie significantly outside the range of natural variability (127). The relatively rapid warming trend since the 1980s is most clearly evident in the summer (124). Nocturnal temperatures have increased more than daytime values (14).


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Heat wave changes in Europe until now

Heatwaves, similar to those which occurred in western Russia in 2010 and Europe in 2003, develop when persistent anticyclonic patterns, often referred to as ‘atmospheric blocking’, initiate a cascade of self-reinforcing, heat-accumulating physical processes (87). It is suggested that the observed increase in extreme summer heat over Europe is attributable to both increasing frequency of blocking circulations and changes in the surface energy balance (88).

Heatwaves in northern Europe are increasingly similar to those in the south

All over Europe, since 1950, the frequency, duration and intensity of heatwaves have increased. In the last two decades, these changes were most dramatic for northwest and central Europe.


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Changes in hottest and coldes extremes in Europe until now

Hot days now about 2.3 °C warmer than in 1950

On average, across Europe, the number of days with extreme heat and heat stress has more than tripled from 1950 to 2018: from less than 2 days to more than 6 days per year. This was concluded from observations during the period 1950-2018 at weather stations all across Europe. In this study, a day is extremely hot when its maximum daytime temperature exceeds the limit of the 1% hottest days over the whole period 1950-2018 (12).


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Precipitation changes in Europe until now

Trends in extreme precipitation events

The number of days with very heavy precipitation over Europe has increased on average by about 45% in observations in the period 1981-2013 compared to 1951-1980. The more intense the heavy rainfall event, the higher the relative increase in frequency. The findings imply that what was a 1-in-1000 day heavy rainfall in 1951-1980 occurred about 45% more often in the 1981-2013 period. Models seem to underestimate the rate of change in daily heavy precipitation compared to observations (123).


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Hail events changes in Europe until now

Hail events are among the most costly weather-related extreme events in several European regions, causing substantial damage to crops, vehicles, buildings and other infrastructure (146). For example, three hailstorm events in Germany in July and August 2013 caused around EUR 4.2 billion of combined damages to buildings, crops, vehicles, solar panels, greenhouses and other infrastructure (147).
 More recently, several hailstorm events with hailstones several centimeters in diameter occurred in Germany in 2019 and in Poland, the Czech Republic, Germany, and Italy in 2021 (263). The maximum hail size reported in Europe in the last decades was 15 cm and was reported in Romania on 26 May 2016 (263).

The number of hail events is highest in mountainous areas and pre-Alpine regions. Since 1951, increasing hail trends have been noted in southern France and Austria, and decreasing (but not statistically significant) trends have been noted in parts of Eastern Europe (146). 


Snow cover changes in Europe until now

Snow cover

Globally, in mountain regions, snow cover extent has reduced by 3.6% ± 2.7% and snow cover duration by 15.6 days ± 11.6 days during the period 1982–2020 (246). Snow cover extent in the northern hemisphere has declined significantly over the past 90 years, with most of the reductions occurring since 1980. Over the period 1967-2015, snow cover extent in the northern hemisphere has decreased by 7 % on average in March and April and by 47 % in June; the observed reductions in Europe are even larger, at 13 % for March and April and 76 % for June (146).


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Ice cover changes in Europe until now

An analysis of long (more than 150 year) ice records from lakes and rivers throughout the northern hemisphere indicated that for a 100 year period, ice cover has been occurring on average 5.7 ± 2.4 days later (± 95% confidence interval), while ice break-up has been occurring on average 6.3 ± 1.6 days earlier, implying an overall decrease in the duration of ice cover at a mean rate of 12 days per 100 years. These results do not appear to change with latitude, or between North America and Eurasia, or between rivers and lakes (26).


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Sea temperature changes in Europe until now

From 1971 to 2010, the ocean has taken up about 93% of the global warming heat entering Earth’s climate system, with 3% melting ice, 3% warming the land and only 1% warming and moistening the atmosphere (where the latent heat energy for evaporation to maintain relative humidity is roughly equivalent to the energy to warm the atmosphere) (231).

On a global scale, ocean surface temperatures have increased, on average, by around 0.7°C since the beginning of the 20th century (2) and 0.17°C between 1969 and 2008 from the surface to a 700 m depth; the temperature increase in the Atlantic Ocean during 1969 and 2008 was 0.30°C (57). Observational records of ocean heat content show that ocean warming is accelerating (184).

For the period 1982–2019, a trend in the warming rate of Mediterranean Sea surface temperature of 0.35 °C/decade was found, with an accumulated warming of 1.3 °C from 1982 to 2019 (186, 260). 

Wind climate changes in Europe until now

Storminess in Europe has shown considerable variation over the past century, but with no clear long-term trend (27,146). The past 60 years have been characterised by an increase in European storminess, with a strong increase from the 1960s to the 1990s and a decline thereafter. The extent to which this is part of natural variability or related to anthropogenic climate change is not known and needs further investigation. Long-term changes in European storminess are not yet clear as studies taken as a whole are inconclusive, with sometimes conflicting results (70).


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Impacts on glaciers until now

Europe

A general loss of glacier mass since the beginning 
of the measurements has occurred in all European glacier regions, except some glaciers in Norway. The Alps have lost roughly 50 % of their ice mass since 1900 (148). Norwegian coastal glaciers were expanding and gaining mass up to the end of the 1990s owing to increased winter snowfall on the North Atlantic Coast; now these glaciers are also retreating (149).


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Main contributors to global sea level rise, update 2000-2023
Contributor Period of observations Contribution to sea level rise Source
Changes in ocean temperature and salinity 2003–2016 1.19 ± 0.17 mm per year Horwath et al., 2022
Glaciers 2002–2021 0.72 ± 0.04 mm per year Zemp. et al., 2025
Greenland Ice Sheet 2002–2021 0.62 ± 0.06 mm per year Otosaka et al., 2023

The data on ice loss in this update are a few percent less negative than estimates in the latest IPCC reports. However, the experts stress that “we are facing continued and possibly accelerated mass loss until the end of this century” (271). 

Globally: previous results 1961-2016

Global glacier mass changes and their contributions to sea level rise have been quantified from 1961 to 2016. This was done by repeated mapping and differencing of glacier surface elevations from in situ, air-borne and spaceborne surveys, in combination with time series of in situ point measurements on glaciers (200).

Glaciers distinct from the Greenland and Antarctic ice sheets cover an area of approximately 706,000 square kilometres globally (201). Their total ice volume equals 0.4 metres of potential sea level rise (202). The quantification of global glacier mass changes reveals that glaciers contributed 27 ± 22 millimetres to global mean sea level rise from 1961 to 2016, or a contribution of 0.5 ± 0.4 mm per year when a linear rate is assumed. The present glacier mass loss is equivalent to the sea level contribution of the Greenland Ice Sheet (203), and clearly exceeds the loss from the Antarctic Ice Sheet (204). It accounts for 25% to 30% of the total observed sea level rise, which ranged between 2.6 and 2.9 ± 0.4 mm per year over the satellite altimetry era (1993 to mid-2014) (205).

When annual rates are averaged over periods of five years, sea level contributions ranged between 0.2 and 0.3 mm per year until the 1980s, and then increased continuously to reach 1.0 mm per year in recent years (2011–2016) (200).

Under present ice-loss rates, most of today’s glacier volume would thus vanish in the Caucasus, Central Europe, the Low Latitudes, Western Canada and the USA, and New Zealand in the second half of this century. However, the heavily glacierized regions of the world would continue to contribute to sea level rise beyond this century, as glaciers in these regions would persist but continue to lose mass (200).

In the northern hemisphere, 1,704 glaciers touched the ocean in 2000. 85.3% of these glaciers retreated between 2000 and 2020 and are now reduced in area. Only 2.5% of glaciers advanced or increased in area. The remaining 12.3% did not change within uncertainty limits. Total area losses were 389.7 ± 1.6 km2 per year over the 20-year period. Glaciers flowing from the Greenland Ice Sheet accounted for over 60% of total area losses (243).

Climate change scenarios

Scenarios for the 5th IPCC report

For the Fifth Assessment Report of the IPCC a different type of climate change scenarios has been defined than for the previous IPCC reports: the so-called Representative Concentration Pathways (RCPs) (73). In contrast to the previous SRES scenarios, RCP scenarios do not specify socioeconomic scenarios, but assume pathways to different target radiative forcing at the end of the twenty first century. For instance, scenario RCP8.5 assumes an increase in radiative forcing of 8.5 W/m2 by the end of the century relative to pre-industrial conditions. The reduction in emissions necessary to limit the forcing to this level is supposed to be reached with air quality legislation but without a strict climate policy. 


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Air temperature changes in Europe in the 21st century

Latest projections (2021) for Europe overall

Mainline: The latest projections of future temperatures over Europe show that warming will be largest both in the northernmost latitudes (Norwegian Sea, Scandinavia, and Russia) and in the southern part of Mediterranean Europe (mainly in the Iberian Peninsula and Turkey). The lowest warming is projected to occur in the British Isles and surrounding areas. In northern Europe, in particular the coldest winters will be less cold in the future; warming will be relatively high for minimum winter temperatures. In southern Europe, on the other hand, the hottest summers will be much hotter; warming will be relatively high for maximum summer temperatures (244).


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Projected change in median surface air temperature (°C) by the mid- and end of the 21st century relative to present day (1986–2005) for northern Europe for RCP2.6 (32 models), RCP4.5 (42 models) and RCP8.5 (39 models) as well as the 25th and 75th percentiles of the model results (numbers between brackets) (106).
Period Season RCP4.5 RCP8.5
2046 - 2065 Winter (December - February) 2.7 (1.8 - 3.5) 3.4 (2.9 - 4.7)
Summer (June - August) 1.8 (1.2 - 2.5) 2.5 (1.9 - 3.2)
Annual mean 2.0 (1.6 - 2.8) 2.9 (2.4 - 3.5)
2081 - 2100 Winter (December - February) 3.4 (2.6 - 4.4) 6.1 (5.3 - 7.5)
Summer (June - August) 2.2 (1.6 - 3.0) 4.5 (3.5 - 5.8)
Annual mean 2.7 (2.1 - 3.5) 5.0 (4.3 - 6.3)

Southern Europe

According to a large number of models (GCM’s), surface mean air temperatures of the larger Mediterranean basin will increase mostly in summer and least in winter in 2070  - 2100 with respect to reference period of 1970 - 2000 under the A2, A1B and B1 emissions scenarios. Especially in summer, it is very likely that extreme climatic conditions will be more severe in the Mediterranean Basin in 2100 (89). 

It is expected that summer warm-up will be twice as fast in Southern Europe than in Northern Europe (39).

An analysys based on the outcomes of a large number of models (GCM’s) shows that the Mediterranean region is likely to warm at a rate about 20% larger than the global annual mean surface temperature in the second half of this century, with values particularly large in summer and in the continental areas north of the basin (where warming will be in general 50% larger than at global scale and locally even twice as large). Day temperatures are likely to increase more than night temperatures and summers more than winters leading to an increase of amplitude of both daily and annual temperature range (179).  

Heat wave changes in Europe in the 21st century

Since 2003, Europe has experienced several extreme summer heat waves (2003, 2006, 2007, 2010, 2014 and 2015). Such heat waves are projected to occur as often as every two years in the second half of the 21st century under a high emissions scenario (RCP8.5). The impacts will be particularly strong in southern Europe (146). 
The average number of heat waves increases from one every 3-5 summers (1961-1990) to about 2-3 heat waves per season at the end of this century (2071-2100), heat waves being defined as a spell of at least six consecutive days with maximum temperatures exceeding the local 90th percentile of the control period (1961-1990) (34).


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Dry spell changes in Europe in the 21st century

The first results of the high-resolution (horizontal resolution of 12.5 km) future climate simulations (from the EURO-CORDEX program) address changes in annual mean temperature and total precipitation across Europe for three scenarios (A1B, RCP4.5 and RCP8.5) and the time periods 2021–2050 and 2071–2100 (compared with 1971–2000). For these simulations a large number of regional and global climate models have been used (72). According to these results, a small increase in the length of extended dry spells is projected for Central Europe in 2071–2100 (compared with 1971–2000) for the moderate scenarios RCP4.5 and A1B. A decrease in the length of extended dry spells is calculated for this period in A1B for parts of Scandinavia. Under RCP8.5 more but shorter dry spells are projected in the alpine region (72). Under RCP8.5, shifts in drought pattern strengthen the projected dryness over the Mediterranean owing to the occurrence of more persistent droughts. In general, the number of droughts will reduce over Europe as consequence of projected increases in length (232).

Changes in temperature variability in Europe in the 21st century

Numerous studies conclude that a change in variance of the temperature Probability Density Function (PDF) has a greater impact on the frequency and duration of extremes than just a shift in the mean (8). Recent studies show that by 2071 to 2100, summer temperature variability is expected to have increased by up to 100% in central Europe (33). Winter temperature variability and the number of cold and frost extremes are projected to decrease further (1,62). In agreement with these results it was concluded a robust signal across a large number of global and regional climate model projections that in summer and south-central Europe hot extremes warm stronger than the mean, and in winter and northern Europe cold extremes warm stronger than mean temperatures (56).

Precipitation changes in Europe in the 21st century

Annual and seasonal precipitation

The first results of the high-resolution (horizontal resolution of 12.5 km) future climate simulations (from the EURO-CORDEX program) address changes in annual mean temperature and total precipitation across Europe for three scenarios (A1B, RCP4.5 and RCP8.5) and the time periods 2021–2050 and 2071–2100 (compared with 1971–2000). For these simulations a large number of regional and global climate models have been used (72). According to these results, in large parts of Central Europe and Northern Europe annual precipitation may increase in 2071–2100 (compared with 1971–2000) up to about 25 % and decrease in Southern Europe. For winter in this period, RCP8.5 projects strongest increases in heavy precipitation (up to 35 %) in Central and Eastern Europe. The moderate RCP4.5 scenario shows a similar pattern of changes, though less pronounced. The spatial pattern for the A1B precipitation changes qualitatively agrees with the described changes for RCP4.5 and RCP8.5, and the magnitude of the changes mostly lies in-between the two RCPs (72).


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Hail events changes in Europe in the 21st century

Future projections of hail events are subject to large uncertainties, because small-scale hail events cannot be directly represented in global and regional climate models. However, model-based studies for central Europe show some agreement that hailstorm frequency will increase in this region (146). For Europe in general, an increase in the frequency and severity of hailstorms is expected, although current and future climate change effects on hailstorms remain highly uncertain (264). 


Lightning frequency changes in Europe in the 21st century

At the local scale, thunderstorms are the most common source of hazardous weather. Projections of future changes are highly uncertain, however. This is because it is very difficult to include the local conditions that induce these local storms in conventional climate models. As a result, it is also very difficult to project changes in the frequency of lightning. This information is more important than you might think at first glance. The vulnerability of the Arctic region to wildfires is increasing, for instance, because of the thawing of the permafrost, and lightning is the main trigger. Observations already indicate an increase in Arctic lightning (248) and convective storms are projected to triple in frequency and extend to the northernmost regions of Alaska under future climate conditions (249).


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Snow cover changes in Europe in the 21st century

The IPCC concluded in 2019 that at lower elevation in many regions such as the European Alps, the snow depth or mass is projected to decline by 25% (likely range between 10 and 40%), between the recent past period (1986-2005) and the near future (2031-2050), regardless of the greenhouse gas emission scenario. This corresponds to a continuation of the ongoing decrease in annual snow cover duration (on average 5 days per decade, with a likely range from 0 to 10). By the end of the century (2081-2100), reductions of up to 80% (likely range from 50 to 90%) are expected under RCP8.5, 50% (likely range from 30 to 70 %) under RCP4.5 and 30% (likely range from 10 to 40 %) under RCP2.6 (216).


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Ice cover changes in Europe in the 21st century

Ice provides a range of ecosystem services, including fish harvest, cultural traditions, transportation, recreationand regulation of the hydrological cycle, to more than half of the world’s 117 million lakes. An extensive loss of lake ice will occur within the next generation. From a comprehensive large-scale assessment of lake ice loss in the Northern Hemisphere it was estimated that 14,800 lakes in the Northern Hemisphere currently experience intermittent winter ice cover, increasing to 35,300 and 230,400 at 2°C and 8°C global warming, respectively, impacting up to 394 and 656 million people (193). 

Wind climate changes in Europe in the 21st century

A belt stretching from the United Kingdom to Poland will experience an increase in extreme wind speed, while Southern Europe and the Mediterranean will rather see a decrease in strong winds (69). An extension of the Atlantic storm track to the northeast is projected in combination with a narrowing of the storm track over western Europe (109). Projections of changes in storm frequency and intensity are still very uncertain, however, and model-dependent. From different studies different, and sometimes contradictory, results have been reported.

In a recent review on storminess over the North Atlantic and north-western Europe, projected changes were summarized in both storm frequency and storm intensity on the basis of numerous recent studies that assessed potential future change in these two aspects of storms on the basis of climate scenario simulations with different kinds of models. For the North Sea region, most of these studies showed a future increase in storm frequency and storm intensity (110). 


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Cyclones in Europe in the 21st century

The chance of a tropical cyclone reaching Europe appears to be increasing. Since the 1970s, the speed at which the onset of a storm over the Atlantic Ocean develops into a cyclone has increased (265). Moreover, the season in which these cyclones can form is becoming longer and longer (266).


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Impacts on glaciers in the 21st century

Changes in glacier mass for all glaciers in the world have been modelled for climate change projections based from 14 global climate models and two emission scenarios (midrange scenario RCP4.5 and high end scenario RCP8.5; these are the scenarios for the Fifth Assessment Report of the Intergovernmental Panel on Climate Change). These results suggest a mean reduction of the current global glacier volume by 29% (RCP4.5) or 41% (RCP 8.5) over the period 2006–2100. This equals a contribution of these glaciers to sea level rise of 155 ± 41 mm (RCP4.5) and 216 ± 44 mm (RCP8.5); these numbers are multi-model means ± one standard deviation (65).


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Arctic sea-ice cover  in the 21st century

The Arctic summer sea-ice cover normally reaches its annual lowest extent in September. The lowest sea ice extent so far was reached in September 2012. The recent Paris Agreement has inspired many scientists to study the differences in impacts between 1.5 °C and 2.0 °C global warming (above pre-industrial conditions). One of these studies focused on the impact on summer Arctic sea ice extent (185).


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Adaptation - Cooling potential - A European-wide impression

The temperature in cities is generally higher than in the surrounding rural environment. This urban heat island effect adds to the impact of climate change and increases heat stress for city dwellers. The observed increase of heat-related mortality during heatwaves is not only due to the weather itself but also results from this urban heat island effect. We can’t do much about the weather, but we can reduce this additional heat island effect. Two of the most promising measures are greening (trees, shrubs and grass) and less pavement. The resulting increase of shading, evaporation and transpiration by plants will reduce air temperature.


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Adaptation - The cooling potential of trees

Trees can cool cities on a hot day. For 293 European cities, this effect was clear from an analysis of satellite data of land surface temperatures and land-cover (233). Trees influence urban climate primarily via shading and transpiration. In addition, differences in albedo between urban trees and urban fabric play a minor role.


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References

The references below are cited in full in a separate map 'References'. Please click here if you are looking for the full references for Europe.

  1. EEA, JRC and WHO (2008)
  2. IPCC (2007)
  3. Böhm et al. (2001), in: EEA, JRC and WHO (2008)
  4. Klein Tank (2004), in: EEA, JRC and WHO (2008)
  5. Klein Tank et al. (2002), in: EEA, JRC and WHO (2008)
  6. Luterbacher et al. (2004), in: EEA, JRC and WHO (2008)
  7. Schär and Jendritzky (2004), in: EEA, JRC and WHO (2008)
  8. Della-Marta et al. (2007)
  9. Klein Tank and Können (2003); Alexander et al. (2006); Moberg et al. (2006), all in: Della-Marta et al. (2007)
  10. Klein Tank et al. (2005); Moberg and Jones (2005), both in: Fischer and Schär (2009)
  11. Stott et al. (2004), in: Nicholls and Alexander (2007)
  12. Lorenz et al. (2019)
  13. Jones and Moberg (2003), in: Alcamo et al. (2007)
  14. Eisenreich (2005)
  15. Norrant and Douguédroit (2006), in: EEA, JRC and WHO (2008)
  16. Klein Tank et al. (2002), in: EEA, JRC and WHO (2008)
  17. Nicholls and Alexander (2007)
  18. Klein Tank and Können (2003); Groisman et al. (2004), both in:Nicholls and Alexander (2007)
  19. Scherrer et al. (2004), in: EEA, JRC and WHO (2008)
  20. Vojtek et al.(2003), in: EEA, JRC and WHO (2008)
  21. Rodriguez et al. (2005), in: EEA, JRC and WHO (2008)
  22. Petkova et al.(2004), in: EEA, JRC and WHO (2008)
  23. Falarz (2002), in: EEA, JRC and WHO (2008)
  24. Kohler et al.(2006), in: EEA, JRC and WHO (2008)
  25. Hyvärinen (2003), in: EEA, JRC and WHO (2008)
  26. Magnuson et al. (2000), in: EEA, JRC and WHO (2008)
  27. von Storch et al. (2002), in: EEA, JRC and WHO (2008)
  28. Lionello (2005), in: EEA, JRC and WHO (2008)
  29. Christensen et al. (2007), in: EEA, JRC and WHO (2008)
  30. Giorgi et al. (2004); IPCC (2007a), both in: EEA, JRC and WHO (2008)
  31. IPCC (2007a, 2007b); ACIA (2004), all in: EEA, JRC and WHO (2008)
  32. Kjellström (2004)
  33. Schär et al. (2004); Weisheimer and Palmer (2005), both in: Della-Marta et al. (2007)
  34. Fischer and Schär (2009)
  35. Beniston et al. (2007), in: Alcamo et al. (2007)
  36. Räisänen et al. (2004); Kjellström et al. (2007), both in: Alcamo et al. (2007)
  37. Meehl and Tebaldi (2004)
  38. Beniston et al. (2007)
  39. Eisenreich (2005)
  40. Sillmann and Roeckner (2008), in: EEA, JRC and WHO (2008)
  41. Frei et al. (2006)
  42. Kiktev et al. (2003, 2004); Hegerl et al.(2004), all in: Frei et al. (2006)
  43. Good et al. (2006), in: Alcamo et al. (2007)
  44. Kjellström, 2004; Räisänen et al., 2004, both in: Alcamo et al. (2007)
  45. ACIA (2004)
  46. Jylhä et al. (2007), in: EEA, JRC and WHO (2008)
  47. Hosaka et al. (2005), in: EEA, JRC and WHO (2008)
  48. Bender et al. (2010)
  49. IPCC (2000)
  50. Beniston (2004)
  51. Min et al. (2011), in: Coumou and Rahmstorf (2012)
  52. Wang et al. (2006); Chang and Guo (2007); Seidel et al. (2008); Ulbrich et al. (2009); Vilibic and Sepic (2010); Bender et al. (2011), in: Coumou and Rahmstorf (2012)
  53. Coumou and Rahmstorf (2012)
  54. Barriopedro et al. (2011)
  55. Luterbacher (2004), in: Barriopedro et al. (2011)
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