The eastern Mediterranean and Middle East, a region with diverse socioeconomic and cultural identities, is exposed to strong climatic gradients between its temperate north and arid south. Model projections of the twenty-first century indicate increasing hot weather extremes and decreasing rainfall. We present model results, which suggest that across the Balkan Peninsula and Turkey climate change is particularly rapid, and especially summer temperatures are expected to increase strongly. Temperature rise can be amplified by the depletion of soil moisture, which limits evaporative cooling, prompted by the waning of large-scale weather systems that generate rain. Very hot summers that occurred only rarely in the recent past are projected to become common by the middle and the end of the century. Throughout the region, the annual number of heat wave days may increase drastically. Furthermore, conditions in the region are conducive for photochemical air pollution. Our model projections suggest strongly increasing ozone formation, a confounding health risk factor particularly in urban areas. This adds to the high concentrations of aerosol particles from natural (desert dust) and anthropogenic sources. The heat extremes may have strong impacts, especially in the Middle East where environmental stresses are plentiful.
Climate gradients in the eastern Mediterranean and Middle East (EMME) can be very pronounced (Issar and Zohar 2007; Lionello et al. 2006). Given the proximity of the EMME to the Indian and Atlantic Oceans and the extensive land areas of Eurasia and Africa, associated with contrasts between maritime and continental air masses and diverse meteorological characteristics, it is at the crossroads of many global weather and climate patterns. A large fraction of the annual precipitation in the area falls during winter, often related to major North Atlantic synoptic systems, promoted by low-level baroclinicity and moisture from the Mediterranean Sea and modulated by the local orography (Krichak et al. 2007; Lionello et al. 2006). During spring, the mid-latitude zone of baroclinicity retreats northwards, and in summer, the region is subject to tropical influences, primarily the South Asian monsoon, leading to enhanced subsidence which suppresses clouds and rain (Alpert et al. 2005; Rodwell and Hoskins 1996; Tyrlis et al. 2013). Data analyses and climate model projections suggest an overall drying and warming of the region, especially in summer (Christensen et al. 2007; Evans 2009, 2010; Gao and Giorgi 2008; Kitoh et al. 2008; Lelieveld et al. 2012; Önol and Semazzi 2009; Tanarhte et al. 2012). This is accompanied by enhanced risks of heat extremes, which are the focus of the current study.
Heat waves can have profound impacts on human health, power systems, economies, ecosystems and agriculture (Battisti and Naylor 2009; Beniston et al. 2007; Haines et al. 2006). Mortality rates can more than double due to cardiovascular, cerebrovascular and respiratory ailments, while infants and the elderly bear the greatest risk (Anderson and Bell 2011; Knowlton et al. 2009). Cities are most strongly affected because of the accumulation of air pollution under stagnant meteorological conditions and other confounding health risk factors (Basu and Samet 2002; Fischer et al. 2012; Knowlton et al. 2004). In summer 2003, an extensive heat wave hit large parts of Europe. Average summer temperatures were about 3 °C higher than the long-term mean, and in major cities, the daily maximum temperature exceeded 35 °C for more than a week, causing about 70,000 excess deaths in parts of southern, western and central Europe (Robine et al. 2006; Schär et al. 2004; Vandentorren et al. 2006). Global and regional climate model simulations suggest that heat waves will increase in particular in southern Europe (Diffenbaugh et al. 2007; Meehl and Tebaldi 2004; Fischer and Schär 2010). Here, we extend these studies to the EMME, based on climate and atmospheric chemistry model projections for the twenty-first century, focusing on heat extremes and air pollution in metropolitan areas.
We used the regional climate model PRECIS (Providing Regional Climates for Impact Studies) at 0.22° latitude/longitude, that is, ~25-km grid resolution (Jones et al. 2004). It applies the same formulation of the climate system as its parent atmosphere–ocean general circulation model, HadCM3, which provides the lateral boundary conditions (Collins et al. 2006). The PRECIS model describes the dynamical flow, the atmospheric sulfur cycle, clouds and precipitation, radiative processes, the land surface and the deep soil (Jones et al. 2004). The sulfur cycle has been included to account for the direct effects of sulfate aerosols on climate through the scattering of solar radiation. The version of PRECIS used includes the Met Office Surface Exchange System (MOSES), which represents soil and vegetation processes and calculates energy, moisture and CO2 fluxes (Cox et al. 1999; Zittis et al. 2013).
We simulated climate conditions in the EMME over the period 1950–2099 driven by the Special Report on Emissions Scenarios (SRES) intermediate scenario A1B, accounting for greenhouse gases, including ozone, and sulfate aerosols. The emission scenarios A1B, A2 and B2 applied in the PRECIS model have been developed for the Intergovernmental Panel on Climate Change, described by Nakićenović and Swart (2000) (see also http://en.wikipedia.org/wiki/Special_Report_on_Emissions_Scenarios). We also performed sensitivity simulations based on the SRES emission scenario B2 with relatively low greenhouse gas emissions and the A2 scenario with relatively high emissions for the period 2070–2099. The results for the future are contrasted to those obtained for the reference period 1961–1990.
We compared the PRECIS output to observations of recent climate conditions and found that the model realistically simulates observed weather patterns and indices of extremes. For example, the mean number of days per year with maximum temperatures above 25 °C agrees within about ±10 % with meteorological data since 1950, and the number of consecutive dry days per year matches the analyses of observations within about ±15 % (Lelieveld et al. 2012). We used the model to calculate temperature trends for the period 2000–2099 and changes in heat waves for the three scenarios. The heat wave day index (HWD90) is defined as a spell of at least six consecutive days with maximum temperatures exceeding the local 90th percentile of the reference period. It is calculated using the RClimDex software of X. Zhang, as mentioned by Klein Tank et al. (2009) and applied by Zhang et al. (2005) and Klok and Klein Tank (2009). Although we also present results for the 95th and 99th percentile, HWD95 and HWD99, respectively, we focus on HWD90 because only for this metric observational data are available to compare with the model results.
It should be emphasized that even though the model does not explicitly resolve metropolitan areas, hot weather is related to synoptic-scale conditions which are generally well represented. The calculated daytime maximum temperatures (TX) in the EMME agree well with observations collected in the Climatic Research Unit (CRU) TS3.0 dataset until the year 2005 (Lelieveld et al. 2012; Mitchell and Jones 2005). Note that this CRU dataset has been compared to other meteorological datasets available for the region, and outliers and inconsistencies were not detected, in contrast to other datasets (Tanarhte et al. 2012). The PRECIS predictions are consistent with other climate projections as the results of the parent global model (HadCM3) are well within those of the ensemble mean of the 23 atmospheric-ocean general circulation models of the Intergovernmental Panel on Climate Change (IPCC) (Meehl et al. 2007). Kharin et al. (2007) analyzed the weather extremes calculated by the global climate models participating in the IPCC Fourth Assessment Report and concluded that the models simulate present-day warm extremes reasonably well compared to meteorological re-analysis data. Furthermore, the PRECIS results are qualitatively consistent with those of previously published high-resolution climate model studies (Evans 2010; Kitoh et al. 2008; Krichak et al. 2011; Önol and Semazzi 2009; Smiatek et al. 2011).
To test the performance of PRECIS against other regional climate models, we computed changes in TX for 12 capital cities in the EMME between the reference period 1961–1990 and 2021–2050 and compared with the ensemble mean of nine regional climate models (Fig. 1). The comparison is limited to the eastern Mediterranean and the period 2021–2050 because the projects ENSEMBLES (http://www.ensembles-eu.org/) and CIRCE (Climate Change and Impact Research: The Mediterranean Environment, http://www.circeproject.eu/), for which these calculations have been performed, focused on the European-Mediterranean domain, and they did not extend beyond 2050 (Gualdi et al. 2011; Kjellström and Giorgi 2010). The model inter-comparison indicates that the PRECIS results overlap with the ensemble mean. The model inter-comparison indicates that the PRECIS results are generally within the range of the ensemble mean. In addition to Fig. 1, this is illustrated in Figure S1 in the Supplementary Data, showing the annual and seasonal mean TX changes for 12 cities throughout the region. However, especially in summer (June–August), the maximum temperatures tend toward the high end of the multi-model spread, possibly indicating a warm bias, especially in the northern part of the model domain, for example, in Belgrade and Sofia. Nevertheless, the PRECIS results agree very well with the ensemble mean in autumn, winter and spring (Figure S1), while the model simulation of relatively warm summers leads to a slight warm bias in the annual mean (Fig. 1).
Further, we employed the ECHAM5/MESSy Atmospheric Chemistry (EMAC) general circulation model to investigate changes in the regional air quality (Jöckel et al. 2005; Roeckner et al. 2006; Sander et al. 2005). Extensive model evaluations have been performed based on in situ and remote sensing observations (Jöckel et al. 2006; Pozzer et al. 2007, 2010; Tost et al. 2007; Pringle et al. 2010; Liu et al. 2011). The model has been used at T106L31 resolution, corresponding to a latitude × longitude grid spacing of about 1.1° × 1.1° and a vertical resolution of 31 levels up to 10 hPa in the lower stratosphere. The model setup used in this work has been described and evaluated by Pozzer et al. (2012a) for the year 2005, which we use as a baseline simulation.
We also simulated a future air quality scenario for 2050, comparable to the SRES scenario A1B (Pozzer et al. 2012b). The emission scenario includes nitrogen oxides (NOx), carbon monoxide (CO), non-methane volatile organic compounds (NMVOCs), ammonia (NH3), sulfur dioxide (SO2), black carbon (BC) and particulate organic matter (POM) from fossil fuel and biofuel combustion, industrial processes and the production and usage of solvents, agriculture and waste treatment. The emission totals of all countries in the base year 2005 were projected up to 2050. Comparable to Shindell et al. (2012), the projections differentiate between climate change and air pollution control measures because the implementation of the former requires a longer process of structural changes compared to the latter. The scenario assumes that no additional emission control measures are taken beyond those implemented in 2005. The future emissions of pollutants lead to a stabilization of present-day air quality. For example, the projected global CO and BC emissions for the year 2050 are 559 and 5.4 Tg/year, respectively, being 4.7 and 8.4 % less compared to those in 2005.
Beyond 2005, no change in technologies for combustion (power industry, transport), industrial processes (steel, cement, chemicals), waste treatment and agriculture is assumed. Either the activity data or the emission factors are scaled up. Nevertheless, improvements in energy efficiency of the technologies already in place in the year 2005 are expected for the projected years. The solvent-related activities are driven only by population, while the energy-related activities are driven by population and economic growth, following the projected oil, gas and coal markets for the different world regions (Pozzer et al. 2012a, b). This assumes a continuation of the trend from 1990 to 2005, hence the energy consumption relative to the GDP is assumed to decline further, which is more than offset by economic growth and is projected to be 79 % above 2005 levels by 2050.
The fossil fuels dominate (75 %) the fuel mix until 2030, and then, they are expected to decrease by 10 % assuming that renewable and nuclear power will grow. These assumptions are in line with those incorporated in world energy models from the International Energy Agency (IEA) World Energy Outlook 2006. The agriculture-related activities are mainly driven by population and corresponding food demand and follow the projected global agricultural trade with regional food prices and with livestock cropland. The global agricultural production is assumed to grow by more than 50 % through increased productivity and an extension of the agricultural area with about 10 % (Pozzer et al. 2012b).
It should be emphasized that these air quality model calculations do not account for climate change, and the comparison between the results for 2005 and 2050 is based on differences in atmospheric composition only. Preferably, the air quality and climate change calculations should be performed with an online coupled regional chemistry-climate model. Since such models that also include comprehensive representations of atmospheric chemistry and aerosols are not commonly available, also because computational costs are prohibitive, recent studies have used offline regional air quality models (Jiménez-Guerrero et al. 2012) or statistical relationships between air pollution and meteorological variability related to meteorological fields projected by global climate models (Tai et al. 2012). The effects of climate change on air quality found in these studies are relatively small. The largest impacts are expected from the changing emissions of biogenic compounds (Langner et al. 2012; Young et al. 2013), being insignificant in the region considered here, and of dust emissions. Since we apply our global model at relatively high resolution and focus on anthropogenic air pollution we expect that inconsistencies between our regional and global models are not significant.
Results and discussion
Tables 1 and 2 present the model-calculated temperature trends and the projected future changes of high temperature extremes at 18 major metropolitan locations in the eastern Mediterranean and Middle East. For comparison, Table 2 also includes observations (Klok and Klein Tank 2009; Zhang et al. 2005). For the cities Baghdad (at 33.3°N, 44.4°E) and Damascus (at 33.5°N, 36.3°E), the nearby stations of Kut-Al-Hai (32.2°N, 46.1°E) and Mafraq (32.4°N, 36.3°E) have been used, respectively. The Iranian city Abadan is included because it is located in the Arabian Gulf region for which observations are otherwise scarce. Table 1 indicates that in the northern EMME, TX generally increases more rapidly than the mean temperature TM (e.g., Ankara, Belgrade, Damascus, Sofia, Tehran, Tirana), which we attribute to atmosphere-surface feedbacks, as discussed in more detail below. In the southern EMME, the daily minimum temperature TN increases more rapidly than TM (e.g., Baghdad, Cairo, Riyadh, Tripoli and along the Arabian Gulf) related to an increase in cloudiness, which reduces nighttime radiative cooling.
Figures 2 and 3 show model projections of daytime maximum (TX) and nighttime minimum (TN) temperature during summer by the middle and the end of the twenty-first century. They also show the 95-percentile confidence ranges obtained by bootstrapping (Giannakopoulos et al. 2009). The ranges in the lower panels are the differences between the upper and lower confidence limits. For example, our analysis indicates 95 % confidence that the rise in TX by the end of the century will be between 3.5 ± 0.4 in southern Iran and 7 ± 1.3 °C in the northern Balkan region, that is, varying with subregion, signifying an uncertainty range of about 15 % (similar for TN). In the northern EMME, from Italy, the Balkans, Turkey, Georgia up to southern Russia, TX increases very steeply up to 4–5 °C by mid-century and 5–7 °C by the end of the century; more strongly than TN.
The latter is a consequence of a decrease in cyclonic weather events, notably in the spring transition season when the baroclinic zone weakens rapidly. The weakening of the Mediterranean storm track may be considered a robust result of climate change studies, based on observations and model projections (Bengtsson et al. 2006; Trigo et al. 2000; Ulbrich et al. 2009). Consequently, the cloud cover decreases, which enhances solar radiation absorption at the surface and increases TX. This accelerates evaporation and promotes the depletion of soil moisture, which is also influenced by a general decrease in the relative humidity. In turn, this reduces evaporative cooling, which is balanced by sensible heating. Since the soil moisture reservoir can act as a “memory” of precipitation anomalies for weeks to months, the effect persists into the summer (Seneviratne et al. 2010; Zittis et al. 2013). We refer to Zittis et al. (2013) for a more in depth analysis.
This positive feedback mechanism through soil moisture has been proposed as an important cause of heat stress intensification, including the European heat wave in 2003 (Diffenbaugh et al. 2007; Vautard et al. 2007). Its importance is corroborated by direct observational evidence in southeastern Europe (Hirschi et al. 2011) and indirectly by the observed increase in heat waves in the Balkans and Turkey (Kuglitsch et al. 2010). Further north this mechanism is less relevant since precipitation either declines less or increases, and temperatures are lower, whereas further south the soils are barren anyhow. In the region around the Arabian Gulf, we actually find a reverse tendency, as the model predicts that clouds and precipitation increase. This is a consequence of the expanding influence from the humid tropics (Evans 2009, 2010). The increasing cloudiness moderates the trend in TX and increases it in TN by limiting radiative cooling during the night. This explains why TN increases more uniformly throughout the EMME than TX. The lack of nighttime cooling in this region can actually exacerbate the impact of heat waves.
Even though the Gulf States may expect increasing precipitation, the absolute amounts are small and the model predicts an overall regional rainfall reduction throughout the domain of 10–25 % by 2040–2069, up to about 30 % by 2070–2099, mostly in the eastern Mediterranean, Greece, southern Turkey, the coastal Levant and North Africa, similarly as projected by previous studies (Evans 2009, 2010; Gao and Giorgi 2008; Kitoh et al. 2008; Önol and Semazzi 2009). This implies, for example, that by 2040–2069, the discharges of the Tigris-Euphrates and Jordan River systems will decrease by about 10 and 20–25 %, respectively, with further decreases by the end of the century (Önol and Semazzi 2009; Chenoweth et al. 2011). By also accounting for population growth rates, the per capita available internal water resources in several countries may decline strongly. In Jordan, Cyprus and Syria, they may fall by 50 % or more by mid-century, and substantial decreases are also expected for Greece, Lebanon, Israel and the Palestine territories (Chenoweth et al. 2011).
Our model results suggest important changes in heat extremes. In view of the particularly harmful effects of heat waves in cities, we focus on the main capitals in the region. In the EMME, most people live in the urban environment and more than 20 % in cities with more than one million inhabitants. A classification of heat waves must relate high temperatures to local conditions to which indigenous populations are accustomed and have adapted. Accordingly, the heat wave days HWD90 index is defined relative to the local temperature regime during the reference period 1961–1990 (Fischer and Schär 2010; Zhang et al. 2005). Clearly, the dangers of dehydration and hyperthermia, when the body is unable to dissipate its metabolic heat, are highest in areas where summers are hottest. In parts of the Middle East, for example, mean summer temperatures close to the human body temperature of 37 °C are already common.
Our model calculations for the twenty-first century predict strong mean temperature trends in all major cities, varying between 0.35 and 0.49 °C per decade (Table 1). Relatively strong trends are projected to occur in inland locations such as Ankara, Baghdad, Belgrade, Damascus, Riyadh and Sofia where the annual mean temperature increases more than 0.4 °C per decade. Smaller trends are calculated at coastal and island locations, such as Beirut, along the Arabian Gulf, Nicosia and Tripoli. The results indicate that the trends of warm extremes typically follow those of the mean summertime temperatures. An important aspect of the growing occurrence of heat extremes in the EMME is that the summer temperatures increase relatively strongly, that is, more rapidly than in winter. This contrasts with model predictions for central and northern Europe where temperatures are expected to rise more strongly in winter instead (Christensen et al. 2007). Therefore, the relatively steep increase in the maximum temperature TX in summer and the number of heat wave days is remarkable but perhaps not surprising.
In Section 11.3 of IPCC (2007), the relatively strong increase in summer temperatures in the Mediterranean area is classified as “likely” based on climate change projections by global and regional models. Figure 4 and Table 2 (also Figures S2 and S3) show that the rising temperatures are associated with sharp increases in the number of heat wave days HWD90, notably since 1990, in agreement with observations from the 1950s up to the early 2000s (Efthymiadis et al. 2011; Zhang et al. 2005). It should be noted that the PRECIS projections of TX in summer tend toward the high end of the ranges derived from the ensemble mean of nine regional European climate models, as shown in Figs. 1 and S1. This pertains in particular to locations in the Balkans and the Anatolian Peninsula, where the positive feedback between reduced precipitation and the loss of soil moisture is expected to be most relevant. Therefore, it cannot be ruled out that our results are to some degree model dependent and may overestimate the summertime heating anomalies.
The PRECIS results also suggest a general increase in the inter-annual variability, which can add substantially to the intensity of heat extremes (Fischer and Schär 2010; Schär et al. 2004). The number of heat wave days typically increases by a factor of 4–10 by the middle and 7–15 by the end of the century, with the strongest increases in the Middle East. Tables S1 and S2 also present calculations for stricter definitions of heat extremes to account for the exceeding of local 95th and 99th percentiles (HWD95 and HWD99), which indicates similar rates of increase. Sensitivity simulations based on different greenhouse gas emission assumptions suggest that the more pessimistic scenario A2 further enhances the number of heat wave days compared to the A1B projections, though not very strongly in all cities. The more optimistic scenario B2 substantially reduces their number by 30–50 %, though they are still strongly enhanced compared to the reference period (right panels of Fig. 4 and Figure S3).
Our results for the A1B scenario suggest that by the end of the century, the frequency of very hot days (TX > 35 °C) may increase up to 1–2 weeks per year in mountainous parts of the northern EMME and by about a month in much of the rest of the region. The strongest increases appear in the coastal Levant and North Africa (>2 months/year). The frequency of “tropical” nights (TN > 25 °C) also increases strongly, by nearly a month per year in the Balkans and coastal areas, and more than two months in the Gulf region, exacerbating the daytime heat stress. A measure of seasonal heat extremes is the frequency distribution of TX anomalies in summer. Figure 5 suggests that by the end of the century in most cities, the coolest summers may be warmer than the hottest ones during the reference period, which appears to be the case for all three scenarios considered (Figure S4).
Figure S4 presents additional frequency histograms for three emission scenarios and the 18 cities, corroborating that even the relatively optimistic scenario B2 is associated with strong changes in TX. The TX anomalies under scenario A2 are even larger, with significant frequencies of TX increasing up to 10 °C in several cities. Furthermore, especially in the Middle East, the environmental stress is aggravated by deteriorating air quality, associated with the strong growth of population, traffic and economic development. This includes several megacities such as Teheran, Istanbul and Cairo. The latter is among the megacities with poorest air quality worldwide, leading to an estimated excess mortality of about 14,000/year in the past decade (Gurjar et al. 2010). The regional meteorological conditions are conducive of photochemical air pollution, sometimes leading to extraordinary high levels of ozone and airborne desert dust (Smoydzin et al. 2012). In contrast to most of Europe, air pollution is increasing strongly in the Middle East, augmented by rising temperatures, decreasing removal by rain and the emergent fossil energy consumption for air conditioning and desalination.
The combination of anthropogenic air pollution with the abundant desert dust in the region leads to an extensive haze, especially in summer when removal by rain is inefficient. The annual mean particulate mass concentrations, calculated for the year 2005, reach up to 100 μg/m3 in the Middle East and higher over North Africa, whereas in southern Europe and over Turkey, they are typically 20–30 μg/m3. The levels are highest in the urban environment, often exceeding the European air quality standard for annual mean particulate matter (PM2.5) of 25 μg/m3 (http://ec.europa.eu/environment/air/quality/standards.htm). Recent trends of aerosol particles over most of the Mediterranean, downwind of Europe, are negative, whereas they are positive over Turkey and the Middle East (Papadimas et al. 2009; de Meij et al. 2012). Although the aerosol mass concentrations in the EMME are dominated by desert dust, our model calculations suggest that the contribution to fine particulates by air pollution will increase significantly (Pozzer et al. 2012b).
Figure 6 presents model-calculated frequency distributions of ozone mixing ratios during summer in major capitals in the EMME, both for 2005 and 2050. Clearly, in 2005 and in particular in 2050, the 8-hourly EU air quality standard of about 60 ppbv is exceeded regularly (http://ec.europa.eu/environment/air/quality/standards.htm). Whereas in many cities, such as Ankara, Athens, Beirut, Istanbul, Nicosia and Tehran, the peaks of the distribution were around 60 ppbv in the recent past, they are projected to shift to much higher values in future. While in many cities in the EMME high ozone values in summer are already typical (Lelieveld et al. 2009), it appears that by the middle of the century exceedingly high ozone mixing ratios will be commonplace, with extreme values well above 100 ppbv, especially in the Middle East. In Kuwait, for example, very high mixing ratios up to 200 ppbv are projected (Fig. 6). Since these high ozone mixing ratios typically occur during hot and stagnant weather conditions, we expect that photochemical air pollution will become an increasingly important confounding health risk factor during heat waves. It may be anticipated that the high ozone air pollution, for example, will be associated with significantly increased respiratory diseases and premature mortality (Lelieveld et al. 2013; Pozzer et al. 2012b).
Ideally, the atmospheric chemistry and climate simulations should be linked (Sect. 2). Projected climate change in the twenty-first century will likely be associated with increasingly stagnant weather conditions. Since surface ozone concentrations are correlated with temperature, a detrimental effect of warming is expected (Jacob and Winner 2009). The projected reduction in precipitation in most of the EMME will reduce the removal of particulate air pollution and increase fire events and air pollution. Nevertheless, a recent study of climate change effects on air pollution over the Iberian Peninsula indicates that the resulting increase in ozone in the twenty-first century (A2 scenario) is typically less than 10 % (Jiménez-Guerrero et al. 2012). On the other hand, emissions of black carbon and the formation of tropospheric ozone can enhance climate warming. Further, aerosol pollution exerts a surface cooling, and the particles may nucleate more cloud droplets, which makes the clouds more reflective. The surface cooling decreases evaporation and thus slows down the hydrological cycle (Ramanathan and Feng 2009). In addition, feedbacks may exist between climate change and the emissions of dust and biogenic compounds with unknown consequences. In future, work will be interesting to account for these interactions between climate change and air pollution with online coupled regional air quality–climate models, also accounting for vegetation and fire dynamics and desert dust emissions.
Our model results corroborate that climate change in the EMME is disproportionally precipitous. With 400 million inhabitants in two dozen countries, some with rapidly growing populations, the EMME may be one of the most populous areas on Earth to suffer severe impacts by climate change. In the northern EMME, a positive feedback between reduced cloudiness and rainfall and increased surface heat fluxes may accelerate climate warming during summer; though these results are to some degree model dependent and will need to be investigated further. In the southern EMME, summer temperatures are already high, and hot weather conditions are projected to increase importantly in the twenty-first century. Irrespective of the emission scenario considered (B2, A1B, A2), cities in the EMME will need to cope with strongly increasing heat extremes, and adaptation measures should be pursued. This may involve city planning, housing conditions, air conditioning and social factors (e.g., clothing). Typically, summer temperatures are expected to increase by 5°–7° by the end of the century, and in some cities increases up to 10 °C may occur, associated with very high numbers of heat wave days. Concurrently, increasing photochemical air pollution, associated with peak ozone levels in excess of 100 ppbv and high concentrations of particulates by desert dust and anthropogenic aerosols, is expected to considerably reduce air quality during heat wave conditions. Considering the multiple environmental stresses in metropolitan areas, including confounding factors such as the urban heat island effect and growing air pollution, the cities in this region will become true hot spots of climate change.
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We thank the CIMME project team for the regional climate assessment (Climate change and Impacts in the Eastern Mediterranean and Middle East) and the Hadley Centre (UK) for providing the PRECIS model. This work contributes to the European Union project CIRCE. The research leading to these results has received funding from the European Research Council under the European Union’s Seventh Framework Program (FP7/2007–2013)/ERC grant agreement no 226144.
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Lelieveld, J., Hadjinicolaou, P., Kostopoulou, E. et al. Model projected heat extremes and air pollution in the eastern Mediterranean and Middle East in the twenty-first century. Reg Environ Change 14, 1937–1949 (2014). https://doi.org/10.1007/s10113-013-0444-4
- Climate change
- Heat extremes
- Air pollution
- Urban environment
- Middle East
- Eastern Mediterranean