Strongly increasing heat extremes in the Middle East and North Africa (MENA) in the 21st century

The definition of the MENA, applied here, encompasses the larger region between Morocco and Iran, including all Middle Eastern and Maghreb countries, sometimes indicated as Greater Middle East (http://en.wikipedia.org/wiki/MENA). The 29 countries included are Algeria, Armenia, Azerbaijan, Bahrain, Cyprus, Djibouti, Egypt, Georgia, Iran, Iraq, Israel, Jordan, Kuwait, Lebanon, Libya, Mauretania, Morocco, Oman, Palestine, Qatar, Saudi Arabia, Somalia, Sudan, Syria, Tunisia, Turkey, United Arab Emirates, Western Sahara and Yemen, with a current population of about 550 million people. While focusing on these countries, we will likewise present climate model output for the MENA-CORDEX area, which includes part of Central Africa, also addressed within Africa-CORDEX (http://www.cordex.org).

Notice that the domain of Africa-CORDEX does not fully cover the Anatolian Peninsula and the Middle East. Because the climate of Central Africa deviates strongly from that in the MENA, being humid – monsoonal rather than hot and arid, respectively, these results are not analyzed in the present context. To evaluate the CMIP5 model data for the MENA we define four subregions that are climatically coherent (Fig. 1, top panel), based on the Köppen-Geiger climate type classification (Kottek et al. 2006). Geographical coordinates of the subregions are the following. A: 9.25 W-12.0E, 30.0–39.0 N; B: 12.0–34.0E, 25.0–33.0 N; C: 25.5–46.5E, 33.0–41.0 N; D: 34.0–60.0E, 18.0–33.0 N. In Section 4 we compare the CMIP5 model output with temperature observations in these subregions. The Supplementary Information includes a Köppen-Geiger analysis of the CMIP5 calculations for recent, mid- and end-century conditions in the MENA, showing that the main climate types are not expected to change much in the 21st century, i.e., remaining hot and arid (Figure S1).

Open image in new window

From the CMIP5 output we applied results from an ensemble of 26 models that have been interpolated to a common spatial resolution of 2.5 degrees, about 280 km at the equator (Table S1) (Taylor et al. 2012; Sillmann et al. 2013a, 2013b). Here we use CMIP5 model results for two Representative Concentration Pathways (RCPs), RCP4.5 and RCP8.5, adopted by the IPCC for its fifth Assessment Report (IPCC 2013). Greenhouse gas emissions according to RCP4.5 are assumed to peak around 2040 and then decline, while in RCP8.5 emissions continue to rise throughout the 21st century and hence represent a business-as-usual scenario. Following IPCC (2013) we compare the mid-century period 2046–2065 and the end-century period 2081–2100 with the recent period 1986–2005, the latter used as reference.

We evaluate the CMIP5 model results for the reference period, based on observations compiled in the gridded datasets of the Climate Research Unit (CRU, version 3.22) (Mitchell and Jones 2005) and the University of Delaware (UDEL, version 3.01) (Willmott and Matsuura 1995), also used and inter-compared by Tanarhte et al. (2012). To characterize changes in temperature conditions and hot weather extremes, we follow the procedure of Sillmann et al. (2013a, 2013b) by applying the climate indices defined by the Expert Team on Climate Change Detection and Indices (ETCCDI) of the World Meteorological Organization (WMO) (Klein Tank et al. 2009; Zhang et al. 2011) to the MENA, i.e., over the area of the 29 countries listed in Section 2, as well as the subregions defined in Fig. 1. The indices are calculated for the RCP4.5 and 8.5 scenarios, and are available from the ETCCDI archive at http://www.cccma.ec.gc.ca/data/climdex/index.shtml. The CMIP5 model output is compared with historical observations in the period 1950–2010 from the HadEX2 data set of the UK Met Office Hadley Centre. Monthly and annual indices, based on selected high-quality station observations in 14 MENA countries, have been obtained from http://www.climdex.org/index.html (Donat et al. 2013, 2014).

To test the level of consistency of the climate model projections we performed robustness calculations as proposed by Knutti and Sedlacek (2012); see also Proestos et al. (2015). The projection maps of near-surface (2-m) temperature and precipitation for the RCP4.5 and RCP8.5 scenarios are overlaid by stippling and cross-hatching to indicate robustness R, based on the signal-variability ratio and the probability skill score, adopted from weather forecasting applications (Weigel et al. 2007). The signal-variability ratio is calculated from the CMIP5 model spread and the projected change in a particular parameter such as temperature or precipitation. R = 1 – X₁/X₂, in which X₁ is the integral of the squared area between cumulative density functions of individual and multi-model mean projections, and X₂ the integral of the squared area between cumulative density functions of the multi-model projection and the historical reference period. A value of R = 1 indicates absolute model agreement.

Figure 1 shows a comparison between observations and CMIP5 model output of the ensemble mean monthly temperature, including the standard deviation of all model results. The spatial correlation between CMIP5 and observations is high, especially with the CRU dataset. In all four regions the agreement between model and observations is very good for the summer months (June–August), being the focus of the present work. For the winter, typically October to February, differences can be up to several degrees. In regions B and D the CMIP5 ensemble mean appears to be cold-biased and in region C warm-biased during these months.

Figure 2 presents the projected changes in near-surface temperature, including R, for the mid- and end-century periods and the RCP 4.5 and 8.5 scenarios. The interested reader is referred to Figure S2 for the accompanying results for precipitation. We present projections for winter, i.e., the wet season (December, January, February – DJF) and summer, i.e., the dry season (June, July, August – JJA). While our focus is on the summer, we also present results for the winter to emphasize the seasonal differences in warming trends. This illustrates that the rate of warming is much higher in summer. Please notice the temperature scale differences between the two scenarios. Figure 2 shows that the level of robustness is high, especially for the summer warming, and is highest for the end-of-century projections, in particular for the RCP8.5 scenario, indicating overall agreement among the models. The robustness for precipitation projections, on the other hand, is generally much lower (Figure S2).

Open image in new window

On average the CMIP5 models project a drying tendency in the Mediterranean area, which is partly robust in the RCP8.5 projections (Figure S2) and in accord with previous analyses (IPCC 2013). Conversely, northeastern Africa, including part of the Sahara and the Sahel as well as the Arabian region, are subject to moistening, which is less robust though consistent with observations in the recent past (Tanarhte et al. 2012). The drying is most significant in the northern Mediterranean region with a warm temperate climate, associated with rainfall in winter and spring. In this area declining precipitation in the 21st century amplifies warming through the depletion of soil moisture, which suppresses surface cooling by limiting evapotranspiration (Seneviratne et al. 2010; Hirschi et al. 2011). This positive soil moisture feedback on temperature, however, is absent in the arid MENA where the surface energy budget is governed by radiative rather than evaporative cooling (Zittis et al. 2014b).

Figure 2 demonstrates that climate warming in the MENA is particularly strong in summer, whereas during winter the projected rate of warming does not seem exceptional. In summer, subsidence leads to cloud-free and hot weather conditions over a region that extends from northwestern Africa to the Middle East (Tyrlis et al. 2013). At the surface a strong west-east pressure gradient between the Azores high and the Persian trough gives rise to northerly winds that ventilate North Africa by advection of relatively cooler air from Europe (Ziv et al. 2004), illustrated by the arrows in the upper panel of Fig. 3. The Persian trough is a thermal low that can be understood as an extension of the South Asian monsoon trough (Bitan and Saaroni 1992; Alpert et al. 2004). Remote diabatic heating by the South Asian monsoon induces a westward Rossby wave pattern, which enhances subsidence over the MENA with a maximum near the eastern Mediterranean (Rodwell and Hoskins 1996; Tyrlis et al. 2013).

Open image in new window

According to IPCC (2013) global mean warming is projected to reach about 2 °C around 2050, i.e., slightly less for the RCP4.5 and slightly higher than 2 °C for the RCP8.5 scenario. Figure 2 indicates that the 2 °C approximately coincides with the mid-century warming in the MENA during winter in the RCP4.5 scenario, albeit that IPCC (2013) relates to pre-industrial times while Fig. 2 refers to the 1986–2005 period. It also illustrates that the magnitude of warming during summer is about twice that during the winter. According to the RCP8.5 scenario, by the end of the century large parts of the MENA in summer are projected to experience a temperature increase in excess of 6 °C relative to 1986–2005. Figure 2 moreover shows that climate warming in the MENA is stronger than in tropical Africa, where hydrological feedbacks through cloud formation limit the increase of temperature at the surface.

In many areas climate warming is associated with an increase in evaporation and latent heat flux that cool the surface, including the Mediterranean Sea. However, in arid regions this is different, while the capacity to store heat within the soil is small, and surface heat imbalances are primarily compensated by longwave radiation flux adjustment (Vizy et al. 2013). This corresponds to the energy-controlled (vs. evapotranspiration-controlled) regime defined by Koster et al. (2009). Furthermore, increasing greenhouse gases, including water vapor, enhance the downward component of the longwave flux, which is particularly relevant under clear skies. Vizy et al. (2013) analyzed CMIP5 model results, concluding that the coupling of longwave radiation between the desert soil surface and lower atmosphere amplifies warming and intensifies the summertime heat low over the Sahara. Evan et al. (2015) also diagnosed CMIP5 model output and corroborate the deepening of the North African heat low, which they furthermore connect to an intensification of the West African monsoon and increasing precipitation in the Sahel (Figure S2).

The CMIP5 multi-model projections of mean sea level pressure (SLP) in the winter season suggest a significant increase over the Mediterranean and southern Europe, with a maximum around 40°N, while SLPs south of 25°N decrease, with negligible changes in-between over North Africa. This can be understood as an impact of the widening tropical belt (Seidel et al. 2008). During summer, on the other hand, the CMIP5 projections show a reduction of mean SLP over the entire area between the tropics and mid-latitudes (Fig. 3). This coincides with decreasing geopotential height (GPH) at 1000 hPa (Figure S3). This GPH decrease only occurs near the surface, while at higher altitudes, e.g., at 500 and 200 hPa, increases of GPH are projected, both in winter and summer. The CMIP5 model projections for the summer furthermore suggest that over northeastern Africa and the Middle East northerly winds weaken, so that ventilation from the north is reduced (Fig. 3). In spite of the low level heating in summer, indicated by the decrease in SLP, subsidence remains strong, which suppresses cloud formation.

The GPH increase throughout most of the troposphere in summer is consistent with the projected poleward shift of the subtropical jet stream (Yin 2005; Bengtsson et al. 2006). This is a consequence of the weakening meridional temperature gradient and the westward expansion of the upper level ridge induced by the monsoon. The latter also causes and increase of tropopause fold activity during summer (Tyrlis et al. 2014). The shift of the jet stream contributes to decreasing precipitation in the Mediterranean region. These projected changes are a continuation and therefore consistent with an observed and CMIP5 model simulated negative SLP trend over the period 1951–2011 (Gillett et al. 2013). Thus the SLP decrease in the MENA during summer can be interpreted as an extension of the Persian trough across the eastern Mediterranean and the Middle East, in combination with the intensifying thermal low over North Africa, and is associated with excessive heating.

The temperature-based indices are calculated for the selected 20-year reference and future periods, defined by IPCC (2013), as well the entire CMIP5 simulated time period 1950–2010. The results are presented in Table 1 and Figs. 4 and 5. Figure 4 shows results for the RCP8.5 scenario while the accompanying results for the RCP4.5 scenario are shown in Figure S4. A major difference between the two is that in RCP4.5 greenhouse gas emissions are curbed by mid-century, whereas they are not in RCP8.5. The indices presented here are a subset of those used by Sillmann et al. (2013a, 2013b), as we have disregarded the ones for summer days, tropical nights and cold spell duration, because the MENA temperatures already exceed the relevant thresholds in the reference period. The percentile indices are the rates (in percent) at which thresholds are exceeded, based on the annual cycle of the percentiles calculated for 5-day windows in the reference period of 1986–2005.

Table 1

Temperature extreme indices recommended by the ETCCDI calculated from CMIP5 model results according to the RCP4.5 and RCP8.5 scenarios, and from HadEX2 observations, averaged over the MENA countries. The ± ranges indicate 1σ standard deviations of the mean

	Reference period 1986–2005		Mid-century 2046–2065		End-century 2081–2100
ETCCDI index	HadEX2	CMIP5	CMIP5 RCP4.5	CMIP5 RCP8.5	CMIP5 RCP4.5	CMPI5 RCP8.5
TN10p (%)	6.70 ± 2.13	7.16 ± 0.57	1.83 ± 0.62	1.03 ± 0.51	1.37 ± 0.56	0.28 ± 0.20
TN90p (%)	16.45 ± 1.53	15.52 ± 1.30	41.44 ± 8.22	53.61 ± 8.77	47.51 ± 9.11	75.67 ± 7.52
TX10p (%)	7.91 ± 0.96	8.07 ± 0.44	2.94 ± 0.56	2.09 ± 0.55	2.30 ± 0.51	0.85 ± 0.40
TX90p (%)	13.81 ± 1.38	14.91 ± 1.27	37.30 ± 8.24	46.49 ± 9.08	42.93 ± 9.25	66.79 ± 8.73
TNn (°C)	−1.18 ± 6.66	−0.50 ± 7.25	1.24 ± 7.10	2.13 ± 7.13	1.74 ± 7.10	4.25 ± 7.08
TNx (°C)	27.09 ± 2.97	28.38 ± 3.01	30.58 ± 2.99	31.64 ± 3.02	31.07 ± 2.98	34.32 ± 3.08
TXn (°C)	9.92 ± 8.13	9.90 ± 8.02	11.60 ± 7.90	12.30 ± 7.92	12.04 ± 7.90	14.29 ± 7.85
TXx (°C)	41.99 ± 3.20	43.44 ± 3.79	45.67 ± 3.77	46.67 ± 3.83	46.23 ± 3.77	49.23 ± 3.90
WSDI (days)	10.64 ± 4.34	16.24 ± 3.61	83.17 ± 31.41	118.16 ± 38.55	104.39 ± 37.72	204.32 ± 41.59

Open image in new window

Open image in new window

The numbers of cool nights (TN10p) and cool days (TX10p) are the fractions of time when the daily minimum and maximum temperature, TN and TX, respectively, are below the 10th percentile (in %). The numbers of warm nights (TN90p) and warms days (TX90p) are the fractions of time when TN and TX exceed the 90th percentile (in %). TNn and TNx indicate the coldest and warmest nights, i.e., the monthly minimum and maximum values of daily minimum temperatures, respectively. TXn and TXx represent the coldest and hottest days, i.e., the monthly minimum and maximum values of the daily maximum temperature, respectively. The warm spell duration index (WSDI) is the annual count when at least six consecutive days of maximum temperature exceed the 90th percentile.

Sillmann et al. (2013a) showed that the CMIP5 model ensemble realistically represents climate extremes as well as trend patterns in comparison to the HadEX2 observational data. This is confirmed for temperature indices derived for the MENA in Table 1 and Figs. 4 and 5. Figure 4 shows that discrepancies between CMIP5 and HadEX2 indices are relatively largest in the early part of the record, e.g., for cool nights and days, the coldest and warmest night, the coldest and hottest day, while especially for the most recent decades – since about 1980 – the agreement is good; see the second and third columns of Table 1. In particular the agreement between CMIP5 and HadEX2 data for warm days and nights (TX90p and TN90p) is very good (Fig. 5), being important indices for hot weather extremes and their impact on human health (Lubczyńska et al. 2015). Figure 5 also shows that the differences between the subregions are small for the reference period, while the projected increases of TX90p and TN90p in regions C and D are slightly larger than in regions A and B.

In general, the multi-model mean trends are close to the observations. Both, the observations and model calculations in Fig. 4 reveal that in the past decades the occurrence of heat extremes (TX90p and TN90p) has increased significantly while cool days and nights (TX10p and TN10p) have decreased. Sillmann et al. (2013b) mention for the future CMIP5 scenarios that Mediterranean extreme temperatures increase more strongly in summer than in winter, while in the rest of the world the reverse is more typical (see also Fang et al. 2008). This is corroborated by the results presented here, while we find that it actually applies to the entire MENA rather than only the Mediterranean.

The projected changes for both scenarios include steep decreases of the number of cool nights (TN10p) from about 7 % in the reference period to about 1–2 % by mid-century (Table 1 and Fig. 4). Additional decreases by the end of the century are small for RCP4.5 while TN10p approaches zero for RCP8.5. A similar tendency is projected for the number of cool days (TX10p), decreasing from about 8 % to 2–3 % by mid-century, and 1–2 % by the end of the century. The numbers of warm nights and days are also projected to change strongly in the first half of the century. Warm nights (TN90p) increase from about 16 % in the reference period to 41–54 % by mid-century and warm days (TX90p) from 15 % to 37–46 %, whereas both additionally increase by more than 20 % towards the end of the century according to RCP8.5.

While the coldest nights (TNn) in the reference period are below the frost point, temperatures turn positive in the first half of the century, increasing further to more than 4 °C by the end of the century for RCP8.5. The coldest days (TXn) change from below 10 °C to about 12 °C, and the warmest nights (TNx) from below to above 30 °C by mid-century, up to more than 34 °C by the end of the century for RCP8.5. In the reference period the hottest days (TXx) are about 43 °C, increasing to about 46 °C by mid-century to more than 49 °C by end-century for RCP8.5. The WDSI is projected to increase steeply from about 16 days in the reference period to 83–118 days by mid-century to more than 200 days by end of the century for RCP8.5.