Impacts of warm and cold situations in the Mediterranean basins on the West African monsoon: observed connection patterns (1979–2006) and climate simulations
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Using both empirical and numerical ensemble approaches this study focuses on the Mediterranean/West African relationship in northern summer. Statistical analyses utilize skin temperature, sea surface temperature, in situ and satellite rainfall, outgoing longwave radiation (OLR) observations and reanalyzed data winds and specific humidity on isobaric surfaces. Numerical investigations are based on a large set of sensitivity experiments performed on four atmospheric general circulation models (AGCM): ARPEGE-Climat3, ECHAM4, LMDZ4 and UCLA7.3. Model outputs are compared to observations, discussed model by model and with an ensemble (multi-model) approach. As in previous studies the anomalous Mediterranean warm events are associated with specific impacts over the African monsoon region, i.e., a more intense monsoon, enhanced flux convergence and ascendances around the ITCZ, a strengthening of low level moisture advection and a more northward location of ascending motion in West Africa. The results show also new features (1) thermal variability observed in the two Mediterranean basins has unalike impacts, i.e. the western Mediterranean covaries with convection in Gulf of Guinea, while the eastern Mediterranean can be interpreted as Sahelian thermal-forcing; (2) although observations show symmetry between warming and cooling, modelling evidences only support the eastern warming influence; (3) anomalous East warm situations are associated with a more northward migration of the monsoon system accompanied by enhanced southwertely flow and weakened northeasterly climatological wind; (4) the multi-model response shows that anomalous East warm surface temperatures generate an enhancement of the overturning circulation in low and high levels, an increase in TEJ (Tropical Eeasterly Jet) and a decrease in AEJ (African Eeasterly Jet).
The potential role of surface temperatures over the Mediterranean in West African climate dynamics has been largely less investigated than that of the tropical Atlantic or of the El Nino Southern Oscillation (ENSO) phenomenon. Moreover these investigations are recent and hence only based on a few empirical and/or numerical studies. The seminal work, based on observed (1947–96) data, long-term atmospheric general circulation model (AGCM) simulations and idealized experiments forced by warmer (colder) sea surface temperatures (SSTs) in the Mediterranean, has been published by Rowell in 2003. It demonstrates that “in years when the Mediterranean is warmer than average the Sahel tends to be wetter than normal” (and vice versa) with a significant positive correlation (r = +0.47) between the whole Mediterranean SST and JAS Sahel during 1947–1996.
The same year Fontaine et al. (2003) used observational precipitation data and atmospheric reanalyses on the period 1968–1998 for studying moisture fluxes. They founded that part of the moisture fluxes vertically integrated in the layers 1,000–300 hPa or 1,000–925 hPa advected into the West African Monsoon area originates from the Mediterranean Sea and Central Africa and presents significant relationship with atmospheric water budget over the Sahelian belt during the rainy season. Contemporary, Raicich et al. (2003) found that the Sahel rainfall anticorrelates with sea-level pressure in the southeastern Mediterranean basin, suggesting the physical mechanism might involve variations in the local inter tropical convergence zone (ITCZ).
More recently, Peyrillé et al. (2007) analyzed the effect of changes in SST in the Mediterranean and the Gulf of Guinea using a 2-d zonally-symmetric model (30S to 40°N), in modifying the thermal forcing (5°C warming from May to July). They showed that such a warming moistens the lower layers of the Sahara through advection and reduces the thermal gradient between the Saharan heat low and the Mediterranean, tending to decrease the NE winds (Harmattan). Finally using observations and reanalyses over multi decadal periods, Joly (2008) provided evidence of a significant intensification of the Mediterranean/West African relationship in last years.
However, up to date, there are some intriguing results regarding the thermal forcing of the Mediterranean Sea into the West African monsoon (WAM) system. For instance, Rowell (2003) and Jung et al. (2003) described similar outcomes though using different SST patterns, prescribing thermal anomalies in the eastern and western Mediterranean basins respectively. There are also puzzling features concerning the atmospheric response related to Sahel precipitation, as local circulation anomalies (Raicich et al. 2003; Peyrillé et al. 2007) or 3-D evidences for mechanisms favoring the northward migration of the monsoonal rainbelt (Peyrillé et al. 2007; Peyrillé and Lafore 2007). Indeed these empirical and numerical studies are either cases studies focusing on specific processes (i.e., Peyrillé et al. 2007), or analyzes taking into account the climatic transition which affected West Africa during the second par of the XXth century, i.e., the existence of a succession of anomalously wet years in the 50 and 60 s followed by abnormally dry years in the 70 and 80 s as in Rowell (2003). So the purpose of this study is not to reproduce and discuss previous results for resolving the questions above, but to reexamine the relationship through both historical data covering a period which does not include the negative tendency in West African precipitation between the 50 and 90 s, and a lot of dedicated numerical GCM experiments.
This article focuses on the relationship between surface Mediterranean temperatures and the West African monsoon using Satellite observations and atmospheric reanalyses over the period 1979–2006 along with control and sensitivity experiments performed on 4 GCMs with an ensemble approach. The following section presents briefly the data used while Sect. 3 portrays the basic features of the Mediterranean/African linear relationship through different SVD analyses of the temperature and outgoing longwave radiation (OLR) fields and correlations with observed precipitation. Section 4 focuses on the observed contrasted impacts in Warm and Cold situations over the western and eastern Mediterranean basins to analyze both the linearity of the connection with the OLR signal and its impacts on observed atmospheric dynamics and Hadley circulation. In Sect. 5, we will present different sensitivity experiments relative to the Mediterranean thermal variability performed on four climate models before analyzing the results in terms of rainfall impacts and atmospheric dynamics though an ensemble approach. Section 6 will propose a short discussion before the conclusion.
2 Selected historical datasets
Land-based precipitation data (stations) do not allow accurate description of the West African rainfall variability at short time scales (i.e., lower than 1 month), especially in the recent years. This is mainly due to the anisotropy of the network, the number of stations documenting correctly rain falls being too low, especially along the meridional plane. For example the global surface summary of day dataset (GSOD) exhibits large areas without any station in the Benin, Togo and Burkina Faso positioned over the central parts of West Africa. Moreover some daily values are either not reported, or very underestimated or false which changes the coverage with days, months and years. After the year 2000 the series are too incomplete for analysing accurately the daily or 5-day fields.
So for describing the monthly and seasonal time scales, we selected first the monthly precipitation from the high-resolution gridded CRU TS 2.1 data-set. These files comprise 1224 grids of observed climate, for the period 1901–2002, and cover the global land surface at 0.5 degree resolution (see New et al. 2002; Mitchell et al. 2004). For shorter time scales, rainfall information has been selected from the CPC Merged Analysis of Precipitation (CMAP, Xie and Arkin 1997) and from the Global Precipitation Climatology Project (GPCP, Adler et al. 2003; Xie et al. 2003) estimates on a 2.5 × 2.5 degree latitude/longitude grid at a 5-day time-scale over the period 1979–2006. These satellite-derived estimates do not describe exactly the real world but have many advantages over current in situ data: they are coherent in space and time at 5-day scale, they have been often described and used and they give access to different information. However in northern summer, the mean precipitation differences (CMAP–GPCP) are positive over land and negative over Ocean with a typical difference of ±0.1 mm/day (Gruber et al. 2000). This could be due to the fact that, by contrast with GPCP, CMAP uses uncorrected rain gauge over land (Gruber et al. 2000). Moreover, Yin et al. (2004) indicate that (1) the GPCP/CMAP spatial correlation is higher over land than over ocean; (2) in general precipitation over ocean represented by the GPCP is more accurate while over land the two products are close. More details can be found in Louvet et al. (2007).
The Sea Surface Temperatures provide from the most current version of the Kaplan dataset produced by taking the MOHSST5 version of the GOSTA data set from the U.K. MET office and using EOF projection, optimal interpolation, Kalman Filter analysis, and an optimal smoother for filling in any missing data. The data set is stored on a 5° × 5° grid.
Skin temperatures and atmospheric data in all the troposphere provide from National Centers for Environmental Prediction (NCEP) and is called NCEP/DOE AMIP-II Reanalysis (R-2) over the period 1979–2006. This dataset can be hence considered as a mix of in situ and satellite observations and modelling. It improves however upon the NCEP/NCAR Reanalysis (R-1) by fixing the errors and by updating the parameterizations of the physical processes. It has been also extensively used and described (Kanamitsu et al. 2002; Maurer et al. 2001 among others). To be very concise one can say that R-2 provides more accurate pictures of soil wetness, near surface temperature and surface hydrology budget over land, and radiation fluxes over Ocean. The new boundary layer and convection schemes have also modified the water vapor profile: R-2 has more moisture in low levels than R-1.
The daily NOAA Interpolated Outgoing Longwave Radiation (OLR) data are used in a 2.5° × 2.5° version where all gaps have been filled with temporal and spatial interpolation as described in Liebmann and Smith (1996). OLR is an interesting additional dataset for our purpose since it measures the direct emission from the surfaces (Earth, clouds). It allows therefore clear depiction between clear-sky regions which concentrate the highest OLR values from the warmest surfaces and deep convective regions where the highest and coldest clouds (cirrus and tops of cumulonimbus) dominate. However OLR values in W/m2 are not direct measurements of deep convection since for example in clear-sky situations, OLR measures the direct emission from the warmer land or oceanic surfaces.
3 Basic features of the Mediterranean/African relationship
The relationship is here examined through several spatial indices and objective field analyses using SSTs, skin temperatures, precipitation and OLR.
3.1 Composite and correlation analyses through observed precipitation
Observed relationship between Mediterranean surface temperatures and North African (5–20°N) and Sahel (13–18°N) rainfall amounts averaged between 15°W and 30°E for the seasons July–September (JAS) and the months May–October
North Africa: 05–20°N
Mean rainfall amounts (mm)
W − C West Medit (%)
W − C East Medit (%)
Sahelian belt: 13–18°N
Mean rainfall amounts (mm)
W − C West Medit
W − C East Medit
Correlation coefficients between July and September surface temperatures in the Western/Eastern Mediterranean and July–September CMAP and GPCP rainfall estimates averaged over western Sahel (WSAH), central Sahel (CSAH), Eastern Sahel (ESAH) and central Sudan (CSUD) with and without time filtering
Filtered series: variability < 8 years
3.2 Robustness of the relationship
Percentages of covariance and covariance fractions explained by the leading July–September mode (SVD1) at a daily timescale and time correlations (Corr SVD1) with and without linear trend (detrend) and as a function of time filtering in different ranges for capturing the 3–5 days (AEWs), < 10-day (synoptic), 10–90 days (intraseasonal) variability over the period 1979–2006
T, OLR, days
Figure 1 refers to a synchronous (no lag) analysis performed between monthly skin temperatures observed over an extended Mediterranean region (5°W–40°E; 20–45°N) and monthly OLR values referring to an extended WAM region (20°W–40°E; 10°S–20°N). The total covariance equals 32.7% of the total variance and the squared covariance fractions of the two leading modes match 33.4 and 22.5% respectively. The first heterogeneous mode and its related time coefficients are displayed in Fig. 1a, b. They clearly attest the statistical linkage between warm anomalies restricted to Eastern Mediterranean and low OLR anomalies expanding along 10–15°N and eastward to about 10°W. As noticed above, the Eastern Mediterranean concentrates the highest positive loadings, while the western basin and continental regions somewhat northward to the mean ITCZ position accumulates the strongest negative loadings (meaning enhanced deep convection) with the maximum located in the central and eastern Sahel. Such a result agrees well with those shown by Polo et al. (2008) at monthly-interannual scale, suggesting an active role of the eastern Mediterranean SST into the Sahelian variability. In fact, the coupled OLR and temperature time series in Fig. 1b are largely correlated (r = +0.70, significant at p = 0.01 taking into account autocorrelation in the series); they display both an in-phase interannual signal and the recent rainfall recovering since the 90 s. When these coefficients are averaged over the successive JAS season its correlation increases to +0.87, while the temperature and OLR time series are positively correlated with JAS rainfall averaged over central (10°W–10°E) Sahel: +0.50 and +0.67, significant at p = 0.05 and p = 0.01 respectively, taking into account autocorrelation in the series.
By construction the second skin temperature-OLR mode (Fig. 1c, d) is less energetic and registers lower serial correlation between time series (r = +0.61, significant at p = 0.01 taking into account autocorrelation in the series). However it is the direct complement of the first one: the strongest (positive) temperature loadings are here restricted to the West Mediterranean. A surface warming in this region is linked to lower OLR values (deeper convection) extending both in the Western parts of the Sahel (Senegal, Mali) and over equatorial eastern Atlantic (Gulf of Guinea). When time coefficients are averaged over the JAS seasons the correlation increase to +0.70 (p = 0.01), and the temperature and OLR time series are positively correlated with JAS rainfall over the western parts (18–10°W) of the Sahel: +0.31 and +0.43 respectively, this last value being significant at p = 0.05.
In fact the Mediterranean/WAM relationship is not purely synchronous as illustrated in Fig. 1c. This diagram displays the lead/lag correlation coefficients computed between spatial indexes averaging OLR values in the Sahel zone (10–20°N; 15°W–30°E) in JAS, at the heart of the rainy season and 3-month surface temperatures in the whole Mediterranean basin (32–40°N; 6–36°W) moving with a 5-day (pentad) time-step before and after JAS. Near all the values are significant at p = 0.05 but the strongest correlation is registered when the Mediterranean temperatures are leading OLR by 6 pentads (1 month).
3.3 Evolution of the leading skin temperature/OLR mode at the monthly scale
In order to assess better the robustness of the Mediterranean/WAM lagged relationship, Fig. 2 refers to SVD analyses performed at the monthly scale between Mediterranean skin temperatures and WAM OLR values 1 month later referring to the same domain that in Fig. 1. Here linear trends in the series have been removed and the display focuses on the May/June to October/November evolution of the lagged temperature/OLR relationship. The results confirm first the statistical linkage between the East Mediterranean and WAM domains shown above (Fig. 1a). Second they show that there is no negative OLR anomaly over the Sahel before June/July (Fig. 2b), confirming the previous dry regime as indicated from Table 1 (in May/June; Fig. 2a). There, warm anomalies are associated with positive values of OLR over Sudan-Sahel, meaning decreased convection. From Jul/Aug to Oct/Nov temperature loadings reinforce on the eastern Mediterranean according to the leading monthly coupled mode (Fig. 1a), while OLR anomalies are related to increased deep motions (Fig. 2c–f).
Once again, the East Mediterranean concentrates the highest positive temperature loadings in connection with WAM deep convection, which points out largest anomalies along 10–15°N and mainly located over inland regions. Also at daily scales, Table 3 summarizes the percentages explained by each leading JAS-mode, time correlation between time series before and after removing all linear trends at each grid point (columns 1–2). In fact the field coupling is slightly lower when the series are detrended with a leading mode, spatially similar to Fig. 2a but less energetic (29 vs. 52% of squared covariance fraction) and positively correlated (+0.42 vs. +0.51). Other columns underline possible connections with oscillatory modes at synoptic scale (<10 days) such as African Easterly Waves (AEW) in the 3–5 day range, when longer-term mean coefficients are removed.
To test the linearity of the connection the next section contrasts the signals observed in warm and cold situations over the Western and Eastern Mediterranean.
4 Contrasted impacts in warm and cold situations
4.1 OLR signal
The warm (cold) composites relative to the Western and Eastern Mediterranean are shown in Fig. 3b, c, respectively (Fig. 3d, e). They contrast the 8 warmest and the 8 coldest seasons versus all the remainders (caption in Fig. 3 indicates the selected years). Once again the signal is more significant in Fig. 3c and e, i.e. when the possible thermal forcing involves the East Mediterranean: warm (cold) anomalies in the Eastern basin are associated with lower (higher) OLR values. This denotes an enhancement (a reduction) of deep convection in the monsoon region when the East basin is abnormally warm (cold) and suggests hence the existence of associated signals in atmospheric dynamics.
4.2 Atmospheric dynamics
Warm composites in Fig. 4c–f exhibit significant signals in both meridional circulation and specific humidity especially. Warm conditions in the Western basin are associated, westward to 0°, with lower-levels convergence and upper-levels ascending motions in the northern subtropical latitudes, and with significant moisture increase (shadings in Fig. 4c) in the low and mid troposphere above the equatorial Atlantic. However only 3% of the area can be considered as significant and there is no clear meridional-connection between the former and the latter. Neither a clear signal appears eastward to 0°. By contrast warm conditions in the Eastern basin reinforce the southern (monsoon) cell circulation between 0° and 30°E (Fig. 4f) with 5% of global field significance): low level advections from the South in temperature and moisture are significantly enhanced, while air ascents within the ITCZ and air descents above the Southern Tropics strengthen. This is accompanied by a significant moisture increase (shading in Fig. 4f) under 400 hPa over the continent (5–20°N). To a lesser extent, but of equal statistical significance, the northern Hadley cell is also reinforced showing a closed circulation.
The results reported in Sects. 3 and 4 are thus compatible with the existence of a significant statistical relationship between the East Mediterranean and the WAM-Sahel region. In order to check whether this is interpretable in terms of Mediterranean forcing, we will analyze multi-model outputs using SST sensitivity experiments performed on 4 AGCMs. This approach allows production of more reliable climate features than a single model method since climate simulations performed on any given model are sensitive to systematic errors, as previously shown by, among others, Bader and Latif (2003) and Giannini et al. (2003).
5 Numerical study
5.1 Description of the sensitivity experiments
ARPEGE-Climat Version 3 IPCC-AR4 in truncature 42 with 45 levels run at CNRM (Centre National de Recherches Météorologiques, Météo-France)
ECHAM Version 4 in truncature 30 with 32 levels run at ENEA (Italian National Agency for New Technologies, Energy and Environment)
LMDZ Version 4 (96 long, 71 lat and 19 levels) run at IPSL (Institut Paul-Simon Laplace)
UCLA Version 7.3 (2° long × 2.5°lat, 29 levels) run at UCM (Universidad Complutense de Madrid)
The ENEA, IPSL and UCM institutions performed 10 simulations with different initial conditions for each experiment (cold, warm, and control with no superimposed SST anomaly) while CNRM performed 20 simulations, allowing available a total of 150 simulations. However to give each model the same weight, we will consider 10 simulations for each model and each experiment (control, cold and warm), hence 10 × 4 × 3 = 120 simulations. Experiments have been run from 15th of April to 15th of October and each SST pattern have led to a set of 10 runs (20 runs for CNRM). Initial conditions have been taken from a long-term AMIP-type run with conditions representative of the end of the 20th century. A good way to do this was to take conditions around the 15th of April for 10 (or 20 for CNRM) different years in the set of possible initial conditions. The 10 (or 20) years for initial conditions have been taken from years 1979 to 1988 (or 1979–1998 for CNRM).
It is noteworthy that using such prescribed SST as a lower boundary condition implies that the sea acts as a reservoir of infinite heat capacity which is not the case in the real world where the Mediterranean has finite heat capacity. This tends to damp the surface heat fluxes and therefore to decrease the amplitude resulting from the model runs.
5.2 Multi-model rainfall outputs
The 40 warm (W) and 40 cold (C) experiments limited to the Mediterranean are now compared to the 40 control simulations (CTL = climatology) regarding rainfall outputs from each model. The focus is made on the two main West African rainy seasons, i.e., the first Guinean rainy season in May–June (MJ) and the northern tropical rainy season in July–September (JAS).
In MJ (Fig. 8a, c) there is no significant rainfall difference: no model causes a significant dispersion of the rainfall amounts produced by the cold and warm experiments (circles and asters in 8a, respectively). This is similar when using a model-ensemble approach: the histograms relative to the cold and warm simulations (white and blue bars in Fig. 8c, respectively) are alike. In JAS, at the opposite, the same experiments create contrasted responses, i.e., less (more) rainfall in cold (warm) situations. However, there is a more consistent signal in warm outputs than in cold ones: (1) the latter fail 32.5% in distinguishing the precipitation sign, against only 12.5% in the former (Fig. 8b); (2) and, considering 4-models together, the cold (warm) experiments model-ensemble generate a ratio of 9/18 (27/2) between excess/deficits (Fig. 8d). Warm situations in the Mediterranean seem therefore to impact more on West African precipitation in contrast with empirical findings, which showed a symmetrical signal (Fig. 3c, e). For all above, the rest of the work will focus on both the rainy season (JAS) and the forced-response in warm conditions.
5.3 Large-scale wind circulation
Additionally, this anomalous low-level convergent inflow is associated with positive streamfunction anomalies at upper-levels, revealing a baroclinic structure in the atmosphere (Fig. 10b, f, j): along the whole subtropical belt in CNRM, confined into the eastern Mediterranean in UCM, and isolated over the Arabian Peninsula in IPSL. Similar thermally-driven response to changes in the Mediterranean SST has been reported by Li (2006), who found a circumglobal wintertime-teleconnection initiated in the Mediterranean basin. Experiments analyzed here seem to corroborate this direct global-response to Mediterranean summer forcing (García-Serrano et al. manuscript in preparation); while previous evidences support this finding (Jung et al. 2006).
5.4 Moisture fluxes
The moisture transport is mainly organized with a SW maximum at 925 hPa by 10°N (positive values in panels a, b) and an easterly maximum at 700 hPa around 10°N, hence just under and southward to the main AEJ axis, as shown by the negative values in Fig. 11a. Warm-CTL composites in Fig. 11c, d present larger significant signals. In particular the zonal moisture transport by the AEJ is shifted northward (negative/positive dipolar patterns at 700 hPa in Fig. 11c) while in lower levels, negative/positive differences northward/southward to 20°N in Fig. 11c, d reveal a significant increase of northeasterly and southwesterly monsoonal flux. This finding implies an enhanced deep convection in the WAM area. Additional analyzes (not reported here) have shown that the increase in northeasterly moisture flux is mainly due to an augmentation of the specific humidity in low-level over the warmer eastern Mediterranean. This strengthens the flux and together with the reinforcement of the southwest monsoon augments moisture convergence in low levels, according to Rowell (2003). This feedback mechanism would also help to the anomalous northward displacement of the ITCZ, providing above-average precipitation over the Sahel.
5.5 Response in low levels
The Warm-CTL significant differences at p = 0.10 are presented in Fig. 12b, d, f with shadings when the v component is positive. The 3 models give anomalous surface westerlies over the Sahelian area, although the location of the signals is different from one model to another. Thus, CNRM concentrates the strongest signals over the Atlantic (under 12°N) and the eastern Sahel, UCM over a large part of the West African continent north to the equator and subtropical Atlantic (12–24°N), while IPSL produces significant westerlies in the Sahelian domain but with a similar amplitude south of the equator. Despite these differences, common features emerge from the multi-model approach (Fig. 12g, h). This multi-model ensemble retains large anomalous westerlies coming inland from the Atlantic (Rowell 2003) and reaching the Sahel region, but does not take into account the southerly component from Gulf of Guinea. Additionally, as also shown in each model (Fig. 12b, d, f), the weakening of the climatological northeasterly flow from the eastern Mediterranean is apparent. These anomalous surface winds have a clear southerly component east of 10°E over Egypt. This feature is consistent with the anomalous low-level convergence in the southeastern Mediterranean basin, as discussed above (Fig. 10d, h, l), and is in agreement with Peyrillé et al. (2007) regarding the penetration decrease of the mean circulation depending on the thermal contrast between the African continent and the Mediterranean Sea (or SST-forced in this case).
5.6 Response in mid and high levels
6 Discussion and conclusion
The purpose of this study was twofold: (1) reexamining the observed relationship between the Mediterranean thermal variability (Western and Eastern basins) and Sudan-Sahel rainfall estimates over the recent period, i.e., not marked by long wet and dry phases (as in the 50–70 s); (2) reporting some rainfall and atmospheric impacts generated by warm JAS anomalies in the Mediterranean Basin using multi-model sensitivity experiments. The results provide from both empirical and numerical ensemble approaches. The analyses use 3 types of datasets: in situ observations (rainfall, sea surface temperature…), satellite estimates (GPCP, CMAP data) and reanalyzed data from the NCEP-DOE AMIP II (winds and specific humidity on isobaric surfaces…).
Considered together the statistical and numerical results let suppose the existence of a thermal forcing of the Mediterranean on the African monsoon. Basically Mediterranean warming, with maximum amplitude in the eastern basin, leads to enhanced moisture convergence and therefore rainfall over Sudan-Sahel latitudes in agreement with Rowell (2003) who reports also a strengthening of moist advection across the Eastern Sahara by the mean flow. Peyrillé et al. (2007) insist more on a reduction of northerlies both in magnitude and extension, compatible with a deeper northward migration of the ITCZ into the continent. In accordance with the latter, Raicich et al. (2003) evidenced that the Sahel monsoonal season is associated with below-normal surface pressure in the eastern Mediterranean. All above has been also verified here, implying that this Mediterranean-WAM connection was robust during recent decades. Thus, when the warming concerns the East basin, a strong link with Sahel precipitation has been found, involving the reinforcement of both the ITCZ-deep motion and westerly transport of humidity thereby, in short, strengthening the main WAM circulation regime. An open question to be addressed concerns the WAM teleconnection with the West basin. Our observational analysis suggests a relationship with deep convection over Gulf of Guinea, possibly related to the Atlantic equatorial SST mode.
The Eastern Mediterranean concentrates the highest SVD temperature variance, while a large continental region, located somewhat northward to the mean ITCZ position, accumulates the strongest loadings in terms of enhanced deep convection and ascendance. This connection has been found in both synchronous and 1 month-lead performances, suggesting an important influence of the East basin on the WAM system.
Additional results have confirmed the existence of a 1 month delay between thermal variability in the Mediterranean and deep convection over Africa. There are also preferred time scales for correlations, i.e., synoptic variability (<10 days) and AEWs (3–5 days). This last connection is mainly observed eastward to the 0° longitude, a region known for a long time as an area of AEW development. These features will be also further analysed in the future through AGCMs and WRF simulations.
When the Eastern basin is abnormally warm the northward migration of the monsoon system and ascendances around the ITCZ reinforce through deeper moist convection south of the Sahara. These air ascents strengthen northerlies at 200 hPa and hence the monsoon cell, air descents above the Southern Tropics and low level moist winds from the South. This increases moisture transport under 400 hPa over the continent (5–20°N), low level convergence via the SW monsoonal flow in the Sahel zone and hence rainfall surplus just northward to the rain belt in July–September. Additional analyses (not produced here) and Fig. 3 show that the reverse tends to occur in cold situations, in accordance with Rowell (2003).
The SST sensitivity experiments linked to normal, warm and cold situations over the Mediterranean and performed on four AGCMs allowed us first to illustrate the relative good accuracy of the models to reproduce the May–September evolution of several key-elements of the monsoon circulation. The more reliable latitudinal-migration of the rainbelt climatology has been found for CNRM and UCM models.
Second, in the models the response between warm and cold situations in the Eastern Mediterranean is not symmetric: the sensitivity experiments showed that warm occurrences impact more on West African precipitation than cold ones. In fact, cold-SST runs have not been conclusive, becoming separated from the linear hypothesis of Rowell (2003). Perhaps, it is because of the AGCM difficulty for well simulating the reduced-latent heat release in cold situations. It is also important to mention that climatological summer SST conditions in the Mediterranean Sea resemble a zonal gradient with maximum located in the eastern basin quite similar to forcing fields prescribed in the simulations (not shown). Hence, the Mediterranean-Sahel connection in cold conditions continues being an issue to be explored. By contrast, the positive empirical relationship between warm SSTs in the Mediterranean and the West African monsoon can be interpreted in terms of thermal Mediterranean forcing.
In this way, warm experiments generate an enhancement of the southern meridional cell in low and high levels, related to reinforced monsoonal southwester lies, a more northward location of its ascending branch (ITCZ) over West Africa in association with more (less) intense monsoon and TEJ (AEJ). It is however important to bear in mind that such changes in the overturning circulation are not necessarily directly forced by Mediterranean SST since the enhanced moisture transport from the Mediterranean into the Sahel region increases also the latent heat and diabetic heating. This tends to fuel the rising motion in the WAM area and subsequently the downward motion in the overturning circulation.
An integrating picture has been evidenced from AGCM simulations presented here. According to Rowell (2003) and Fontaine et al. (2003), the favoured humidity transport from the Mediterranean Sea into ITCZ is accompanied by both anomalous surface-influx from the tropical Atlantic and reduced export via AEJ at mid-levels (two of the Rowell’s feedbacks). The former could help to displace more northward the WAM-deep convection up to the Sahelian region. In addition, another mechanism has been shown contributing to this anomalous poleward ITCZ-extension. Consistent with the lower-tropospheric convergence found in the southeastern Mediterranean basin, which could explain the surface pressure anomalies suggested by Raicich et al. (2003), is the weakening of the climatological northeasterly flow east of 10°E over Egypt. This finding is in agreement with the penetration decrease of the mean circulation depending on the thermal contrast between African continent and the Mediterranean Sea (or SST-forced in the simulations; Peyrillé et al. 2007). This feature reflects a substantial northward migration of the monsonal rainbelt, and hence above-normal precipitation over the Sahel. This result does not contradict the anomalous moisture transport originated in the Mediterranean; since although weakened, the additional evaporation would be advected southward across the eastern Sahara by the flow.
The authors are very grateful to the anonymous reviewers for their interesting comments, and to the National Center for Atmospheric Research (USA), Climate Prediction Centers and the National Oceanic and Atmospheric Administration for providing the data. J. G.-S. greatfully acknowledge the founds from the ESF-MedCLIVAR Programme of grants (E.G/1694). The study was mainly supported by the Global change and Ecosystems programme (EU Integrated project: African Monsoon Multidisciplinary Analysis (AMMA) and the French component of AMMA. Based on a French initiative, AMMA was built by an international scientific group and is currently funded by a large number of agencies, especially from France, UK, US and Africa. It has been the beneficiary of a major financial contribution from the European Community’s Sixth Framework Research Programme. Detailed information on scientific coordination and funding is available on the AMMA International web site http://www.amma-international.org.
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