Figure 1. The study area, red indicates the Sahel region (10˚N - 20˚N, 20˚W - 40˚E) within the Great Green Wall (GGW) corridor countries. The map highlights the transition from the northern Sahara Desert to the southern savanna grasslands, representing the primary focus of the study region.

The study focuses on the Sahel [10˚N - 20 ˚N] and [−18˚W - 40˚E] (Figure 1), which is a semi-arid region, found in Northern Africa, situated over 5500 km from the Atlantic Ocean to the Red Sea ([4]; [20]). It separates the Sahara Desert to the north from the Sudanian savanna and equatorial forest to the south ([35]). Moist static energy over the Sahel is composed of sensible and latent heat components that vary dramatically with the season, with latent heat dominating during the wet season and sensible heat during the dry season ([30]). [39] found that during the dry season, sensible heat dominates (balancing solar heating with longwave radiation), whereas by the rainy season, radiative forcing at the surface is balanced by latent heat and longwave fluxes. [42] and [52] quantified this seasonality across the Sahelian surfaces and revealed sensible heat ranging from ~20 W·m⁻² (wet season) to 100 W·m⁻² (dry season), where the latent heat reached 100 - 150 W·m⁻² in the wet season. [15] and [23] documented that moist static energy meridional gradients are stronger over the continent. The severe drought from 1970 to 1980 caused food insecurity and mass migration. In response to these, the ambitious land restoration initiative, the Great Green Wall (GGW), was initiated in 2007 ([35]). It is a pan-African initiative to combat desertification in the Sahara and Sahel regions (Figure 1) through a land restoration and revegetation project aimed at environmental and human well-being, including afforestation and assisted natural regeneration ([53]). It includes 11 Sahelian countries (Figure 1) working together to address land degradation and climate change ([35]) and desertification, while improving the livelihoods of smallholder farmers and pastoralists ([11]). The GGW decreases drought length and increases rainy days; however, it increases heat extremes during the pre-monsoon ([24]). The Sahel green belt/GGW/increases evapotranspiration and moisture convergence, enhancing latent heat while reducing sensible heat, by decreasing summer temperature; however increases diurnal temperature range ([46]).

2.2.1. Model Description

The study applied the full spell community Earth System Model version 2 (CESM2), which is a fully coupled Earth system model, with substantial scientific and infrastructure improvements over its predecessor, featuring interactive atmosphere, land, ocean, and sea ice components, along with optional advanced modules for chemistry and ice sheet dynamics. The evidence for CESM2’s sophistication ([8]), revealing a major reduction in low-latitude precipitation and shortwave biases, improved representation for MJO, and better El Niño Southern Oscillation teleconnection as compared to CESM1, is accessible at: https://www.cesm.ucar.edu.

2.2.2. Experimental Design

The Community Earth System Model version 2 (CESM2) was configured with its atmospheric component at a horizontal resolution of 1.9˚ × 2.5˚ with 32 vertical levels, and the oceanic component (POP2) at a nominal resolution of 1˚ with 60 vertical levels. To isolate land-atmosphere-driven climate responses, the model was forced with constant year-2000 external forcings following ([8]).

Two numerical experiments were conducted to assess the climatic impacts of large-scale vegetation restoration. The control experiment (CTRL) uses the present-day land cover with no vegetation alteration and was integrated for 50 years. The sensitivity experiment (GGW) is identical except for a prescribed vegetation perturbation over the Sahel (10˚N - 18˚N, 20˚W - 40˚E), simulating the Great Green Wall initiative by increasing vegetation cover by 70%.

This perturbation was implemented by modifying surface boundary conditions in the Community Land Model (CLM5) following ([32]). Specifically, the fractional cover of the dominant Plant Functional Type (PFT) in each grid cell within the target region was increased by 70% relative to its original value, with a corresponding reduction in bare soil fraction. This modification implicitly alters key biophysical parameters, including Leaf Area Index (LAI), surface albedo, surface roughness length, and rooting depth, consistent with the prescribed vegetation change. The modified land surface was applied as a permanent, year-round change, allowing prognostic vegetation-atmosphere interaction throughout the simulation.

To ensure both simulations reached equilibrium before analysis, we examined key stability indicators, Top-of-Atmosphere (TOA) net radiation balance, and regional soil moisture trends. These indicators exhibited no significant drift during the final 30 years of either integration, confirming a quasi-equilibrium state suitable for diagnostic analysis ([8]).

The sensitivity experiment required a longer integration (100 years) than the control (50 years) because perturbed land surface conditions need additional time for the fully coupled system to adjust and reach a new equilibrium ([32]). This ensures our comparison reflects the equilibrium climate response rather than transient adjustment. Accordingly, the final 30 years from each experiment were used to capture steady-state conditions. To quantify vegetation impacts, all calculations are based on Case surface minus Case differences.

2.2.3. Model Simulation Output

Monthly mean outputs from the CESEM2 model simulation are used to investigate land-atmosphere interactions and the moist static energy change induced by GGW. Simulated outputs are categorized into three: 1) atmospheric state variables, including three-dimensional winds, specific humidity, air temperature, and geopotential height. 2) surface and energy flux variables: including latent and sensible heat flux, surface radiation components, convective precipitation, and temperature. 3) hydrological variables: including large-scale and convective precipitation and surface pressure.

All the data are processed for the summer monsoon season (JJA), and GGW minus Control is applied to quantify the impact of GGW.

The thermodynamic and dynamic effects of afforestation are diagnosed in this study using a column-integrated Moist Static Energy (MSE) budget framework ([23]). The steps of the calculation are mentioned below.

1) Moist static energy per unit mass is defined as:

where c_p stands for the specific heat of air at constant pressure, T for air temperature, L_v for latent heat of vaporization, q for specific humidity, g for gravitational acceleration, and z for geopotential height. Kinetic energy is neglected, so Equation (1) represents the total internal, latent, and potential energy available to convection.

2) For the JJA climatological mean, the column-integrated MSE budget equation is written as:

where the mass-weighted vertical integral is:

where {⋅} stands for the mass-weighted vertical integration between the surface and the top of the atmosphere.

V = ( u , v ) is the horizontal wind vector (m/s), ω is vertical pressure velocity (Pa/s), ℱ is net column forcing (radiative + surface turbulent fluxes) (W·m⁻²), ∂ t { h } is the column tendency, and NL is the residual (including nonlinear and unresolved subgrid-scale terms). In steady seasonal climatology (JJA), the tendency term is negligible, reducing the budget to a balance between advection, forcing, and residuals.

For a steady seasonal climatology, the storage term is negligible:

Thus, the budget simplifies to

The net column forcing term is expressed as

where F TOA is net top-of-atmosphere radiation, H is surface sensible heat flux, and E is evaporation, Lv is the latent heat of flux.

3) Mean-Anomaly Decomposition of Advection Terms

To diagnose the mechanisms influencing GGW-induced MSE changes, all fields are decomposed into climatological means and anomalies using Equation (3):

Horizontal MSE Advection: horizontal advection is decomposed into mean and anomalous.

V1: mean horizontal advection, V2: mean flow on anomaly, V3: anomalous flow on mean, V4: eddy/nonlinear.

Vertical MSE Advection: vertical advection is decomposed into mean and anomalous components.

(6)

where ω 1 : mean vertical advection, ω 2 : mean ω on anomaly, ω 3 : anomalous ω on the mean, ω 4 : eddy/nonlinear term.

These decompositions allow separation of dynamic (circulation-related) and thermodynamic (temperature/humidity-related) processes.

4) GGW minus Control Perturbation Framework

The influence of afforestation is evaluated as the difference between the GGW and the control simulation.

All MSE budget components are computed as case surface minus case anomalies and then averaged over the Sahel domain to analyze the role of the Sahel greenbelt.

To ensure reproducibility and budget closure, all MSE budget terms were derived from monthly mean CESM2 outputs. Horizontal and vertical advection, radiative, and turbulent fluxes were computed directly from these monthly fields. Calculations were performed on 32 model pressure levels, with mass-weighted vertical integration from the surface to 100 hPa. All variables were re-grid to a uniform 1.9˚ × 2.5˚ horizontal resolution. The residual term, representing unresolved and nonlinear processes, was diagnosed as the imbalance in the budget and remained below 10% of the total MSE tendency over the Sahel, indicating robust closure.

Figure 2 shows the JJA climatological distribution of MSE at the 850 hPa. The control (Figure 2(a)) reveals that the MSE maxima are located at 5˚N - 12˚N, south of the Sahel, with a value increasing from the Guinea Coast towards the central and western Sahel. In the GGW (Figure 2(b)), MSE is strongly enhanced over the western Sahel, extending northward to approximately 15˚N. Whereas the greenbelt induced vegetation change (Figure 2(c)) demonstrated, the Sahel greenbelt shifted the MSE maxima northward around 15˚N - 18˚N, strongly increased over the central Sahel from approximately 1.254 kJ·kg⁻¹ to 1.507 kJ·kg⁻¹, implied increased atmospheric moist enthalpy and convective potential over the Sahel, and enhanced surface moisture availability and latent heat flux under the Sahel greenbelt ([1]). These confirm that Sahel-greenbelt-induced vegetation recovery strengthens land-atmosphere coupling, moistens the lower troposphere, and shifts convective potential northward to the central Sahel.

Figure 2. JJA climatological distribution of moist static energy (MSE: J·kg⁻¹): (a) control, with no vegetation added, maxima located at 5˚N - 12˚N; (b) the GGW, the green belt with a slight shift in MSE maxima northward; (c) GGW minus Control.

Figure 3. Annual cycle of moist static energy (MSE: J·kg⁻¹): (a) control annual cycle; (b) GGW annual cycle; (c) GGW minus Control, represents the seasonal progression of MSE, during the pre-, peak, and the outset of monsoon.

Figure 3 reveals the JJA annual cycle of moist static energy (MSE) distribution. In the control of climatology (Figure 3(a)), the MSE intensifies during the monsoon season JJA with maxima located from the Guinea Coast to approximately 12˚N - 15˚N. In the GGW (Figure 3(b)), the GGW preserves the same feature as the control, with a slight extension in MSE maxima northward to ~15˚N. More importantly, the change (Figure 3(c)) marks seasonal redistributions. During the pre-monsoon (MAM), MSE increases with maxima around 14˚N - 16˚N, extending from the Guinea Coast to the Sahel, implying an enhanced surface moisture supply and atmospheric preconditioning for monsoon onset. By contrast, during the Peak monsoon phase (JJA), the MSE decreases over the Guinea Coasts but increases farther north (16˚N - 18˚N) over the central Sahel (Figure 2(c)), forming a clear meridional dipole. This pattern suggests enhanced inland moisture transport and a northward shift of convective energy. Renewed enhancement during the outset of monsoon (OND) implies delayed soil moisture release ([49]), which contributes to the reorganization of monsoon energetics, with greenbelt-induced vegetation restoration shifting MSE and associated convective potential northward into the Sahel.

Figure 4presents the area-averaged anomalies of the moist static energy (MSE) budget components over the Sahel in response to the Great Green Wall (GGW) forcing. Error bars denote the 95% confidence interval derived from interannual variability across the 30 JJA seasons, and asterisks indicate the significance level of a one-sample t-test against zero (*p < 0.05, **p < 0.01, ***p < 0.001). The net column-integrated MSE increases by +7.00 ± 0.36 W·m⁻² (p < 0.001), signaling a robust atmospheric energy surplus. Vertical advection dominates the budget: the anomalous vertical velocity acting on the mean MSE gradient contributes +1.48 ± 0.11 W·m⁻²; however, it is not significant, while the mean vertical motion acting on the anomalous MSE adds +1.58 ± 0.12 W·m⁻² (p < 0.001). Together, these two terms account for 43% of the net gain, indicating that strengthened ascent efficiently transports high-MSE air from the boundary layer into the free troposphere, enhancing column moist enthalpy and conditional instability.

Figure 4. Area-averaged JJA anomalies of the moist static energy (MSE) budget components (GGW minus Control) over the Sahel (10˚ N - 20˚ N, 20˚ W - 40˚ E). The six terms are: (a) net MSE tendency (Fnet); (b) anomalous vertical velocity × mean MSE gradient ( 〈 ω ′ ∂ p ¯ h 〉 ); (c) mean vertical motion × anomalous MSE ( 〈 ω ¯ ∂ p h ′ 〉 ); (d) mean horizontal flow × anomalous MSE ( − 〈 V ¯ · ∇ h ′ 〉 ); (e) anomalous horizontal flow × mean MSE gradient ( − 〈 V ′ · ∇ h ¯ 〉 ); and (f) residual. Error bars indicate the 95% confidence interval based on interannual variability over 30 JJA seasons. Asterisks mark statistical significance from a one-sample t-test against zero (*p< 0.05, **p < 0.01, ***p < 0.001). All terms are significant at p < 0.001, all in (W·m⁻²).

Horizontal advection partially offsets this energy gain. The mean flow acting on anomalous MSE exports energy (−2.53 ± 0.21 W·m⁻², p < 0.001), contributing 35% of the net change, whereas the anomalous circulation acting on the mean MSE gradient imports energy (+1.29 ± 0.10 W·m⁻², not significant), contributing 18% and reinforcing low-level moisture convergence. The residual term (−5.54 ± 0.53 W·m⁻², p < 0.001) remains within acceptable bounds, confirming satisfactory budget closure. Overall, circulation-driven advection supplies two-thirds of the total MSE increase, with enhanced ascent as the primary mechanism sustaining the northward expansion of convective energy. All budget terms are statistically significant at the 99.9% confidence level, underscoring the robustness of the greenbelt-induced energetic reorganization.

Figure 5. Spatial distributions of area-averaged JJA moist static energy (MSE) budget anomalies (GGW minus Control) over the Sahel (10˚N - 20˚N, −20˚W to 40˚E): (a) net MSE tendency; (b) anomalous vertical velocity × mean MSE gradient; (c) mean vertical motion × anomalous MSE; (d) mean horizontal flow × anomalous MSE; (e) anomalous horizontal flow × mean MSE gradient; and (f) residual (all in W·m⁻²).

Spatially, Figure 5(a) reveals that the net MSE anomaly (GGW minus Control) is strongly enhanced over the central Sahel, indicating increased atmospheric energy gain. This further supports deep convection and intensified monsoon circulation. The anomalous ascent acting on the mean MSE gradient (Figure 5(b)) shows strengthened upward motion over the central Sahel, which signifies lifting of high MSE air into the free atmosphere and increases column moist enthalpy. Similarly, mean ascent acting on anomalous surface MSE (Figure 5(c)) remains positive over the greening region, implying that elevated low-level MSE (Figure 2(c)) further amplifies convection. However, horizontal advection exerts a compensating yet reorganizing influence. The mean flow acting on anomalous MSE (Figure 5(d)) reveals negative values, indicating partial energy export. By contrast, anomalous wind (Figure 5(e)) becomes positive, importing high MSE air onto the Sahel, enhancing low-level moisture convergence. Intensified ascent and reorganized moisture transport sustain the MSE surplus ([22]); the residual term (Figure 5(f)) revealed decreasing value over the entire Sahel.

Figure 6 presents the area-averaged energy flux anomalies and their spatial distributions, now with 95 % confidence intervals derived from 30-year interannual variability and significance testing. The Sahel greenbelt forcing produces a net atmospheric energy flux gain of +7.67 ± 3.61 W·m⁻² (p < 0.001), while the surface net flux decreases (−2.85 ± 2.47 W·m⁻², p < 0.05) and the TOA net flux increases (+4.82 ± 2.64 W·m⁻², p < 0.01). This contrast implies enhanced radiative input at the top of the atmosphere and stronger upward turbulent energy transfer from the surface, resulting in atmospheric energy accumulation.

Among the individual components, the shortwave flux at the surface (FSNS: +5.73 ± 1.65 W·m⁻², p < 0.001) is the dominant contributor, accounting for approximately 75% of the atmospheric net flux gain, followed by latent heat flux (LHFLX: +4.33 ± 0.97 W·m⁻²,p < 0.001; 56% contribution), net shortwave at the top of atmosphere (FSNT: +3.18 ± 1.16 W·m⁻², p < 0.001), and sensible heat flux (SHFLX: +3.07 ± 0.66 W·m⁻², p < 0.001). By contrast, the longwave components at the surface (FLNS: −1.19 ± 1.41 W·m⁻², p > 0.05) and at the top of the atmosphere (FLNT: −1.65 ± 2.37 W·m⁻²,p > 0.05) partially offset the energy surplus through enhanced radiative cooling, although these terms are not statistically significant. The dominance of shortwave radiation and latent heat flux indicates increased solar absorption and evapotranspiration, which are the primary drivers of atmospheric moist static energy enhancement.

Spatially, the TOA net flux (Figure 6(a)) shows widespread positive anomalies over the northern and central Sahel, implying strengthened radiative forcing. Stippling indicates that these positive anomalies are statistically significant (p < 0.05) over most of the Sahel. Conversely, the surface net flux (Figure 6(b)) exhibits negative anomalies over the entire Sahel, revealing enhanced upward turbulent fluxes (latent and sensible heat), with significant negative anomalies (p < 0.05) widespread across the region. These patterns result in increased atmospheric net flux markedly over the central and eastern Sahel (Figure 6(c)), where significant positive anomalies (p < 0.05) cover large areas, confirming that vegetationinduced surface energy redistribution favors atmospheric energy accumulation. Enhanced shortwave absorption together with strengthened turbulent heat flux transfers energy from the surface into the atmosphere, amplifying moist static energy ([36]).

Overall, TOA net flux increases over the northern and central Sahel while surface net flux decreases, confirming energy transfer from land to atmosphere and reinforcing Sahelian convection and monsoon circulation. All reported area-averaged values are accompanied by their 95% confidence intervals, and the spatial significance hatching provides robust evidence for the greenbeltinduced energetic changes.

Figure 6. Area-averaged energy flux anomalies (case surface minus case) (W·m⁻²) over the Sahel [10˚N - 20˚N, 20˚W - 40˚E]. The bar plot shows the mean anomalies (horizontal bars) with 95% confidence intervals (error bars) based on interannual variability over 30 JJA seasons. Asterisks denote statistical significance from a one-sample t-test against zero (*p < 0.05, **p < 0.01, ***p < 0.001). The individual radiative and turbulent components shown are: FSNS, FSNT, FLNS, FLNT, LHFLX, and SHFLX, along with the derived TOA net, surface net (Fnet), and atmospheric net fluxes. The maps display the spatial patterns of (a) TOA net flux; (b) surface net flux (Fnet); and (c) atmospheric net flux anomalies over the Sahel. Stippling on the maps indicates grid cells where the difference is statistically significant at the 95% confidence level (p < 0.05).

Building on the flux budget analysis (Figure 6), the spatial structure of individual flux components reveals distinct patterns of energy redistribution (Figure 7). The shortwave flux anomalies FSNT (Figure 7(b)) and FSNS (Figure 7(a)) exhibit widespread positive anomalies over the central and eastern Sahel, with values ranging from approximately +3 to +8 W·m⁻². Hatching confirms that these increases are statistically significant (p < 0.05) across most of the region. Enhanced turbulent heat fluxes, particularly LHFLX (Figure 7(e)) and to a lesser extent SHFLX (Figure 7(f)), also show significant positive anomalies (p < 0.05) over the central and eastern Sahel, with mean areaaveraged increases of +4.33 ± 0.97 W·m⁻² and +3.07 ± 0.66 W·m⁻², respectively. The increased latent heat flux reflects enhanced evapotranspiration and moisture supply, which in turn shifted the MSE maxima northward (Figure 2(c)).

In contrast, the longwave fluxes FLNT (Figure 7(d)) and FLNS (Figure 7(c)) reveal widespread negative anomalies over the entire Sahel, implying enhanced radiative cooling at the surface and to space. However, these negative anomalies are largely not statistically significant (p > 0.05), as indicated by the absence of hatching over most of the region. This cooling promotes turbulent heat transfer to the atmosphere ([34]), but the lack of significance suggests greater interannual variability in longwave components. Overall, shortwave fluxes and latent heat flux emerge as the dominant and statistically robust contributors to the MSE enhancement, driving the northward shift in convective energy.

Figure 7. Spatial patterns of individual radiative and turbulent flux anomalies (case surface minus case) (W·m⁻²) over the Sahel [10˚N - 20˚N, 20˚W - 40˚E]. The six components shown are: (a) FSNS (surface net shortwave); (b) FSNT (TOA net shortwave); (c) FLNS (surface net longwave); (d) FLNT (TOA net longwave); (e) LHFLX (latent heat flux); and (f) SHFLX (sensible heat flux). Hatching (stippling) indicates grid cells where the difference is statistically significant at the 95% confidence level (p < 0.05) based on a paired t-test over 30 JJA seasons. The Sahel analysis box (10˚N - 20˚N, 20˚W - 40˚E) is outlined in black. All values are in W·m⁻².

Figure 8 represents the JJA climatology of vertically integrated components of MSE over the Sahel. The total MSE in the Control (Figure 8(a)) reveals a maximum south of the Sahel near 15˚N, while the GGW (Figure 8(b)) shows a modest enhancement with a similar core location. The change field (Figure 8(c)) shows a pronounced increase in total MSE over the central Sahel and shifts its maxima northward (Figure 2(c)). The temperature component in the GGW (Figure 8(e)) increases above 15˚N, whereas the change field (Figure 8(f)) shows a notable decrease in the central Sahel and shifts northward, reflecting the redistribution of thermal energy. The moisture component, the GGW (Figure 8(h)), decreases above 15˚N, whereas the change field (Figure 8(i)) reveals a substantial increase in moisture above 15˚N, especially over the central Sahel. This contributes to MSE enhancement (Figure 2(c)), whereas the geopotential component, the change (Figure 8(l)), reveals a widespread decrease, implying potential energy, which favors convection.

Figure 8.JJA climatology of vertically integrated MSE components over the Sahel. Panels show (a) - (c) total MSE; (d) - (f) temperature component; (g) - (i) moisture component, and (j) - (l) geopotential component for control (left), GGW (middle), and Sahel greenbelt induced change (GGW minus Control, the right one).

Figure 9. JJA climatology of MSE energy components over the Sahel. Panels show (a) - (c) sensible heat; (d) - (f) latent heat; and (g) - (i) geopotential energy for the Control, GGW, and Sahel greenbelt change (GGW minus change).

Increased moisture, reduction in temperature, and geopotential enhance MSE and shift energy maxima northward ([5])

Figure 9represents the JJA climatological distribution of MSE energy components; from these, the latent heat energy change (GGW minus Control) (Figure 9(f)) dominates the MSE response, driving both the amplification and northward migration of total MSE change (Figure 2(c); Figure 8(c)). This pronounced increase in latent heat energy north of 15˚N and its poleward displacement (Figure 9(f)) provide the primary positive contribution to the enhancement of MSE. In contrast, sensible heat change (Figure 9(c)) and geopotential energy change (Figure 9(i)) exhibit widespread decreases over the Sahel, enhancing the total MSE by lowering surface temperature and increasing atmospheric moisture. The reduction in sensible heating (Figure 9(c)) weakens surface thermal contributions, while the decline in geopotential energy change (Figure 9(i)) reduces the gravitational component of the column energy. However, these negative contributions remain secondary to the strong moisture-driven enhancement.

Overall, the result indicates that Sahelian MSE variability is primarily moisture-controlled (Figure 8(i)), with latent heat changes (Figure 9(f)) governing the net MSE intensification and shifting northward (Figure 2(c)).

In the next term, we will explain the vertical profile of MSE components.

Figure 10 shows the vertical cross-section of MSE components along 0˚E for the control, GGW, and the green belt-induced vegetation change (GGW minus Control). Sensible heat (Figures 10(a)-(c)), the control (Figure 10(a)), exhibits an increase over the monsoon region (1000 - 850 hPa) (10˚N - 20˚N) and decreases with altitude, reflecting strong surface heating and a decrease in boundary layer humidity. The impact of the greenbelt/change/(Figure 10(c)) reveals a reduction in lower-tropospheric sensible heat, indicating suppressed turbulent fluxes, with minor compensation above 700 hPa, consistent with slight vertical redistribution of thermal energy. Latent heat (Figures 10(d)-(f)): control (Figure 10(d)) shows a pronounced increase in latent heat in the lower troposphere over the monsoon core, indicative of active moisture convergence and convection. The change (Figure 10(f)) reveals positive anomalies intensifying throughout the lower troposphere, extending northward to the Sahel, with persistent signals above 700 hPa, highlighting enhanced vertical moisture transport and amplified column-integrated MSE.

Geopotential energy (Figures 10(g)-(i)), in the control (Figure 10(g)), geopotential height decreases in the lower troposphere over the monsoon region, supporting ascent. The change (Figure 10(i)) produces further reduction in the lower troposphere, aligned with stronger ascent, and modest increases aloft, reflecting vertical redistribution and reinforcing convective organization ([3]).

In summary, across the vertical column, greenbelt-driven vegetation restoration enhances latent heat fluxes and lower-tropospheric MSE while reducing sensible and geopotential energy. The moisture process is the dominant driver of tropospheric energy organization in the Sahel, promoting energy maxima northward.

Figure 10. Vertical cross-section of JJA MSE components along 0˚E over the Sahel. Panels show sensible heat (a) - (c); latent heat (d) - (f); and geopotential energy (g) - (i) for the Control, GGW, and Sahel greenbelt induced change (GGW minus Control).

Next, we will observe the changes in MSE transport.

Figure 11 illustrates the JJA climatological distribution of moist static energy (MSE) and winds at 850, 600, and 200 hPa, revealing vertical dynamical controls of Sahelian moist static energy.

At 850 hPa, the GGW (Figure 11(b)) reveals enhanced MSE peaks near 15˚N, fed by strengthened southwesterly moisture advection from the tropical Atlantic. Intensified northeasterly trade winds limit northward moisture penetration, which weakened MSE’s northern part. The change (Figure 11(f)), stronger low-level westerlies and weakened northeasterly trade winds, reduced dry air intrusion, allowing moisture to extend farther north and east, favoring the MSE maxima northward.

At 600 hPa, the GGW (Figure 11(e)) African easterly jet flows deeper southward, and the enhanced northeasterly flow promotes mid-level dry intrusion, suppressing MSE north of 12˚N. The change field (Figure 11(f)) northeasterly dry intrusion becomes weaker, and enhanced southwesterlies strengthen enhanced meridional moisture transport and shift the MSE core northward.

At 200 hPa, the GGW (Figure 11(h)) strengthened the tropical easterly jet with a core found in the eastern part, with MSE decreasing over the entire Sahel. The change field (Figure 11(i)) reveals that the TEJ becomes strongly retreated and weakens, as well as the northeasterly trade wind weakening; however, the MSE still decreased, implying that TEJ has an indirect role in regulating MSE ([41]). Overall, Sahelian MSE variability is dominated by low-level moisture advection and vertical warm air transport, while the TEJ plays a secondary role.

Figure 11. JJA climatological distribution of MSE and wind vectors at 850 hPa (a) - (c); 600 hPa (d) - (f) and 200 hPa (g) - (i) for Control, GGW and GGW minus Control.

Figure 12. JJA zonal mean meridional structure of total MSE and its components over the Sahel. Panels show the climatological mean for (a) the control experiment, (b) the GGW experiment, and (c) their difference (GGW minus Control), highlighting the meridional distribution and moisture-driven amplification of MSE in response to vegetation restoration.

Figure 12 presents the JJA zonal mean meridional structure of total moist static energy (MSE) and its components. Panels (a) and (b) show the climatological means for the control and GGW experiments, respectively, while panel (c) displays their difference (GGW minus Control). In the control experiment (Figure 12(a)), the climatological zonal mean shows that total MSE and its latent heat component are higher south of 15˚N, while they are lower over North Africa. In contrast, the sensible heat and geopotential components are higher north of 15˚N. This meridional contrast indicates that thermodynamic drying and enhanced static stability dominate over North Africa, whereas moisture-driven energy increases are confined to the Sahel in the mean state. The GGW experiment (Figure 12(b)) reveals that total MSE becomes the dominant component north of 15˚N, closely followed by latent heat. Concurrently, the sensible heat and geopotential contributions weaken, implying a transition from dry static energy to moisture-dominant energy amplification.

The greenbelt-induced change (GGW minus Control, Figure 12(c)) further supports this: sensible heat and geopotential energy show negative anomalies over the northern Sahel, while total MSE and latent heat exhibit positive anomalies poleward of 15˚N. This response is primarily moisture-driven rather than dynamically forced ([12]). Overall, the GGW amplifies the latent heat component of MSE, playing a dominant role in moisture and associated energy transport in modulating Sahelian thermodynamic structure.