{'fraction_non_alphanumeric': 0.0324759385377385, 'fraction_numerical': 0.03067484662576687, 'mean_word_length': 4.859993403693931, 'pattern_counts': {'":': 0, '<': 0, '<?xml version=': 0, '>': 3, 'https://': 2, 'lorem ipsum': 0, 'www.': 0, 'xml': 0}, 'pii_count': 0, 'substrings_counts': 0, 'word_list_counts': {'cursed_substrings.json': 0, 'profanity_word_list.json': 0, 'sexual_word_list.json': 0, 'zh_pornsignals.json': 0}}
Investigating the response of the Botswana High to El Niño Southern Oscillation using a variable resolution global climate model

The Botswana High is an important component of the regional atmospheric circulation during austral spring, summer and autumn. While the high tends to be stronger during El Niño and weaker during La Niña, its direct response to El Niño Southern Oscillation (ENSO) remains unknown. To that end, a variable resolution global climate model (Model Prediction Across Scales version 7, hereafter MPAS) is applied with relatively high resolution (48-km grid spacing) over Southern Africa and a coarser resolution (240-km grid spacing) over the rest of the globe for the study period 1980–2010. The first model experiment uses observed sea surface temperatures (SSTs) everywhere during the study period, while the second experiment uses observed SSTs everywhere except over the Pacific Ocean, where monthly climatological SSTs are imposed. The model results were validated against satellite data (Global Precipitation Climatology Project, GPCP) and reanalysis datasets (Climate Forecast System Reanalysis, CFSR; European Centre for Medium-Range Weather Forecasts version 5, ERA5). The results of the study show that the MPAS model gives a credible simulation of the temporal variability of the Botswana High, the seasonal rainfall and 500-hPa geopotential heights over Southern Africa. In the absence of ENSO forcing, the amplitude of the Botswana High variability reduces but the signal of the variability remains. Hence, this study shows that ENSO enhances the strength of the Botswana High but does not aid in the formation of the high.


Introduction
The Botswana High, a prominent feature in the mid-levels (~ 500 hPa) over Southern Africa, is an important component of the regional atmospheric circulation during austral spring, summer and autumn (Reason 2016;Driver and Reason 2017;Maoyi and Abiodun 2021). While the system is named "Botswana", a large part of it is located over eastern Namibia (see Fig. 1). The high typically forms around August, shifting south as it strengthens throughout spring becoming stronger in the late summer (January, February and March). In April, the high moves northwards from its March position, weakens over the landmass and dissipates around May. It links its movement as it shifts south-eastwards to the movement of regions of high rainfall over the Congo basin and the intertropical convergence zone (ITCZ), which lie to its northeast (Driver and Reason 2017). The strengthening of the high is typically characterised by increased subsidence over Southern Africa that suppresses moisture convergence and the development of tropical-extratropical cloud bands or tropical temperate troughs (TTTs) and may lead to less rainfall. Conversely, the weakening of the high favours the development of TTTs, the main summer rainfall producing systems and anomalous wet summers. According to Driver and Reason (2017), the Botswana High variability also affects the frequency of dry spells during summer (JFM), maximum surface temperatures and maximum temperature extremes. These parameters strongly influence drought, which significantly impacts food supply as the people's livelihood highly depends on rain-fed agriculture. Considering this, a better understanding of the Botswana High variability may lead to a better seasonal forecasting of drought over Southern Africa and a better response capacity. The aim of the present study is in that direction.
Several studies have been conducted to understand the summer variability of the Botswana High, some of which have identified the El Niño Southern Oscillation (ENSO) to be one major cause of the variability (Driver and Reason 2017;Reason 2018;Maoyi and Abiodun 2021). In general, the high tends to intensify during El Niño associated summers over Southern Africa and weaken during La Niña events; however, the magnitudes of the Botswana High anomalies are not necessarily proportional to the strength of ENSO events. For example, Driver and Reason (2017) showed that the anomaly in the high during the intense 1997/1998 El Niño event was less than the weaker 1986/1987 El Niño event. Furthermore, there have also been summers over Southern Africa that were unusually wet or dry but did not coincide with an ENSO event but did correspond to significant anomalies in the Botswana High. As a result, gaining a better understanding of the Botswana High variability may provide useful information and another metric for monitoring and evaluating rainfall over the subcontinent. Despite that, we should note that previous studies have used analyses such as correlation and composite analyses in determining the relationship between ENSO and the Botswana High, which cannot determine cause and effect relationships. Therefore, it is unknown if the Botswana High variability is a response to ENSO. That is the motivation for this study.
This study presents a global climate model (GCM) sensitivity experiment using Model for Prediction Across Scales (MPAS; Skamarock et al. 2012) to demonstrate the causal relationship between ENSO and the Botswana High. The MPAS model has been used in several sensitivity experiments (Davis et al. 2016;Fowler et al. 2016;Zhao et al. 2016;Judt 2020). Zhao et al. (2016) used four different quasi-uniform resolution meshes (30, 60, 120 and 240 km) and a variable resolution mesh (120-30 km) in studying the impacts of resolution and physics (CAM4 vs CAM5) on the precipitation, clouds and large-scale circulation in an aquaplanet simulation. Using two configurations on MPAS, Davis et al. (2016) compared a uniform 15-km mesh to a variable resolution mesh (60-15 km) in simulating tropical cyclones in the eastern Pacific and found that the two configurations performed nearly identical to each other and performed comparably to the Global Forecast System. Fowler et al. (2016) evaluated the performance of the Grell-Freitas parameterisation scheme using variable resolution meshes, which varied between hydrostatic (50 km) and nonhydrostatic (3 km) scales and found that by increasing horizontal resolution, the subgrid-scale motions become increasingly resolved. Judt (2020) studied atmospheric predictability by using a set of twin experiments (Judt 2018;Zhang et al. 2007) and found that tropics have longer predictability than midlatitudes and polar regions (tropics, > 20 days; midlatitudes and polar regions, a little over 2 weeks).
This study investigates the response of the Botswana High to 1982/1983, 1991/1992/1998and 2009/2010(hereafter 1983, 1992, 1998and 2010respectively) El Niños and 1984/1985, 1988/1989, 1999/2000/2008(hereafter 1985, 1989, 2000and 2008 respectively) La Niñas. Although this set does not include all ENSO events, we selected those years as they represent the strongest ENSO events between 1980 and 2010. Furthermore, we focus on the late summer season (JFM), when ENSO impacts are typically more significant and consistent than early summer (October to December) (Driver et al. 2018). The paper is organised as follows: Section 2 describes the data used in the study and the methods. The results of the study are discussed in Section 3, while Section 4 presents the conclusion.

Data
We analysed observational, reanalysis and model simulation data for the study period 1980-2010. The observational data included monthly rainfall data obtained from the Global Precipitation Climatology Project Version 2.3 dataset (hereafter GPCP; Adler et al. 2003). The GPCP dataset has a resolution of 2.5° × 2.5° grid resolution and is used to evaluate the model-simulated rainfall over Southern Africa. Six hourly observed sea surface temperatures (SSTs) and sea-ice data were retrieved from the Climate Forecast System Reanalysis (CFSR; Saha et al.2014). The CFSR data is provided by the National Centers for Environmental Prediction (NCEP) and is obtainable from https:// rda. ucar. edu/ datas ets/ ds093.1/. The SST dataset has a grid resolution of 0.31° × ~ 0.31° and is used to force the model simulation and calculate the ENSO index.
The monthly geopotential height, with a horizontal resolution of 0.25° × 0.25° and 37 levels, was obtained from the 5th generation European Centre for Medium-Range Weather Forecast reanalysis (Hereafter ERA5;Hersbach et al.2018) data (https:// cds. clima te. coper nicus. eu) and was used to evaluate how well the MPAS model simulates the seasonal characteristics of the 500-hPa geopotential height over Southern Africa as well the interannual variability of the Botswana High.
The monthly 500-hPa geopotential height and rainfall data with a spatial resolution of 240 km were obtained from the MPAS version 5.2 (MPAS5) simulation output of Maoyi and Abiodun (2021). The MPAS5 uniform grid output (240 km) was used to evaluate how well the MPAS variable resolution grid (240 km globally and 48 km over Southern Africa) improves the climatic features over Southern Africa and the interannual variability of the Botswana High.

Model description and experiments
The model utilised in this study is the most recent version of the Model for Prediction Across Scales version 7.0 model (MPAS), which is a fully compressible nonhydrostatic global climate model that utilises Voronoi tessellations (Du et al. 1999) to generate variable resolution meshes. The variable resolution grid structure allows high-resolution areas to transition to lower resolution areas, avoiding boundary issues that plague conventional regional climate models.
MPAS uses Advanced Research WRF (ARW) model physics as well as an atmospheric fluid-flow dynamical core. The numerical schemes used in MPAS are similar to those used in the ARW model with the exception that ARW uses rectangular meshes and a hydrostatic vertical coordinate while the fully compressible nonhydrostatic equations in MPAS are derived in terms of a geometric height vertical coordinate, and the solvers use a split-explicit time integration scheme which is described in Klemp et al. (2007). For meteorologically significant modes, the time integration scheme employs a 3rd Order Runge-Kutta method, a large time step and a forward-backward method with a smaller time step for acoustic modes.
In the present study, the MPAS model grid is set to a variable resolution of 48 km over Southern Africa and 240 km worldwide (Fig. 2). The variable resolution grid contains 30,210 grid cells and refines by a factor of 5 (from 240-km grid spacing to 48 km grid spacing), satisfying the Caian-Geleyn condition of limiting the refinement factor to less than 8 in order to minimise pole symmetric dilations (Caian and Geleyn 1997). The prevailing advantage of using variable resolution grids is applying higher resolution over an area of interest without requiring substantial computational power as with uniform high-resolution grids. The model simulation uses 41 vertical levels with an integration time step of 240 s and an output rate of daily data. The model topography was obtained by interpolating the U.S. Geological Survey (USGS) Global Multi-resolution Terrain Elevation Data (GMTED2010) dataset into the MPAS grid ( Fig. 1). Two experiments were performed in this study, consisting of a 32-year control integration and a set of SST perturbation experiments. The control integration (hereafter CTRL) runs from the 1st of January 1979 till the 31st of December 2010; however, the results from 1979 were discarded as spin-up and only data from 1980 till 2010 was considered. For the control run to give a more realistic simulation, the integration was configured to update with 6 hourly CFSR SST and sea-ice data. For the second experiment, a series of August-April integrations with perturbed SST (hereafter NoENSO) were conducted for four El Niño (1983, 1992, 1998 and 2010) and four La Niña (1985, 1989, 2000 and 2008) years. In the 9-month integrations, the SST is the same as in the control run except that monthly climatological SSTs are imposed over the Pacific Ocean in order to remove the influence of ENSO. For each 9-month integration, 10 ensembles were carried out with slightly different initial conditions to represent internal atmospheric variability. The initial conditions are taken from the previous years' August 20th-29th snapshots (restart files) of the control run.

Model validation
To evaluate the capability of MPAS in simulating the climatic features over Southern Africa, we compared the simulated data (rainfall and 500-hPa geopotential height) to observed, reanalysis and MPAS model data. In the evaluation, we used spatial correlation and root-mean-square error (RMSE) to measure the model's similarity with climatic patterns over Southern Africa with respect to the observational and reanalysis datasets. In addition, we used R 2 analysis to quantify the proportion of the Botswana High variance that ENSO predicts and Pearson correlation to assess the strength and direction between the MPAS simulation, MPAS5, reanalysis and SST data.

ENSO quantification
The ENSO index was quantified using the Ocean Niño Index, which is the most common index used to monitor ENSO. We calculated the ENSO index as a 3-month running mean of SST anomalies in the Niño 3.4 region (5°N-5°S, 170°W-120°W). El Niño (La Niña) periods were defined when SST anomalies in the Niño 3.4 region are above (below) + 0.5 (− 0.5) for five consecutive months. For this study, the ENSO index was calculated using CFRS SST data for the period 1980-2010.

Identification of Botswana High
To identify the Botswana High feature, an empirical orthogonal function (EOF) analysis of the 500-hPa geopotential height was performed over Southern Africa on the ERA5 reanalysis and the monthly model-simulated data between 1980 and 2010. The analysis was performed for the late summer (JFM) season. The Botswana High typically lies on the southern portion of the continent, and therefore, the region lying between 10°E and 40°E and from the equator to 33°S was chosen to exclude the influence of oceans and their anticyclones. Additionally, we also quantified the Botswana High index using a spatial average of the 500-hPa geopotential height anomalies over the Botswana High core region (5°-22° E; 20°-25°S) in order to verify whether the EOF analysis is physically related to the temporal variability of the 500-hPa geopotential height over the Botswana High core region.

Assessing the response of the Botswana High to ENSO
To assess the response of the Botswana High to ENSO, two model experiments are conducted. The first experiment uses observed SSTs everywhere (CTRL), while the second experiment uses observed SST everywhere except over the Pacific Ocean, where monthly climatological SSTs are used. By prescribing monthly climatological SSTs over the Pacific, we essentially removed the ENSO signal and therefore referred to this experiment as NoENSO. These experiments are aimed to better understand the sensitivity of global and regional climatic features to ENSO events and how those impact the Botswana High. To further investigate the link between the Botswana High and ENSO, we analysed anomalies in the 500-hPa geopotential height, velocity potential and eddy stream function from the MPAS simulation data. We calculated the velocity potential and stream function from the MPAS model output of horizontal (U) and vertical wind (V). Figure 3a shows a strong association in the interannual variability of the Botswana High and ENSO. The MPAS, MPAS5 and ERA5 show a high correlation between the Botswana High and ENSO (r = 0.84, r = 0.81 and r = 0.89, respectively). In addition, the Botswana High in MPAS shows a higher correlation with the one in ERA5 (r = 0.89) as compared to MPAS5 Botswana High (r = 0.87). These results show that the MPAS model improves the simulation of the interannual variability of the Botswana High, although by a small margin. Both models and reanalysis indicate the strongest Botswana High during the strong El Niño years (1983, 1998 and 2010), while the weakest Botswana High occurred in La Niña years (1985, 1989 and 2000) (Fig. 3a). This is in agreement with previous studies by Driver and Reason (2017 Figure 3b shows a scatter plot between the Botswana High and ENSO. As mentioned above, there seems to exist a quasi-linear relationship between the Botswana High and ENSO. At a 95% confidence limit, the adjusted R 2 values indicate that ENSO explains about 70%, 65% and 79% of Botswana High variability in the MPAS, MPAS5 and ERA5 datasets, respectively. Again, the MPAS model improves the relationship between Botswana High and ENSO (70%) as compared to MPAS5 (65%). Given the strong association between the Botswana High and ENSO, the question then arises as to whether the Botswana High is a result of forcing from ENSO. To address this, the response of the Botswana High to the removal of ENSO forcing is discussed in Section 3.3.

Composite anomalies over Southern Africa
We evaluate the MPAS simulation over Southern Africa by comparing it with GPCP observation, ERA5 reanalysis and MPAS5 model data (Figs. 4 and 5). The validation focuses on the spatial distribution of rainfall (Fig. 4) and the 500-hPa geopotential height (Fig. 5) in JFM of El Niño years (1983, 1992, 1998and 2010) and La Niña Years (1985, 1989, 2000and 2008. Figure 4 shows that MPAS simulates the well spatial distribution of rainfall over Southern Africa, except that the simulation generally has a better agreement with GPCP during El Niño years composite (r = 0.85; RMSE = 1.67) than during La Niña years composite (r = 0.80; RMSE = 2.12). During the El Niño years, the model captures well the band of maximum rainfall over the tropics (associated with the South Indian Convergence Zone, SICZ) with a wet bias of about ± 1 mm day −1 . It also reproduces well the rainfall over the eastern parts of the continent and areas of minimum rainfall over the central and western parts of South Africa and Namibia. However, over Madagascar, the model fails to capture the local maximum rainfall as in GPCP. This lack of maximum rainfall over Madagascar may be attributed to the overestimation of deep convection over the Mozambique Channel (MC) area (Figs. 4b, f, j, n and r), which may suppress convection over adjacent areas leading to the inability of MPAS to stimulate the local maximum rainfall over Madagascar. Despite that, the MPAS composite (r = 0.85; RMSE = 1.67) shows that the MPAS variable resolution generally improves the rainfall simulation over the region compared to the uniform resolution MPAS5 composite (r = 0.83; RMSE = 1.78) during El Niño years.
During the La Niña years, the MPAS model underestimates the summer rainfall over the eastern and central parts of Botswana, Mozambique and South Africa (by about 3 mm day −1 ). This may be attributed to the overestimated deep convection extending farther south of the MC (Figs. 4d, h, l, p and t), leading to the suppression of convective rainfall and a dry bias over the eastern and central parts of the Southern African continent. Furthermore, the overestimation of deep convection over the MC is greater in the MPAS variable grid than the MPAS5 uniform grid during La Niña. This reduces the accuracy of the MPAS in simulating the regional rainfall as compared to MPAS5. This result is consistent with Maoyi et al. (2017) and Driver et al. (2018), who noted a similar wet bias over the MC using a 50-km stretched grid GCM (called CAM-EULAG). The wet bias could be due to the convective parameterisation in the model, which might be too sensitive to the warm boundary layer over the region. Another cause for this wet bias could be the horizontal resolution sensitivity of moist physics as highlighted by Williamson (2008) or the parameterisation time step in the model simulation as indicated by Williamson and Olson (2003).
MPAS shows good agreement with ERA5 on the 500-hPa geopotential height spatial pattern during El Niño years composite (r = 0.96; RMSE = 10.08) and La Niña years composite (r = 0.96 RMSE = 7.63). In general, both the MPAS and reanalysis show higher values of the 500-hPa geopotential height during El Niño years and lower values during La Niña years, suggesting that El Niño (La Niña) summers may be the driving force in the strengthening (weakening) of the 500-hPa geopotential height over Southern Africa, which may lead to the strengthening (weakening) of the Botswana High. This result is in agreement with previous studies by Reason (2016) and Driver and Reason (2017), who also found that the high is always stronger (weaker) during El Niño (La Niña) summers. Furthermore, the strong spatial correlations (r > 0.9) indicate that the model has adequate skill in reproducing the dominating features of the 500-hPa geopotential height over Southern Africa but with some discrepancies. For instance, the model shows enhanced geopotential heights in the subtropics and lower anomalies poleward of 30°S as in ERA5. In addition to that, the model captures the local maximum geopotential height pattern over Southern Africa (which is reminiscent of the Botswana High) as in ERA5 (e.g. Figures 5a, e, i, m and q). Despite the higher resolution of MPAS variable grid simulation (48 km) than the MPAS5 uniform grid simulation (240 km) over Southern Africa, the MPAS results do not seem to always improve on that of MPAS5, as shown by the correlation and RMSE. While the MPAS simulation outperforms the MPAS5 simulation in some years (i.e. 1992, 2010, 1989 and 2008), the opposite is true in other years (1983, 1998, 1985 and 2000). Several factors could make the higher resolution MPAS simulation not to always outperform the coarserresolution MPAS5 simulation. For example, both models use different land-use and topography data, which may impact results over high lying regions over Southern Africa. Another reason could be the difference in the physics scheme between MPAS (WRF v4.0.3 physics) and MPAS5 (WRF v3.8.1 physics), which might have their strengths and weaknesses over Southern Africa. Figure 6 shows the interannual variability of the Botswana High in the CTRL and NoENSO for the EOF analysis Fig. 4 The spatial distribution of JFM rainfall (mm/day; shaded) over Southern Africa as depicted by GPCP and MPAS during the El Niño years (columns 1 and 2) and La Niña years (columns 3 and 4). The contours in the GPCP panels show the bias in the MPAS5 model simulation with reference to the GPCP (i.e. MPAS5-GPCP), while contours in the MPAS panels show the bias in the MPAS model simula-tion with reference to the GPCP (i.e. MPAS-GPCP). In the GPCP panels, the r-value represents the spatial correlation between GPCP and MPAS5 and RMSE represents the root-mean-square error. In the MPAS panels, the r-value represents the spatial correlation between GPCP and MPAS, and RMSE represents the root-mean-square error ( Fig. 6a) and spatial average analysis (Fig. 6b). The time series associated with the EOF Botswana High index (Fig. 6a) shows good similarity with the spatial average Botswana High index. This result indicates that the EOF Botswana High is physically related to the temporal variability of the 500-hPa geopotential height over the Botswana High core region. In light of this, the impact of ENSO on the temporal variability of the Botswana High is evident. In general, NoENSO shows that with the removal of the ENSO forcing (El Niño or La Niña), the amplitude of variability in Botswana High reduces; however, the signal of the Botswana High variability still remains. This indicates that the Botswana High mode is independent of ENSO forcing while the magnitude of the variability is enhanced during ENSO events. Figure 6 also suggests that there are cases when ENSO forcing may alter the signs of the Botswana High mode, either from + ve phase to − ve phase (as in 1992) or from + ve phase to − ve phase (as in 2008). This may be due to the internal variability of ENSO SST anomalies within the Pacific Ocean, creating different ENSO flavours that may impact the Botswana High distinctively. The 500-hPa geopotential height composites show good agreement with the Botswana High's interannual variability during El Niño Years (Figs. 7a and 8a). At regional scale (over Southern Africa), there is an overall decrease in the 500-hPa geopotential height over Southern Africa (Figs. 7a, c, e, g and i) which is consistent with the decrease in the interannual variability of the Botswana High index in 1983, 1992, 1998 and 2010; however, the largest decrease is over the northeastern parts of the Southern African region, which is typically an area of high precipitation associated with the SICZ. Basically, the removal of El Niño influence leads to increased convection over the SICZ area leading to increased precipitation over northern Madagascar, Mozambique Channel and much of the northeastern parts of the subcontinent. At global scale (Figs. 8a, c, e and g), all El Niño years (1983,  Fig. 4 but for JFM 500-hPa geopotential height Fig. 6 The interannual variability of the simulated Botswana High in the control (CTRL) and no ENSO (NoENSO) experiments. a The Botswana High index is derived from the score of EOF-1 of the JFM 500-hPa geopotential height over the study area (10-14°E, 0-33°S). b The Botswana High index is derived from the spatial average of the 500-hPa geopotential heights over the Botswana High core region (15°-22° E; 20°-25°S) shown in Fig. 1   Fig. 7 Impact of the removal of ENSO forcing (NoENSO minus CTRL) on the 500-hPa geopotential height over Southern Africa during El Niño and La Niña Years 1992, 1998, 2010 show that with the removal El Niño event, there is a decrease in the 500-hPa geopotential height over the tropics and an increase in the subtropics. This response represents a weakening of the Hadley circulation (Cook 2000), and it is generally known from modelling and observational studies (Oort and Yienger 1996;Roeckner et al. 1996). In addition to that, this decrease in the 500-hPa geopotential height over the tropics leads to a reduction in subsidence in the 500-hPa pressure level over Southern Africa (Figs. 7a, c, e, g and i), which in turn reduces the strength of the Botswana High as seen in Fig. 6.

The response of the Botswana High to the removal of ENSO forcing
La Niña composites (Figs. 7b and 8b) show an opposite pattern in the 500-hPa geopotential heights compared to El Niño composites. The regional circulation anomalies show an increase in subsidence over the region, especially over the Mozambique Channel, northern Mozambique and northern Madagascar (Figs. 7b, d, f, h and i). This anomalous increase in subsidence over the SICZ area may inhibit convection, increase temperatures and weaken the SICZ, and lead to decreased precipitation. Reason (2016) attributed the formation of the Botswana High to heat released by tropical regions of high precipitation near the SICZ area. In light of this, the anomalous increase in subsidence and temperature over the SICZ may lead to the formation and strengthening of the Botswana High, as Reason (2016) stated. However, a model experiment similar to Lenters and Cook (1997) is required to prove the veracity of the results, which is beyond the scope of this work.
Globally, there is an overall increase in the 500-hPa geopotential height (NoENSO minus CTRL) over the tropics  (Cook 2000). This increase in the 500-hPa geopotential height leads to an increase in subsidence over Southern Africa and strengthens the Botswana High, as shown by Maoyi and Abiodun (2021). The years 1985 and 1989 indicate a large increase in the 500-hPa geopotential height in the northeastern regions of Southern Africa, which are the same years where there was the highest increase in the Botswana High strength due to the absence of La Niña (see Fig. 6). In agreement with Maoyi and Abiodun (2021), this result implies that the Botswana High strength is sensitive to subsidence over this area during La Niña summers.

Atmospheric dynamics associated with El Niño
The difference in the 200 hPa velocity potential between NoENSO and CTRL years shows an upper tropospheric divergence (negative velocity potential) over the Indian and Western Pacific Ocean (Figs. 9a,c,e,g and i). This upper-level divergence is more pronounced over the northwest pacific and maritime continent, coinciding with deep convection from the warmer SSTs in the region. In contrast, there is a strong upper tropospheric convergence (positive velocity potential) over the eastern Pacific and South America, which coincides with cooler SSTs over that region. This convergence-divergence pattern across the Pacific is a reverse pattern of normal El Niño years and similar to a typical La Niña pattern. In normal El Niño years, the upper-level divergence is located over the eastern Pacific and South America, while the upper-level convergence is typically located over the western Pacific and maritime continent, including Australia. This normal pattern indicates a weakening of the Walker Circulation, which is typical during El Niño years (Reason and Jagadheesha 2005;Ashok et al. 2007;Yuan et al. 2014;Gore et al. 2019). Therefore, the reverse pattern, which is the difference between NoENSO and CTRL, indicates that the Walker Circulation will strengthen in the absence of El Niño. 1983 and1998 show the most strengthening of the Walker Circulation as they were the strongest El Niño years in the study period.
The Southern African continent generally shows divergent flow, with some discrepancies. For example, the divergent flow over Southern Africa is weaker in 1998 and 2010 than it was in 1983 and 1992. This could be due to the Indian Ocean Dipole factor, which could also explain differences in ENSO impacts over Southern Africa (Chikoore and Jury 2021). Despite that, the divergent flow over Southern Africa may strengthen the SICZ and aid in forming tropical temperate troughs (Tyson and Preston-Whyte 2000) while weakening the strength of the Botswana High. Figure 10a, c, e, g and i show the difference between NoENSO and CTRL in the 200 hPa eddy stream function for each El Niño year, highlighting the large-scale stationary wave response. Taking the difference filters out the zonal mean response and only shows the difference in the wave response. All El Niño years show a strengthening of the cyclonic flow in the upper troposphere over the central and eastern Pacific Ocean, associated with the intensity of cooling of SSTs in the region. The strong ENSO event of 1998 generated the strongest anomalies, which indicate that the SST cooling was more intense during that year while the cyclonic flow extended as far as the western Pacific as in 2010. On the contrary, the South Atlantic and South Indian oceans show an increase in the upper tropospheric anticyclonic flow, indicating the warming of SSTs in the region. This warming of the two ocean basins may increase convergence over the Southern African continent, leading to an overall weakening of subsidence in the 500-hPa level as in Fig. 7, thus reducing the Botswana High's strength. Figure 9b, d, f, h and i show changes in the upper tropospheric divergence flow between NoENSO and CTRL. 1985, 1989and 2008 show upper tropospheric divergence over much of the central and eastern Pacific and over much of the Atlantic Ocean, which coincides with deep convection from warmer SSTs. Contrary to that, there is an upper-level convergence (positive velocity potential) over much of the Indian Ocean, including Australia and the maritime continent, which corresponds to colder SSTs. This upper-level convergence over the Indian Ocean may result in a northeastward shift of the SICZ (Cook 2001) and tropical temperate troughs (Tyson and Preston-Whyte 2000), strengthening drier conditions over Southern Africa. This convergencedivergence pattern is reminiscent of the weakening of the Walker Circulation (Gore et al. 2019) and typically occurs during El Niño events. In general, the weakening of La Niña events will lead to an El Niño type of response in the atmosphere and vice versa. The year 2000 showed a similar pattern with other La Niña years, except for a weak convergence over the Pacific. 1985 and 1989 had the highest velocity potential over Southern Africa's northeast regions corresponding to the increase in subsidence over the region due to cooler SSTs. This corresponds well to the increase in the 500-hPa geopotential height as in Fig. 8d and f and the larger strengthening of the Botswana High (1985,1989) as in Fig. 6 as compared to other La Niña Botswana High years (2000,2008).

Atmospheric dynamics associated with La Niña
The difference in the eddy stream function at 200 hPa (NoENSO minus CTRL) shows anticyclones over the eastern and western Pacific Ocean (Figs. 10b, d, f, h and i). These anticyclones are characteristic of a Gill-Matsunotype response that is imminent due to the warming of Pacific Ocean SSTs (Cook 2001;Wilson et al. 2014;Gore et al. 2019). This increase in the strength of anticyclones leads to a reduction in the cyclonic flow over the Pacific Ocean and the weakening of the Walker Circulation. All La Niña years indicate an increase in the cyclonic flow over the southern parts of South America, Africa, the Atlantic Ocean and the Indian Ocean. This anomalous cyclonic flow in the upper troposphere indicates cooling SSTs over the region and may increase subsidence over Southern Africa, thus strengthening the Botswana High.

Conclusions
Previous studies have shown a strong relationship between ENSO and the Botswana High (Reason 2016;Driver and Reason 2017;Maoyi and Abiodun 2021); however, the studies applied correlation and composite analysis, which cannot determine cause and effect in the relationship. In light of that, the present study investigated the Botswana High response to ENSO using a variable resolution GCM (MPAS) to better understand the relationship between the Botswana High and ENSO. Two experiments were performed. The first experiment used observed SST everywhere (control experiment, CTRL), while the second experiment used observed SSTs everywhere except over the Pacific Ocean, where monthly climatological SSTs were used (NoENSO experiment). The capability of MPAS in simulating the climatic features over Southern Africa and the temporal variability of the Botswana High were evaluated by comparing the models' historical simulations (CTRL, 1980(CTRL, -2010 with GPCP observation, ERA5 reanalysis and MPAS5 model data. The results of the study can be summarised as follows: The MPAS variable resolution simulation reproduced the interannual variability of the Botswana High as in the ERA5 reanalysis. In all datasets, the Botswana High variability shows a strong link with ENSO (r > 0.8) and suggests a quasi-linear relationship between the Botswana High and ENSO.
MPAS generally captures the summer (JFM) climatic variables over Southern Africa during El Niño and La Niña years, although with some biases across the region. However, in most cases, the results are comparable with GPCP observation and ERA5 reanalysis. Sensitivity experiments show that the Botswana High mode is independent of ENSO, but the modes' amplitude amplifies during ENSO events. Removing the El Niño forcing strengthens the Walker Circulation and results in upper-level divergence (200 hPa) over Southern Africa. This upper-level divergence weakens the 500-hPa geopotential height over the region resulting in a weak Botswana High. The opposite is true with the removal of the La Niña signal.