The MISR instrument, launched more than two decades ago, is equipped with nine cameras that view the earth at nine different angles: nadir, then 26.1, 45.6, 60.0, and 70.5 forward and backward of nadir above the planet to monitor climate trends. With each camera, MISR acquires spatial sampling every 275 m and for about 7 min to cover a swath view of 360 km of the earth's surface . Different datasets are produced from the instrument, ranging from raw observation to further processed data by subjecting it to various screening operations. In this work, parameters from the level-3 monthly aerosol product (MIL3MEA_4) gridded at a resolution of 0.5×0.5 is used. Level-3 datasets represent a summary of level-2 data, so most uncertainties assessment and quality flags initiated in the level-2 algorithm processing are applicable. Generally, MSIR aerosol products are prone to aggravated uncertainties due to events like cloud and sun glitter contamination, complex topographical terrain, and instrument calibration. The data assessment and quality flags are initiated to minimise uncertainties during the pre-processing stage , especially cloud contamination.

Furthermore, additional processing is employed for aerosol retrieval over different surfaces, such as land and dark water , to better characterise aerosol over a region. Following the implementation of the screening processes, data available in the level-3 aerosol product is often reduced by a significant amount. However, several validation exercises performed by coincident MISR and AERONET data have demonstrated considerable agreement e.g.. Besides, several improvements in aerosol retrieval algorithms have been sought during the last decade to enhance aerosol product qualities over both land and dark water. See https://asdc.larc.nasa.gov/documents/misr/misr_qual_stmts_current.html (last access: 27 February 2022) for further information on quality statements and maturity level. For the current study, datasets consisting of AOD, Ångström exponent (AE), and absorbing AOD (Aabs), together with aerosol index (AI) derived from the expression AOD⋅AE, are utilised to present part of the result.

MODIS measures the radiances from the earth's surface to acquire data in 36 spectral bands from 0.4 to 14.4 µm to provide information on the state of atmosphere, land, and ocean. Two bands of the 36 wavelengths image at a nominal resolution of 250 m, five other bands at 500 m, and the 29 remaining bands at 1 km. The instrument achieves a 2330 km viewing swath and reaches near-global coverage every 1 to 2 d. MODIS, like MISR, provides different scientific data products from monitoring global dynamics and processes spanning the atmosphere, land, and the ocean. All data products are available to the science community at different processed levels. This study uses cloud optical properties from collection 6.1, level-3 monthly aerosol–cloud dataset (MOD08) gridded at 1∘×1∘ horizontal resolution to present additional results.

MODIS level-3 data is computed from the level-2 data statistics and inherits the data quality embedded in the corresponding level-2 products. For data quality assurance (QA), level-2 atmosphere products are processed by initiating the validity flags algorithm (runtime QA flags) to better the data quality. Hence, runtime QA flags are unavailable in level-3 (L3) atmosphere products; instead, they are only used in computing (aggregating and weighting) L3 statistics and apply to selected parameters. Therefore, the selection of datasets by considering aggregation (e.g. day/night-time, liquid/ice clouds only, cloudy/clear, and surface type) and QA (mainly confidence level) in L3 data requires factoring in the characteristics of the study area. For this study, datasets including cloud optical thickness (COD), cloud fraction (CF), cloud top height (CTH), liquid water path (LWP), cloud effective radius (CER), and atmospheric water vapour content (AWV) are used to derive more results. In MODIS retrieval, all cloud properties are obtained using the infrared channel except for the AWV retrieved at the near-infrared band.

Data obtained from SAWS stations were utilised to examine the impacts of aerosol and cloud on the meteorological condition over the region. SAWS monitors and provides weather information services at several ground measurement stations across the nine provinces. The agency provides different ranges of data, from hourly to monthly data. The datasets used in this study include surface precipitation (PRECP), wind speed (WS), and ambient temperature (TEMP). Each parameter over the three sub-regions under investigation is evaluated by statistically averaging data from meteorological stations under the sub-regions. A summary of the number of stations and hours of data incorporated in the sub-regional analysis is presented in Table 1.

The aerosol optical depth (AOD) still represents an important parameter in estimating the extent of aerosol loading over an area. Figure 2 shows the monthly averages for 10 years (2007–2016) of MISR AOD measurement at 555 nm over South Africa. The adoption of AOD and other aerosol properties data from the MISR instrument against that of MODIS lies on the higher grid resolution (0.5∘×0.5∘) of the former compared to the latter, which is coarser (1∘×1∘). Besides, previous studies demonstrated that MISR retrieved aerosol properties are in better agreement with ground-based instruments such as the Aerosol Robotic Network (AERONET), than MODIS . As was pointed out earlier, the season over South Africa is typically similar to what is obtainable over the Southern Hemisphere region such that summer begins in December to February, autumn from March to May, winter from June through August, and spring from September to November. However, the meteorology characteristics are divided into two, such that the upper and central parts mainly experience hot wet summer and cold, dry winter. Contrarily, the lower parts experience warm, dry summer, and cold, wet winter, which influences the characteristics of aerosol emission over the different parts of the region. Also, the population and number of industrial activities in the upper part are more than in the central part, followed by the lower location. See the information on the meteorology characteristics and population of the sub-regions in Table 2.

Subsequently, from Fig. 2, AOD shows seasonality for the entire region. Hence, AOD increases in July through September (mainly during the spring months), followed by a general decline from October through June (mainly in winter). The maximum aerosol loading (AOD>0.25) occurred during the September months and is primarily associated with biomass burning in the upper part of the country and the surrounding bordering countries. Besides, aerosol emissions emerging from industrial and other human activities aggravate the aerosol particle suspension over the northern-most part of the region. Perhaps the dryness condition extending through the spring is instrumental in enhancing aerosol build-up, especially around Richard Bay (central east part of the country), where a coal loading terminal is located, and other industrial emissions occur. The removal of aerosol particles by wet deposit is absent at this period of the year, thereby allowing these particles to remain in the air for a more extended period. Furthermore, there are drifts of aerosol particles transported by air masses from the northern to the southern part of the region. Most of these particles are fine mode aerosols, such as aged smoke and dust particles of coal debris emitted into the atmosphere in the upper area, and undergo different interaction and complex reactions along the transit path.

Meanwhile, the minimum AOD (typically <0.05) is observed in June and is mainly linked with aerosol removal process (e.g. dry and wet deposition, cloud scavenging) and less biomass burning activities. This result is similar to the observation of and that high aerosol loading of mainly biomass burning and industrial smoke originating from northern and border communities dominate aerosol loading over South Africa. Over the lower or southernmost part, biomass burning due to forest fires and industrial activity emissions also account for aerosol emission from November to March. However, due to the low turbidity, the effect is minimal compared to the central and upper parts. Furthermore, the region's central sub-region, especially around the west, contributes significantly to mineral dust (MD) suspension due to its arid nature. However, the impact is weaker compare to other forms of aerosols over the region. The weakness could be due to the coarse nature of MD aerosol and the susceptibility to dry deposition. Although the process of aerosol removal or exit over South Africa (SA) has not received much attention, there is a need for such studies to give a better insight into the mechanism of aerosol emission, residence, and removal over the region.

To complement the possible identification of biomass burning and general smoke emission observed from the AOD variation, Fig. 3 illustrates the absorbing aerosol optical depth (Aabs). Like the AOD, the Aabs demonstrates a seasonality pattern such that an increase is observed from July to September and then a decrease from October through June. The maximum Aabs (>0.025) occurs in September, and the minimum (<0.005) during January. This variation indicates a concurrent increase in AOD and Aabs during the spring season, thus demonstrating a significant increase in absorbing aerosol emissions such as biomass burning, fossil fuel combustion smoke, and carbon-related fine mode particles. Also, two essential characteristics of the Aabs observation include revealing the period of high AOD associated with massive emission of absorbing aerosol particles and the area dominating in concentration level. High absorbing properties appear more at the upper parts than the central and lowest at the southernmost sub-region. Interestingly, a more significant portion of the absorbing trait is around the eastern parts than in the west. Hence, considering the timing and location of peak values, biomass burning activities during the pre-farming period around Limpopo and bordering countries such as Botswana, Mozambique, and Zimbabwe contribute significantly .

The variation of Ångström exponent (AE) in Fig. 4 shows the predominance of fine mode aerosol in most periods of the year. An increase in fine mode aerosols from January to September, followed by a decrease during October to December, is evident over the region. The maximum AE value (AE>1.7) is obtained chiefly during August, and the minimum (AE<0.5) occurred in December. This observation is consistent with the changes in AOD and Aabs in the previous figures. There are strong indications from both Figs. 2 and 3 that activities such as biomass burning, smoke emission from industries, and carbon-related dust samples are responsible for high aerosol loading over the area. Besides, the regime of high aerosol loading exhibits seasonality pivoted around the summer and usually diffuses from the upper through the centre then to the lower parts aided by the motion of air masses. Nevertheless, the lower and a fraction of the central sub-region are more of a coarse mode and less absorbing aerosol dominated areas. The characteristics of aerosol particles over this area earned their influence from proximity to the ocean, where sea salt aerosols are prevalent, and the arid region with a significant presence of MD, respectively. Furthermore, some element of high presence of fine mode particles is noticeable around the coasts. Perhaps, these cases may be prompted by the occasional inflow of aged smoke over the Atlantic Ocean from the Amazon Forest to the west coast see and the spread of aerosols to the Indian Ocean through the east coast.

In this section, all parameters are based on MODIS instrument measurements and characterised by a horizontal resolution of 1∘×1∘, as was explained earlier. The variation of atmospheric water vapour (AWV) or precipitable water is as shown in Fig. 5. The observation of high precipitable water during summer and low precipitable water towards winter is evident for all parts of the region. The highest vapour value (AWV>3.5 cm) occurs during January and the lowest (AWV<2.3 cm) occurs in August. The evidence of seasonality in the pattern of atmospheric vapour is apparent here. Generally, AWV declines from February to August and then rises from September through January. One important thing worthy of observation is that high atmospheric vapour during the summer coincides with the precipitation season over the summer rainfall areas (mainly the upper and central parts of the region). Perhaps, there are chances of the high amount of vapour enhancing rainfall intensity over the region.

Another important observation from the AWV variation is that it declines from north to south, similarly to AOD, except for the coastal environments, where the vapour content is relatively higher than the lower inland areas. The high value of vapour in summer in contrast to other seasons is due to warmer air conditions, since warm air expands more and possesses the capability to hold more water than cold air. A similar pattern is noticeable over the oceans around the region. AWV is higher over the Indian Ocean coast due to the warm air front from that direction compared to the lower value seen over the Atlantic Ocean, where cold wind emerges to the region. Earlier studies demonstrated the seasonality of water vapour following the plunge to a minimum in June and rises to the maximum value in January . Apart from the observation over this region, globally, AWV is found to increase in most areas during the summer, which is often associated with higher air temperature e.g..

For the liquid water path (LWP) over South Africa, Fig. 6 shows the distribution of cloud liquid content over the country. During winter months with extension to May and September, LWP is mainly low over the inland areas except for the coastal locations where relatively or higher values prevail. During this period, the values around the coasts reaches more than 40 % higher than measurements obtained inland and most pronounced in June. In contrast, LWP is more distributed over the entire region during summer, including November to April. The maximum values (LWP>20.0 gm-2) are witnessed in June and are mainly associated with the region's coasts. The minimum values (LWP<10.0 gm-2) are predominant over the inland areas, particularly in August. Interestingly, both maximum and minimum values occurred in the same seasonal period. Although the min–max happened during the same temporal domain seasonally, their spatial spaces are exclusively different.

Meanwhile, the pattern demonstrated by LWP over this region does not show a discernible link with AWV, especially considering the distribution of both parameters over the country. While AWV is more distributed spatially over the central and upper sub-regions, LWP is more around the lower area. Nevertheless, carefully observing the variation of AWV and LWP, mainly during the summer and autumn seasons, gives further insight. There is a sign AWV influences the changes in LWP, but other factors such as the aerosol types and, perhaps, temperature could be significant. For instance, there are periods of low AWV noticeably corresponding to relatively high LWP. Previous studies identified less water vapour condensation resulting from less hygroscopic aerosol accountable for this feature . This observation is analogous to the spotted variation over South Africa, taking into account the high values of LWP over sea-salt endowed lower parts compared to the inland (mainly central and upper) areas.

In Fig. 7, the variation of cloud optical depth (COD) is illustrated. Therein, COD is high mainly around the coastal areas compared to the inland environments. Besides, the eastern parts of the country domicile most optical thick clouds while the western parts of the region, except for the lower coastal parts, are more optical thinner clouds. Over the 10-year study period, COD sparingly shows seasonality trends with the alternating increase and decrease in COD across the seasons. Higher values are seen mainly during summer and spring rather than the early parts of winter and autumn. Meanwhile, May, August, and September are also characterised by the lower value of COD. The high COD value with extension to autumn corresponds to high atmospheric vapour and low aerosol turbidity during summer. In contrast, high COD during the spring season overlaps with the emission of a considerable amount of aerosol, predominantly fine mode particles.

In the two cases, there is the possibility that the high AWV and fine AOD significantly influenced the high COD, respectively. Meanwhile, the increase observed during winter might be accountable to cloud scavenging, since both AWV and AOD are generally low in this period. Hence, there is a need for specific studies for us to understand aerosol removal processes over South Africa better. The maximum COD (>22.0) occurred in June and the minimum (<7.0) in May, just like the LWP. The high value of COD during winter and, to some extent, in autumn, correspond to the period of high LWP and low AWV. In contrast, during the spring and summer seasons, high COD coincides with high LWP and increasing AWV. In the two cases, there is evidence of robust affinity between the variation of LWP and COD. By mapping the idea of aerosols acting as nucleating seeds during cloud formation, the variation demonstrates the albedo effect proposed by . However, the exception lies in the constant LWP in Twomey's postulation, which differs from the variation of this parameter as observed over the study region. Observations from other studies have also shown that COD increases with LWP, especially when there is a proportionate rise in the number of cloud droplets Nd .

Evaluation of the amount of cloud cover based on the cloud fraction in Fig. 8 shows a high value spreading from over the coastal environments towards the inland areas. Also, more cloud cover is observable around the upper eastern parts than the central and lower western parts, except for marine areas. Furthermore, high CF occurs during the summer and spring months and often declines towards autumn and winter, and then rises through spring to summer again. The maximum values (CF>0.7) were mainly recorded during the December months, while the minima (CF<0.25) were often around the August periods. A vital outlook from the CF trend is that it increases with AWV. The fraction of cloud covered plays a crucial role in the amount of solar radiation reaching the surface and, hence, can significantly influence the thermodynamics of the clouds depending on the cloud type. Large cloud cover often reduces the amount of solar radiation per unit area reaching the earth's surface. At the same time, less CF will enhance the quantity of the incoming sun energy arriving on the earth.

There are several other important cloud properties, such as the COD, (Nd), and droplet size distribution that influences the solar radiative energy over the earth. However, based on the surface area and relationship with cloud albedo, CF is an important factor defining the amount of sunlight reaching the ground . Over South Africa, coldness generally prevails during most periods of the years, with temperatures typically lower than 17 ∘C. The high-altitude feature of the region is one known factor that influences the low temperature. However, a rise in solar intensity is not uncommon over South Africa during the winter and spring months, which gives rise to high temperatures during the day. During these periods, the low CF over the region could enhance the temperature profile, thereby causing a slight warmth in the afternoon. Also, the eastern coast of the region is warmer than its western counterpart. The two air fronts from the Indian Ocean (the warm Agulhas current) and the Atlantic Ocean (cold Benguela current), respectively, are accountable for this and constitute the significant differences in climate and vegetation over the region .

As shown in Fig. 9, the cloud effective radius (CER or Re) is highest over the surrounding oceans and the coastal environment compared to the country's inland areas. Besides, Re is generally lower in the upper parts of the country and increases through the central location to the southernmost parts where values are maximum. Furthermore, high Re values are more spread over the western parts of the region than the eastern parts. In terms of temporal variation, CER basically increases during the autumn months and extends until winter. Then a declining pattern follows from the spring months until the end of summer in February. Also, over the upper and central parts, Re is slightly higher than in the lower location during the summer. Thus, the maximum values (Re>15 µm) are mainly observed in June, while the minimum values (Re<11 µm) are found to be more in July. The high value of Re over the coastal area could be linked to the considerable presence of larger particle size aerosols, mostly of sea salt. In contrast, the lower value at the upper and central sub-regions, particularly towards the east, is associable with the dominance of fine mode particles. Several studies have elaborated on the role of cloud droplet size influencing the effective radius e.g.. Hence, the dominance of Nd by large-sized particles will result in Re having high values, and small particles accounting for the most Nd will mostly result in low Re. The variation played out over this region significantly aligned with the conventional theory by comparing the fine mode aerosol dominated upper and central parts with low CER values and the coarse mode associated lower parts with high CER.

The distribution of cloud top height (CTH) over the region is illustrated in Fig. 10. As expected, CTH is low over the ocean and to an extent at the coasts. Over the inland areas, CTH is more than two times greater than the height over the sea, depending on the period of the year. Temporally, CTH shows strong seasonality such as the elevation increase during the spring months through summer, then declines in autumn through winter. Also, cloud top height is highest over the upper, followed by the central and lower parts. The maximum value for the cloud top height (CTH>7500 m) occurred during the summer months, especially in January, and the minimum (CTH<4 km) occurred in the winter period, mainly in July. A comparable variation is noticeable between AWV and CTH, following their dramatic seasonal changes. Perhaps this characteristic could represent an increase in AWV, aiding more cloud development, especially at high updraft velocity.

This section examines various aerosol and cloud properties observations based on the current understanding of aerosol–cloud interactions (ACI) and other distinct observable characteristics peculiar to the study region. The analysis attempts to enhance the knowledge of the influence of aerosol climatology on clouds and the reverse impacts (cloud effects on aerosol) during different temporal periods. Further, this will provide an insight on the possible response of precipitation, which is valuable for future studies. Previous sections identified AOD as high mainly during the spring (August–November) and lowest in the winter season. To examine the interrelations amongst aerosol and cloud properties, Fig. 11 shows the monthly mean variations of all parameters under consideration generated by statistical averaging of measurements over selected locations (Johannesburg 26.25∘ S, 28.05∘ E; Polokwane 23.90∘ S, 29.44∘ E; Nelspruit 25.47∘ S, 30.96∘ E; Mafikeng 25.81∘ S, 25.50∘ E) in each of the provinces within the upper part. Critically scrutinising the three aerosol properties (AOD, Aabs and AE), one can generally split the variation into two cases based on the combined AE-Aabs relationship with AOD. The first case (case-I) represents the change in AOD with low AE<1.0 and no significant influence of absorbing aerosol as seen from November to March. In comparison, the second case (case-II) represents the period (April–October) of changes in AOD associated with AE>1.0 and corresponding variation in aerosol absorbing properties (AOD influenced by Aabs increase).

In terms of the atmospheric vapour, case-I represents the relationship between AWV and AOD. From observations, AOD changes in the same manner (increase or decrease) as atmospheric vapour, while the particle size increases/decreases accordingly. This characteristic demonstrates a shift in the optical properties of aerosol particles (e.g. size and scattering albedo) due to water uptake. In the presence of high AWV, as particles with high affinity for water increase in size, AOD simultaneously increases, and AE decreases. The described pattern is especially true for an environment dominated by hygroscopic aerosol and under humid conditions . Subsequently, the particles act as cloud condensation or ice nuclei (CCN or IN) and are later activated to cloud droplets at supersaturation by vapour condensation. The continuous and rapid growth of these cloud droplets explains the strong dependency of CF on AWV and AOD. In contrast, case-II illustrates AOD variation in response to rising absorbing particles such as organic carbon (OC) and black carbon (BC), where AWV is low. One should note the decreasing particle size (AE>1.0) and the sharp drop of CF with AWV. Coalescence of cloud droplets formed reduces, compelling a proportionate reduction in the cloud cover (CF decreases). Besides, at the intersecting peak (in September) of the aerosol properties, a slight rise in vapour does not immediately increase particle size due to atmospheric water overwhelmed by fine mode aerosols.

Cloud thickness was explained to be influenced by LWP in the previous section. Hence, considering case-I, COD and LWP demonstrate strong dependency, suggesting a proportionate cloud water to nucleating particle ratio. Contrarily, the dependence of the parameters (COD and LWP) is relatively weak during case-II, such that the LWP does not directly quantify COD. Instead, cloud thickness increases with the aerosol particle size, and mostly the same occurs for cloud droplets. Also, one can relate this to the variation of the CER in case-I, where COD is closely dependent on LWP corresponding to a high effective radius (Re>12 µm), hence a large cloud droplet size and more cloud growth due to increased collision and coalescence. Furthermore, the increase in cloud top height along the effective radius and thickness will likely enhance radiative cooling at the top due to increasing cloud albedo. Interestingly, the surface temperature is relatively high to invigorate a convective scene, prompting corresponding precipitation dynamics over upper SA. Therefore, any shortfall in these parameters (CER, LWP, COD, CTH) to complement the aerosol concentration could be detrimental to precipitation occurrence.

During case-II, AOD is predominantly fine mode and mainly influenced by absorbing particles. Vapour is generally low, the same as COD and LWP compared to the aerosol loading that can potentially act as CCN. This situation is portrayable as a polluted condition, whereby aerosols nucleate a more significant amount of smaller cloud droplets, thereby affecting the alignment of LWP and COD, resulting in lower CER and cloud cover. Consequently, cloud droplet collision and coalescence rates are slower, while cloud albedo increases according to the Twomey effect, causing warm rain suppression . A vital observation is the radiative effect ushered by the smaller cloud droplets amid low surface temperatures. Radiative cooling at cloud-top along with low surface temperatures enhances atmospheric stability and creates an unsuitable condition for convective developments .

Figure 12 represents the variation over the central part of South Africa, made up of Bloemfontein (29.12∘ S, 26.22∘ E), Durban (29.92∘ S, 31.01∘ E), and Upington (28.39∘ S, 21.27∘ E). The dynamics does not diverge much from the upper part, considering the drift of aerosol southward of the region and the shared similar meteorological conditions. Here, the aerosol–cloud interaction regime can be divided into two case studies, as done for the upper part. Case-I covers the period (November to April) of high aerosol loading dominated by large size particles (i.e. AE<1.0) and generally low absorbing aerosols. Meanwhile, case-II is the period (May to October) where aerosol loading is fine particle dominated and linked with absorbing aerosol emission. Just as for upper SA, the vapour is higher during case-I, and CF maintains close variation as AWV. Cloud thickness varies significantly with cloud water following changes in AOD. A rise in AOD at high AWV corresponds to increasing COD, LWP, CER, CTH, and more precipitation. This process possibly follows the formation of larger size cloud droplets due to the concentration of bigger-sized particles yielding a proportionate increase in LWP and COD with a high value of CER and CTH, thereby leading to more precipitation. The ambient temperature and wind speed are relatively high to drive the dynamic and thermodynamic aspects of the process. Noteworthy is the changes in precipitation rate due to characteristic features of aerosol–cloud interactions.

For the second pattern (case-II) covering May to October, AOD shows substantial variation with absorbing aerosols and is primarily fine mode particle dominated. The meteorological condition is characterised by general low precipitation, temperature drop, and a slight reduction of horizontal wind speed. An increase in aerosol loading mainly corresponds to a decrease in COD and LWP. Besides, CER generally decreases, while CF and CTH decline in most parts of the period. On account of generally low AWV during case-II, CF and CTH decreased to a minimum but increased as AOD even in the presence of less water vapour around September. From the patterns (i.e. I and II), precipitation formation is motivated by relatively larger cloud droplet size (higher CER), high atmospheric water, and ambient temperature. COD and LWP increased and maintained proportionate variation, coupled with a slight increase in temperature, serving as a potential invigorator of atmospheric instability, thereby raising the precipitation chances.

Over the lower part (Cape Town 33.92∘ S, 18.42∘ E and Port Elizabeth 33.95∘ S, 25.59∘ E) in Fig. 13, the aerosol loading is generally low (AOD<0.1) and is further characterised by the low cloud (CTH<3 km) typical of marine environments. Amazingly, this part presents high atmospheric vapour, ambient temperature, and wind speed during the summer and spring like the other parts (upper and central), yet low precipitation. Following a convention similar to the other parts, case-I represents the period between October and March, where lower absorbing properties and AE≤1.0 typify aerosol, while rainfall is deficient. In contrast, case-II during April–September demonstrates an increase in precipitation, absorbing aerosols and AE>1.0 with lower AWV and temperature. During case-I, the general low aerosol loading corresponds to clouds with less water (low LWP), even though the cloud is optically thicker (COD>15.0). There is notable contrast in the proportionate variation of LWP and COD coupled with a low effective radius (CER<14 µm). Precipitation decline here is linkable with low cloud water, droplet size, and reduced CER. The size of the cloud droplet effective radius plays a vital role in precipitation forming clouds. A low value in shallow clouds, particularly of less than 14 µm, leads to slower collision and coalescence rates and precipitation suppression. This is because more evaporation occurs in smaller sized cloud droplets when mixing with dry ambient air, thus causing loss of cloud water. Several studies, including modelling experiments, have presented similar observations .

Meanwhile, case-II presented an increased aerosol loading period dominated by fine mode particles with strong absorbing properties, where atmospheric vapour slightly dropped. Here, a rise in cloud water is observable and proportionately varies with cloud depth, while the ambient temperature dropped to minimal along with a slight decrease in wind speed. More importantly, CER is greater than 14 µm, and cloud height, on average, increased sparingly. Thus, precipitation is here boosted by the increase in CER and LWP coupled with the low ambient temperature that will enable a faster reach of the supersaturation level. Because of the rise in CER, collision and coalescence will increase along cloud water since the coalescence rate is a function of droplet size.

Similarities in the weather characteristics over central and upper South Africa constitute a vital outlook in the interannual variation in Fig. 14. Critically observing the figure, the meteorological state of the region shows a close relationship amongst temperature (TEMP), wind speed (WS), and AWV, and a general increasing tendency from 2013. AOD, AE, and Aabs show a similar declining trend between 2012–2013, then increasing tendencies during 2008–2010 and 2013–2015 over the lower area. Aerosol loading is generally low over this part (mostly AOD<0.1), which is typical of a maritime environment . Even though a substantial amount of anthropogenic aerosols is emitted internally in this environment due to the high human population and industrial activities, long-range external emissions mainly trigger the aerosol loading and fine mode particle concentration see.

Cloud cover and top height over the lower sub-region experienced increments to two major peaks in 2009 and 2015, coinciding with the rise in AOD. An increase in aerosol loading can enhance CF and CTH through the addition of CCN, invigorate existing cloud droplet concentration (Nd) to enhance vertical development . The case is typical of warm clouds such as shallow cumuli and stratocumuli found over the marine environment as observed in previous studies . For atmospheric vapour, a distinct rise in the highest value in 2010 corresponds to high AOD, CF, and CTH. Meanwhile, CER, LWP, and COD increased in 2008 and during 2012–2014, which fall into the years of moderate to highest rainfall and lower aerosol loading and AE. Likewise, less precipitating years such as 2010 and 2015, mainly associated with drought events across the region , coincide with high AOD and AE, while the effective radius, cloud water, and optical thickness are lower.

Over the central and upper sub-regions, AOD follows a series of increase and decreases almost along subsequent years. Nevertheless, AOD, AE, and Aabs simultaneously rose to peaks in 2010 and 2015, just as water vapour. During these peaks, cloud cover was high over both upper and central parts except for the sharp drop at the upper area in 2015. Consequently, the growth in aerosol loading over these sub-regions mainly enhanced by fine mode particles generally results in more cloud covers. In contrast, increasing aerosol loading largely negatively impacts cloud water and optical depth over the central sub-region, which resembles the trend over lower SA. However, the reverse is mostly the case over upper SA. The disparity in aerosol–cloud interaction behaviour might be due to differences in particle size distribution and the general aerosol composition over each area. As for the effective radius, an overall decrease prevailed during years associated with rising aerosol loading over the central and upper sub-regions. This feature is more evident for 2010 and 2015 and is consistent with observation over the lower sub-region.

From the interannual variations, several distinct characteristics of aerosol and cloud over each sub-region are noticeable, apart from the dynamics of aerosol–cloud interactions. For instance, the hierarchy by location of aerosol loading and optical depth of absorbing particles demonstrates a declining trend from upper to lower sub-regions. Meanwhile, for most cloud parameters, the reverse is the case, such that an increasing trend prevails from upper to lower area. Furthermore, parameters like CER, CTH, and CF are higher over the lower part, followed by the central and upper parts. These characteristics alone tend to set varying conditions for precipitation to occur.

From the previous sections, different patterns of aerosol and cloud properties in tandem with precipitation changes had been observed to spread over the region. Notably, all the cloud properties have been observed to influence precipitation formation differently over the geographical parts of the region. However, the impacts of CER and LWP show dominance among peers over the entire area of study. Meanwhile, the effects of other cloud properties (i.e. CF, CTH, and COD) are mainly pronounced in the central and upper parts only. Conventionally, aerosols are observed to modulate clouds through aerosol–cloud interactions (ACI), which affects precipitation depending on the feedback from ACI and other atmospheric circumstances. Studies have demonstrated that an increment in CER and LWP often results in precipitation enhancement . Observation consistently found the increments to result from the rising collision and coalescence rates that enhance cloud droplet size and precipitation formation . Numerous investigations and numerical studies have often found CER to increase (decrease) with AOD depending on the size characteristics of aerosols. Also, some studies have demonstrated the impact of rising aerosol loading on the decline in LWP and CER, thereby suppressing rainfall . Meanwhile, CF and CTH rise owing to increasing aerosol loading, although sometimes depending on the cloud type . Irrespective of these various findings, most of them are somewhat associated with considerable uncertainties, especially regarding the observations from some other studies. To this end, more studies are required regionally and globally for us to understand the mechanism fully.

This section explores the relationships between aerosol and cloud, and then cloud and precipitation to understand ACPI over South Africa. Since the particle size influences cloud properties (i.e. CCN and IN are predominantly fine mode aerosols), the correlation analysis for aerosol properties considers AOD and aerosol index (AI). Figure 15a shows the correlation between AOD and cloud properties (COD, LWP, CER, CF, and CTH). Generally, weak correlation coefficients (R) in the range of -0.4<R<0.24 exist between AOD and cloud properties over all parts of the region. In the case of the lower and central parts, all cloud parameters except for CF and CTH (significance value P>0.05) significantly related to AOD (i.e. P≪0.05) despite their weak correlations (i.e. -0.4<R<-0.20). Besides, their negativity regarding the correlation coefficient is consistent with earlier studies since aerosols inhibit cloud development through the warming effect . The low correlation might result from aerosol types, atmospheric effects, and various uncertainties (e.g. aerosol and cloud retrieval and data coarseness).

Several observations and numerical evaluations have documented growth in both CF and CTH due to an increase in aerosol loading . The cause of the insignificant and almost negligible R-value for CF and CTH for the lower region and similar pattern for cloud cover in the upper parts is unclear and requires a close look. Further, regarding the upper sub-region, both CER (R=-0.22) and CTH (R=0.23) are significant with P<0.05. Again, the negative relation (i.e. AOD vs. CER) is consistent with the intuition that a high concentration of AOD results in more cloud droplets of smaller CER, just as postulated by . The positive relationship between AOD and CTH is explained by the cloud invigoration mechanism initiated through increasing aerosol loading, leading to vertical cloud development and increasing height .

In Fig. 15b, the relationship between AI and cloud properties demonstrates a random correlation coefficient for each sub-region. For the lower part, only the relationship with COD seems significant with R=-0.25 (weak correlation) and P≪0.05. The cause of the weak R-value is not clearly understood, mainly when no meaningful relationship is noticeable over other parts. However, COD is expected to be an essential radiative modulator of the cloud, which should be more inclined to the aerosol types. A previous study also indicated no significant relationship between AI and COD . Over the central part, a much more significant but moderate correlation coefficient (R>0.55) is observed for CF and CTH. This outcome suggests enhancing cloud cover and height with increasing concentration of CCN and IN in the cloud. Observational studies have shown growing aerosol loading to enhance CF and CTH . According to numeric simulation, this feature is further stressed to be enhanced by aerosol thermodynamic invigoration . Such an occurrence is well observable in the transition from open to closed-cell clouds. Results from satellite observation also demonstrate the increase in AI with stratocumulus clouds over the ocean . On the contrary, the case is much different over the upper sub-region, with a mainly negative correlation between AI and CF and CTH. The negativity is traceable to the changes in the thermodynamic properties of cloud by freshly induced aerosols since the upper part constitutes and is closer to primary sources of aerosols over the region.

A positive correlation occurs between cloud properties and precipitation for the entire region, as illustrated in Fig. 15c. The correlation coefficients range between 0.15<R<0.9 with ≈80 % of the R-value representing moderate to strong correlation (i.e. 0.32<R<0.9). Nevertheless, weak relationships are observed for selected cloud properties (COD, CF, and CTH) in the lower part of the region, with R typically <0.18 for all properties. The weak correlation between rainfall and these cloud parameters at the lower sub-region lies mainly in the low aerosol loading and the general characteristics of shallow clouds. Notably, the significance of increasing cloud water and effective radius in enhancing precipitation is evident according to this chart, as it cuts across the entire region. Hence, CER and LWP have demonstrated a critical role in deep and shallow clouds, as observed from this region. In general, based on the climatology of aerosol and cloud as described in the previous sections, precipitation formation is a function of the characteristics of aerosol–cloud interactions. ACI leading to varying states of cloud properties, particularly CER, LWP, CF, and CTH, have differing effects on precipitation, which is summarised in Table 3.