The ground-based Sun-sky photometer measures both direct and diffuse solar radiation. Direct solar irradiance is observed across ultraviolet, visible, and near-infrared bands, and AOD is retrieved from these measurements using the Beer–Lambert law after accounting for Rayleigh scattering and gaseous absorption. During Almucantar scans, diffuse sky radiance is recorded at 30 RAAs (2, 2.5, 3, 3.5, 4, 5, 6, 7, 8, 10, 12, 14, 16, 18, 20, 25, 30, 35, 40, 45, 50, 60, 70, 80, 90, 100, 120, 140, 160, 180°). AOD and radiance measurements at RAA greater than 7° are used to retrieve aerosol parameters including SSA, g, size distribution, and refractive index (Dubovik and King, 2000). AERONET inversion products are classified into Level 1.0 (unscreened), Level 1.5 (cloud-screened and quality-controlled), and Level 2.0 (quality-assured). Level 2.0 data are produced through uniform instrument calibration and rigorous manual inspection, with quality control criteria such as AOD >0.4, SZA >50°, and sky residual <5%, which considerably reduces data volume but ensures high reliability. The uncertainties of Level 2.0 retrievals are typically about 0.03 for SSA and 0.02 for g (Giles et al., 2019; Sinyuk et al., 2020).

We downloaded coincident Level 2.0 AOD and aerosol inversion products from January 1993 to December 2024, along with the corresponding raw Almucantar radiance measurements, from AERONET global sites to construct a testing set of 132 067 samples. This dataset was used to evaluate the retrieval capability of the proposed EML-based algorithm on real observations. To supplement aerosol types under low-AOD conditions, Level 1.5 inversion products were also collected and matched with their corresponding radiance and AOD observations, yielding an additional 87 144 cases. Aerosol size distributions, refractive indices, and surface albedo from the Level 2.0 and Level 1.5 inversion products were separately resampled and randomly combined to generate aerosol inputs for the forward radiative transfer simulations (Sect. 2.2), ensuring both parameter validity and statistical consistency with observed aerosol properties. In addition, radiation measurements were analyzed to characterize observational noise, which was then added to the training and validation sets (Sect. 2.3).

We employed VLIDORT v2.8.1, a linearized vector radiative transfer model, to simulate Almucantar observations from the photometer (Sect. 2.1), thereby generating a comprehensive training and validation dataset. VLIDORT computes the full Stokes vector [I, Q, U, V] for any specified viewing geometry and optical depth (Spurr, 2006). Here, I denotes radiance intensity, while Q and U represent linear polarization components. The model solves the radiative transfer equation for multilayer multiple scattering, requiring inputs such as solar spectral irradiance (SSI) at the top of atmosphere, surface albedo, and atmospheric and aerosol profiles (Table 3 and Fig. C1). Its accuracy and flexibility make it well suited for simulating radiative measurements under diverse aerosol and atmospheric conditions.

SSI is obtained from the Solar Spectral Irradiance Climate Data Record, which provides the solar energy flux reaching the top of Earth's atmosphere for different wavelengths. Observations indicate that SSI variability under stable solar conditions is very small (less than 0.3 % on daily to annual timescales), with an even smaller impact on ground-based measurements. Therefore, a fixed SSI was adopted, with values of 1824.85, 1487.16, 970.44, and 689.27 W m⁻² at 440, 675, 870, and 1020 nm, respectively. Surface reflectance is treated as a Lambertian boundary, since ground-based observations are dominated by downward solar radiation, with minimal contribution from surface reflection. In our algorithm, surface reflectance is neither an inverted nor an input variable. It is only used in radiative transfer simulations, with values sampled from AERONET inversion products (Sect. 2.1).

Radiative transfer is also controlled by both the column loading and vertical distribution of aerosols and gas molecules. The aerosol particle size distribution is assumed to follow a bimodal lognormal volume distribution: 1dVdln⁡r=CVf2πln⁡σfexp⁡-(ln⁡r-ln⁡rvf)22ln⁡2σf+CVc2πln⁡σcexp⁡-(ln⁡r-ln⁡rvc)22ln⁡2σc where CV, rV and σ denote the volume concentration, volume mean radius and geometric standard deviation, respectively, and the subscripts f and c represent fine and coarse modes. Many studies have shown that the scattering properties of particles can be fully characterized using only their reff and effective standard deviation (Hansen and Travis, 1974; Davies, 1974; Whitby, 1978; Ott, 1990; Mishchenko et al., 2004). The effective radius reff and FMF are calculated as:

2reff=∫rminrmaxr3dN(r)dln⁡rdln⁡r∫rminrmaxr2dN(r)dln⁡rdln⁡r3FMF=∑rmin1µmdVdln⁡rdln⁡r∑rminrmaxdVdln⁡rdln⁡r Many aerosol types, particularly dust, are non-spherical, which significantly affects their scattering properties. To account for this, we employed the randomly oriented rotating ellipsoid model, a simple extension of the spherical model characterized by an additional axis ratio parameter. The T-matrix algorithm (Mishchenko and Travis, 1994) computes SSA, the scattering phase matrix, and other optical properties for ensembles of ellipsoidal particles. In radiative transfer simulations, aerosol parameters are averaged over various shapes, making the exact geometry of individual particles less critical; the optical characteristics are primarily determined by the overall axis ratio distribution (Mugnai and Wiscombe, 1986; Bohren and Singham, 1991; Mishchenko et al., 1997). The ellipsoid axis ratios were sampled according to the probability distribution observed for typical dust events (Dubovik et al., 2006). The aerosol extinction coefficient, β, decays exponentially with height: 4βh=β0e-h/H where h is the altitude and H is the extinction scale height, ranging from less than 1 km in winter to more than 2 km on turbid summer days (Turner et al., 2001). Atmospheric profile information was obtained from the ERA5 (European Centre for Medium-Range Weather Forecasts Reanalysis Version 5) monthly mean data (2020–2024) on pressure levels, including temperature, specific humidity, and ozone mass mixing ratio. Data from low- to mid-latitude land areas were extracted and spatially thinned to a 5°×5° grid to serve as the sampling database. Based on these meteorological fields, Rayleigh scattering and gas absorption were calculated. The Rayleigh scattering optical thickness τR at a specific visible wavelength λ was computed using the empirical formula of Dutton et al. (1994): 5τRλ=pressure1013.25hPa×0.00877×λ-4.05 which strictly applies under an exponentially decreasing atmospheric density. Water vapor and ozone absorption coefficient were calculated using the High-resolution Transmission Molecular Absorption Database (HITRAN). A Voigt line shape (Armstrong, 1967), accounting for both Doppler and pressure broadening, was applied to accurately model gas absorption under varying temperature and pressure conditions.

The EML has emerged as a powerful approach for capturing complex nonlinear relationships among variables by integrating multiple machine learning models, thereby leveraging their strengths while compensating for individual limitations. In this study, Random Forest (RF), Gradient Boosting (GB), and Multi-Layer Perceptron (MLP) were employed as first-level models to construct a higher-level ensemble retrieval framework. Random Forest represents a bagging approach that aggregates predictions from multiple decision trees trained on randomly sampled subsets of data and features (Breiman, 2001). In our RF model, 100 trees were constructed with a maximum depth of 20, and out-of-bag (OOB) estimation was enabled to assess generalization performance. Gradient Boosting is a boosting technique that builds weak learners sequentially, with each learner focusing on the residuals of its predecessors, which enables high predictive accuracy through iterative refinement (Ma et al., 2018). For our GB model, regression decision trees (CART) are employed as weak learners, with 100 boosting iterations and a learning rate of 0.01. The maximum tree depth is set to 8 to control model complexity. The Multi-Layer Perceptron is a feedforward neural network composed of multiple layers of interconnected neurons with nonlinear activation functions, offering strong fitting ability and architectural flexibility for capturing complex relationships (Hornik et al., 1989). This MLP model consists of five hidden layers (54-100-54-32-16 neurons), with a learning rate of 0.0001 and L2 regularization (α=0.01) to enhance training stability and prevent overfitting. For the entire EML model, the predictions generated by these first-level models are used as input features for a higher-level meta-learner. Specifically, a Ridge regression model with cross-validated regularization (RidgeCV) is employed to learn the optimal linear combination of the first-level predictions. This stacking strategy enables the ensemble model to adaptively weight the contributions of RF, GB, and MLP, thereby improving the model's overall retrieval performance and generalization ability.

To enhance robustness, Gaussian white noise was injected into the training dataset. Proper noise perturbation is essential: too little noise reduces resistance to real-world observational errors, while too much can obscure true patterns. Noise characteristics were derived by comparing raw Almucantar observations with corresponding VLIDORT simulations based on AERONET inversion products (Sect. 2.1). From these differences, the signal-to-noise ratio was calculated to estimate the mean amplitude and standard deviation of the noise. Because solar radiation strongly depends on wavelength and angle, noise parameters vary with wavelength and RAA. Moreover, diffuse sky radiance spans a wide dynamic range, from about 10⁻¹ W m⁻² sr⁻¹ at large angles to over 10² W m⁻² sr⁻¹ at small angles. To address this, all input and output variables were standardized to the interval [-1, 1].

Ten-fold cross-validation (CV) was performed on the 100 000-sample training set to assess the EML model's generalization performance, with results summarized in Table 4 and discussed in Sect. 3.1. In this procedure, the training set is partitioned into ten equal subsets, and the model is iteratively trained on nine subsets while validated on the remaining one, repeating the process until each subset has served as the validation set once. After CV, the final EML model was trained on the entire training set to fully leverage all available data.

To ensure physical interpretability, the EML-based inversion algorithm incorporates SHAP, a game-theoretic method that attributes model outputs to individual features while accounting for feature interactions (Zhao et al., 2019; Hou et al., 2022; Wang et al., 2023; Zhang et al., 2024). The SHAP value for a feature Xj is defined as: 6ϕj=∑s∈NS!p-S-1!p!fS∪j-f(S)

where p is the total number of features, N is the set of all feature subsets excluding Xj, S is a subset of N, f(S) denotes the model prediction based on features in S, and f(S∪{j) is the prediction when Xj is added. The difference fS∪j-f(S) represents the marginal contribution of Xj for that subset, and the SHAP value ϕj is the weighted average of these contributions across all subsets. A larger SHAP value indicates a stronger influence of the feature on the model's predictions.

Six statistical metrics were used to evaluate the predictive performance of the EML-based retrieval algorithm: correlation coefficient (R), determination coefficient (R2), root mean square error (RMSE), linear bias, and error envelope (EE). These metrics quantify the agreement between the true values y and the predicted values y^: 7R=Covariance(y,y^)Variance(y)Variance(y^)8R2=1-∑i=1n(yi-y^i)2∑i=1n(yi-y¯)29RMSE=1n∑i=1n(yi-y^i)210Bias=1n∑i=1n(y^i-yi)11EE=#y|y^-y<±uncertaintyn where n is the number of samples, # is a counting symbol representing the number of points in the subsequent set. The uncertainty thresholds for EE follow the standards of existing ground-based aerosol inversion algorithms (Dubovik et al., 2000), with reference values of 0.03 for SSA, 0.02 for g, 0.1 for reff, and FMF.

The total inversion uncertainty σ was decomposed into systematic error σs and propagation error σp. Systematic error arises from the ill-posed nature of the inversion problem and the inherent limitations of the retrieval algorithm, and was quantified by applying the algorithm to the noise-free validation set, thereby excluding propagation effects. Propagation error results from the forward propagation of observational uncertainties and was evaluated through perturbation experiments. Gaussian perturbations (100 realizations) were applied to the model input variables to simulate random observational errors, and the standard deviation of the resulting outputs was taken as σp. Perturbation magnitudes were scaled according to the uncertainty of each variable: geometric angles were assumed exact, AOD was assigned an absolute uncertainty of 1m (where m is the optical air mass), and radiance was assumed accurate to within 5 % across all wavelengths (Holben et al., 1998; Eck et al., 1999). The total uncertainty σ was then calculated as the quadratic mean of σs and σp: 12σ=σs2+σp2 In theory, if the aerosol parameters retrieved by the algorithm are sufficiently accurate, they can be input into the RTM to reproduce the raw photometer measurements. The discrepancy between the simulated sky radiance y from the RTM and the observed radiance y∗, expressed in logarithmic scale, is defined as the optical residual: 13Residual(%)=∑i=1N(ln⁡y∗-ln⁡y)2N×100 where N denotes the total number of sky radiance observations in a single Almucantar scan. In this study, N=64, corresponding to radiance measurements at four wavelengths with RAAs greater than 20°.

In addition, the relative deviation is defined as the difference between the observed radiance y∗ and the simulated radiance y at a specific angle within a given band: 14RelativeDeviation=y∗-yy∗×100% This metric is used in Sect. 3.4 and illustrated in Fig. 7. Since the algorithm does not directly retrieve the complete aerosol size distribution required for radiative transfer calculations, the distribution was reconstructed using six-dimensional nearest-neighbor interpolation. The look-up table was generated from 110 000 sets of aerosol parameters prepared during the construction of the training and validation dataset. Its six search dimensions consist of g at four wavelengths, reff, and FMF.

The training and validation of our model are entirely based on the simulated dataset generated using the forward RTM. This design avoids dependence on instrument measurements or existing inversion products, and instead anchors the algorithm in radiative transfer theory for aerosol-laden atmospheres under clear-sky conditions. The performance of the EML model in the ten-fold CV is summarized in Table 4. The prediction score for each fold is the determination coefficient R2 between the predicted value of the trained EML model and the ground truth of the output variable. The prediction scores for all retrieved variables exhibit strong consistency across the folds. For SSA, the standard deviation of the prediction scores ranges between 0.0025 and 0.0056, whereas those for g, reff, and FMF range from 0.0104 to 0.0120. Such consistency demonstrates that the algorithm maintains reliable predictive capability irrespective of data partitioning, further underscoring its stability and robustness.

The inversion performance on the validation set is presented in Fig. 2. As noted in Sect. 2.1, the validation dataset contains 10 000 independent cases generated by forward radiative transfer simulations, excluded from training but constructed with the same noise characteristics. The results confirm that the EML-based algorithm retrieves SSA, g, reff, and FMF simultaneously across four wavelengths with high accuracy and without evidence of overfitting. The scatter points are tightly distributed around the 1:1 line, indicating minimal systematic bias. Among the retrieved parameters, SSA achieves the strongest performance, with an EE of about 90 %, an RMSE near 0.02, and R above 0.90. For SSA and g, the reported error statistics (e.g., RMSE) are wavelength-averaged. The asymmetry parameter g exhibits a slightly lower EE (∼70%), which can be attributed to its stricter uncertainty threshold and increased bias at longer wavelengths. Nevertheless, g still achieves reasonable accuracy, with R around 0.95 and RMSE around 0.018. For the microphysical parameters reff and FMF, the EE values are approximately 75 % and 66 %, respectively, with both parameters showing R above 0.9. Overall, these results suggest that the algorithm achieves satisfactory retrieval performance across the validation set, with errors generally within acceptable bounds.

To further test the real-world applicability of our EML-based retrieval algorithm, we applied the model to ground-based photometer observations and compared the retrieved parameters with those from AERONET. This testing set comprises 132 067 cases derived from AERONET Level 2.0 inversion products paired with raw Almucantar sky radiance measurements, entirely excluded from model training and validation. Figure 3 shows the comparison results, with data points diluted by one-tenth to improve visualization. The EML-retrieved parameters exhibit strong agreement with the AERONET products. Except for g at 440 nm, the R for all variables exceeds 0.9. The RMSEs of SSA and g are within 0.03, while those for reff and FMF are approximately 0.1. A notable advantage of the EML-based algorithm is its computational efficiency. It requires only 0.18 ms to invert a single measurement, which corresponds to a speed improvement on the order of 105, since traditional numerical retrieval algorithms often take several minutes per case. Dubovik et al. (2011) attempted to accelerate numerical inversion by optimizing forward radiative transfer calculations, such as reducing terms in the phase matrix expansion and quadrature integration. However, the time required for a complete retrieval still remained at the minute scale. In contrast, by eliminating iterative radiative transfer calculations, our algorithm increases the retrieval speed by a factor of ∼105 compared with conventional numerical inversion schemes.

Regarding wavelength dependence, the retrieval accuracy for SSA decreases with increasing wavelength λ in both the validation set (Fig. 2) and the testing set (Fig. 3), whereas the accuracy for g improves. As λ increases, the aerosol size parameter (x=2πrλ) decreases, leading to weaker single scattering and stronger multiple scattering in the total radiation field at longer wavelengths (Moosmüller et al., 2009; Moosmüller and Sorensen, 2018), which makes SSA more difficult to constrain. The relatively poorer performance of SSA retrieval at 440 nm observed in Fig. 3 may be attributed to the higher AOD uncertainty at this wavelength, which serves as input for both our EML-based algorithm and the AERONET official algorithm. Specifically, the AOD uncertainty is approximately ±0.01 for λ>440 nm and ±0.02 for λ≤440 nm (Holben et al., 1998; Eck et al., 1999). The improved retrieval accuracy of g at longer wavelengths can be explained by two mechanisms. First, the sensitivity of the radiative transfer equation to g, as quantified by the magnitude or norm of the Jacobian matrix (∂I∂g), increases with wavelength (Hasekamp and Landgraf, 2005; Kokhanovsky, 2013). At longer wavelengths, the range of retrieved g values broadens noticeably, as illustrated in Figs. 2 and 3. Second, the influence of aerosol size distribution on g becomes more pronounced at longer wavelengths. The forward-scattering peak of the phase function broadens with increasing λ, enhancing sensitivity to coarse-mode particles (Osborne et al., 2008; Kalashnikova et al., 2013). Consequently, retrieval errors for g decrease from about ±0.05 in the visible to ±0.02 in the near-infrared (Dubovik et al., 2006). This trend is also reflected in Fig. 3, where the RMSE of g decreases from 0.039 at 440 nm to 0.025 at 1020 nm.

Retrieving aerosol microphysical parameters is generally more challenging than deriving optical properties, and the retrieval accuracy of reff slightly decreases in the testing set relative to the validation set. Both reff and FMF are frequently recognized as key indicators of aerosol size distribution: fine-mode aerosols, such as sulfates, nitrates, and biomass burning particles, dominate when reff<0.3 µm and FMF >0.5, whereas coarse-mode aerosols, typically originating from natural sources like mineral dust and sea salt, prevail when reff>1.0 µm and FMF <0.3. In Fig. 3, FMF exhibits two distinct peaks near 0.3 and 0.7, corresponding to reff values of 0.6 and 0.28 µm, representing the coarse and fine modes, respectively. These results indicate that our algorithm can provide a basic classification of aerosols based on their retrieved optical properties (SSA and g) and size distribution (reff and FMF).

The normalized feature importance of input variables on the predicted outputs was quantitatively assessed using SHAP values, as shown in Fig. 4. First, the EML model effectively extracts and utilizes band-specific observational data for aerosol parameter retrieval at the corresponding wavelengths, as evidenced by the fact that radiance at a given wavelength exhibits the highest SHAP value when inverting SSA or g at the same wavelength. For instance, the radiance at 440 nm shows the highest feature importance for retrieving SSA at 440 nm (20.4 %), which is markedly greater than its contribution to SSA at other wavelengths. Similarly, when retrieving g at 440 nm, its feature importance reaches 31.8 %, again clearly exceeding its importance for g at other wavelengths. Rayleigh scattering is stronger at shorter wavelengths, and absorbing aerosols such as black carbon and brown carbon more heavily impact the blue light band. The sensitivity of SSA and g at 440 nm to radiation at 440 nm is stronger than in longer wavelength bands. Second, the SHAP values for each retrieved parameter indicate that the EML model also leverages observations across all wavelengths, particularly for g and reff, reflecting the physical relationship between aerosol properties, such as particle size, and the spectral dependence of scattered radiation. Thirdly, when inverting SSA, AOD in the same band shows the highest feature importance, ranging from 21.3 % to 45 %. This is expected because SSA is defined as the ratio of scattering to total extinction (scattering plus absorption), making accurate AOD essential for SSA retrieval from sky diffuse radiation measurements. In contrast, the importance of AOD diminishes when predicting reff and FMF, whereas sky diffuse radiance across multiple bands and scattering angles (SCAs) becomes more influential. According to Mie scattering theory, scattering phase functions differ substantially between fine- and coarse-mode aerosols, which increases the sensitivity of measured scattered radiation to particle size. For ground-based observations, diffuse radiance predominantly arises from aerosol forward scattering and stronger diffuse radiance indicates greater forward-backward scattering asymmetry, suggesting a larger column-averaged aerosol radius. Finally, auxiliary observation geometry information (SZA, VZA, and RAA) also plays a critical role in retrieving all aerosol parameters. These variables control both the magnitude and angular distribution of the measured radiance, thereby directly affecting the radiative transfer pathlength and scattering regime characterization. Consequently, the importance associated with observation geometry remain stable at around 10 % across all retrieval targets. Overall, the SHAP-based feature importance analysis demonstrates that the EML-based retrieval model successfully captures the underlying physical processes governing aerosol scattering of solar radiation, supporting its applicability for broader aerosol retrieval practices.

We quantify the uncertainties in retrieving SSA, g, reff, and FMF with the EML-based aerosol retrieval algorithm using the method described in Sect. 2.4. Systematic errors are defined as the RMSE of retrievals from the noiseless validation set, whereas propagation errors are estimated from the standard deviation of retrieval variability across 100 noise-perturbed realizations of AOD and radiance. As shown in Fig. 5, the two types of errors are comparable in magnitude for SSA, while for the other parameters the systematic errors exceed the corresponding propagation errors. The total absolute uncertainties for SSA and g both tend to increase with wavelength. Specifically, for SSA the uncertainties are 0.0154, 0.0198, 0.0222, and 0.0307 at 440, 675, 870, and 1020 nm, respectively, while for g they are 0.0149, 0.0147, 0.0191, and 0.0222 at the same wavelengths. For the microphysical parameters, the total uncertainties are 0.082 for reff and 0.096 for FMF. These levels are comparable to those reported for existing aerosol inversion algorithms. For example, the official AERONET algorithm reports uncertainties of 0.02–0.03 for SSA and about 0.02 for g (Dubovik et al., 2002), while relative uncertainties in reff can exceed 20 % due to the complexity of aerosol mixing states (Andrews et al., 2017). According to Sect. 2.4, the evaluation of propagation error depends on the intensity of perturbation to the input radiation. The stronger the perturbation, the greater the error. In the future, the accuracy of the instruments will likely improve, and we hope to achieve better accuracy in the inversion results. The 95 % confidence interval (CI) coverage measures the probability that the true parameter value lies within the model-predicted uncertainty range for a single noise-perturbed inversion case, whereas the EE denotes the fraction of cases that satisfy the predefined uncertainty criteria. Both metrics decrease in the order SSA >g>reff> FMF, indicating that, compared to aerosol optical parameters, the retrieval of microphysical parameters generally requires higher observation data quality and greater algorithmic accuracy.

We further evaluated the capability of our EML-based retrieval algorithm by using the aerosol parameters it retrieves to reproduce photometer observations. The accuracy of these retrieved parameters is reflected in the optical residual, which quantifies the discrepancy between the RTM-simulated radiance and the observed photometer measurements (see Sect. 2.4 for the detailed definition). Smaller optical residuals indicate higher retrieval accuracy, providing a quantitative measure of the retrieval quality. This assessment was performed using the testing set described in Sect. 2.1. Site-averaged retrieval residuals from our algorithm were compared with those from the AERONET official algorithm in Fig. 6. Across most sites, the residual magnitudes of the two algorithms are consistent, with differences generally within ±4% (Fig. 6c). From the perspective of algorithm design, the AERONET-type numerical algorithm minimizes the optical residual as a convergence criterion, whereas the EML model is trained to minimize the RMSE between predicted aerosol parameters and their reference values. That the EML-based algorithm achieves residual magnitudes comparable to the physics-based AERONET algorithm underscores its reliability.

Spatially, both algorithms exhibit similar residual distribution patterns: smaller residuals are observed over North and South America, East Asia, and Europe, whereas larger residuals occur over dust source regions such as North Africa and the Arabian Peninsula. Interestingly, the spatial pattern of residual differences between the two algorithms mirrors that of the mean reff retrieved by the EML model. Notably, the spatial pattern of residual differences between the two algorithms closely resembles that of the mean reff retrieved by the EML model, highlighting that the model's performance is less certain in regions dominated by coarse, non-spherical particles and pointing to potential areas for improvement. Sites in North Africa, South Asia, and inland China – where coarse-mode aerosols such as dust prevail – exhibit higher retrieval uncertainties. This effect is most pronounced at the shortest wavelength (440 nm, Fig. A1), where aerosol scattering exerts the strongest influence. Although both algorithms account for non-spherical particle scattering, neither fully resolves this complexity (Mishchenko et al., 1996), indicating that further algorithmic refinement is needed. In addition, strong parameter coupling among coarse-mode effective radius, volume concentration, and asymmetry factor may increase the ill-posedness of the inverse problem. The distribution of training samples may also play a role, as coarse-mode-dominated cases are typically less frequent than fine-mode-dominated cases in observational datasets, potentially limiting the representation of extreme coarse regimes in the training process. Additionally, some stations display substantially higher residuals relative to neighboring sites. At these locations, observational data are often sparse, potentially due to limited instrument maintenance or calibration. In certain cases, such as at some European sites, consistently low aerosol loading means the AOD rarely exceeds the 0.4 threshold required for AERONET Level 2.0 inversion products, contributing to larger residuals (Fig. B3).

Figure 7 shows the relative deviation between radiances simulated from the inversion results and those observed by the photometer, plotted as a function of RAA. Across all four observation wavelengths, the relative deviation exhibits a similar dependence on RAA. Minimal deviations (<10%) and peak correlation coefficients (>0.95) are observed at RAAs between 20 and 100°, indicating optimal agreement within this angular range. The current AERONET V3 retrieval algorithm excludes measurements with RAA <20° to minimize cloud contamination and forward-scattering effects (Giles et al., 2019). Similarly, the SKYNET algorithm prioritizes radiance observations within SCAs of 20–70° for aerosol property retrieval (Nakajima et al., 1996, 2020). For a SZA of 60°, RAAs between 20 and 100° correspond to SCAs of approximately 17–83°. These SCA ranges align closely with those designed for passive visible-light remote sensing sensors, such as MODIS (Levy et al., 2013), VIIRS (Hsu et al., 2019), and POLDER (Deschamps et al., 1994).

Physically, a broader SCA range generally provides more information for the inversion of aerosol optical and microphysical properties. However, very small RAAs increase the likelihood of interference from direct solar radiation, and Sun-sky photometer measurements with RAA <7° are often overexposed or saturated. Conversely, as RAA approaches 180°, the photon flux along single-scattering paths diminishes, leading to a sharp drop in the measured radiance and a lower signal-to-noise ratio.