Articles | Volume 14, issue 8
Atmos. Meas. Tech., 14, 5535–5554, 2021
https://doi.org/10.5194/amt-14-5535-2021
Atmos. Meas. Tech., 14, 5535–5554, 2021
https://doi.org/10.5194/amt-14-5535-2021

Research article 13 Aug 2021

Research article | 13 Aug 2021

Data imputation in in situ-measured particle size distributions by means of neural networks

Data imputation in in situ-measured particle size distributions by means of neural networks
Pak Lun Fung1,2, Martha Arbayani Zaidan1,2,3, Ola Surakhi4, Sasu Tarkoma5, Tuukka Petäjä1,3, and Tareq Hussein1,6 Pak Lun Fung et al.
  • 1Institute for Atmospheric and Earth System Research/Physics, Faculty of Science, University of Helsinki, 00140 Helsinki, Finland
  • 2Helsinki Institute of Sustainability Science, Faculty of Science, University of Helsinki, 00140 Helsinki, Finland
  • 3Joint International Research Laboratory of Atmospheric and Earth System Sciences, School of Atmospheric Sciences, Nanjing University, Nanjing 210023, China
  • 4Department of Computer Science, The University of Jordan, Amman 11942, Jordan
  • 5Department of Computer Science, Faculty of Science, University of Helsinki, 00140 Helsinki, Finland
  • 6Department of Physics, The University of Jordan, Amman 11942, Jordan

Correspondence: Pak Lun Fung (pak.fung@helsinki.fi) and Tareq Hussein (tareq.hussein@helsinki.fi)

Abstract

In air quality research, often only size-integrated particle mass concentrations as indicators of aerosol particles are considered. However, the mass concentrations do not provide sufficient information to convey the full story of fractionated size distribution, in which the particles of different diameters (Dp) are able to deposit differently on respiratory system and cause various harm. Aerosol size distribution measurements rely on a variety of techniques to classify the aerosol size and measure the size distribution. From the raw data the ambient size distribution is determined utilising a suite of inversion algorithms. However, the inversion problem is quite often ill-posed and challenging to solve. Due to the instrumental insufficiency and inversion limitations, imputation methods for fractionated particle size distribution are of great significance to fill the missing gaps or negative values. The study at hand involves a merged particle size distribution, from a scanning mobility particle sizer (NanoSMPS) and an optical particle sizer (OPS) covering the aerosol size distributions from 0.01 to 0.42 µm (electrical mobility equivalent size) and 0.3 to 10 µm (optical equivalent size) and meteorological parameters collected at an urban background region in Amman, Jordan, in the period of 1 August 2016–31 July 2017. We develop and evaluate feed-forward neural network (FFNN) approaches to estimate number concentrations at particular size bin with (1) meteorological parameters, (2) number concentration at other size bins and (3) both of the above as input variables. Two layers with 10–15 neurons are found to be the optimal option. Worse performance is observed at the lower edge (0.01<Dp<0.02µm), the mid-range region (0.15<Dp<0.5µm) and the upper edge (6<Dp<10µm). For the edges at both ends, the number of neighbouring size bins is limited, and the detection efficiency by the corresponding instruments is lower compared to the other size bins. A distinct performance drop over the overlapping mid-range region is due to the deficiency of a merging algorithm. Another plausible reason for the poorer performance for finer particles is that they are more effectively removed from the atmosphere compared to the coarser particles so that the relationships between the input variables and the small particles are more dynamic. An observable overestimation is also found in the early morning for ultrafine particles followed by a distinct underestimation before midday. In the winter, due to a possible sensor drift and interference artefacts, the estimation performance is not as good as the other seasons. The FFNN approach by meteorological parameters using 5 min data (R2= 0.22–0.58) shows poorer results than data with longer time resolution (R2= 0.66–0.77). The FFNN approach using the number concentration at the other size bins can serve as an alternative way to replace negative numbers in the size distribution raw dataset thanks to its high accuracy and reliability (R2= 0.97–1). This negative-number filling approach can maintain a symmetric distribution of errors and complement the existing ill-posed built-in algorithm in particle sizer instruments.

1 Introduction

Particulate matter (PM) is the principal component of air pollution. PM includes a range of particle sizes, such as coarse particles (1< particle diameter, Dp, <10µm), fine particles (0.1<Dp<1µm) and ultrafine particles (UFPs, Dp<0.1µm). Through humans' inhalation, coarse particles usually are partly deposited in the head airway (5–30 µm) by the inertial impaction mechanism and are partly deposited in the tracheobronchial region mainly through sedimentation (1–5 µm). The particles may be further absorbed or removed by mucociliary clearance (Gupta and Xie, 2018). The remaining fine and ultrafine particles, due to their high surface-area-to-mass ratios (Kreyling et al., 2004), penetrate deeply into the alveolar region, where removal mechanisms may be insufficient (Gupta and Xie, 2018). Evidence suggests that the adverse associations of short-term UFP exposure with acute and chronic problems ranging from inflammation, exacerbation of asthma, metal fume fever to fibrosis, chronic inflammatory lung diseases and carcinogenesis (Spinazzè et al., 2017) might be at least partly independent of other pollutants (Ohlwein et al., 2019). Various studies have demonstrated that inhaled or injected UFPs could enter systemic circulation and migrate to different organs and tissues (Londahl et al., 2014; Xing et al., 2016).

Other than health effects, particles of various sizes also contribute to Earth's ecosystem and climate differently. For instance, fine and ultrafine particles are capable of growing up to diameters of 0.02–0.1 µm within a day (Kulmala et al., 2004; Kerminen et al., 2018), where they constitute a fraction of cloud condensation nuclei, thus indirectly affecting the climate (Kerminen et al., 2012). The drivers behind aerosol particles vary between natural and anthropogenic as well as primary and secondary. Primary particles are emitted to the atmosphere as particles, such as sea salt or dust particles, while secondary particles form in the atmosphere through gas-to-particle transformation, which has been known as new particle formation (NPF) observed in various environments and contributing to a major fraction of the total particle number budget (Kulmala et al., 2004; Kerminen et al., 2018). In addition, while fine particles cool the climate by predominantly scattering shortwave radiation, coarse particles warm the climate system by absorbing both shortwave and longwave radiation (Kok et al., 2017). Indeed, the complexity of urban aerosols is tribute to the fact that several sources can contribute in the same particle size range (Rönkkö et al., 2017).

Currently, the most commonly reported aerosol variables are particle mass concentration and particle number concentration. The former metric, which is dominated by coarser particles, is included as air quality indicators (e.g. mass concentrations of both thoracic particles, PM10, and fine particles, PM2.5); however, it has been argued that this might ignore the potential adverse effect of UFPs on health (Zhou et al., 2020). The latter one describes better the distribution of finer particles, but it neglects the influence of coarse particles. Using either particle mass concentration or particle number concentration solely is not enough to fully review the health effects and the Earth's climate system by aerosol particles. Therefore, in order to understand the origin of atmospheric aerosol particles and their potential impacts at a specific location, the whole size distribution of these particles needs to be studied (Zhou et al., 2020).

Recently, due to urbanisation and increased population, megacities have increased their contribution to atmospheric aerosol pollution massively (Lelieveld et al., 2015). The Middle East and North Africa (MENA) region, with an average annual growth rate of 1.74 % in 2019 (World Bank Group, 2019), has one of the world's most rapidly expanding populations. With a population of 578 million, several cities in the MENA region are among the 20 most polluted cities in the world. The annual average concentrations of some pollutants, for example PM2.5 in MENA (54.0 µg m−3), often exceed 5 times the WHO-recommended levels (10.0 µg m−3) (World Health Organisation, 2019). Many countries in MENA are dealing with negative impacts of air pollution in terms of both economic burden and health aspect (Ahmed et al., 2017; Goudarzi et al., 2019). Air Pollution in this region is estimated to cause 133 000 premature deaths annually, almost half of which are attributed to natural sources of air pollution, such as windblown sea salt and desert dust (Gherboudj et al., 2017). Apart from natural pollutants, anthropogenic activities also play a major role in driving the air quality. They include the extensive development of petrochemical industry, vehicular emissions and open burning of waste (Arhami et al., 2018).

However, aerosol studies in this region have not paid attention to the aerosol number size distribution so far. Among the few studies published, most report mass concentration (Goudarzi et al., 2019; Arhami et al., 2018; Borgie et al., 2016), while some focused on the total particle number in MENA regions. Studies on the size-fractionated number concentrations are, nonetheless, scarce (e.g. Hakala et al., 2019) due to the unavailability of instruments for measuring UFPs in many air quality monitoring stations (Spinazzè et al., 2017). Determining aerosol number size distribution for a wide size range in a reliable manner is a challenging task. The fact that the ambient distributions range from nanometres to several micrometres dictates the use of multiple sizing techniques. For the submicron size range, electrical mobility equivalent diameter is commonly used as the size parameter, and the measurements are performed with differential mobility particle sizer (DMPS) or scanning mobility particle sizer (SMPS) instruments (e.g. Wiedensohler et al., 2012). These systems determine the aerosol size according to electrical mobility equivalent size. The larger particles (approximately >0.3µm) can be classified according to their aerodynamic or optical size (Kulkarni et al., 2011). In order to obtain the full aerosol size distribution, these data need to be merged. Unfortunately this task is not trivial as the merging requires knowledge of the chemical composition (influencing the refractive index and thus the optical size), shape (influencing electrical mobility equivalent size) or effective density (influencing aerodynamic size) (Kannosto et al., 2008).

In addition, the raw data from these instruments must be inverted to obtain the particle size distribution. This is not a straightforward problem. A proper inversion algorithm is required to restore the particle size distribution from the raw response (Cai et al., 2018) using recorded kernel functions which describe the probability of particles of a certain size being measured at a certain flow rate, influenced by the measured activation curves and the detection efficiencies of the instruments (Lehtipalo et al., 2014). Depending on the instruments used and the measurement environments, some use a built-in inversion algorithm in the instruments, which replace negative raw values with artificial non-negative numbers. Some develop their own inversion methods; however, they all have their drawbacks. For example, the least-squares method may magnify the random errors in the raw counts in the condensation particle counter (CPC) into relatively large uncertainties (Enting and Newsam, 1990), the stepwise method may cause non-negligible errors (Lehtipalo et al., 2014) and the smoothing step method may introduce bias in the shape of the inverted distribution function (Markowski, 1987). Kandlikar and Ramachandran (1999) pointed out that there is not a single universal inversion algorithm applicable to all situations. In this study, the built-in inversion algorithm was used. This algorithm can lead to negative values when the kernel functions are not optimally configured, especially in the size range of low number concentration. These negative values have no physical meanings. Some experts in the in situ measurement community might just omit the negative values or simply use nearest-neighbour linear interpolation to replace the negative values. However, the former method might cause asymmetric error for very small measured number concentration values (Viskari et al., 2012), while the latter could result in too high values concurrently. To fill this knowledge gap, statistical estimation methods can serve as an alternative to estimate of size-fractionated number concentration by using other available measurements.

The main objective of the paper is to estimate particle number concentration and/or fill the negative values making up for the shortcomings of the built-in inversion algorithm in particle sizer instruments. Extending from the previous study by Zaidan et al. (2020), we build our imputation method with a finer temporal and size-bin resolution. In order to do so, we place emphasis on estimating the particle number concentration of a specific size bin using the interaction with other size bins and meteorological variables. In this study, we propose three approaches in terms of different input variables by means of neural networks: (1) only meteorological parameters, (2) only particle size distribution, and (3) both particle size distribution and meteorological parameters. Based on the general data analysis of the particle size distribution and the meteorological condition, we explain the source of different size bins at certain weather conditions and the correlation among the particle size distribution and meteorological parameters in Sect. 3. We evaluate the proposed neural network method and compare it with other simpler methods in Sect. 4.1. In Sect. 4.2, we further discuss the temporal pattern of the proposed method in terms of its diurnal cycle, weekend effect and seasonal variation. Besides, we examine the possible technical reasons for the pattern found and the application of the proposed method.

2 Methods

2.1 Measurement sites and instruments

In this study, we collected a dataset obtained from a measurement campaign in Amman, the capital city of Jordan, between 1 August 2016 and 31 July 2017. The city represents an area with Middle Eastern urban conditions within the Middle East and North Africa (MENA) region. This region serves as a compilation of different aerosol particle sources including natural dust, anthropogenic pollution (e.g. generated from the petrochemical industry and urbanisation) and new particle formation.

https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f01

Figure 1The block diagram describing the methodology of the proposed FFNN method.

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The database includes particle size distribution and meteorological parameters, as mentioned in the first step in Fig. 1. The aerosol measurement was carried out at the aerosol laboratory located on the third floor of the Department of Physics of the University of Jordan (3200 N, 3552 E) in the neighbourhood of Al Jubeiha. The campus is situated in an urban background region in northern Amman. In particular, the campaign measured the particle number size distribution using a scanning mobility particle sizer (NanoScan SMPS 3910, TSI, MN, USA) with default settings. It monitors the particle size distributions as electrical equivalent diameter 0.01–0.42 µm (13 channels). The size range of the SMPS system can be extended to coarse particles with an additional compact instrument: an optical particle sizer (OPS 3330, TSI, MN, USA). OPS measures optical diameters from 0.3 to 10 µm (13 channels). This optical sizing method reports an optical particle diameter, which is often different from the electrical mobility diameter measured by the SMPS technique. The measurements were combined to provide a particle size distribution of a wider particle diameter range from 0.01 to 10 µm, which is further described in Sect. 2.2. The SMPS inlet consists of copper tubing with a diffusion drier (TSI 3062-NC). The inlet flow rate was 0.75 L min−1 (±20 %), while the sample flow rate was 0.25 L min−1 (±10 %). The flow rate of OPS was about 1 L min−1. The aerosol transport efficiency and losses through the aerosol inlet assembly and the diffusion drier were determined experimentally in the laboratory: ambient aerosol sampling alternatively with and without sampling inlet as well as the aerosol data were corrected accordingly. The penetration efficiency was ∼47 % for 0.01 µm, ∼93 % for 0.3 µm and ∼40 % for 10 µm (Hussein et al., 2020). This deficiency of measurement at the upper and lower edges is somewhat in agreement with other literature. Particle size measured by NanoSMPS (Tritscher et al., 2013) tended to be underestimated for spherical particles larger than 0.2 µm by up to 34 % (Fonseca et al., 2016). Liu et al. (2014) clearly portrayed that the detection limit of particle size below 0.03 µm is about 80–500 cm−3, which is up to 10 times larger than that of coarser particles, for other versions of SMPS. Stolzenburg and McMurry (2018) explained that discrepancies could result from differential mobility analysers (DMAs) with transfer functions that were degraded (i.e. broadened) by flow distortions caused by particle deposition within the classifier tube, sizing errors due to errors in flowmeter calibrations or leaks, CPC concentration errors due to improper pulse counting, and continuity failure in the DMA high-voltage connection.

The meteorological measurement was performed with a weather station (WH-1080, Clas Ohlson model 36-3242, Helsinki, Finland) with a time resolution of 5 min. The meteorological data were comprised of ambient temperature (T, resolution 0.1), relative humidity (RH, resolution 1 %), wind speed (WS), wind direction (WD, 16 equal divisions) and air pressure (P, resolution 0.3 hPa) (Hussein et al., 2019, 2020; Zaidan et al., 2020). Wind direction is resolved into north and east direction, as WD-N and WD-E, respectively. The data collection process is illustrated in the first step in the database block in Fig. 1.

2.2 Data pre-processing

The next step in the database block in Fig. 1 is data pre-processing. Since the sampling time resolution of SMPS and OPS was 1 and 5 min, respectively, we synchronised the data into 5 min averages. Since parts of the size ranges in both instruments are overlapping with each other, the last two size bins in SMPS and the first size bin in OPS were neglected. Finally, we merged the size range of electrical mobility diameter 0.01–0.25 µm by SMPS and optical diameter 0.32–10 µm by OPS, and we obtained a wider particle size distribution which covers the diameter range 0.01–10 µm. Merging the electrical mobility diameter and optical diameter can be a challenge, and the overlapping region is often calculated with high uncertainty (DeCarlo et al., 2004; Tritscher et al., 2015). The challenge arises because the optical diameters are measured based on the refractive index of the particles, which depends on their chemical composition. Therefore, the sizing will vary over time. There is also a slight dependency with the SMPS system that is linked to the shape of the particles, which influences their sizing.

We also calculated the particle number concentration with four particle diameter modes (size-fractionated number concentration): nucleation (0.01–0.025 µm), Aitken (0.025–0.1 µm), accumulation (0.1–1 µm) and coarse mode (1–10 µm). Subsequently, the total number concentration was obtained as the sum of all these fractions. The size-fractionated number concentrations were obtained by summing up the measured particle number size distribution over the specified particle diameter range.

In order to perform data imputation with neural networks, aerosol and meteorological data were first linearly interpolated in time in case of short missing data periods. For missing data over longer periods, the whole rows are eliminated. The shorter missing data period occurs due to technical faults, while the longer missing periods are attributed to instrument maintenance (Zaidan et al., 2020). Only 71.8 % of total data were retained for the next step in the measurement period. Since the data were obtained from different measured variables with various physical units and magnitudes, it was crucial to normalise the data. The scaling factor depends on which activation function is chosen. In this case, the datasets were scaled so that it has a mean of 0 and a standard deviation of 1 to transform them into the range of the activation function. The standardised data were then separated into different months for the reason of the seasonal variation in the atmospheric condition. The data were further divided into a training set (70 %) and testing set (30 %). The processed data were also converted to hourly and daily averages for reporting purposes.

https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f02

Figure 2Schematic diagram of a neural network with one hidden layer of sigmoid activation function.

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2.3 Setting of the neural network

After data collection and data pre-processing procedures, the next step is method optimisation (Fig. 1). ANN models have been utilised in predicting air quality (Freeman et al., 2018; Maleki et al., 2019; Cabaneros et al., 2019; Zaidan et al., 2020; Fung et al., 2020). Neural networks provide a robust approach for approximating real-valued target functions because they can mimic the non-linearity of the functions and their optimisation methods are well developed (Zaidan et al., 2017). The architecture of neural networks consists of nodes as an activation function (Fig. 2), and the activation function in each layer determines the output value of each neuron that becomes the input value for neurons in the next hidden layer connected to it. In this paper, a feed-forward neural network (FFNN) is used instead of a more sophisticated time delay neural network (TDNN) because some of the rows in the dataset were removed in the data pre-processing step due to the existence of missing data, and TDNN cannot be performed without time continuity. FFNN usually consists of a series of layers. The first layer has a connection from the network input. Each subsequent layer has a connection from the previous layer. The final layer produces the network's output. A neuron can be thought as a combination of two parts:

(1) z j ( L ) = σ ( i = 1 n w j i ( L ) x i + b j ( L ) ) ,

where zj(L) and bj(L) are the intermediate output and the bias term for the jth neuron at the Lth layer, respectively. wji(L) is the jth weight for each data point xi at the Lth layer. The second part performs the activation function (sigmoid function in this study) on zj to give out the output of the neuron:

(2) σ z j ( L ) = 1 1 + exp - z j ( L ) .

The FFNN method was created, trained and simulated with MATLAB (version: 8.3.0.532), using the Neural Network Toolbox. We initialised the weights randomly, and the weights were updated through Levenberg–Marquardt algorithm optimisation, which was the fastest available back-propagation training function (Chaloulakou et al., 2003). We performed several iterations within a cycle to minimise the training loss with Bayesian regularisation. These steps were done iteratively until the best combination of the number of hidden layers and the corresponding number of neurons that provided the minimum error were found. According to the review paper by Cabaneros et al. (2019), a shallow neural network with one hidden layer and enough neurons in the hidden layers can fit any finite input–output mapping problem for non-linear relationship. In the network training process, the number of neurons varied (i) from 2 to 10 neurons per layer with an incremental factor of 2 neurons in each simulation and (ii) from 10 to 25 per layer with an incremental factor of 5 neurons in each simulation. To keep the method simple, we consider only one or two layers in the simulation process because the computing requirements could rise exponentially with the number of layers and neurons. Once we pick the suitable method configuration, the method estimates number concentration using testing data. Finally, the selected performance metrics, described in Sect. 2.4, can be calculated, and we evaluate which approach is the most suitable for size distribution estimation.

2.4 Other methods as comparison with the neural network method

In order to demonstrate the performance of the FFNN method, we perform similar procedures applying other simpler methods, which have been widely used as means of data imputation (Junger and Ponce De Leon, 2015). They include univariate and multivariate methods. The former includes unconditional mean (UM), median (MD), linear interpolation (LinI), logarithmic interpolation (LogI), next-neighbour interpolation (nNI) and previous-neighbour interpolation (pNI), where nNI was implemented as the next value carried backward, while pNI was implemented as the previous value carried forward. The multivariate methods used in this study are the conditional mean based on a linear regression of meteorological parameters and other particle size number concentrations as inputs (CM–met and CM–PSD, respectively). These methods are implemented as a comparison with the FFNN method.

2.5 Performance metrics

We choose the optimal combination of the number of hidden layers and the corresponding number of neurons by checking its mean absolute error (MAE), which is a simple way to illustrate the residuals of the estimated values by the estimation method. In order to identify which size bin manages to be predicted best, two metrics are used, namely coefficient of determination (R2) and normalised root-mean-square error (NRMSE). R2 measures how well the observed outcomes are replicated by the estimation method, based on the proportion of total variation of outcomes explained by the estimation method. NRMSE represents the standard deviation of the estimated errors with respect to its mean. NRMSE is used rather than the commonly used RMSE because the number concentrations of the different size range are of different magnitudes. The comparison of the different size range becomes different if RMSE is not normalised with its mean.

(3)MAE=i=1nyi-yi^n,(4)R2=1-i=1n(yi-yi^)2i=1n(yi-y)2,(5)NRMSE=i=1n(yi-yi^)2ny,

where yi, yi^ and y represent the ith measurement value, the yth estimated value by the estimation method and the mean of the all the measurement data, respectively. n denotes the total number of the valid measurement data.

3 General data analysis

3.1 Environmental condition

Hussein et al. (2019) and Zaidan et al. (2020) investigated and described the effect of local weather conditions, respectively. Here we describe briefly the meteorological conditions during the measurement period as background information. Starting from August 2016, the daily temperature decreased gradually from 40 to its minimum 0 in February 2017. It rose gradually to 40 in August 2017. During the measurement period, the hourly median value was 19.9 (Fig. 3a). RH varied quite a lot from 10 % to 100 %, with an hourly median of 52.3 %, and did not seem to have a seasonal pattern (Fig. 3b). In summer months, wind appeared be stronger, but the wind direction was more stable, mostly from the northwest (270–360). In cold months, averaged wind speed was lower but wind blew from a fluctuating direction. During the whole measurement period, wind speed ranged between 0–6 m s−1, and its median was 1.39 m s−1 (Fig. 3c–d). Air pressure varied in a range from 892 to 912 hPa, and its hourly median was 900 hPa. In spite of the narrow range of variation, winter months seem to have slightly higher air pressure than summer months (Fig. 3e).

https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f03

Figure 3Time series of meteorological conditions during the measurement period August 2016–July 2017. (a–e) Temperature, relative humidity, wind speed, wind direction and air pressure, respectively. Black and red represent hourly and daily averaged data, respectively.

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https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f04

Figure 4Wind rose diagram of total particle number concentration at a different direction (in the theta axis) and different wind speed (in the radical axis). Wind direction and wind speed data are grouped in every 10 and 0.5 m s−1. Warmer colour represents higher total particle number concentration. (a) Total number concentration, log scale; (b) coarse mode, linear scale. Note the colour scales are different.

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Meteorological conditions have been suggested to influence particle number concentration. Hussein et al. (2019) demonstrated that number concentration had a rather complex relationship with temperature. Furthermore, number concentration of submicron particles had a decreasing trend with respect to the wind speed, which indicates that most of the submicron fraction originated from local sources such as combustion processes. Meanwhile, the number concentration of coarse particles had higher concentrations at stagnant conditions and when the wind speed is higher than 5.5 m s−1. It is mainly because of road dust resuspension and might also be attributed to dust storm via long-range transport (Hussein et al., 2019). In this study, we further explore how wind direction influences the particle number concentration (Fig. 4). Wind coming from the northwest (225–325) was generally stronger, but lower particle number concentration was detected because the measurement area is at the outskirts of downtown. Wind from the east and south (45–225) has a lower wind speed, but a more intense hourly particle number concentration can be detected. From that direction is situated the Amman urban city where all kinds of industrial activities take place. When considering only coarse particles, a relatively high number concentration is found when south-westerly wind is strong. This can further serve as evidence that the source of coarse particles in that region might come mostly from long-range sea salt from the Dead Sea or dust particles from nearby deserts.

https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f05

Figure 5Time series of total particle number concentration (in cm−3) of 0.01–10 µm (a). (b–c) The contribution in percentage of nucleation mode and Aitken mode, respectively. (d–e) The number concentration in accumulation mode and coarse mode, respectively. Black and red represent hourly and daily averaged data, respectively.

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Table 1Table showing the descriptive statistics (in cm−3) of total number concentration, nucleation mode, Aitken mode, accumulation mode and coarse mode. The statistical values include mean, standard deviation (SD) and percentile (10 %, 25 %, 50 %, 75 % and 90 %).

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3.2 General pattern of particle size distribution

Hourly total number concentration ranged from 1.90×103 to 1.52×105 cm−3, and its median was 1.36×104 cm−3. Figure 5a shows a moderate seasonal pattern in general: lower in summer months and higher in colder months. Hussein et al. (2019) also characterised the modal structure of the particle number size distribution for the same site. Four modes have been detected by the automatic lognormal fitting algorithm (DO-FIT, Hussein et al., 2005, 2019), which revealed that the mode number concentrations of the nucleation, Aitken and coarse modes were lognormally distributed around their geometric mean values: 0.022, 0.062 and 2.3 µm respectively. However, the accumulation mode number concentration had two distinguished modes with particle diameter centred at 0.017 and 0.39 µm. As seen in Table 1, the total number concentration of all particle size fractions (1.70±1.26×104 cm−3) is mostly accounted for by the Aitken mode (45 %–80 %, average: 1.09±1.01×104 cm−3) followed by the nucleation mode (10 %–50 %, average: 0.48±0.32×104 cm−3). The accumulation mode (0 %–15 %, average: 0.13±0.08 cm−3) comes third, and only less than 0.5 % of the total particle number concentration contains coarse particles with an average of 2.13±2.80 cm−3 (Fig. 5b–e). The seasonal pattern of the total number concentration resembles the Aitken composition: lower proportion in summer months and higher in colder months. The ratio of the nucleation mode performs in an opposite way. The seasonal variation of the total number concentration is due to the more suppressed boundary layer in winter (Teinilä et al., 2019) and the elevated wood combustion (Hellén et al., 2017). The particle number of accumulation and coarse mode steadily stay at a low proportion line, which did not account for the total number concentration. It is also noticed that dust episodes occurred with the concentrations that often exceeded 2 cm−3, and the daily concentration in the course of these episodes can rise to 20 cm−3. These episodes were often found in spring from February to May, and some episodes can last for up to 1 week.

https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f06

Figure 6(a) Diurnal cycle of the (i) nucleation mode, (ii) Aitken mode, (iii) accumulation mode and (iv) coarse mode in warm (red) and cold months (blue) during workdays (solid) and weekends (dashed). (b) Particle size distribution in (i) cold and (ii) warm months, coloured by particle number concentration (cm−3). Cold and warm months refer to December–February and June–August, respectively.

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Similar to many other urban environments, the diurnal pattern observed in this study reflects the combustion emissions from traffic activity, which is higher during the workdays (Hussein et al., 2019). The two peaks of the nucleation mode and Aitken mode in the cold months are relevant for the morning and the afternoon traffic rush hours, which are similar to those noticed in most cities in other countries. In warmer months, the diurnal cycles are not as distinct, but a sharp peak of the nucleation mode around noon is found, which is associated with the occurrence of new particle formation. These events occurred very often in the summer as suggested by Hussein et al. (2020). The amplitude of diurnal cycles of the coarse mode is small, while the patterns of accumulation are not clear (Fig. 6).

3.3 Correlation analysis

Figure 7 demonstrated the interaction among the whole measured spectrum shows three range clusters based on their correlation with the number concentration at other bin sizes: 0.01–0.205, 0.205–0.875 and 0.875–10 µm. The sizes 0.01–0.205 and 0.875–10 µm fall entirely within the size range detected by SMPS and OPS, respectively. The 5 min number concentration of smaller size and larger size bins have clear and strong correlation with the concentration of its neighbouring size bin. However, particles of size 0.205–0.875 µm are located in the overlapping regions by the two instruments; as a result, they do not correlate well with the other size bins. The correlation of 5 min particle size distribution with meteorological parameters is generally low. Temperature appears to be the most correlated parameters for all bin sizes among all the parameters we used in this study. Smaller size ranges have a higher Pearson correlation coefficient (R) than larger size ranges for WD, WS and P.

https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f07

Figure 7Matrix plots showing the Pearson correlation coefficient (R) of particle size distribution of (a) 5 min, (b) hourly and (c) daily averaging with (i) particle size distribution itself and (ii) meteorological parameters. Darker colour represents a higher correlation.

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The 5 min averaged data show a similar correlation for the particle size distribution except for the smallest size bin. The hourly and daily data have higher correlation with the other size bins, which are also monitored by SMPS. The 5 min averaged data show different correlation from the hourly and daily averaged data performed by Zaidan et al. (2020). The correlations of 5 min size distribution with all meteorological variables are below 0.5 for all size ranges. However, for hourly and daily averaged data, R is much higher in specific size bins. Hourly and daily temperature, in particular, show increasing R with larger particle size for accumulation and coarse mode. Overall, the correlations increase with the longer averaging windows. This might be due to the buffer period in which the meteorological conditions act on the dispersion of particles. Based on this result, using data with finer temporal resolution might be considered to be less influential to the estimation accuracy.

4 Evaluation of the proposed method

4.1 General evaluation

Figure 8 illustrates how well the three approaches of the proposed FFNN perform in terms of R2 and NRMSE.

https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f08

Figure 8Bar chart showing the evaluation of the FFNN approach with (a) only meteorological parameters (approach 1, FFNN–met), (b) particle size distribution itself (approach 2, FFNN–PSD), and (c) both particle size distribution and meteorological parameters (approach 3) as inputs. The evaluation metrics for the proposed method include the (i) coefficient of determination (R2) and (ii) normalised root-mean-square error (NRMSE).

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4.1.1 Approach 1 (size distribution estimation based on meteorological parameters only, FFNN–met)

For more than half of the 23 size bins, two layers and 15 neurons is the best combination where the residuals are the lowest (Table 2). Owing to the poor correlation with meteorological condition, we expect a low correlation of determination even using the optimal configuration neural network (R2= 0.22–0.58). The R2 values are low at the nucleation mode (0.01<Dp<0.03µm) of the whole size distribution (R2∼0.2). The rest of the size bins have better and more stable performance (R2= 0.4–0.58). This shows that the instrument might have a poor detection efficiency for particles of smaller size. The performance of the FFNN method using 5 min data for all size bins (R2= 0.22–0.58) is worse than using daily data (R2=0.77) performed in Zaidan et al. (2020). Compared with hourly data (R2=0.66), the overall performance of the method using 5 min data is comparable (R2=0.67).

Table 2Table showing the best configuration in the form of (the number of layers; the number of neurons) for the approach by meteorological parameters (FFNN–met) and the number concentration at the other size bins (FFNN–PSD) as inputs. Mean absolution error (MAE, in cm−3), coefficient of determination (R2) and normalised root-mean-square error (NRMSE) are listed for different size bins on each row. The last row concludes the overall selection of the approach with the best configuration and its corresponding evaluation metrics.

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4.1.2 Approach 2 (size distribution estimation based on other particle sections only, FFNN–PSD)

This approach works well with most combinations of number of layers and neurons. They do not show a clear difference among the combinations we choose. There is no single combination which entirely outperforms the others in all size bins. We summed up the MAE for all size bins and decided to stick to two layers and 10 neurons with the overall lowest residuals (Table 2). R2 values are all above 0.97 for all bin sizes, and NRMSE values are 0.01–0.25 for all bin sizes. The results are expected because there are 22 inputs and one output. Relatively worse correlation at the edges of size bins (0.01<Dp<0.02µm; 6<Dp<10µm) is found because of the lack of nearby size bins which have high correlation with the corresponding size bin. Another reason could be that the instrument has a higher detection limit for smaller particles (Liu et al., 2014). The poorer performance for smaller sizes might be due to a coarser size resolution compared to other SMPS components (Tritscher et al., 2013), so that NanoSMPS does not reflect the real-enough size distribution in the atmosphere. Relatively poor estimation performance at the middle size range (0.15<Dp<0.5µm) in the whole measured spectrum is because of the overlapping of instruments. This also ascertains the importance of creating a better algorithm when we merge two or more size distributions by different instruments. In this study, the measuring techniques and the measuring targets are different between the SMPS and OPS. The merging of the two measuring targets, the optical particle diameter and the electrical mobility diameter, might create significant uncertainties (DeCarlo et al., 2004; Tritscher et al., 2015). The estimation of certain bin size by other bin sizes can be thought of replacing negative values in the raw data by particle sizers. While some instrument manufacturers create built-in algorithms to replace with artificial non-negative numbers, most end users simply remove the seemingly impossible negative values from the dataset. The perfect way to do it is to have a parallel instrument that overlaps with that particle size range. However, in many cases, this is not possible as a result of financial constraints. Therefore, we shall rely on the mutual relationship between the size sections in the aerosol population. Negative values appear often at size bins with very low number concentration (usually in coarse mode). Instead of eliminating them, this alternative could maintain the symmetry of the error distribution of the number concentration (Viskari et al., 2012) and minimise the uncertainties caused.

Table 3Table showing the comparison of different estimation methods, including unconditional mean (UM, column 2), median (MD, column 3), linear interpolation (LinI, column 4), logarithmic interpolation (LogI, column 5), next-neighbour interpolation (nNI, column 6), previous-neighbour interpolation (pNI, column 7), and conditional mean by regression of meteorological parameters and other particle size number concentrations as inputs (CM–met and CM–PSD, columns 8 and 9, respectively) and the feed-forward neural network with meteorological parameters and other particle size number concentrations as inputs (FFNN–met and FFNN–PSD, columns 10 and 11, respectively). The coefficient of determination (R2) of each method is listed for different size bins on each row. Negative R2 values are represented by “0” to indicate poor accuracy at the particular particle size bin, while “NA” means the data are not available. The last row concludes the overall evaluation metrics.

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4.1.3 Approach 3 (size distribution estimation based on meteorological parameters and other particle sections)

The general results are similar to those in PSD. However, more input variables do not enable the approach to work better. At some bin size the R2 values are even slightly smaller than PSD solely, since meteorological data show low correlation with most portions of the measured spectrum. In that approach, the addition of meteorological parameters is not beneficial to the estimation process. Due to the lack of improvement in the method development, we will only focus on the two methods: FFNN–met and FFNN–PSD.

Table 4Table showing the comparison of different estimation methods, including unconditional mean (UM, column 2), median (MD, column 3), linear interpolation (LinI, column 4), logarithmic interpolation (LogI, column 5), next-neighbour interpolation (nNI, column 6), previous-neighbour interpolation (pNI, column 7), and conditional mean by regression of meteorological parameters and other particle size number concentrations as inputs (CM–met and CM–PSD, columns 8 and 9, respectively) and the feed-forward neural network with meteorological parameters and other particle size number concentrations as inputs (FFNN–met and FFNN–PSD, columns 10 and 11, respectively). The normalised root-mean-square error (NRMSE) of each method is listed for different size bins on each row. NA means the data are not available. The last row concludes the overall evaluation metrics.

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https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f09

Figure 9Scatter plots showing the estimated particle concentration (y axis, in cm−3) against the in situ-measured particle concentration (x axis, in cm−3). (a–f) Univariate methods including unconditional mean (UM), median (MD), linear interpolation (LinI), logarithmic interpolation (LogI), next-neighbour interpolation (nNI) and previous-neighbour interpolation (pNI), respectively, in dark grey dots. (g–h) Multivariate methods including conditional mean by regression of meteorological parameters and other particle size number concentrations as inputs (CM–met and CM–PSD, respectively) in light grey dots. (i–j) The proposed feed-forward neural network with meteorological parameters and other particle size number concentrations as inputs (FFNN–met and FFNN–PSD, respectively) in red dots. The black solid line is the 1:1 line, which gives a reference of perfect estimation. The coefficient of determination (R2) and the normalised root-mean-square error (NRMSE) of each method for all particle size bins are shown on the corresponding subplots.

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In order to highlight the performance of the FFNN methods in terms of accuracy and reliability, we compare the FFNN methods with other simpler methods; the results are shown in Table 3 for R2 and Table 4 for NRMSE. The R2 values of the univariate methods UM and MD are close to 0 because their imputation is oversimplified and implies the replacement of a missing value by a constant. This can be further validated by the narrow range of the estimated particle concentrations in Fig. 9a–b. The remaining univariate interpolation methods LinI, LogI, nNI and pNI showed good results in general (R2= 0.82–0.92, NRMSE= 0.57–0.88) but failed to perform even fairly at some particle size bins. This implies that these methods are not stable for the whole spectrum of the particle size distribution. Some of the estimated particle concentrations are off from the 1:1 line, which implies that the estimation of some particle bins are not as accurate (Fig. 9c–f). The performance results of the multivariate methods CM–met and CM–PSD are comparable to FFNN–met and FFNN–PSD, but both CM methods show weaker performance than FFNN methods in terms of R2 and NRMSE regardless of whether meteorological data (CM–met: R2=0.52, NRMSE=1.39; FFNN–met: R2=0.67, NRMSE=1.13) or particle size distribution data (CM–PSD: R2=0.99, NRMSE=0.17; FFNN–PSD: R2=1.00, NRMSE=0.07) are used as inputs. The pattern of performance of the multivariate methods is also similar to those of FFNN, i.e. relatively poor performance at the edges of size bins (0.01<Dp<0.02µm; 6<Dp<10µm) and the overlapping region (0.15<Dp<0.5µm). When combining the whole spectrum, FFNN methods (Fig. 9i–j) appear to have narrower bands than CM methods (Fig. 9g–h) along the 1:1 line, which indicates the methods work similarly across the particle size spectrum. Although the multivariate method CM–PSD (Fig. 9h) also relies on the mutual relationship between the size sections in the aerosol population, this method is not as accurate and stable as our proposed FFNN–PSD.

From the perspective of physics, particles in the nucleation mode (0.01<Dp<0.03µm) are more sensitive to transformation processes due to their volatility and rather unstable nature (Morawska et al., 2008). This leads to a relatively short lifetime in the atmosphere (Al-Dabbous et al., 2017); hence, the relationships between the input variables and the nucleation mode are not well established. Al-Dabbous et al. (2017) demonstrated that accumulation mode particles (0.1<Dp<0.3µm) have much longer lifetimes compared to smaller particles, causing them to be transported for larger distances (Laakso et al., 2003); therefore, the mapping of the relationships between long-range-transported accumulation mode particles and covariates is not well understood. However, the relative prediction ability in this study is not lower given that local meteorological variables were used as input variables. The possible reason is that this mode falls exactly in the instrumental overlapping regions, which leads to a lower predictability. The locally produced Aitken mode particles (0.03<Dp<0.1µm) are less effectively removed by transformation processes (e.g. evaporation and coagulation) from the atmosphere, compared with nucleation mode particles (0.01<Dp<0.03µm), allowing the estimation methods to better understand their relationships with the input variables, which is in agreement with Al-Dabbous et al. (2017).

4.2 Temporal pattern

Figure 10 shows the diurnal discrepancies during workdays and weekends. Relative particle number concentration was defined by the estimated concentration with respect to the measured concentration. Values above 1 indicate overestimation, while values below 1 suggest underestimation. For approach 1 (FFNN–met), except for the overlapping size bin, which is underestimated by more than 50 % at all time ranges, the difference between estimated and measured hourly number concentration is within 50 % during both workdays and weekends. Overestimation is found in the early morning before 03:00 UTC+2 (UTC+3 in summer) during workdays for all size bins, especially for UFPs. Following the overestimation, at about 06:00 in the morning, the estimated number concentration appears to be understated by up to 40 %, especially at size bins below 0.1 µm. During the day, the estimation uncertainties are rather small until in the evening from 06:00 to 23:00, where estimated UFP number concentration shows moderate overestimation one more time. This reveals that FFNN–met fails to detect the diurnal pattern from 18:00 to 07:00 in particular for UFPs. The pattern of the performance for weekends does not appear to be as distinctive as on workdays. This shows the overestimation not only for UFPs in the early morning around 03:00, but also at the upper edge larger than 5 µm from 03:00 to 16:00. From 19:00 until midnight, an underestimation is found at all size bins. For approach 2 (FFNN–PSD), except for the overlapping size bin, which has a significant overestimation from 18:00 to 07:00, most size bins show a negligible 10 % uncertainty during both workdays and weekends. The performance over weekends shows relatively stronger uncertainties. The smallest bin at 0.01 µm is slightly understated for all hours of a day. Other than these, FFNN–PSD manages to detect the diurnal pattern for all size bins fairly well.

https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f10

Figure 10Heat map showing the hourly median relative particle number concentration of the approach with (a) meteorological parameters (approach 1, FFNN–met) and (b) particle size distribution (approach 2, FFNN–PSD) as inputs across different hours of a day (i) on workdays and (ii) on weekends. The relative particle number concentration is defined as the estimated concentration with respect to the measured concentration. Red colour shows overestimation while blue shows underestimation.

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https://amt.copernicus.org/articles/14/5535/2021/amt-14-5535-2021-f11

Figure 11Heat map showing the coefficient of determination (R2) of the approach with (a) meteorological parameters (approach 1, FFNN–met) and (b) particle size distribution (approach 2, FFNN–PSD) as inputs for different months at different size bins. Darker colour represents a higher R2.

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Figure 11 further shows the monthly deviation in estimation performance. For approach 1 (FFNN–met), higher R2 is found in November, February and April in the range of SMPS. Other than that, there is no observable variation in R2 in approach 1 (FFNN–met). For approach 2 (FFNN–PSD), except in January when all the rows were eliminated because of the lack of wind information, performance in the other months is steady for most size ranges. At 0.21 µm, the difference in estimation performance varies across different months. R2 values in winter months are 0.76, 0.36 and 0.61, in November, December and February, respectively, while R2 exceeds 0.9 in other months. This unexpectedly low R2 only occurs in the winter months at the overlapping size range. It can be speculated that the measurements by the two instruments differ in a larger extent during winter. This might be attributed to sensor drift and a number of interference artefacts for particle measurements associated with several factors, such as relative humidity, temperature and other gas-phase species, which were demonstrated by several researchers (e.g. Lewis et al., 2016; Popoola et al., 2016). Another reason for the difference in estimation performance can be that the percentages of complete rows in these months are lower than the other months. The drop in data points might influence the estimation performance. Especially in June, at the few size bins close to the larger edge, R2 ranges from 0.9 to 0.7. Besides that, some low R2 values can be also found in individual months at both edges of the size range, which does not appear to show any patterns.

In short, the estimation ability for the lower edge (0.01<Dp<0.03µm) is found to be worse in both approaches. The performance of the FFNN method in the mid-range (0.15<Dp<0.5µm) and upper edge (6<Dp<10µm) is relatively worse for the approach with other fractionated size bins as input variables according to the aforementioned statistical performance indicators. All statistical estimation simulations are based on the previous history of relationships between the inputs and outputs. As a result, the estimation simulations for different size ranges have significantly unique connections. The approach by meteorological parameters considers only six predictor variables so the accuracy is lower than FFNN–PSD. It might not seem surprising that the deviations between the measured and estimated size distribution were not substantial (R2>0.97, NRMSE<0.25) because FFNN–PSD takes 22 other size bins as predictor variables. This, nevertheless, gives a clue that the proposed FFNN method can provide adequate solutions to particle size distribution prognostic demands. Furthermore, this FFNN method outperforms the other selected widely used methods in terms of its accuracy and reliability. The estimation of certain bin size by other bin sizes can be thought of as replacing negative values in the raw data by particle sizers, including the SMPS which we used in this paper. Instead of eliminating the negative values, they can be estimated by other size bins with a high accuracy in order to keep the symmetry in data error distribution (Viskari et al., 2012).

5 Conclusion

This paper presents the evaluation of imputation methods by means of a feed-forward neural network (FFNN) for estimating particle number concentration at various particulate size bins. Input predictors include a merged particle size distribution, by a scanning mobility particle sizer (NanoSMPS) and an optical particle sizer (OPS), which covers the size range from 0.01 to 10, and meteorological parameters, including temperature (T), relatively humidity (RH), wind speed (WS), wind direction (WD) and ambient pressure (P). The measurements were collected in an urban background region in Amman, the capital of Jordan, in the period of 1 August 2016–31 July 2017. The total number concentration (1.70±1.26×104 cm−3) in the measurement period shows moderate seasonal variability owing to the more suppressed boundary layer (Teinilä et al., 2019) and the elevated wood combustion (Hellén et al., 2017) in wintertime. Similar to many other urban environments, the diurnal pattern observed in this study reflects the traffic activity, which has a more pronounced pattern during workdays (Hussein et al., 2019). The amount of coarse particles is negligible in terms of number concentration, but dust episodes were found often in spring during the measurement period.

We proposed three approaches with different input variables: (1) only meteorological parameters, (2) only number concentration at the remaining size bins and (3) both of the above. We performed an optimisation to obtain the optimal configuration of the FFNN methods, which are two layers with 10–15 neurons, balancing the accuracy and the computing resources. The 5 min averaged meteorological parameters give a varying number concentration estimation for various size bins (R2= 0.22–0.58), which is outperformed by hourly and daily averaged data (R2= 0.66–0.77), as demonstrated by Zaidan et al. (2020). The methods using the number concentration at the remaining size bins, both with or without meteorological data, show the expected perfect performance (R2>0.97). We also compared the FFNN methods with other commonly used methods, and the results highlight the high accuracy and reliability of methods by means of neural networks.

Relatively poor performance of the proposed FFNN methods is found in three regions. At the lower edge (0.01<Dp<0.02µm) and the upper edge (6<Dp<10µm), the number of neighbouring size bins is limited, and also the detection efficiency by the corresponding instruments is lower compared to the other size bins. Another noticeable region (0.15<Dp<0.5µm) is the overlapping section measured by the two particle sizers, and the reason is because of the deficiency of the merging algorithm. For all the above approaches, the poorer performance for smaller particles in the nucleation mode could be due to the fact that it is more effectively removed from the atmosphere compared to other modes (Al-Dabbous et al., 2017). An observable overestimation is also found in the early morning for ultrafine particles followed by a distinct underestimation before midday. A larger derivation between the measured and the estimated number concentration is found in the winter, which might be caused by sensor drift and interference artefacts (e.g. Lewis et al., 2016; Popoola et al., 2016). Despite the high number of input predictors, the good estimation performance provides an alternative method to fill up the negative values in the size distribution raw dataset, which often exist due to misconfiguration problems. Instead of removing the factually impossible data point, this way of replacing negative numbers can maintain a symmetric distribution of errors (Viskari et al., 2012) and minimise the uncertainties caused.

Code and data availability

The code and data are available upon request.

Author contributions

TH and MAZ designed the experiments and TH carried them out. PLF and OS developed the code of the proposed FFNN methods. PLF prepared the manuscript with contributions from all co-authors.

Competing interests

The authors declare that they have no conflict of interest.

Disclaimer

Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

Financial support

This research has been supported by the Scientific Research Support Fund (SRSF, project no. BAS-1-2-2015) at the Jordanian Ministry of Higher Education and the Deanship of Academic Research (DAR, project no. 1516) at the University of Jordan. This research is part of a close collaboration between the University of Jordan and the Institute for Atmospheric and Earth System Research (INAR/Physics, University of Helsinki), supported by European Regional Development Fund through the Urban Innovative Action Healthy Outdoor Premises for Everyone (HOPE, project no. UIA03-240). Grants were also received from the European Research Council through the European Union's Horizon 2020 research and innovation framework programme (ATM-GTP (grant no. 742206) and ACTRIS-2 (grant no. 654109)), and ERA-PLANET (http://www.era-planet.eu/, last access: 13 July 2021) and its transnational project SMURBS (http://smurbs.eu/, last access: 13 July 2021) provided funding under the same programme (grant agreement no. 689443). The authors have been supported by the Academy of Finland Flagship funding under a project from the Atmosphere and Climate Competence Center (ACCC, project no. 337549).

Review statement

This paper was edited by Otto Hasekamp and reviewed by two anonymous referees.

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Short summary
Aerosol size distribution measurements rely on a variety of techniques to classify the aerosol size and measure the size distribution. However, due to the instrumental insufficiency and inversion limitations, the raw dataset contains missing gaps or negative values, which hinder further analysis. With a merged particle size distribution in Jordan, this paper suggests a neural network method to estimate number concentrations at a particular size bin by the number concentration at other size bins.