## 1 Introduction  
Aerosols are liquid or solid particles suspended in gas with a certain level of stability that have significant impacts on the global radiative energy balance and climate change. The aerosol vertical distribution is an important parameter associated with the retrieval of highly precise aerosol microphysical properties (a previous study has shown the spectral dependence of the radiation effect on the aerosol layer height) that plays an important role in the study of radiative forcing [1]. For example, it is necessary to consider aerosol scattering in trace gas and ocean color retrieval and modify the aerosol vertical distribution parameters accordingly [2; 3; 4]. The aerosol layer height (ALH) is a major determining factor in the passive remote sensing monitoring of atmospheric fine particulate matter, such as PM\({}_{2.5}\), near the ground. One such approach is the spaceborne PM\({}_{2.5}\) remote sensing method (PMRS) [5; 6]. ALH is commonly used in model calculation, while in the passive remote sensing measurements, it can be always be replaced by planetary boundary layer height (PBLH). The planetary boundary layer is the lowest layer of the atmosphere and, which contains the vast majority of aerosols of the low troposphere [6; 7]. At the same time, the height information on smoke, volcanic, and dust aerosols can provide the initial conditions for the modeling of their emissions and the physics of plume formation [8; 9; 10]. Consequently, it is imperative to observe the vertical distribution of aerosols on a global scale in order to validate transport models and better understand the impact of aerosols on the climate and environment of the Earth [10; 11]. Satellite remote sensing offers the possibility of measuring aerosol height information on a global scale. Active remote sensing measurements, such as ground-based, flight-based, and space-based measurements, can effectively measure the vertical distribution of aerosols. For instance, Cloud-Aerosol Lidar with Orthogonal Polarization (CALIOP) can measure the backscatter at each vertical layer, resulting in detailed aerosol extinction coefficient profiles based on the backscatter ratio [12]. Passive remote sensing measurements, while not having the same accuracy or resolution as active remote sensing, can provide considerable spatial coverage and higher temporal resolution by using ultraviolet (UV), visible/near infrared (VNIR), and thermal infrared (TIR) band observations [10]. In passive remote sensing, most studies focus on the O\({}_{2}\) A band [12; 13; 14]. Comprehensive studies have shown that the vertical distribution of oxygen absorption bands is generally stable and not affected by the emissions [13], which is one of the important ways to retrieve ALH. In practice, it is challenging to reach an agreement between the retrieved aerosol height from real O\({}_{2}\) A band measurements and LIDAR measurements, which depend on ad hoc assumptions. Often, higher spectral resolution sensors are used or, given the advantage of reducing interference from the surface, measurements are combined with the O\({}_{2}\) B band to improve the retrieval accuracy [14]. The stereoscopic technique, which relies on the principle of parallax, is applicable for the retrieval of plume-type aerosols with discernable textures, while it is not affected by complex aerosol microphysical properties and radiative transfer computation [15; 16]. Applying the UV-A band (315-400 nm) is another approach for ALH passive retrieval, because in the ultraviolet and near-ultraviolet bands, the elevated aerosol layer partly shields the polarization signal from Rayleigh scattering, providing sensitivity to the aerosol layer height [17; 18]. On the other hand, the aerosol information will be improved when the surface albedo decreases, and the lower surface reflectance in the UV wavelength is also beneficial for the retrieval of ALH. A previous study performed retrievals with Research Scanning Polarimeter (RSP) measurements in the near-ultraviolet and blue spectral bands.