## 1 Introduction  
Lightning activity associated with meteorological and atmospheric conditions is studied continuously with modern technology. Lightning flashes are frequently observable during thunderstorms, and different types of lightning activity are primarily dependent on the change in the number of storms [1]. Refs. [2, 3, 4] studied the relationship between cloud-top height and lightning flashes. Ref. [4] specifically examined infrared cloud-top measurements to determine the relationships for regional lightning rates for use in global chemistry models. Differences in lightning generation in thunderstorms over ocean and land were studied by [5, 6, 7]. Additionally, the relationship between lightning and thunderstorm updraft growth [8] and between lightning and rainfall rates [5, 6, 7] is significant for understanding the connection between lightning activity and associated meteorological conditions. Incloud (IC) flashes typically initiate at the upper boundary of the negative charge and discharge between the main negative and positive charge regions in cloud [9]. In contrast, positive/negative cloud-to-ground (CG) flashes are typically associated with the main positive/negative charge regions [10, 11]. Cloud flashes may manifest as extensive horizontal channels, commonly referred to as \"spider lightning\". The term \"spider lightning\" comes from the branched nature of its discharge path that resembles a spider web and its gradual development that resembles the crawling motion of a spider [12]. Spider lightning is a visually observable, horizontally stratified discharge that exhibits multiple branches (positive/negative leaders have variable behavior [13; 14]) and propagates along the cloud base [15; 16]. The propagation path of spider discharges extends tens to hundreds of kilometers and lasts for tens to hundreds of milliseconds [12]. The sustained luminosity observed in spider lightning is attributed to the continuing current along the discharge path. During the dissipating stage of storms, a significant accumulation of space charge occurs within storm clouds, leading to the thickening of the sub-cloud space charge layer. This stratified space charge layer has a significant influence on the discharge path [17; 18]. In this stage, the rate of lightning discharges is low [17]. Spider lightning discharges are occasionally observed in conjunction with positive CG lightning flashes [19]. Spider lightning discharges have been documented both during [20] and towards the end of storms [21] in Florida. In cloud regions with similar background radiances, oceanic lightning flashes tend to be larger, brighter, more energetic, and likely to have longer horizontal propagation over the ocean than those over land [22], and these characteristics suggest a physical distinction in the nature of the flashes. In GLM measurements, bright emissions are typically caused by positive CG lightning strokes with high peak currents in long horizontal flashes [23]. Most of the spectra of a return stroke, with temperature of about 30,000 K, of a CG flash are radiated by nitrogen ions (N\({}_{2}\)+) [24], with wavelength ranging from 400 nm to 650 nm [25] and the spectra of a stepped leader, with temperature ranging from 15,000 K to 30,000 K, are radiated by neutral nitrogen (N), N\({}_{2}\)+, and neutral oxygen (O), for which wavelength ranged from 600 to 1050 nm [26]. The spectral lines of ionized oxygen (O\({}^{+}\)) with high excited energies in IC flashes are stronger than those in CG flashes within the same area [27]. Ref. [28] reported that nitrogen molecules (N\({}_{2}\)) absorb energy under a high electric field, transitioning from their ground state to a higher energy state known as the transition state, resulting in the emission of light, particularly in the near ultraviolet region of the spectrum. When those N\({}_{2}\), N\({}_{2}\)+, N, and O are in an excited state, their emission spectra include many distinct bands within the visible light [29; 30].