Analysis of Ten-Year Variations of Lightning Activity in Italy and Correlation with Land and Sea Surface Temperatures

Abstract

This study investigates the evolution of lightning activity in Italy by comparing two biennia: 2010–2011 and 2020–2021. Lightning data were obtained from a lightning location system (the SIRF network) and processed to focus exclusively on cloud-to-ground (CG) strokes. The analysis covers both land and surrounding sea areas, with data filtered and validated according to the study objectives. A detailed statistical comparison of CG activity between the two periods is presented, along with an assessment of spatial distributions across the Italian territory. Furthermore, correlations between CG stroke occurrence and both sea surface temperature and land surface temperature are examined. The findings highlight temporal and spatial variations in lightning patterns over the decade and provide insights into their possible relationship with environmental conditions.

1. Introduction

Lightning constitutes a major hazard to human life, the natural environment, and various infrastructures, including power and telecommunication systems [1]. Its complexity attracted extensive investigation by physicists, meteorologists, and electrical engineers, with three main purposes: (i) exploiting it as a dependable indicator for forecasting severe weather events, (ii) advancing the understanding of its physical development, and (iii) improving the design of protection strategies for energy, communication, and civil installations.

With respect to forecasting applications, a robust characterization of lightning occurrence (both in terms of quantitative metrics and spatial distribution) is essential to define threshold values that, once exceeded, may indicate anomalous and potentially hazardous weather conditions. Such thresholds can be integrated into meteorological alert systems. Numerous studies across different regions [2,3,4,5,6,7,8,9,10,11,12,13,14] have demonstrated a strong link between lightning activity and the evolution of heavy rainfall processes within thunderstorms. As highlighted in these works, lightning measurements enable the near-real-time identification of the most intense convective cells and the tracking of their spatial development [15,16,17,18]. This has promoted the growing interest in lightning-based forecasting and nowcasting methodologies [19,20,21,22,23,24,25].

Experimental data represent a fundamental resource for advancing investigations and developing models in lightning research and protection design. Within this field, particular attention is typically given to the return-stroke phase of the lightning flash, due to its dominant energy content and impact. Nonetheless, other stages of the lightning flash (such as the preliminary breakdown) are also the subject of dedicated studies, especially in view of specific applications (see the review in [26]). Research on the lightning return stroke has attracted significant interest in electrical engineering, with contributions mainly addressing (i) the detailed modeling of its current waveform [27,28,29,30,31], (ii) the computation of lightning electromagnetic fields under varying assumptions regarding soil conductivity and channel geometry [32,33,34,35,36,37,38,39,40], (iii) the evaluation of overvoltages induced on overhead transmission and distribution systems [41,42,43,44,45,46,47,48,49], (iv) the analysis of interactions with elevated structures such as pylons, towers, and wind turbines [50,51,52,53], and (v) the development of machine learning-based lightning location methods that exploit overvoltage waveforms induced on overhead power lines [54,55,56,57,58].

Lightning local data are mainly provided by lightning location systems (LLSs). As reported in [59], LLSs provide continuous coverage over large geographical domains, potentially up to continental scale, making them valuable for quantifying the exposure of technical infrastructures to lightning hazards. These systems, which consist of distributed networks of electromagnetic sensors, produce parameters such as Ground Flash Density (GFD), Ground Stroke Density (GSD), peak current distributions, flash multiplicity, and polarity. Many investigations have explored how these properties vary with geographical and climatological factors (seasonality, sea–land contrast, latitude, and altitude). Early results from the U.S. East Coast network [60,61] indicated that positive flashes represented less than 5% of summer lightning but peaked at about 80% in February, with winter storms being predominantly oceanic and positive. Subsequent work [62] confirmed minimum positive flash occurrence in July–August and a maximum in January–February. In Europe, the authors of [63] examined Greek lightning records from 2008 to 2009, identifying summer and autumn as peak seasons. Latitude effects remain debated, with some works (e.g., [64,65]) reporting significant correlations, while others (e.g., [66]) found no such relationship. Altitude-related patterns were observed in [67], who detected increasing lightning activity between 500 m and 2000 m, followed by a marked decline above 2000 m.

Recent observations from the JASA Lightning Detection Network of five isolated small thunderstorms in East China showed that single-stroke flashes accounted for over 30% of all negative CG flashes and were generally associated with weaker initial stroke peak currents compared to multiple-stroke flashes [68]. Moreover, building on waveform analysis, the authors of [69] proposed a convolutional neural network to classify lightning Low Frequency (LF)/Very Low Frequency (VLF) signals into five types, including CG, Intra-Cloud (IC), preliminary breakdown pulses, and narrow bipolar events, achieving an average accuracy above 95%, highlighting the potential of deep learning for automated lightning type identification.

In recent decades, lightning studies have been performed for Europe [70,71,72] and for parts of the Mediterranean [63,73,74,75]. The authors of [73], using Zeus LLS data, investigated correlations between lightning occurrence and factors such as elevation, slope, vegetation, and sea surface temperature (SST), identifying a positive link between SST and lightning frequency over a 10-year record. In [63], spatial and seasonal patterns of CG and IC flashes in Greece were analyzed, while the authors of [70] evaluated monthly and seasonal GFD variability across European latitudes. In [72], a continental-scale investigation was conducted of annual, monthly, and diurnal GFD cycles, CG polarity ratios, and cumulative distributions of peak current and multiplicity by exploiting data of national LLSs integrated within the European network EUCLID. National-scale reports include [76] for Austria and [77] for Belgium, both detailing GFD, polarity, and lightning current properties, with spatial correlations to elevation in the Belgian case. The authors of [74] analyzed 19 years of LLS records, identifying significant spatial clustering and detecting local trends potentially linked to Mediterranean warming. In [75], a 10-year analysis of lightning activity over Bulgaria and the Black Sea was conducted, revealing seasonal and diurnal variations with summer peaks over land and sea, autumn dominance over the Black Sea, and a strong nighttime influence of sea surface temperature on thunderstorm formation.

For Italy, early assessments were carried out in [78] shortly after the deployment of the SIRF (Italian System for Lightning Detection) network, part of EUCLID, revealing spatial variations in peak current for positive and negative flashes, seasonal distributions, and seasonal influences on peak current magnitudes. The analysis of [79] reported the performance of the Italian Air Force’s LAMPINET network to derive peak current probability density functions for both polarities and their seasonal modulation, without differentiating between first and subsequent strokes, a distinction which is significant for lightning performance studies (e.g., [80,81,82,83,84,85,86,87,88]). Other analyses quantified seasonal CG stroke densities without accounting for sea–land separation or latitudinal and altitudinal variability. An extensive analysis of lightning activity over Italy from 2010 to 2019 was conducted in [89], using data from the SIRF network. Such a study examined GSD and the positive-to-negative stroke ratio (assessing the influence of seasonal, geographical, and orographic factors), peak current characteristics, flash multiplicity, and the spatial separation between stroke impact points within individual flashes.

The reliability of such studies is strongly related to the accuracy of LLS data, which are generally validated through comparison with direct measurements from instrumented towers or artificially triggered lightning. Comprehensive validation of EUCLID is provided in [90].

This study contains an analysis of lightning activity in Italy, more precisely about how the lightning activity has been changed between the 2010–2011 biennium and the 2020–2021 biennium. Lightning data have been acquired from the SIRF network. The area of interest is Italy and the surrounding (sea and ground boundary).

Global temperatures rising is altering atmospheric conditions such as humidity, stability, and convection dynamics [91]. Since lightning formation is closely tied to these factors, particularly through convection and the interaction of ice and graupel particles [92], temperature increases are expected to influence its occurrence [93]. Several studies have projected that lightning activity will increase with global warming, with estimates ranging from a 5% to 16% increase per degree of temperature rise [94,95,96,97]. Observations also suggest a positive correlation between surface temperature and lightning frequency on shorter timescales [16,98]. However, longer-term trends remain uncertain, and alternative modeling approaches indicate that lightning responses may vary significantly depending on how it is parameterized [99,100].

Because temperature affects both cloud development and storm intensity, understanding how land and sea surface warming influence lightning activity is essential for improving climate projections. More precise modeling of these relationships will help refine estimates of future atmospheric composition and the role of lightning in climate feedback mechanisms [101,102,103].

Since lightning activity has been increasingly investigated as a potential marker of climate and global change, in this contribution, a correlation analysis between lightning occurrence and land and sea surface temperatures is proposed.

The organization of the article is as follows. Section 2 explains the SIRF data processing and the relationship between lightning activity and the geographical area where the analysis has been carried out. Section 3 reports the results obtained through this analysis, and a comparative study of lightning statistics between data recorded by SIRF in 2010–2011 and in 2020–2021 is proposed. In Section 4, a correlation analysis between CG stroke occurrence and sea surface temperature and land surface temperature is performed. Finally, some concluding remarks are proposed in Section 5.

2. Lightning Data

Data are extracted from the SIRF database covering the 2010–2011 period and the 2020–2021 period. The SIRF network is an Italian LLS, owned and operated by Centro Elettrotecnico Sperimentale Italiano (CESI S.p.A., Milan, Italy) since 1994. In the 2010–2011 configuration, it was made of 16 LF/VLF electric field sensors, VAISALA IMPACT 141-T, distributed across Italy (including the two main islands), plus 11 sensors across the Alps owned by the French, Swiss, Austrian, and Slovenian networks, using both time-of-arrival and magnetic-direction-finding methods to detect and locate lightning strikes; sensors’ distribution and distances were optimized to give a uniform and high performance detection. Between 2014 and 2015, SIRF was upgraded by replacing the IMPACT units with VAISALA LS7002 sensors, using LF/VLF detection as well. During the same period, a new location algorithm was introduced, designed to optimize the selection of signals linked to each return stroke. This upgrade resulted in improved performance, specifically in terms of detection efficiency, location accuracy, and classification accuracy. With respect to the previous configuration, the upgraded system shows some improvements in performance. The earlier setup provided detection efficiencies of about 90% for CG flashes and 80% for CG strokes above 2 kA, with a median location accuracy close to 500 m and an overall classification capability of 95% in distinguishing CG from IC events. In the post 2015 configuration, the detection efficiency is estimated at 95% for CG flashes and 90% for CG strokes above 2 kA, while the median location accuracy is around 250 m. The classification capability is also slightly higher (98%). According to [90], the median error for the peak current estimate is about 20%, compared with direct tower measurements. Further details can be found in [89]. The SIRF network is always operated with redundancy and operational scheme to guarantee 24 h/24 and 7 d/7 of availability and steady performances.

It is worth to specify that, since 2020, the management of the SIRF network has been transferred from CESI S.p.A. to the French company METEORAGE. During 2020–2021, METEORAGE underwent several changes in the Italian sensor network (including relocations and replacements). These variations, together with the sensor upgrade introduced in 2014–2015, may affect the performance of the network. Consequently, the results obtained for the two considered periods (2010–2011 and 2020–2021) must be interpreted in light of these differences.

In this contribution, not all types of lightning flashes detected by SIRF are involved: it was considered appropriate to exclude all data concerning IC strokes, because they represent a minor risk for power systems. Thanks to this operation, the dataset was significantly reduced. It is worth to specify that the IC are events of higher frequency and weaker peak current, hence the farther from the network they occur, the more difficult it is for the PLS (Precision Lightning Sensors) to detect them. As pointed out in [104,105], there is always the uncertainty that IC strokes are misinterpreted as positive CG strokes. However, SIRF classification tool is assumed to be robust for the purpose of this analysis

Since one of the aims of the analysis is lightning occurrence variability between sea and land, it was decided to consider the area under investigation depicted in Figure 1, which extends for 750,072 km² and includes part of the Mediterranean Sea, to perform sea-based and land-based analyses.

In order to enable a rigorous comparison, as previously performed in [89], the spatial extents of marine and terrestrial surfaces were selected to be as similar as possible. Specifically, the marine domain considered in this work encompasses 448,734 km², while the corresponding terrestrial domain covers 301,338 km². The maritime region was additionally defined so as to remain sufficiently close to the Lightning Detection Network, ensuring comparable detection capabilities, supported also by the contribution of nearby sensors located in other countries throughout the observation period.

The analysis also incorporates the potential influence of topographic elevation on lightning occurrence within the Italian territory. Since the SIRF dataset does not provide elevation at the point of ground impact, this parameter has been integrated as a new attribute. Elevation values were derived using a Digital Elevation Model (DEM), which represents the terrain surface in three dimensions on the basis of elevation data. For each recorded strike, the DEM was linked to the geographical coordinates supplied by SIRF, thereby providing the corresponding ground altitude. Typically, a DEM is available in raster form, where each cell stores the elevation above mean sea level. When employed within a Geographic Information System (GIS), DEMs can generate additional layers of information whose applications are numerous, particularly in the field of geospatial analysis and natural hazard mitigation.

The parameters investigated in the present study are listed below, with further details provided in the subsequent section:

• Seasonal maps and monthly variation in GSD;
• Monthly variation in the negative-to-positive cloud-to-ground stroke ratio;
• Diurnal cycle lighting occurrence across different seasons;
• Seasonal distributions of strike-point elevation and its dependence on latitude;
• Monthly variation in the mean peak current at the channel base;
• Distribution of flash multiplicity and the spatial separation between stroke impact points within a flash;
• Distribution of the current peak for positive first strokes, negative first strokes, and negative subsequent strokes.

3. Lightning Activity: Results and Discussion

3.1. Seasonal Maps of CG Strokes

Figure 2 and Figure 3 show the seasonal spatial distribution of the negative (left column), positive (central column), and total CG (right column) events over the 2010–2011 and 2020–2021 periods, respectively. For this purpose, measurements were reported to a 1 × 1 km² grid, cumulated by season and divided by the length of the considered period. The same data are collected in

Table 1. Count of negative, positive, and total CG strokes over the 2010–2011 and 2020–2021 periods.

	2010–2011			2020–2021			Increment in 10 Years
	Neg.	Pos.	Tot.	Neg.	Pos.	Tot.	Neg.	Pos.	Tot.
Spring	249,678	23,491	273,169	125,698	18,896	144,594	−50%	−20%	−47%
Summer	1,000,779	76,000	1,076,779	1,078,750	150,354	1,229,104	8%	98%	14%
Autumn	1,227,407	110,244	1,337,651	1,893,481	221,442	2,114,923	54%	101%	58%
Winter	123,840	21,205	145,045	122,037	31,469	153,506	−1%	48%	6%
Tot.	2,601,704	230,940	2,832,644	3,219,966	422,161	3,642,127	24%	83%	29%

.

Comparing the total number of strokes, a significant seasonal variability in lightning activity is highlighted: for both periods the highest number of total strokes is recorded in autumn (September–October–November—SON, panel I), followed by summer (June–July–August—JJA, panel F); much less events are detected during spring (March–April–May—MAM, panel C) and winter (December–January–February—DJF, panel I). However, it should be noted that, in summer and winter a similar number of total strokes has been detected in the two periods; on the other hand, strong differences in 2020–2021 records with respect to 2010–2011 records appear in spring (−47%) and autumn (+58%), mainly due to negative strokes. Although the impact of positive strokes on the total count is less relevant; it is worth noting that their increment is +83%, with strong contributions given by summer (+98%) and autumn (+101%) events.

Some local differences in seasonal spatial distributions of CG lightning can be observed in the two periods. In 2010–2011 during spring, the negative CG strokes (and therefore the total ones) are concentrated along the western coast of the peninsula and around the northeast regions, whereas in 2020–2021 are more concentrated on the Po valley. Similar considerations can be made for the total CG strokes in summer. On the other hand, considering the total CG strokes in autumn, the areas with the greatest concentration are, in general, the same in both periods (i.e., on the coastal regions of western Italy and especially over the sea); however, the stroke density of 2020–2021 is much higher than that of 2010–2011. In winter, the areas with the greatest concentration remain practically the same in both periods, i.e., the western coast of the peninsula. The only difference is the presence of an additional hot spot, located to the northeast in Friuli Venezia-Giulia, in the biennium 2020–2021.

3.2. Monthly Variation in CG Stroke Density

The monthly behavior of the stroke density, i.e., the ratio between the yearly number of lightning strokes occurring over an area and the corresponding surface in km², is investigated in this section. Figure 4 shows the monthly mean density of negative CG strokes (panel A) and positive CG strokes (panel B) over the sea and land for the 2010–2011 and 2020–2021 periods.

The extension of sea and land surfaces has been considered similar in size as much as possible to make a robust comparison. Thus, in this study, the land surface is 448,734 km² and that of the sea is 301,338 km².

It is important to point out that the monthly mean density of positive CG strokes both over the sea and land in 2010–2011 and in 2020–2021 are always lower than 0.05 and 0.07 strokes km² yr⁻¹, respectively. Thus, their values are almost negligible with respect to those of negative CG strokes.

Despite a slightly different magnitude, a similar trend can be observed in all panels. Very low values from January to April are followed by an increase until a maximum is reached between July and September. Then, during autumn and winter, a decrease to values comparable with those of the first months of the year.

CG stroke density in 2010–2011 reaches greater values over the land in summer, whereas in 2020–2021, the highest densities are over the sea during autumn. Regardless of the polarity, in the 2010–2011 (2020–2021) period, CG lightning activity is more relevant over the sea than over land from October (September) to January.

3.3. Monthly Variation in the Negative/Positive CG Strokes Ratio

Figure 5 represents the monthly behavior of the ratio between negative CG and positive CG strokes over the sea and over the land for the 2010–2011 and 2020–2021 period.

As regards the 2010–2011 period, the negative CG strokes are between 4.5 and 26.5 times the positive ones, whereas in the 2020–2021 period, the negative CG strokes are between 3.5 and 12 times the positive ones.

The most significant difference that can be highlighted by observing the two figures is that in 2020–2021, the ratio between negative CG and positive CG strokes is always higher over the land than over the sea, except for January, February, April, and December; for the 2010–2011 period the opposite holds true: in 2021, the ratio between negative CG and positive CG strokes is always lower over the land than over the sea, except for April, May, and September.

The ratio recorded in 2020–2021 over the sea is remarkably lower than that recorded in 2010–2011. Indeed, in 2010–2011, the ratio varies between 4.5 and 26.5, whereas in 2020–2021, between 3.5 and 12.0. Over the land, this feature is less marked, since the stroke ratio is between 4.5 and 14.0 in 2010–2011, 3.5 and 12.0 in 2020–2021.

3.4. Seasonal Diurnal Cycle Distributions

Knowledge of the diurnal cycle variability in lightning distribution supports comprehension of severe weather development. Thus, the seasonal diurnal cycle distributions are obtained by evaluating the percentage of CG strokes per hour of the diurnal cycle for each season. The total number n_h of CG strokes (positive or negative that over the sea or the land) occurring between hour h and h + 1 is evaluated. Finally, the frequency of occurrence F% is evaluated for each h as follows:

$$F\%=100\ast {\displaystyle \frac{n_h}{{\sum }_{\mathrm{h}=0}^{23}{n}_h}}$$

(1)

Regardless of the polarity, in both Figure 6 and Figure 7, the lightning activity over the sea (panels A and C) appears quite constant throughout the diurnal cycle for all seasons. For what concerns both negative and positive CG strokes over the land, the highest concentration occurs between the late morning and the afternoon (10–18 UTC) (panels B and D) in each season, except for winter. Moreover, generally in spring and summer, the lightning activity peak measured during midday hours is more relevant than in other seasons. The reason is due to the excessive heating from sunlight on land during the warmest hours of the diurnal cycle that increases turbulent mixing of heat and moisture in the boundary layer supporting the convective initiation. During the warm season, strong daytime heating makes surface air parcels warmer and more buoyant, enhancing their rise. As these moist parcels ascend, latent heat release further accelerates the updrafts. Higher buoyancy allows more of the available Convective Available Potential Energy (CAPE) to convert into kinetic energy, producing stronger convection. Stronger updrafts promote charge separation in clouds, favoring electrified storms and lightning formation [106]. Land heats up much faster than the sea during the daytime because it has a lower heat capacity. As a result, air parcels over land become warmer and more buoyant than over the sea, producing stronger updrafts. These results are consistent with the findings of the study conducted in the Mediterranean region by [73].

3.5. Seasonal Distribution of the Point of Impact Elevation and Its Latitude Dependence

Several investigations have examined the link between lightning occurrence and terrain elevation, with the objective of assessing the influence of orographic uplift on the initiation of convection and the potential for lightning development. In many climatological analyses, lightning activity over the Italian peninsula is often generalized within the broader context of Southern Europe (e.g., [73]), without accounting for the distinctive characteristics of the Italian landscape, which includes diverse climatic regions. The presence of markedly steep topography (particularly in the northern sector, dominated by the Alps, and along the spine of the peninsula, shaped by the Apennines) renders broad-scale information on lightning frequency inadequate. Such generalized assessments fail to provide the level of detail required to support civil protection strategies or to guide industrial operations (including wind energy production and the management of electrical distribution networks) in the implementation of safety measures and operational procedures.

Within this context, the present analysis evaluates the spatial distributions of negative and positive cloud-to-ground (CG) stroke impact points occurring over land across three major subdivisions of the Italian territory. Specifically, the first subdivision, referred to as Northern Italy (N), extends from the Alps down to the latitude of 43.45°; the second, Central Italy (C), covers the belt between 41.20° and 43.45° latitude; while the third, Southern Italy (S), encompasses all regions situated at latitudes below 41.20°.

Figure 8 and Figure 9 show the cumulative frequency of occurrence [%] of the number of negative (N-left column) and positive (P-right column) CG strokes as a function of the orography elevation in the Northern (A, B), Central (C, D), and Southern (E, F) parts of Italy for each season. Moreover, a DEM of the Italian peninsula is shown in panel G, whereas the cumulative distributions of the orography elevation for the three sub-areas (N, C, S) are depicted in panel H.

From a general overview of the first six panels of both figures, it can be noticed that the range of elevation variability at which lightning occurs is different among the three zones. In Northern Italy, where mountains typically range between ~2000 and 3000 m, and the highest peaks are between ~4000 and 5000 m, a much higher seasonal variability of the lightning height of impact is evident with respect to South and Central Italy.

The main difference between the two periods regards the distribution of the elevation of winter CG strokes: a significant increase in the 50% and 90% percentiles is detected in 2020–2021 and is appreciable in all panels of Figure 9, except for panel B (positive events in North Italy) in which the behavior is similar to that of 2010–2011. Another interesting observation can be made by comparing the South Italy distributions in the two periods: a remarkably higher seasonal variability appears during 2020–2021. The observed differences in CG lightning elevation may reflect natural interannual variability in convective activity.

3.6. Monthly Variation in the Peak Current

Figure 10 represents the monthly behavior of the peak current mean value in 2010–2011 and 2020–2021.

It can be noticed that peak currents reached in 2020–2021 are quite similar to those of 2010–2011 in the case of negative strokes (panel A) and lower in the case of positive strokes (panel B). Nevertheless, the trend of the peak current is almost identical in the two periods. Indeed, the highest values are reached around February and March, i.e., between the end of winter and early spring, then a decrease until a minimum is reached in the middle of summer (July–August). Then the peak current mean value grows in the following months.

In both periods, the higher negative peak currents are always recorded over the sea. On the other hand, the positive ones are slightly different. In fact, in 2010–2011, values over the land are lower than those over the sea from January to June, and higher from July to December. In the biennium 2020–2021, the larger peak currents are always over the land.

A feature that needs to be highlighted is the inverse correlation of the peak current with the monthly GSD. It can be noticed that towards the end of spring and during the summer, the GSD tends to increase, whereas the peak current decreases, thus the highest current values are during periods of less lightning activity.

3.7. Distribution of Flash Multiplicity and of the Distance Between the Stroke Points of Impact Within a Flash

This subsection addresses the Probability Density Function (PDF) of flash multiplicity, defined as the number of strokes composing a single CG flash [76], as well as the PDF describing the separation between the ground contact point of subsequent strokes and that of the first stroke within the same flash, as derived exclusively from the lightning location system (LLS).

Naturally, both parameters are influenced by the clustering criteria adopted in the LLS algorithms, specifically the selection of the spatial radius and the temporal window used to associate individual strokes into a single flash [59]. In the case of the SIRF network, one or more strokes are grouped into a flash when they occur within a 10 km radius and within 1 s from the first event, with a maximum interstroke interval of 500 ms. Additionally, until 2016, a limit of 15 strokes per flash was imposed.

Figure 11 represents the distribution of flash multiplicity for negative (A) and positive (B) flashes in 2010–2011 and 2020–2021.

In 2010–2011, the mean negative flash multiplicity is 1.85, while the positive one is 1.06. Thus, the value of the mean positive flash multiplicity is significantly lower than the corresponding negative one; this observation is consistent with the established literature, which indicates that the flash multiplicity of positive flashes is typically slightly higher than 1 [107]. The obtained results are in agreement with other authors (e.g., [72]), finding a mean multiplicity for negative CG flashes of 2.1 for the EUCLID network. However, the reported mean negative flash multiplicity is lower with respect to values found in ground truth data [105,106,107,108].

In the two-year 2020–2021, the mean negative flash multiplicity is 1.85 and the positive flash multiplicity is 1.07. Hence, it can be noticed that no significant differences in flash multiplicity have been detected with respect to the 2010–2011 period, for both negative and positive events.

Figure 12 represents the PDF of the distance between the stroke points of impact within a negative (A) or positive (B) flash as calculated by LLS over 2010–2011 and the 2020–2021, respectively. Analyzing the case of subsequent negative strokes, it can be observed that the trend is quite similar in both periods, but those of 2020–2021 are more concentrated around the first stroke impact point than those of 2010–2011. On the other hand, the subsequent positive strokes show different trends in the two periods. In 2020–2021, they are mainly concentrated around the first stroke impact point (even though with lower extent with respect to negative strokes), whereas in 2010–2011, the distribution of their distance from the corresponding first stroke is more uniform. This effect could be due to a different approach in the grouping algorithm set by METEROAGE.

3.8. Distribution of the Peak Current for Positive First Strokes, Negative First Strokes, and Negative Subsequent Strokes

Understanding the distribution of lightning peak currents is essential for assessing the lightning performance of transmission and distribution lines, namely the expected yearly number of flashes that generate overvoltages exceeding a prescribed limit [80]. Classical reference values originate from the pioneering measurements conducted by Karl Berger and collaborators [109,110,111,112] at the summit of Monte San Salvatore in Lugano, Switzerland. This site is located at an altitude of 915 m a.s.l., rising approximately 640 m above Lake Lugano. Following measurements performed in various geographic regions [113,114,115,116], together with triggered-lightning experiments [117], demonstrated substantial variability in peak current distributions, a variability largely attributable to the differing characteristics of the measurement environments. These observations highlight the necessity of acquiring reliable region-specific datasets.

The present analysis therefore examines the distributions of peak current separately for positive first strokes, negative first strokes, and negative subsequent strokes. It must be emphasized, however, that the values under consideration are inferred rather than directly measured. In typical LLSs, the peak current is estimated from the maximum amplitude of the electric field recorded by the sensors, after applying corrections for propagation attenuation and assuming the Transmission Line model for current propagation along the return-stroke channel [29,118], together with a prescribed return-stroke velocity.

A number of studies have investigated the accuracy of this inference method [119,120,121,122,123], providing reasonable estimates of the associated uncertainties. In this subsection, the results obtained from the present analysis are compared both with other outputs derived from LLS data and with direct current measurements available in the literature.

Figure 13 reports the Probability Density Function (PDF) of peak current for negative first strokes (A), negative subsequent strokes (B), and positive first strokes (C), and the Cumulative Distribution Function (CDF) of peak current for negative first strokes (D), negative subsequent strokes (E), and positive first strokes (F) over 2010–2011 and 2020–2021. The three lines appearing in the CDF plots indicate the values of current corresponding to the 5%, 50%, and 95% percentiles of the distribution, respectively.

In the literature, the most widespread and acknowledged reference for lightning current data consists of the direct tower measurement campaign on Monte San Salvatore (Switzerland) [109,110,111,112]. From such measurements, the median peak current values for negative first strokes, negative subsequent strokes, and positive strokes are 30 kA, 12 kA, and 35 kA, respectively. Therefore, from

Table 2. Peak current [kA] percentiles (5%, 50%, and 95%) in Italy over the 2010–2011 period.

Strokes	5th Percentile	50th Percentile	90th Percentile
Negative first	8.4	18.1	63.2
Negative subsequent	7.3	17.4	38.8
Positive first	7.3	24.1	111.7

and

Table 3. Peak current [kA] percentiles (5%, 50%, and 95%) in Italy over the 2020–2021 period.

Strokes	5th Percentile	50th Percentile	90th Percentile
Negative first	3.0	10.7	41.4
Negative subsequent	5.2	13.5	39.7
Positive first	5.4	15.9	89.4

, one can conclude that in both periods, the median values for negative and positive first strokes are lower with respect to the measurements obtained by Berger and his co-workers, even though the median current values in 2010–2011 are much closer to the ground truth data than those of 2020–2021. On the other hand, in both periods, the median value of negative subsequent stroke peak current is higher than that of Monte San Salvatore. It is worth noting that in both periods, the distributions of negative first and subsequent strokes are quite similar, and this is clearly different from what Berger recorded.

According to [59], the EUCLID network estimates a median current of approximately 10 kA for negative first strokes in Austria. As extensively discussed in previous studies [124,125], measurements obtained from towers are subject to a systematic bias: they preferentially register discharges characterized by higher peak currents and tend to record predominantly upward lightning events. The authors of [59] provided a comprehensive examination of the underlying causes for the discrepancies observed between current values inferred by tower-based measurements and those derived from LLS observations.

4. Correlation of Lightning Occurrence with Land and Sea Surface Temperatures

Lightning activity has been increasingly investigated as a potential marker of climate and global change, given its sensitivity to atmospheric thermodynamics and composition [126,127,128,129,130]. Warmer temperatures enhance the availability of CAPE, leading to more frequent and intense thunderstorms, which in turn can increase lightning occurrence. Therefore, in this contribution, a correlation analysis between lightning occurrence and land and sea surface temperatures is proposed. Correlation is calculated by means of the Spearman rank correlation coefficient [131], which is appropriate when the relationship between two variables is not necessarily linear but is monotonic, meaning one variable consistently increases or decreases as the other does, but not necessarily at a constant rate. Spearman’s rank correlation coefficient ($\rho$) between two variables $x$ and $y$ is calculated using the following formula:

$$\rho (x,y)={\displaystyle \frac{{\sum }_{k=1}^n(x_k-\overline{x})(y_k-\overline{y})}{\sqrt{{\sum }_{k=1}^n{\left(x_k-\overline{x}\right)}^2} \sqrt{{\sum }_{k=1}^n{\left(y_k-\overline{y}\right)}^2}}}$$

(2)

where $x_k$ and $y_k$ are the ranks of the observations, $\overline{x}$ and $\overline{y}$ are their mean values, and $n$ is the number of data points. This coefficient measures the strength and direction of the monotonic relationship between two variables. The value of $\rho$ ranges from $-1$ to $1$, where $\rho =1$ indicates a perfect positive monotonic relationship, $\rho =-1$ indicates a perfect negative monotonic relationship, and $\rho =0$ indicates no monotonic relationship.

The temperature data used in this study include surface temperatures over land and sea with a spatial resolution of 0.05° and a temporal resolution of 1 h. Land surface temperature (LST) was obtained from the MLST-AS dataset, which merges the MLST product—based on clear-sky infrared observations from the SEVIRI sensor aboard the Meteosat Second Generation (MSG) satellites—with LST estimates under cloud cover derived from an Energy Balance Model. The MSG series, operated by EUMETSAT, consists of geostationary satellites designed for continuous monitoring of atmospheric and surface conditions, providing high-frequency observations critical for weather forecasting and climate studies. Sea surface temperature (SST) data were provided by the Ocean and Sea Ice Satellite Application Facility (OSI SAF) of EUMETSAT, which develops and distributes operational and climatological datasets related to key ocean–atmosphere interface parameters, including sea surface temperature (SST).

The dependence of the lightning–temperature correlation on timescale, spatial aggregation, and data resolution (both in time and in space) is assessed on both the 2010–2011 biennium and the 2020–2021 biennium.

The Spearman correlation coefficient between CG lightning occurrence and LST/SST is calculated as follows. Hourly temperatures are aggregated into daily average values. Considering the spatial resolution of temperature data, the daily number of CG strokes for each cell of the considered domain (Figure 1) is calculated and labeled as $N_{ij}$. The length of $N_{ij}$ is $730$ ($731$), i.e., the number of days in the 2010–2011 (2020–2021) biennium. $N_{ij}$ is correlated with ${\tilde{T}}_{ij}$, which is a temperature variable taking into account cumulated effects and different scales both in time and space. ${\tilde{T}}_{ij}$ is reference value for the $ij$-cell calculated from the original LST/SST data samples $T$ as a function of the spatial window extension $\Delta s(\in \mathbb{N})$ and the time delay $\Delta t(\in \mathbb{N})$ as

$${\tilde{T}}_{ij}^t\left(\Delta s,\Delta t\right)={\displaystyle \frac{1}{{4\left(1+\Delta s\right)}^2 (1+\Delta t)}}\sum _{l=0}^{\Delta t}\sum _{m=i-\Delta s}^{i+1+\Delta s}\sum _{n=j-\Delta s}^{j+1+\Delta s}{T}_{mn}^{t-l}$$

(3)

Results are reported in Figure 14, Figure 15, Figure 16, Figure 17, Figure 18 and Figure 19 in terms of heatmaps of the Spearman correlation coefficient $\rho$. Figure 14 and Figure 15 study the dependence of $\rho$ on the timescale for the 2010–2011 and the 2020–2021 biennia, respectively. A 0.1° grid resolution is considered and $\Delta s=0$ is assumed, thus, for each time instant $t$ and for each $ij$-cell, only $4 (1+\Delta t)$ temperatures are used to calculate ${\tilde{T}}_{ij}$, i.e., samples between time instants $t-\Delta t$ and $t$ taken around the $ij$-cell:

$${\tilde{T}}_{ij}^t\left(\Delta s=0,\Delta t\right)={\displaystyle \frac{1}{4 (1+\Delta t)}}\sum _{l=0}^{\Delta t}\left(T_{i,j}^{t-l}+T_{i,j+1}^{t-l}+T_{i+1,j}^{t-l}{+T}_{i+1,j+1}^{t-l}\right)$$

(4)

Eight different time delays are assessed, from $\Delta t=1$ day to $\Delta t=180$ days.

In both biennia a modest correlation can be observed (up to 0.4) at short timescales on the land (especially in North Italy, i.e., alpine and subalpine regions), with a decreasing trend (down to $-0.1$) at longer timescales. The opposite trend, but with a reduced variability range, can be observed for the correlation on the sea cells and coastal areas, with the highest values reached on the Sicilian Sea and the lower Tyrrhenian Sea. No significant variations can be appreciated from $\Delta t=1$ day to $\Delta t=30$ days.

Figure 16 (2010–2011) and Figure 17 (2020–2021) show the dependence of the correlation on the spatial window extension, i.e., considering temperature values aggregated at different distances. In particular, $\Delta s=0$ cells, $\Delta s=2$ cells, and $\Delta s=4$ cells are considered, leading to spatial window extensions of 0.1° (i.e., the grid resolution), 0.3° and 0.5°, respectively. In all cases, $\Delta t=1$ day is assumed. However, no remarkable variations can be observed with different $\Delta s$ values.

Figure 18 and Figure 19 report the dependence of the correlation on the grid resolution for the two biennia. $\Delta t=1$ day and $\Delta s=0$ cells are assumed. Slight changes in correlations can be noticed, with an increase in high values over the land and a decrease in values over the sea when larger grid sizes are considered.

As far as the variability between the 2010–2011 biennium and the 2020–2021 biennium is concerned, no significant variation in the CG lightning–temperature correlation is observed.

The same analysis carried out on daily data is also performed with monthly aggregated data. Figures are not reported in this contribution, but results are similar to daily data from a qualitative point of view. However, higher values of the correlation coefficient are reached when monthly data are considered (up to 1 in some cells in the North Italy).

Comparisons between 2010–2011 and 2020–2021 daily average profiles (with a 3-day moving average filter) are shown in Figure 20 for SST and LST. Figure 21. reports the monthly average surface temperature over the sea and over the land for both periods. From 2010–2011 to 2020–2021, a slight temperature increase during summer and autumn and a slight temperature decrease during spring can be observed, which is consistent with the trend of CG lightning occurrence (Table 1) and the calculated correlation.

5. Conclusions

This contribution has attempted to investigate the variation in cloud-to-ground (CG) lightning activity in Italy between the 2010–2011 period and the 2020–2021 period as a function of different geographical and/or temporal parameters. Lightning data have been acquired from the SIRF network. The area of interest is Italy and the surrounding sea. To sum up, the analysis has shown the following results:

• A significant seasonal variability in lightning activity is highlighted in both periods and between them. In general, the highest number of total strokes is recorded in summer and in autumn, while the lowest ones are in winter and in spring. A remarkable increase in the lightning activity in Italy has occurred in 2020–2021 with respect to 2010–2011 (+24%, +83%, and +29% for negative, positive, and total strokes, respectively). Summer and winter total strokes are comparable, but strong differences appear in spring (−47%) and autumn (+58%).
• The monthly mean density has a similar trend in both 2010–2011 and 2020–2021 periods. Positive events are much less than negative ones. CG stroke density in 2010–2011 reaches greater values over the land in summer, whereas in 2020–2021 the highest densities are over the sea during autumn. Regardless of the polarity, CG lightning activity is more relevant over the sea than land from October to January in 2010–2011 and for September to January in 2020–2021.
• The monthly negative/positive CG stroke ratio reaches lower values in 2020–2021 than in 2010–2011. In 2020–2021, the ratio between negative CG and positive CG strokes is almost always higher over the land than over the sea, whereas for 2010–2011, the opposite holds true.
• In each season the lightning activity is almost constant along the day over the sea, regardless of the polarity. For what concerns both negative and positive CG strokes over the land, the highest concentration occurs between the late morning and the afternoon (10-18 UTC) in each season, except in winter.
• The range of elevation variability at which lightning occurs is different among the three zones in which the Italian territory has been divided. The main difference between the two periods regards the distribution of the elevation of winter CG strokes: a significant increase in the 50% and 90% percentiles is detected in 2020–2021, except for positive events in North Italy in which the behavior is like that of 2010–2011. By comparing the South Italy distributions in the two periods, a remarkably higher seasonal variability appears during 2020–2021.
• Monthly mean positive peak currents recorded in 2020–2021 are lower to those of 2010–2011. For monthly mean negative peak current, no significant variability has been observed between the two biennia. In both periods, the higher negative peak currents are always recorded over the sea, whereas the positive values over the land are higher than those over the sea from July to December in 2010–2011 and always higher in 2020–2021. The trend is similar in the two periods and inverse with respect to the Ground Stroke Density.
• Both in the 2010–2011 period and the 2020–2021 period, the value of the mean positive flash multiplicity is lower than the corresponding negative one. Values in the two periods are comparable.
• As regards the distribution of the distance between the stroke points of impact within a flash, negative subsequent strokes are more concentrated around the first stroke impact point in 2020–2021 than in 2010–2011. On the other hand, positive flashes in 2010–2011 contain strokes with more uniform distribution than in 2020–2021, where more than circa 25% of subsequent strokes impact within 1 km from the corresponding first stroke.
• In both periods, the peak current median values for negative and positive first strokes are lower with respect to the measurements obtained by Berger and his co-workers, even though the median current values in 2010–2011 are much closer to the ground truth data than those of 2020–2021.

Finally, a correlation analysis between CG lightning occurrence and land/sea surface temperature (EUMETSAT) has been performed. For daily data, a modest correlation has been observed on the land at short timescales (up to 30 days) for both biennia; on the other hand, the highest correlation on the sea was reached at larger timescales (more than 30 days) for both biennia. For monthly data, the same trends have been observed, but with higher values of the correlation coefficient (up to 1) in several cells of the considered area. This is in accordance with previous literature, suggesting that surface temperature increase may lead to higher lightning occurrence. Indeed, daily average and monthly average temperature profiles are consistent with the observed trend of CG stroke occurrence between the 2010–2011 and 2020–2021 periods and the computed correlation.

It should be noted that the analysis presented in this study is based on two biennia of data, selected according to data availability. While this timescale allows for a preliminary exploration of the relationship between CG lightning activity and sea/land surface temperature in Italy and the surrounding seas, it does not capture long-term variability. Robust assessments of lightning–climate interactions typically require datasets covering at least a decade. Therefore, the results discussed here should be interpreted with this limitation in mind, and future work will benefit from extending the analysis to longer time series.