A Climatology of Mesoscale Convective Systems in Northwest Mexico during the North American Monsoon

: Mesoscale Convective Systems (MCS) may vary greatly with respect to their morphology, propagation mechanism, intensity, and under which synoptic-scale conditions as a function of topographic complexity. In this study, we develop a long-term climatology of MCS during the North American Monsoon focusing on MCS morphology, lifecycle, and intensity as well as possible propagation mechanisms. We employ an MCS tracking and classiﬁcation technique based on 23 years (1995 to 2017) of GOES IR satellite data. MCS intensity is also gauged with 7 years (2011 to 2017) of Vaisala GLD360 lightning data and, ﬁnally, monthly and interannual variability in synoptic conditions are examined with ERA5 reanalysis data. Our results based on 1594 identiﬁed MCS reveal that 98% are morphologically classiﬁed as Persistent Elongated Convective Systems. During the 23 summers (June through September) observed, the number of MCS varied considerably, averaging 70 MCS with minimum of 41 and maximum of 94. MCS typically have an average duration of around 8 h ± with a 2 h standard deviation. Propagation speeds, estimated with Hovmöller diagrams in addition to MCS centroid initial and ﬁnal position, vary slightly depending on the trajectory. A notable result suggests that MCS propagation speeds are more consistent density currents or cold pools and not gravity waves nor steering-level winds. The results of this study could also provide a dataset for examining larger-scale controls on MCS frequency in addition to assesing convective parameterization and convective-resolving models in regions of complex topography. SMO would be needed to verify this mechanism. The present study provided a detailed climatological analysis of the temporal and spatial distribution and electrical activity of the MCS that they occur in a region of complex orography. This study is a basis for future research that seeks to evaluate the effect of climate change on MCS, the performance of numerical models.


Introduction
Understanding the organization, propagation mechanisms, and intensity of Mesoscale Convective Systems (MCS), as well as their representation in numerical models have been a fundamental challenge in the atmospheric sciences for decades. Definitionally, MCS are organized cumulonimbus clouds in a single cohesive entity with precipitation occurring on spatial scales of at least 100 km in a given direction and a lifecycle of several hours to one day [1,2]. Although MCS vary greatly morphologically, the typical morphological structure captured with radar data consists of a deep convective region of intense, but relatively brief precipitation, and a stratiform region with lighter precipitation of greater duration [3][4][5][6]. Intense MCS are associated with severe weather phenomena such as frequent lightning, hail, flash floods, strong wind gusts, and even tornadoes [7][8][9]. MCS occur across the globe in the mid-latitudes, subtropics, and tropics though the dynamical forcing mechanisms or thermodynamic conditions responsible for their formation may differ greatly [10,11]. Given this large geographical range and frequency of occurrence, MCS also play a fundamental role within the climate system vertically redistributing heat, water vapor, and momentum [12][13][14][15][16]. The formation of MCS typically requires sufficient inverted troughs (IVs), favor the initiation and propagation of MCS argued to result from increased upper-level divergence and associated destabilization [77], or, from the intensification of vertical wind shear [53,54,78]. Lang et al. [56] found that MCS not only progress towards the GoC (their Regime A), but also travel parallel to the GoC coastal zone (their Regime B) and there are even occasions when they propagate both along-coast and crosscoast (their Regime AB). MCS propagation speeds of ∼7 m/s, ∼10 m/s and ∼3-5 m/s are found in regimes A, B, and AB, respectively. Lang et al. [56] argue that the mechanism that best explains these propagation speeds is the occurrence of weak and shallow cold pools, not gravity waves as argued, for example, by Mapes et al. [28] for the Panama Bight region. Rowe et al. [61] also argue for the cold pool propagation mechanism employing polarimetric radar data during NAME. Both Lang et al. [56] and Rowe et al. [61] suggest that the melting of large ice hydrometeors strengthens cold pool formation, which then propagates away from the leading convective line and initiates new convection.
To this day, open questions still remain as to the nature of MCS in different topographic as well as climatic zones, with respect to their formation, morphology, propagation mechanism, duration, intensity, and under which synoptic-scale conditions they occur. In this study, we employ a unique combination of observations and reanalysis data to track the temporal and spatial evolution of MCS that develop during the NAM. We intend this study as a proof-of-concept demonstrating the utility of our tracking technique for identifying and classifying MCS and their propagation. We develop a long-term (23 years) climatology of MCS to gain insights into dominant NAM MCS morphology, lifecycle, and intensity as well as likely propagation mechanisms in this region over great topographic complexity. To this end, we employ an MCS tracking and classification technique based on GOES IR satellite data. We employ an unique measure of MCS intensity based on Vaisala GLD360 lightning data and associated synoptic-scale conditions are deduced from ERA5 reanalysis data. Long-term MCS climatologies in the NAM region are few and far between. One recent study, Farfán et al. [70] analyzed the precipitation and diurnal cycle characteristics of MCS from 2009 to 2018, as well as a detailed case study, in the southern portions of the NAM region. For this study region, we focus on the region northward from that of Farfán et al. [70].
The specific objectives of this study can be ennumerated as follows: (1) classifying MCS with respect to their morphology, (2) identifying MCS propagation speeds, paths and duration, (3) assessing possible MCS propagation mechanisms, and (4) evaluating MCS intensity. These objectives are carried out through the creation of a basic MCS climatology, analyzing both monthly and interannual variability, which also takes into account regional variation as of function of tropography as well as synoptic-scale conditions. Developing this MCS climatology is strongly motivated by the need to ascertain and overcome deficiencies in global, operational, and high-resolution models with respect to deep convection. Longterm observations and easily reproducible metrics are necessary and this is particularly true for replicating the MCS lifecycle over the SMO [66,79,80]. In what follows, Section 2 describes our study region, the GOES IR, Vaisala GLD360 lightning and ERA5 data employed as well as detail the methodological approach for identifying and tracking MCS evolution. Section 3 presents the analysis of the characteristics of MCS (Temporal and spatial distribution, trajectories, velocities, and electrical activity). Finally, we discuss and summarize our results in Section 4 and note some of the implications for future studies in Section 5.

Study Area
Northwestern Mexico (see Figure 1), provides an interesting natural laboratory to analyze the interactions between topographic features, environmental conditions, the formation and propagation of MCS as well as typical day-to-day convective activity during the NAM. In terms of frequency, most deep convection occurs over the SMO which extends from the Mexican state of Nayarit to the border of Arizona with an average elevation well above 2000 m. In the southern portion of the NAM region, the SMO closely parallels the Eastern Pacific and GoC coasts resulting in a strong sea-breeze circulation and associated low-level moisture transport inland towards the SMO [51,[81][82][83]. Northward from Sinaloa, the SMO trends inland and the sea-breeze strength as well as the frequency of deep convective precipitation tend to decrease [81,82,84]. The topographic transition on the eastern slopes of the SMO, unlike the western slopes, is much gentler descending towards the arid Mexican Altiplano of north-central Mexico. Though elevated (∼1500 m), deep convective activity is much less frequent over the northern portion of the Altiplano during the NAM. The SMO western slopes steeply descend, transitioning into a complex basin and range topography, particularly in the northern portion of the study region (e.g., Sonora and Arizona). Approaching the GoC, broad coastal plains with much lower relief dominate. On the opposite coast of the GoC, deep convective activity over the Baja California peninsula tends to diminish presumably due to more frequent incursions of stable, drier air above the Pacific Ocean. The near-complete absence of deep convective activity along the Pacific coast of the Baja Peninsula is reflective of the cooler ocean waters associated with the California Current (see, for example, Figure 5 in Holle and Murphy [85]).

Data
To begin with, all MCS studies require an MCS definition for identification and classification purposes. This identification process also necessitates proposing a methodology, which must be robust and replicable. In this section, we elaborate on the various data employed in this study for MCS identification and the methodology utilized for tracking their spatial-temporal evolution.

Satellite Images
A large portion of MCS research is based upon satellite imagery, principally, in the thermal infrared bands. These satellite infrared radiance data can be converted into Brightness Temperature (BT), a variable that is closely tied to the evolution of deep convective activity [41,[86][87][88][89]. Given that there is often a large contrast between cold cloud tops and the surrounding cloud-free environment, infrared imagery is effective in identifying and monitoring MCS growth and propagation [90][91][92]. Here, we utilize a total of 23 years of GOES IR satellite imagery, specifically the IR band at 10.7 µm for June through September from GOES 8 (1995GOES 8 ( -2002, GOES 12 (2003GOES 12 ( -2012, and GOES 13 (2013GOES 13 ( -2017. GOES IR imagery data have a spatial and temporal resolution of 4 km and typically 15 min, respectively. These GOES Satellite retrievals and information on satellite platforms can be found at https://www.ssec.wisc.edu/datacenter/ (accessed on 14 April 2022).

Lightning
Many studies have demonstrated the utility of long-range terrestrial lightning location systems (LLS) data which employ different sensors operating at Very Low/Low Frequencies (VLFs/LFs) up to Very High Frequencies (VHFs) to provide near real-time lightning data globally [93,94]. Lightning data are particularly useful for identifying deep convective activity being continuous in time and space and, unlike radars, do not suffer from blockage issues in complex topography [85,89,95,96]. Moreover, given the strike location accuracy currently available, lightning data have proven useful in differentiating the convective and stratiform regions of MCS [97][98][99][100]. In this study, we utilize Vaisala's Global Lightning Detection Network (GLD360) data which provides: location, time of lightning flash, polarity, and peak current estimates. Several studies have evaluated GLD360 performance and shown cloud-to-ground flash detection efficiency of around 60-70% and the median location accuracy at 2-5 km in North America [101]. A more thorough description of the network and data products are found in [102,103]. GLD360 data were employed in previous NAM studies to gauge the spatial and temporal distribution of convective activity Holle and Murphy [85], and to characterize the intensity/evolution of convective diurnal cycle Serra et al. [35]. For this study, we use GLD360 data from 2011 to 2017 as a means for classifying the development and decay of MCS.

ERA5 Reanalysis Data
Studies have shown that reanalysis data are sufficiently accurate in subtropical and tropical regions for gauging propitious synoptic-scale atmospheric conditions for the formation of MCS [70] as well as at higher latitudes [104,105]. ERA5 has a spatial resolution of 0.25°degrees, a vertical resolution of 37 pressure levels, and a temporal resolution of 1 h [106]. Given this high resolution, ERA5 are used to determine synoptic conditions for examining interannual variability of MCS as well as their relationship to propagation characteristics. Specifically, we employ geopotential height, specific humidity, and u and v wind components at 700, 500, and 200 hPa. For specific details on the creation and accuracy of ERA5, see https://confluence.ecmwf.int/display/CKB/ERA5 (accessed on 14 April 2022). Our region of analysis for GOES and GLD360 data is that of Area 1 limited to 24 • -33 • N and 104 • -115 • W (see Figure 1) which roughly corresponds to the NAME Tier 1 area [64], however, not extending as far south. Area 2 corresponds to the synoptic-scale analysis utilizing ERA5 data, consistent with the studies of [66,80], which examine NAM area convective activity in a nested modeling context.

GOES IR Classification of MCS
One of the pioneering works in the MCS classification employing geostationary infrared satellite images is the study of Maddox [44]. He defined a circular shaped MCS as an MCC according to certain characteristics in its shape, area, and duration (see Table 1 in [44]) for MCS in the central United States. Further studies from various regions around the globe have also found these circular systems to be common [107,108]. Augustine and Howard [109] proposed that the BT threshold of 221 K adequately represented the full development of an MCC; a criterion that has also been utilized in other studies [40,[110][111][112]. Anderson and Arritt [45] define another type of MCS, which meets the size and duration criteria put forward by Maddox [44], but not with the same form, which they denominate PECS, as described above. However, Jirak et al. [40] found that these criteria and thresholds can occur on even smaller scales which they define as Meso-β Circular Convective System (MβCCS) and the Meso-β Elongated Convective System (MβECs) (see Table 1 in Jirak et al. [40]).
These morphological definitions are for the most part derived from relatively flat, mid-latitude regions; for example, the Great Plains in the central United States. There is, in fact, no universal BT criterion nor areal extent for defining an MCS, though, these criteria are not entirely arbitrary. BT criterion values have varied from 208 to 245 K, while the minimum threshold for the area has ranged from 1000 to 100,000 km 2 [59,86,88,[113][114][115][116][117]. Taking this variation in criteria into account, in this study, a histogram of BT values was created ( Figure 2) considering pixels falling into the range of BT values (208-245 K) for the 23 summers of the study. From this histogram, the mean temperature 220 K is taken as an appropriate value for the NAM region. Furthermore, 220 K is similar to values utilized in other shorter-term studies of MCS, such as Valdés-Manzanilla and Barradas Miranda [62] and Mejia et al. [63]. Here, a minimum value of area corresponding to 5000 km 2 was imposed, a value frequently used in MCS studies in tropical and subtropical regions [88,92,113,117,118]. In terms of MCS temporal evolution, the initiation time is defined as when a system meets the following criteria: area (≥5000 km 2 ) and BT (≤220 K). MCS dissipation is designated as the point in the temporal evolution when these criteria are no longer met. Similar to Farfán and Zehnder [59], we only analyze MCS that have a duration of minimally 6 h, hence focusing are longer-lived events. Similar MCS lifetimes have also been utilized in tropical and mid-latitude regions [44]. With these above criteria, 1594 MCS were identified in Northwest Mexico from 1995 to 2017 during the monsoon season from June through September. Once identified, MCS were then classified in terms of cirrus shield excentricity. An MCS is considered circular and elongated when its eccentricity ( ) is greater than or less than 0.7, respectively ( Figure 3). As in previous studies, we classify these MCS, as MCC ( > 0.7) and PECSs ( < 0.7) [40,41,45,119].

MCS Detection Algorithm
MCS identification and monitoring still remain a challenge given that cloud growth and cirrus shield areal expansion can vary relatively quickly. Further complicating their identification, they can split resulting in two or more MCS, or join together with other MCS [86,88]. After identification based on the above-mentioned criteria, the trajectory of each MCS is determined by following its cirrus shield for successive satellite images [113,120,121]. Two methodologies that have proven useful for determining MCS trajectories are the area overlap method (AOL) [113] and the method of maximum spatial correlation [121]. The AOL method is based on the consideration that an MCS, in successive frames, represents the same system if their pixels overlap from the current to the following timestep, for at least 15 to 50% of the pixels or 500 to 5000 km 2 of pixel area [86,113,122,123]. This method has been applied to various regions of the world, for the Amazon region [116], in the La Plata basin [124], in the Sahel [86]. More recently, Huang et al. [88] developed an algorithm based on AOL for tracking MCS in tropical and subtropical regions on a global scale. The maximum spatial correlation method takes into account the relationship between the MCS cloud shield radius and the BT threshold which have a correlation threshold of 0.3 for systems in successive images, thereby representing the same MCS. As such, MCS in relatively close proximity with little change in the horizontal area between consecutive images are considered to be the same system. This technique has been used to track MCS in South America [121], Spain [125], southern Africa [112] and recently in China [41]. In the present study, the AOL methodology was chosen because it offers better tracking and greater certainty compared to maximum spatial correlation, since AOL is not affected by the distance the MCS travels in consecutive images compared to maximum spatial correlation. In the latter method, the calculation of the Euclidean distance is made either from the MCS's center of gravity or from the center of the ellipse and is affected by merging and splitting processes [124]. We speculate that for the NAM region with its complex terrain, processes of merging and splitting should occur with greater frequency during the MCS life cycle. In agreement with previous studies, we employ an overlap of 25% [92,113,116,122,124,126]. The following criteria are utilized in this study: (1) MCS which during their life cycle neither merge nor split, (2) MCS that during their life cycle merge with other systems resulting in an areal extent of at least 5000 km 2 , (3) MCS which during their life cycle split into two or more systems of at least 5000 km 2 ; the system with the greater area is tracked. Finally, MCS that result from the union of different systems remain smaller than 5000 km 2 are excluded in order to analyze MCS with a more clearly defined life cycle [127].

MCS Trajectory Analysis
Given the large number of MCS occurrence, we simplify NAM MCS trajectory analysis, by creating three, 3-degree latitudinal bands. Figure 4 contains the initiation location for MCS for these three different latitudinal bands utilized: 24 • -27 • N, 27 • -30 • N and 30 • -33 • N called Band A, B and C, respectively. Within each one of these bands and for those MCS propagating parallel to the SMO (e.g., crossing latitudinal bands), propagation velocity is estimated by way of Hovmöller diagrams in addition to simply calculating the velocity based on the initial and final position of the MCS centroid. For the purpose of analyzing MCS trajectory at the more extreme ends of interannual variability, we create composites of synoptic conditions for the 2 most active and the 2 least active years in terms of MCS occurrence. Selecting these extreme years provides a measure of the bounds that we may expect on MCS behavior. Likewise, with respect to monthly variability during the evolution of the monsoon, initial and final point of MCS trajectory are plotted for a visual representation of typical paths for each month, June through September.

Spatial Distribution
During the 23 summers from 1995 to 2017, 1594 MCS were identified in northwestern Mexico. In Figure 4, the spatial distribution of MCS initialization is plotted. Not unexpectedly, the number of MCS events is largest along the southern coastal plains of Sinaloa and along the western slopes of the SMO. The number of MCS tends to decrease northward into the state of Sonora. Likewise, MCS tend to be much less frequent on the eastern slopes of the SMO and the Mexican Altiplano. Within Band A, nocturnal MCS are frequent, particularly along the western slopes of the SMO [56,70,85]. In band B, the majority of the MCS initiate near the crest of the SMO. Within B and C, perhaps not surprisingly given results from previous studies, there are relatively fewer MCS with very dispersed points of initiation. The convective development in the Bands A and B are probably most closely tied to low-level, upslope flow from the GoC [52] and resulting abundance of water vapor [56,68,69], although dynamical mechanisms such as increased shear have also been argued to be critical for MCS formation and propagation. In band C, the influence of the position of the subtropical anticyclone, migrating southward, fewer incursions of IVs, as well as intrusions of drier air from the northwest, result in diminished occurrence of MCS and convective activity, in general [78,85,128].
With respect to MCS morphology, the vast majority of the MCS, approximately 98%, belong to the PECS category while only approximately 2%, were characterized as MCC. Therefore, in this region characterized by its complex orography, PECS which also typically initiate of the SMO entirely dominate the morphology classification. This PECS domination associated with the complex terrain and with the orographic uplift is similar to what occurs in the mountain ranges of central Europe (e.g., the Pyrenees and the Alps) [129,130] and the Himalayas [41]. These results are also consistent with those of Jirak et al. [40], who found that in the relatively flat topography of the central Plains MCC and PECS have similar frequency, supporting the argument that complex topography strongly impacts MCS morphology. In addition to their minuscule frequency of occurrence, MCC are quite scattered in terms of their location of origin, including the northern region of the NAM near the United States border (e.g., Sonora-Arizona, Chihuahua-Texas) and both east and west of the SMO.

Interannual and Monthly Variability
Although the NAM occurs every summer, it experiences interannual and inter-seasonal variability in terms of the frequency of convective activity [48,[131][132][133]. During the 23 summers observed, the number of MCS varied considerably, with an average of 70 systems per summer and ranging in number from 41 to 94 MCS. In Figure 5, the interannual as well as monthly variability is presented in the form of a heat map. With ERA5 geopotential, specific humidity, and winds at 500 hPa, in order to frame the boundaries on MCS occurrence, composites were made for the 2 most active years (94 events in 2000 and 91 in 2013) and the two least active years (41 events in 1995 and 53 events in 2009). We found that for the two most active years, the subtropical high was displaced relatively farther north and more intense compared to the least active 2 years. This northward migration and intensification of the monsoon ridge may allow for penetration of lower-level moisture into the southwestern U.S. with attendant decreases in atmospheric stability as well as the passage of transient disturbances which increase vertical wind shear profiles, such as IVs [57,71,134,135]. In the case of IVs Douglas and Englehart [136] found that IVs are the most common transient synoptic factor though the actual mechanism for intensification and occurrence of MCS due to IVs has been debated [54,77]. As with other monsoonal regimes such as Australia [137], Africa [138], and Asia [139], NAM variability in synoptic flow pattern is large and is fundamental to the outbreak or suppression of deep convective activity. Widespread convective activity associated with burst and break periods typically lasts on the timescale of weeks [48,74,140,141]. Intense convective activity and associated MCS occur during burst periods and typically depend on synoptic or subsynoptic disturbances with timescales of several days to a week [78,135]. Figure 6 contains the spatial distribution of the locations of MCS initialization from June to September. The month-to-month variations that can be observed are an increase in the number of organized systems and the geographical region where MCS tend to occur with greater frequency. In June (Figure 6a), there is a very active zone of MCS initialization along the SMO corridor. There are also MCS that initiate far removed from the SMO corridor, for example, along the Baja California peninsula as well as over the Mexican Altiplano, though much less frequently. During the months of July and August, where conditions are hot and humid over a much larger region (Figure 6b,c, respectively), the NAM circulation is well established and there is a notable increase in MCS occurrence along the SMO and along the coastal region of Sinaloa. Approaching the end of the NAM (September, Figure 6d), there is a strong decrease in MCS initiation along with the SMO corridor, though the coastal region of Sinaloa remains relatively active. Regarding monthly variability, as expected, the most active months are July and August where conditions are generally more humid and less frequent intrusions of drier westerly winds compared with June and September [47,48,142]. However, in this longer climatological study, we found that for several years (1999,2000,2001,2015,2016), June was essentially as active as the more typical peak monsoon months of July and August. Likewise, for the years 1997, 2010, 2013, and 2014, September was quite active in terms of MCS occurrence. As mentioned above this variability in MCS has been tied to the occurrence of IVs. In a future study, we will examine possible synoptic conditions that are associated hiked occurrence of MCS in normally more quiescent months. Figure 7 shows the diurnal cycle for two important stages in the life cycle of MCS: initiation and dissipation. While it is true that MCS can commence, grow and dissipate at any time of day, it is important to verify if these stages are strickly linked to diurnal variation of solar radiation as has been noted in other regions of the world [40,41,111,112]. The northerly directed MCS, (Figure 7 middle panel) have a narrower time range of initiation (13:00-20:00 Local Time (LT) (UTC-6)) compared with the other trajectories (14:00-02:00 LT), which indicates that favorable atmospheric conditions for these northerly directed MCS initiation are more constrained. However, independent of trajectory, MCS occur predominantly between 14:00 to 21:00 LT, the time which coincides with intense precipitation events mainly along the western slopes of the SMO [67,69]. This temporal range also coincides with that reported by Valdés-Manzanilla and Barradas Miranda [62], who found that in the summer of 2004, 77% of MCS usually start between 15:00-21:00 LT. In our climatological study, the initiation of MCS increases notably after midday, reaching a maximum value at 16:00-17:00 LT. Nesbitt et al. [69] argued that deep convection typically commences around noon along the highest ridges of the SMO and, similar to our results, the mesoscale organization typically occurs after 15:00 LT when conditions are most favorable in terms of sufficient moisture and thus convective available potential energy (CAPE). On the other hand, we found that 00:00 LT is the most common time of MCS termination which is observed in the Figure 7 right column, except for MCS traveling from SMO eastward towards Chihuahua (02:00 LT). However, independent of trajectory, MCS dissipation occurs between 00:00 to 09:00 LT, a result similar to that reported by Valdés-Manzanilla and Barradas Miranda [62] during the summer of 2004. In contrast to Valdés-Manzanilla and Barradas Miranda [62], our long-term analysis indicates that MCS do dissipate between (18:00-21:00 LT), perhaps due to the lack of a forcing mechanism which enhances MCS organization, propagation, and overall lifetime. With respect to MCS lifetime, our longer term results indicate that MCS typically have an average duration of around 8 h ± with a 2 h standard deviation, a minimum of 6 h (the minimum time criterion employed in this study), and a maximum of 27.50 h.

Lightning Activity of MCS
The increase in lightning activity during the development stage of MCS is a response to the rapid updraft intensification, that is, a strong updraft would lead to an increase in ice particle collisions which increases the separation of charge and with it an increase in lightning occurrence [143][144][145][146]. Although, lightning is typically categorized into three groups, intra-cloud, cloud-to-cloud and cloud-to-ground [146][147][148]; cloud-to-ground, in particular, has been employed in MCS studies [100,[149][150][151][152][153]. Approximately 80% of GLD360 detection strokes are estimated to be cloud-to-ground [85]. The lightning activity of the MCS meeting the criteria of our study (see Section 2.  This decrease in lightning occurrence may be likely the result of a diminution in the number of thunderstorm hours, which are defined by [85] as any hour of UTC time in which one or more lightning strokes is observed within a 40 km by 40 km box. However, the enhanced lightning occurrence, in all trajectories, may be due to the strengthing of convective updrafts by the upslope terrain of the SMO as has been encountered in other regions [101,[154][155][156]. In addition, we found a positive trend, more well-defined especially during stage 1, in the lightning versus area relationship; that is, as the MCS become larger, a greater lightning occurrence is observed. This relationship was also found in previous studies. For example, Mattos and Machado [100] found a rapid linear growth in the area is associated with a strong increase in the electrical activity of MCS in Brazil and Makowski et al. [157] found MCS with higher maximum total flash rates tended to be associated with larger cloud shields (shown for the −52 • C cloud shield) in Oklahoma.

MCS Propagation
Once MCS have been initiated, they may either remain quasi-stationary or propagate at a given speed. For example, Farfán and Zehnder [59] showed typical displacements of 100 km in 6 h. MCS propagation may be either continuous or discrete. The first case occurs when the MCS progresses toward initiating nearby deep convection is starting and joins with it. In the second case, a new convective system develops relatively distant from the already existing MCS, e.g., ∼30 km [1,158]. The actual mechanism responsible for the propagation of MCS such as cold pools, density currents, and/or gravity waves is still widely debated [159][160][161][162]. Houze [1] and Fovell et al. [158] suggest that continuous propagation was due to the persistence of cold pool dynamics. These ideas have been considered by other authors (e.g., [163,164]). In others studies, it has been argued that gravity waves dynamics may be responsible for MCS discrete propagation [21,28,165,166]. With respect to MCS trajectory, our results suggest three types of trajectories: Trajectory 1 (MCS which progress towards the GoC from the SMO), Trajectory 2 (MCS which travel parallel to the SMO), and Trajectory 3 (MCS traveling from the SMO toward Chihuahua) with 44%, 35%, and 14%, respectively. The trajectories 1 and 2 are similar to Regime A and Regime B as identified by Lang et al. [56] during the NAME campaign of 2004. In addition, they both occur in the zone between the SMO and the GoC coast. This same region has been shown to experience the most intense convective rainfall and lightning stroke density [67,84,85]. Investigating the propagation velocity of MCS is not only of fundamental scientific interest, but is also of utility for operational severe weather forecasting given that estimating approximate time-of-arrival is important for early warnings and severe-weather preparedness [167,168]. In addition, for a region of complex terrain such as the NAM, exploring which mechanisms are responsible for MCS propagation is an urgent task [23,159,161,169,170]. For the purpose of this study, we focus on MCS occurring between 2011-2017 so that lightning data can be employed to explore the intensity and convective lifecycle along these three common trajectories. As before, these MCS must have a lifespan of minimally ≥6 h and initiate between 14:00-22:00 LT. Figure 9 contains trajectories, based on their point of initiation and dissipation, for these MCS.
The MCS propagation speed, for the trajectory types 1, 2, and 3 was estimated by way of two techniques: (1) Hovmöller Diagrams and, (2)    The change in centroid position estimate a velocity for MCS, for Trajectory 2, propagating northward or southward of 8.71 ± 2.68 m/s (Table 4) and 9.42 ± 5.11 m/s (Table 5), respectively. However, the Hovmöller technique has problems in this trajectory likely because MCS have very different speeds and directions of propagation and, when averaged, the averaged trajectory is not representative. In addition, it is important to mention that the propagation speed detection limit is 4 km/15 min ∼4.4 m/s due to the temporal and spatial resolution of the GOES data. Table 1. Propagation speed estimation using technique 2 (change in centroid position from initial to final lifecycle stage) for MCS in the Band A. Means and ± one standard deviation in parenthesis. Bold and italic numbers correspond to Trajectory 1 and 3, respectively.

Year
No. Time    Table 3. As Table 1, but for MCS in the Band C.  These results suggest that MCS trajectory 2 propagate relatively more quickly than those trajectory 1. These results are consistent with those of Lang et al. [56] from the NAME campaign. These propagation speeds are much less than those associated with gravity waves (≈15 m/s) as discussed by Mapes et al. [28] and relatively larger than advection speeds associated with "steering-level winds" between 700 and 500 mb from ERA5, where the observed ranges were 5.3-6.0 m/s and 3.3-4.6 m/s for MCS trajectory 1 and MCS trajectory 2, respectively). These velocities are more consistent with propagation associated with density currents or cold pools resulting from MCS downdrafts. A similar mechanism was proposed by Lang et al. [56] and Rowe et al. [61] given the observed MCS propagations speeds during NAME. Nevertheless, the lack of long-term, high spatial density surface meteorological networks impedes the verification of this proposed mechanism.
Previous studies have demonstrated that synoptic-scale conditions can influence certain characteristics of MCS including their initiation, duration, morphology, size, and propagation speed [139,162,[171][172][173]. With respect to the NAM, studies have also shown that synoptic flow can create favorable conditions for MCS development [63,70,71,135,140,141,174]. In Figures 11 and 12 composites of geopotential, winds, and specific humidity in different atmospheric levels (700, 500, and 200 mb) during convective initiation are shown for MCS which propagate towards and parallel to the GoC, respectively. From the figures, it is apparent that the winds are fairly weak and the geopotential height is displaced northward in congruence with the northward progression of the latitudinal band. A similar northward extension in the humidity fields is also observed. In particular, trajectory 2 MCS typically occur in moister environments compared to trajectory 1 indicating the role of atmospheric instability in moisture environments [17,18,22].

Summary and Discussion
The Northwest region of Mexico experiences an increase in convective activity every summer, which tends to produce significant amounts of rain in this semi-arid and arid region with complex orography. Several field campaigns have been carried out in the last few decades in order to understand the formation, spread, and other aspects of convection organization in MCS [64,175]. Through the use of satellite images and lightning, this study is an attempt to gain insight into MCS including their temporal and spatial distribution, their morphology, and their intensification. Using an identification algorithm and a semiautomatic follow-up method, 1594 MCS were identified over the study region during the summers of 1995-2017. Table 6 summarizes the MCS characteristics with respect to their morphology and trajectory. In general, PECS, on average, last longer, propagate greater distances with greater velocity and display a larger initial area when compared with MCC, similar to what has been reported in other studies [40,41]. However, all MCS within the NAM region, independent of their form (PECS and MCC) and their trajectory (1, 2 and 3), have less eccentricity and shorter lifespan compared to MCS reported in the central U.S. perhaps as a function of the topography ( [40]) and the Himalayas region ( [41]) maybe a result of weaker NAM region sinoptic forcing. Regarding their spatial distribution, three latitudinal bands were identified where MCS tend to start with greater frequency. Bands A and B which experience the strongest precipitation events during the monsoonal season resulting from the occurrence and spread of MCS [56,[67][68][69]. It was also observed that the activity tends to be lower in the northern portion of the study area, Band C, most likely due to less frequent moisture incursion [176,177], as well as the lower occurrence of forcing of synoptic scales (e.g., IVs; [78], and a weakening of a diurnal sea breeze circulation [51]. While on the east side of the SMO the little occurrence of MCS are probably the result of weaker convergence, the lack of moisture in the atmospheric column relative to the western slope of the SMO [51,52]. The summers of 2000 and 2013 were the two most active summers with 94 and 91 MCS, respectively, while 1995 and 2009 were the two least active summers in terms of MCS, 41 and 53, respectively. For the two most active years, the subtropical high was displaced relatively farther north and more intense compared to the least active 2 years (Figure 13), which also favors the passage of transitory disturbances (e.g., IVs) which can provide a favorable wind shear profile for the formation and propagation of MCS [53,54]. The monthly frequency shows that the most active month is July, followed by August. While June and September were the least active, confirming what would be expected, since the NAM usually starts in mid-late June, its maturity is observed in July and August, while its dissipation occurs in mid-late September [142].
MCS in this region have an average life of 8.28 h relatively higher than that found (7.46 h) in the summer of 2004 by [62]. It is important to mention that our study covers 23 summers and therefore the discrepancy with [62] is probably explained by the interannual variability in synoptic conditions that favor the development and maintenance of these organized systems [78,134,136]. The maximum duration was 27.50 h, the minimum of 6 h (given by the definition of MCS used in this study). With regards to their morphology, most of the MCS have an eccentricity of less than 0.7, which indicates that these systems tend to have an elongated shape. Considering the diurnal cycle of MCS, approximately 75% usually start during the afternoon and early evening (14:00-20:00 LT); while 50% tend to dissipate in the early morning (20:00-04:00 LT) similar to that reported by [62] and similar to the diurnal cycle of convective activity and precipitation, where MCS start during the afternoon mainly on the western slopes of the SMO and are capable of generating heavy rain in these areas and even in coastal regions while heading towards the GoC [56,[67][68][69].
For this study region, our evaluation of lightning activity with respect to two stages in the life cycle of MCS; Stage 1 (Start-Maturity) and Stage 2 (Maturity-Dissipation), we find that these systems usually have greater lightning occurrence during the Stage 1 similar to what has been reported in both mid-latitudes and certain tropical regions [100,152].
In previous studies employing radar, the strongest updrafts have been seen during the initiation stages [1,2,13]. With respect to MCS trajectory, the results from our long-term climatology using GOES IR data suggest two dominant trajectories: Trajectory 1 (MCS which progress towards the GoC from the SMO) and Trajectory 2 (MCS which travel parallel to the SMO) with 44% and 35%, respectively. In both trajectories, the favorable 500 mb geopotential height pattern is similar, with a broad anticyclonic circulation centered over New Mexico. This positioning of the monsoon ridge to north and east and can provide a favorable environment (e.g., suficient amounts of moisture in the boundary layer, atmospheric instability, vertical wind shear and lifting mechanism that triggers convection) for MCS [71,140,178]. This synoptic pattern corresponds to the type I severe weather pattern previously identified by [71], and first and third mode of empirical orthogonal function analysis by [57,174], respectively. Our examination of propagation speeds suggest that cold pools or density currents and not gravity waves nor mid-level winds are responsible for the propagation of NAM MCS, however, more surface sites are needed to validate this observation. Previous studies have identified two main mechanisms that can explain the MCS motion: (1) Advection by mean wind throughout a representative tropospheric layer, and (2) updraft-wind shear interaction [179][180][181]. In this study, mean wind (direction and speed) in the 500-700 mb layer between Trajectory 1 and 2 suggest the second mechanism (shear effects), however, a sounding site or a radar in the western side of SMO would be needed to verify this mechanism. The present study provided a detailed climatological analysis of the temporal and spatial distribution and electrical activity of the MCS that they occur in a region of complex orography. This study is a basis for future research that seeks to evaluate the effect of climate change on MCS, the performance of numerical models.

Conclusions
Understanding the variety of factors under which convection initiates and experiences upscale growth into MCS over complex topography is challenging, given the interactions over various time and space scales. These types of MCS observational studies which clearly indicate the frequency, intensity, and spatio-temporal evolution of MCS could be particularly useful in the context of examining trends and temporal variability associated with circulations from the synoptic scale (e.g., inverted troughs) up to planetary-scale features such as El Niño-Southern Oscillation and the Madden-Julian Oscillation. Although not considered directly in this study, the explicit representation of deep convective activity or its parameterization in numerical models continous to be widely debated (e.g., see [182]). Both model climatologies and forecasts skill are very sensitive to the representation of deep convection and, hence, can greatly benefit from extended studies such as this one.