Digital Field Mapping and Drone-Aided Survey for Structural Geological Data Collection and Seismic Hazard Assessment: Case of the 2016 Central Italy Earthquakes

In this work, a high-resolution survey of the coseismic ground ruptures due to the 2016 Central Italy seismic sequence, performed through a dedicated software installed on a digital device, is strengthened by the analysis of a set of drone-acquired images. We applied this integrated approach to two active sections of the Mt Vettore active fault segment which, in the Castelluccio di Norcia plain (central Italy), were affected by surface faulting after the most energetic events of the sequence: the 24 August, Mw 6.0, Amatrice and 30 October, Mw 6.5, Norcia earthquakes. The main aim is to establish the range in which the results obtained measuring the same structures using different tools vary. An operating procedure, which can be helpful to map extensive sets of coseismic ground ruptures especially where the latter affects wide, poorly accessible, or dangerous areas, is also proposed. We compared datasets collected through different technologies, including faults attitude, dip-angles, coseismic displacements, and slip vectors. After assessing the accuracy of the results, even at centimetric resolutions, we conclude that the structural dataset obtained through remote sensing techniques shows a high degree of reliability.


Introduction
The new technologies that replace 20th-century field tools are the smartphone, handheld Global Navigation Satellite System (GNSS), tablets, iPad, and drones. Last generation tablets, in particular, offer performances of a hand-compass, plus take pictures and act as both a notebook and mapping device, and gather precise location data using GNSS. They can even be equipped with GIS software. The impressive technological development characterizing the current times have also brought significant improvement in field mapping techniques. The "classical" geological survey can now be integrated by digital mapping carried out using several types of devices, like tablets with dedicated software, and in some particular contexts, by the acquisition of images by drones [1][2][3][4][5][6][7][8][9][10][11][12][13][14]. This work provides a workflow for drone remote-sensing and structural-geological mapping, which offer significant advantages compared to the traditional fieldwork. The collected data enable us to reconstruct three-dimensional models of inaccessible outcrops and to explore in detail areas which, during a repetitive seismic activity, might be affected by rock falls (cliffs or outcrops at the foot of prominent fault scarp).
Furthermore, compared to the traditional methods that employ compass-clinometer and field book, digital mapping, performed either with tablets and/or drones, allow collecting an enormously

Study Area
The study areas are located near the village of Castelluccio di Norcia (42 • 49 42.51" N 13 • 12 28.00" E) in the southern part of the Sibillini Mts. chain, a deeply studied portion of the Umbria-Marche thrust and fold belt in Central Italy [17][18][19]. The stratigraphy of this region includes a Jurassic-Middle Miocene, shelf to pelagic, carbonatic succession, followed upward by Late Miocene siliciclastic turbidites ( Figure 1).
The contractional structures consist of a system of NW-SE to N-S-striking asymmetric box-folds characterized by overturned eastern limbs and bounded by east-verging low-angle thrust faults, Late Miocene-Early Pliocene in age [18,20,21].
Towards E and SE, the outer basal thrust of the chain which, from N-S direction, turns southwards to NNE-SSW direction, causes the superposition of the Sibillini thrust sheet on the Messinian Laga basin turbidites.
Since the Early Pleistocene, extensional fault systems displaced the contractional structures [22][23][24] with associated offset, along the single faults, locally exceeding 1500 m. Despite the fault system showing a certain geometrical complexity, on the whole, the Quaternary normal faults appear arranged in a quite a regular, NNW-SSE-striking regional alignment across the Umbria-Marche and Laga domains (Figure 1a).
During the Quaternary, the activity along the major extensional faults, which dip to W-SW, led to the formation of intra-mountain basins, filled with alluvial and lacustrine deposits [25][26][27].
The easternmost extensional fault, the VBF, is a highly segmented, well-known active structure with a 6.5 ≤ Mw ≤ 6.8 maximum expected magnitude [28] (Figure 1a). It shows an along-strike length of~30 km, a long-term maximum displacement of~1500 m [21,25,29], and a maximum Late Quaternary slip rate of 1.3 mm/y [15]. The Piano Grande basin was developed in the VBF hanging wall during the Middle-Late Pleistocene (Figure 1b). Eluvial-colluvial deposits overlay unconformably the carbonate bedrock along the borders of the basin whereas the major depression is mainly filled by alluvial and lacustrine sediments [30,31].
Well before the 2016 Central Italy seismic sequence, the present activity of VBF had been suggested on the base of the observed displacement of Quaternary deposits and Late Pleistocene-Holocene landforms [21,23,25]; subsequently its seismogenic potential was highlighted by paleoseismological evidence [28].
The diffuse surface faulting observed along the VBF after the 2016 sequence ( Figure 1b) and the good correlation between the activated fault at the surface and the hypocentral distribution of the seismicity unquestionably confirmed the seismogenic role of this fault.
All the three main segments in which the VBF is divided were activated during the 2016 seismic sequence; they are referred to, from south to north, as the Vettoretto-Redentore, Bove-Porche and Cupi-Ussita segments [15] (Figure 1a).
Several synthetic and antithetic splays branch from the three segments at distance up to 4 km west of the main fault trace.
Two of the major splays of the Vettoretto-Redentore segment, located along the eastern border of the Piano Grande di Castelluccio basin, and named hereinafter the Colli Alti e Bassi Fault and Prate Pala fault (CAB and PTP, respectively, Figure 1b) were affected by significant coseismic reactivation and have been studied in detail in this work.
Massive field surveys performed by several research groups after the three earthquakes, allowed to reconstruct and compile very detailed databases of the associated primary ruptures [15,[36][37][38] (yellow and red dots in Figure 1a).
To date, most authors [15,[39][40][41] agree that: (i) the M w 6.0 event caused surface faulting, along a~6 km section of the VRS, with coseismic throws reaching 27 cm, without activating any other splay of VBF; (ii) the 26 October M w 5.9 event ruptured the only northern segment of the VBF, (Cupi-Ussita), with throws ranging from 8 to 10 cm; (iii) the 30 October (M w 6.5) mainshock reactivated and ruptured the entire Vettoretto-Redentore and Bove-Porche segment, with a surface rupture length 32 > L > 22 km and coseismic surface displacements up to 222 cm, and (iv) despite most of the 30 October coseismic ruptures having occurred along the main fault trace, they also partially reactivated synthetic and antithetic splays within a few kilometers off the main fault trace. On the contrary, no evidence of coseismic rupture was observed after the 24 August event along the subsidiary structures.

Selection of Sample Areas
In the Castelluccio di Norcia area (Figure 1b) (Figure 2a,b). The CAB geologic (i.e., long term) expression was previously recognized and reported in published geological maps [21,29].
The PTP was recognized and partially mapped by Galadini and Galli [16] through an aerial photo-geologic survey, integrated by paleoseismological trenching.
Both these reactivated synthetic splays of the VRS crop out close to the eastern border of the Piano Grande basin. We selected the sample area 1, straddling the CAB, and the sample area 2, including the PTP ruptured during the 2016 mainshock (Figure 2a,b).
In neither area, evidence of ruptures were detected after 24 August and 26 October events (Figure 3a,b,e); thus, the total measured displacements can be referred to the 30 October reactivation.
Digital fieldwork carried out on both the sample areas soon after the mainshock provided coseismic displacement values of up to 101 cm along the CAB (Figure 3c The PTP was recognized and partially mapped by Galadini and Galli [16] through an aerial photo-geologic survey, integrated by paleoseismological trenching. Both these reactivated synthetic splays of the VRS crop out close to the eastern border of the Piano Grande basin. We selected the sample area 1, straddling the CAB, and the sample area 2, including the PTP ruptured during the 2016 mainshock (Figure 2a,b).
In neither area, evidence of ruptures were detected after 24 August and 26 October events (Figure 3a,b,e); thus, the total measured displacements can be referred to the 30 October reactivation.
Digital fieldwork carried out on both the sample areas soon after the mainshock provided coseismic displacement values of up to 101 cm along the CAB (Figure 3c Figure 1b); the two sketches (a = plan view, b = bird's eye view) illustrates the mission flight plan for image capturing over the sample area using a manual flight, with an overlap of 80% along the path and 80% in a lateral direction, useful to have a good alignment of images and to reduce the distortions on the resulting orthomosaics; (c,d) Sample area 2, along the Prate Pala Fault; (PTP, location in Figure 1b) the two sketches (c = plan view, d = bird's eye view) illustrates the mission flight plan for image capturing that covers the area using north-south flight paths with 65% along the path and 60% in a lateral direction. Legend: blue point: shot point photo; yellow point: sites of manual and digital mapping; blue line: trace of the CAB (a) and PTP (b) faults; tics indicates the hanging wall block.

Field Mapping
The high-resolution mapping of the surface coseismic ruptures in the field was carried out integrating the traditional survey, performed using a geologic compass-clinometer for measurement

Field Mapping
The high-resolution mapping of the surface coseismic ruptures in the field was carried out integrating the traditional survey, performed using a geologic compass-clinometer for measurement of planar and linear elements (dip azimuth/ dip-angle of fault planes, trend and plunge of slickenlines), with digital mapping technique. The digital mapping was based on a digital compass-clinometer App for portable devices, allowing the direct measurement of georeferenced planar and linear elements accompanied by written notes, sketches, and editable photographs of each survey site ( Figure 4)

Instruments Calibration and Pre-Drone Survey
The use of cameras for the Structure From Motion (SfM) and the creation of tri-dimensional virtual outcrops is now straightforward and fast because the instrumentation at our disposition is very light to transport during the field survey.
The necessity of total stations GPS for the acquisition of more precise and more accurate data positioning is generally required, but in this work, we did not use it. The method used in this research is based mainly on the placement of markers Ground Control Points (mGCPs) at a well-defined known distance during the field survey. The objectives of this work do not take into account the accuracy in terms of positioning of the virtual outcrop in the space (that is in terms of absolute coordinates), but it aims at achieving high-precision in the measurement of the outcrops parameters, as f.i. height of slopes, width, and length of the virtual outcrop, amount of coseismic displacement associated with each part of the rupture. Therefore, this research proposes a method of utilizing photogrammetry for creating a georeferenced and scaled virtual outcrop without the use of total stations GPS. The method is based on the use of an mGCPs of known geometries located close to outcrop during the field survey. The markers located on outcrops are used as ground control points, and their distances are calculated.
The acquisitions of mGCPs are essential in the pre and post-processing phase, to make scale changes, to position, orientate, and rescale the three-dimensional model in the chosen Geographic Reference System. In this work, 25 × 25 cm markers were used as mGCPs.
During the subsequent analysis through the Agisoft Metashape software, the placement of markers were positioned at the center of each mGCPs surveyed, to optimize precision between the images, and for subsequent rescaling of the virtual outcrop. The contrasting black and yellow Several preliminary trials allowed to verify that the internal sensor of IOS provides reliable and precise azimuthal and dip-angle measures. The reliability-trials consisted of repeated comparisons between measures of the same structure carried out using the digital device and the geological compass-clinometer. This testing experience highlighted that the chosen device and software assured accurate compass readings for both azimuthal and clinometric measurements that not exceed ±2 degrees. For the positioning of the elements measured, an internal sensor A-GPS and GLONASS/GNSS also integrated with the high-resolution images from the Google Earth™ Pro 7.3 was successfully used. The accuracy of the waypoints acquired depended on satellite coverage. When the maximum satellite coverage reached the optimum values, the error estimated for the automatic location was of 1-2 m, whereas it reached 3-5 m in the worst coverage conditions. The solution to minimalize the error location (well below one-meter resolution) was the manual adjusting on the iPad screen, taking into account the easily recognizable elements on the Google Earth base map imagery. A further precaution to avoid positioning inaccuracies was the use, as Fieldmove base maps, of previously acquired high-resolution images, orthorectified through ArcGis, and exported from the Move software in mbtiles or geotiff format file.
Field data were organized in a comprehensive GIS-managed dataset for subsequent elaborations. The used software aside from the Fieldmove App for Apple iPad includes Esri ArcMap 10.x and Move 2019 Petex suite [http://www.petex.com/products/move-suite/]. All the geological-structural data acquired were elaborated within the Move suite software Petroleum Experts see Section 3.1.2.

Georeferenced Field Images Dataset
The database of georeferenced images also used for reconstructing virtual outcrops includes the photographs shooted during the digital survey, using the Fieldmove dedicated tool, and hundreds of digital photographs taken through a compact Sony camera with an integrated GPS sensor. Furthermore, it has been improved by several sets of high-resolution aerial photographs acquired through a digital camera transported by a Drone (Figure 4), whose methods of acquisition and processing is reported in the following Section 2.3.
Photogrammetric processing led to elaborate two Digital Surface Models (DSM) at centimetric resolutions for both the study-cases. For

Instruments Calibration and Pre-Drone Survey
The use of cameras for the Structure From Motion (SfM) and the creation of tri-dimensional virtual outcrops is now straightforward and fast because the instrumentation at our disposition is very light to transport during the field survey.
The necessity of total stations GPS for the acquisition of more precise and more accurate data positioning is generally required, but in this work, we did not use it. The method used in this research is based mainly on the placement of markers Ground Control Points (mGCPs) at a well-defined known distance during the field survey. The objectives of this work do not take into account the accuracy in terms of positioning of the virtual outcrop in the space (that is in terms of absolute coordinates), but it aims at achieving high-precision in the measurement of the outcrops parameters, as f.i. height of slopes, width, and length of the virtual outcrop, amount of coseismic displacement associated with each part of the rupture. Therefore, this research proposes a method of utilizing photogrammetry for creating a georeferenced and scaled virtual outcrop without the use of total stations GPS. The method is based on the use of an mGCPs of known geometries located close to outcrop during the field survey. The markers located on outcrops are used as ground control points, and their distances are calculated.
The acquisitions of mGCPs are essential in the pre and post-processing phase, to make scale changes, to position, orientate, and rescale the three-dimensional model in the chosen Geographic Reference System. In this work, 25 × 25 cm markers were used as mGCPs.
During the subsequent analysis through the Agisoft Metashape software, the placement of markers were positioned at the center of each mGCPs surveyed, to optimize precision between the images, and for subsequent rescaling of the virtual outcrop. The contrasting black and yellow rectangles of mGCPs, allow easily recognizable common points on each acquired photo and also facilitate the automatic location of points belonging to different images.
To improve the reliability of the measurement performed on a virtual outcrop, different calibers oriented in the third dimension (zy/zx plane = height, yx plane = width and length), perpendicular to each other were added.
The caliber instruments as hand-ruler 25 m long, aluminum stadia graduated rod 5 m long, and markers positioned at predetermined distances were used.
This method provided good precision in evaluating the virtual outcrop parameters, but it does not take into account the absolute accuracy in terms of geographical positioning; therefore, the whole model could also be shifted by some decimeters. In this work, all the markers were positioned at a distance of 10 m from each other and arranged in two preferential orthogonal directions North-South and West-East.
In the sample area 1, they were positioned at the intersection points of a 10 m sided square grid oriented in N-S and W-E directions (Figures 1b and 2a,b). Overall, in this area, 15 mGCPs, 7 of which in the fault footwall and 8 in the hanging wall, and different calibers were used for scaling the entire model proportionally in both the directions N-S and W-E of the obtained virtual outcrop model.
The area 2, characterized by a narrow and elongated shape (1 × 0.13 km), to reduce the 'doming' effect [eg 10,12,13], a total of 20 mGCPs were arranged in the fault footwall, in the hanging wall, and also at corners and central part of the investigated area (Figures 1b and 2c,d).

Drone Survey
The aircraft used to perform the survey was a quadcopter. The drone is equipped with an autopilot package that, in the presence of internet connection, follows a pre-programmed flight-path using the appropriate app, enabling the user to choose the number of waypoints, the photo shooting, and the desired flight altitude. The mission program for both the study areas included a detailed flight plan, including the flight direction, number of flight lines, flying altitude, and orientation of the camera respect to the flight path. The program was thought taking into account that the awaited resolution of the post-processing images strongly depends on the overlap, side lap, and ground sampling distance.
A drone camera with sensor 1/2.3" CMOS, 12.4 M Effective pixels, lens FOV 94 • 20 mm (35 mm format equivalent), image size of 4000 × 3000 was used for the survey; for more detailed resolution, a camera Sony DSC-HX5V with 10 megapixels and internal GPS sensor was also used.
The flight was followed through a remote controller wirelessly connected with an Apple iPad Air 2.
In the study area 1, a manually piloted flight-mode was carried out due to the lack of coverage of UMTS signal causing, in turn, the complete absence of internet connection. The manual flight paths were organized into three different acquisition methods: (a) three aerial strips at three different altitudes: 30, 60, and 120 m above ground level, shooting the photos perpendicular to the flight direction; (b) two aerial strips very close (3 and 5 m) to the fault plane, with the oblique-oriented camera at 45 degrees; (c) two aerial strips farther from the previous one, with photos shooted perpendicular to the outcrop (Figure 2a,b). A total of 268 photos were acquired, with a minimum front and side overlapping of 80%. During half of the flight, the camera orientation was maintained perpendicular to the main path, whereas, for the second half-flight, a path-parallel arrangement was set. The need to adopt different shooting angles was due to the high slope-angle characterizing the outcrops of this sample area.
In the study area 2, the consistently good internet connection allowed to plan an automatic-mode guided flight through a dedicated application.
In this case, the flight path was planned to maintain a constant elevation of 70 m above ground level (Figure 2c,d). In the second study area, four aerial sweeps were carried out, leading to the acquisition of 100 photos, with overlapping (both in front and side) ranging from 60% to 65%. During the flight, as this area was completely flat, the camera orientation was maintained perpendicular to the main path, and the images were acquired automatically.
The processing with Agisoft Metashape software was necessary to obtain a spatial resolution of 1 cm/pixels for virtual outcrops reconstruction. Digital photogrammetry, obtained from the sequential drone-acquired overlapping images and through the use of Agisoft Metashape software led to the following elaborations: (a) sparse point clouds, (b) dense point clouds, (c) meshes and textures, (d) 3D models, (e) tiled models, (f) DEM and orthomosaic model. Figure 5 shows all the processing steps carried out with Agisoft Metashape software (details in the caption of Figure 5).

Extraction of Fault Slip Data from Cloud Compare
The Cloud Compare [http://www.danielgm.net/cc/] open-source software allowed to perform structural geological analysis of the surveyed coseismic ruptures, directly on a desktop PC. The generated 3D point cloud, including more than 13 million points (Figures 5c and 6), georeferenced in the previous steps, were used to reconstruct the virtual outcrops and for the subsequent kinematic analysis on the fault planes. After the processing of the CAB virtual outcrop, the surface of the~15 m long fault mirror was manually extracted from the density point cloud.
Using the Cloud Compare software, and particularly the plugin qFacets [43] (https://www. cloudcompare.org/doc/wiki/index.php?title=Facets_(plugin)), it was possible to make observable the long-term striae through an "interactive stereogram" (see inset in Figure 6c,d). In fact, by selecting a narrow range of values of dip direction and dip angle, the plugin makes visible only a few facets of fault plane (i.e., as the ridges in grooves lineations). This application of interactive filtering is exceedingly useful to understand the trend of the lineations on the outcrop in a tridimensional space. After choosing and comparing them with the 30 October coseismic slip vector, measured directly in the field (correlating hanging wall and footwall piercing points), the associated net displacement was assessed. Through a "virtual compass" on Cloud Compare, the outcrop orientation was determined, and the use of the "lineation tool" allowed the measurement of the height and dip directions of the coseismic slickenlines. Finally, through Cloud Compare software, all the extracted data obtained from the measurements on the virtual outcrop, were exported in .csv format file, as dip, dip-azimuth, trend and plunge, and plotted onto stereonets for structural analysis.
The described steps are shown in Figure 6, from dense-point cloud import (a) to the extraction of the fault plane (b), to the measurement of coseismic elements (total or net displacement, c-g) until exporting of the database (h) in excel, csv, or txt format.

High-Resolution Topographic Profiling
To optimize the quality of the result of our topographic analysis, we used two different software to extrapolate profiles from the Digital Surface Model, which led to obtaining 1 cm resolution over area 1 and a resolution of 3 cm in area 2 (Figure 7a-d). In particular, serial profiling across the coseismic ruptures of both CAB and PTP fault was performed through the Esri ArcGis v.10.x "3DAnalyst" and through the "Create Sections" tool of Move 2019. From both the sets of profiles, we estimated the fault-scarp height (Figure 7a-d).
To compare our digital field data with those obtained by aero-photogrammetric 3D model, several fault attitudes along the CAB were manually collected, and the height of the scarps measured ( Figure 7b).
The "surface control" is essential to estimate the errors between analogical (real outcrop) and digital (virtual outcrop) measurement data.
In the field, a meter stick was used to estimate all along the fault trace, the height of the scarp, associated throw, and net displacement, both on the long term and coseismic free face. The slope dip angle was measured using a clinometer (Figure 7b).
Then, we compared the morphological height, the strike, the dip, and dip azimuth of the fault plane, measured in the field, with those obtained from the virtual outcrop 3D model.
The observed deviation between the height values of the fault scarp directly measured in the field and those extracted from virtual outcrop never exceed 2 cm (compare the deviations between the curves and the colored dots of Figure 8b), confirming the reliability of the reconstructed digital topography.

Topographic Analysis of CAB
The graphs in Figure 8 show The estimated values of these features (on the Y axis, in meters) are plotted against the along-strike distance of each measurement point (abscissa) from the northern tip point of the fault-scarp outcrop (assumed as X = 0). Dots in the Figure 8 graph mark the values, manually measured on the control points, respectively, for the height of the fault scarp, measured with hand ruler (green dots), and the 30 October 2016 coseismic ruptures (net displacement) from the manual survey (yellow dots). The good agreement between the field data and the assessments obtained from the topographic analysis on the virtual outcrop, confirms the reliability of the adopted method.
The TTO and HFS curves show very similar trends but differ in several points because the former includes the part of the scarp removed by erosion.

Topographic Analysis of CAB
The graphs in Figure 8  The estimated values of these features (on the Y axis, in meters) are plotted against the along-strike distance of each measurement point (abscissa) from the northern tip point of the fault-scarp outcrop (assumed as X = 0). Dots in the Figure 8 graph mark the values, manually measured on the control points, respectively, for the height of the fault scarp, measured with hand ruler (green dots), and the 30 October 2016 coseismic ruptures (net displacement) from the manual survey (yellow dots). The good agreement between the field data and the assessments obtained from the topographic analysis on the virtual outcrop, confirms the reliability of the adopted method.
The TTO and HFS curves show very similar trends but differ in several points because the former includes the part of the scarp removed by erosion.
Interestingly, the CRRA curve, even if characterized by lower values (higher observed net slip = 1.25 m), shows a good correlation with TTO and HFS curves, as regards the position of the maxima and minima. This remarkable consistence suggests that the along-strike height profile of the current fault scarp derives from the add up of a certain number of coseismic displacements, each characterized by slip-profiles similar to the one caused by the mainshock of the 2016 sequence.

Structural and Kinematics Analysis of the CAB
During the fieldwork, several attitudes of the CAB were measured as a dip and dip azimuth, using either a traditional compass-clinometer and a Fieldmove-equipped Apple iPad. After data collection, the whole dataset was managed in a georeferenced digital database.
Subsequently, we extracted attitude and kinematic data from the virtual outcrop reconstructed through remotely acquired images (see Section 2.3.4) A comparison between the three different attitude datasets is shown in Figure 9.
Appl. Sci. 2020, 10, x FOR PEER REVIEW 18 of 30 Interestingly, the CRRA curve, even if characterized by lower values (higher observed net slip = 1.25 m), shows a good correlation with TTO and HFS curves, as regards the position of the maxima and minima. This remarkable consistence suggests that the along-strike height profile of the current fault scarp derives from the add up of a certain number of coseismic displacements, each characterized by slip-profiles similar to the one caused by the mainshock of the 2016 sequence.

Structural and Kinematics Analysis of the CAB
During the fieldwork, several attitudes of the CAB were measured as a dip and dip azimuth, using either a traditional compass-clinometer and a Fieldmove-equipped Apple iPad. After data collection, the whole dataset was managed in a georeferenced digital database.
Subsequently, we extracted attitude and kinematic data from the virtual outcrop reconstructed through remotely acquired images (see Section 2.3.4.) A comparison between the three different attitude datasets is shown in Figure 9. The hand-compass collected dataset shows that on six measurements on the fault plane, the trend of dip-azimuth is variable between N220 and N260, with a mean resultant plane orientation of dip-azimuth at N237 and dip-angle of 68 degrees (Figure 9a). In the same points, the measurements with the Fieldmove app show a dip-azimuth trend on a fault plane, comprised between N220 and N260, with a mean resultant plane orientation of dip-azimuth at N235 and dip-angle of 70 degrees (Figure 9b). However, the results obtained from virtual outcrop, clearly with a huge number of data (77 points measurements), shows a main dip-azimuth trend between N220 and N240 and only a few data comprised between N240 and N260; also in this last case, mean dip-azimuth of the fault plane orientation shows a trend of N233 and dip-angle of 70 degrees (Figure 9c).
In order to compare the measures of the striation trend collected through three different used tools (Figure 9d-f and Table 1), a number of six data were also acquired using hand-compass and Fieldmove integrated compass. In both cases, the dispersion of data varies in the range between N180 and N240, except for the huge data extracted from the virtual outcrop that shows an attitude between N180 and N220 and the mean direction dipping toward N207, well comparable with data acquired with the previously described tools. The hand-compass collected dataset shows that on six measurements on the fault plane, the trend of dip-azimuth is variable between N220 and N260, with a mean resultant plane orientation of dip-azimuth at N237 and dip-angle of 68 degrees (Figure 9a). In the same points, the measurements with the Fieldmove app show a dip-azimuth trend on a fault plane, comprised between N220 and N260, with a mean resultant plane orientation of dip-azimuth at N235 and dip-angle of 70 degrees (Figure 9b). However, the results obtained from virtual outcrop, clearly with a huge number of data (77 points measurements), shows a main dip-azimuth trend between N220 and N240 and only a few data comprised between N240 and N260; also in this last case, mean dip-azimuth of the fault plane orientation shows a trend of N233 and dip-angle of 70 degrees (Figure 9c).
In order to compare the measures of the striation trend collected through three different used tools (Figure 9d-f and Table 1), a number of six data were also acquired using hand-compass and Fieldmove integrated compass. In both cases, the dispersion of data varies in the range between N180 and N240, except for the huge data extracted from the virtual outcrop that shows an attitude between N180 and N220 and the mean direction dipping toward N207, well comparable with data acquired with the previously described tools. As regards the determination of fault attitude data, the good degree of mutual correlability between the differently acquired data is evident and encouraging. In fact, they mostly agree in providing an average fault attitude of~a 235/70 (dip-notation value, compare rose diagrams Figure 9a-c,d-f and Table 1). From such a point of view, the remote sensing survey is advantageous, considering the large number of data collected over a very short time in comparison with both the traditional and digital field mapping techniques.

Study Area 2-Prate Pala Fault (PTP)
Topographic Analysis of PTP Despite the small offset associated with the 30 October coseismic rupture, the reactivation of the PTP has highlighted soon after the mainshock thanks to the displacement of the paved road (S.P.477) from Forca di Presta to Castelluccio di Norcia (Figure 3g,h). A maximum offset of 14 cm was measured in the field in the central part of the coseismic rupture (Figure 3f), whose total length was estimated in~1.3 km, our data are well comparable with the results obtained in Villani & Sapia 2017 [44].
The performed drone-aided mapping, which allowed the detection of tectonic scarps displacing the flat topography of the Castelluccio di Norcia plain, led to reconstruct a 3 cm resolution Digital Surface Model (DSM).
DSM models elaborated using this technique also allow removal of vegetation noise. Fortunately, in the studied cases, this problem was negligible because the periods in which the aerial images were acquired (beginning of November 2016 and afterward in 2018), were preceded by several months of intense grazing with poor grass regrowth, due to deficient rainfall.
Further processing of the DSM allowed to explore and analyze through the functions of the ArcGIS tools, the slope analysis, the shaded relief, and the aspect of the fault scarp.
A set of 27 topographic profiles, perpendicular to the fault scarp, were drawn to investigate the morpho-structural expression of the PTP ( Figure 10) and to reconstruct the along-fault coseismic slip profiles, from north to south.
The systematical counter-slope (i.e., dipping towards east, thus opposite to the fault dip) topography observed west of the PTP trace is interesting, suggesting a back tilting of the hanging wall block, which is coherent with the normal kinematic of the fault. This observation, confirmed by the persistence of a long-term topographic scarp resistant to the intense breeding and plowing practiced in the area, provides further evidence of the present activity of the PTP. A comparison between the along-strike DSM-derived topographic offset and the coseismic slip profile is shown in Figure 11.
In the first case (Figure 11a), from the northern edge of PTP, the profile increases with a medium-high slope reaching the maximum height where the topographic scarp is~2.3 m. Moving south, the scarp shows a gradual decrease to zero at the southernmost surface tip of the PTP. The observed asymmetric trend of the topographic offset suggests, according to Manighetti [45] and Cappa et al. [46], that, during previous events, surface ground rupture propagated mainly from north to south. On the contrary, in Figure 11b, the trend of the coseismic slips shows an opposite triangular shape compared to the previous one, culminating at a maximum value of 14 cm (Figure 3f).
The aforesaid works [45,46], investigating the distribution of the slip along with the fault segments during the coseismic rupture, interpreted the triangular shape, characterizing both the profiles as due to the dynamics of rupture propagation.
In particular, Manighetti et al. [45] show, from the analysis of several normalized displacement profiles, that the geometry of the coseismic slip profile gives information on the polarity of the rupture propagation and the location of the epicenter from the fault tips and the point of maximum displacement.
Brozzetti et al. [15], comparing the 2016 Central Italy coseismic ruptures with the surface faulting of the global earthquakes, agreed with the suggestion of Manighetti et al. [45], showing that the coseismic slip profiles obtained from the field survey have an asymmetric shape (from south to north) for the whole VBF, and also for the single VRS, VBS, and CUS segments of the master fault.
Similarly, the here reported data suggest a polarity of fracture propagation from south to north, as shown by the asymmetry of the graphs Figure 11b.
Possibly the difference in the observed polarity of propagation may depend on the hypocenter location and the magnitude of the earthquakes that provide surface faulting.
Moreover, according to Tao et al. [47] and Iezzi et al. [41,48], the aspect of the surface faulting is influenced by fault geometry and, in particular, fault segmentation and/or change of direction (bending). It is to be taken into account that this work had the opportunity to analyze only a short section of the PTP fault, whose effective length is reasonably much higher than the portion ruptured at the surface during the 30 October mainshock.
Appl. Sci. 2020, 10, x FOR PEER REVIEW 21 of 30 the coseismic slip profiles obtained from the field survey have an asymmetric shape (from south to north) for the whole VBF, and also for the single VRS, VBS, and CUS segments of the master fault. Similarly, the here reported data suggest a polarity of fracture propagation from south to north, as shown by the asymmetry of the graphs Figure 11b.
Possibly the difference in the observed polarity of propagation may depend on the hypocenter location and the magnitude of the earthquakes that provide surface faulting.
Moreover, according to Tao et al. [46] and Iezzi et al. [41,47], the aspect of the surface faulting is influenced by fault geometry and, in particular, fault segmentation and/or change of direction (bending). It is to be taken into account that this work had the opportunity to analyze only a short section of the PTP fault, whose effective length is reasonably much higher than the portion ruptured at the surface during the 30 October mainshock. In Figure 12b,c the measures of coseismic ruptures from hand compass and tablet device are showed whereas Figure 12d displays the direction of fault scarp attitude obtained from DSM analysis.
Comparing the three rose diagrams, we observe that the coseismic ruptures mostly strike in the same direction of the scarp generated from the ancient earthquakes even if, in a few cases, they show oblique directions. The fact that the coseismic ruptures are localized on the long-term fault scarp suggests a preferential growth of the central part of the fault during each seismic event.
The three rose diagrams of Figure 12b-d, reporting on the PTP attitudes measured with the different methods, show a substantial agreement (particularly the b,c ones) but also a certain dispersion. We interpret the latter as due to the remarkable differences in the number of acquired data. In fact, the major deviations occur when the hand compass and Fieldmove collected data are compared with data extracted from virtual outcrops. The 30 October coseismic ruptures were not measured from DSM because the aerophotogrammetric image resolution was insufficient to detect them. A lower elevation flight would have been necessary, especially in the areas of maximum slip, but unfortunately, when this high-precision mission was planned, the area had been erased by agricultural activities, hampering the acquisition of new images useful for making these measurements. In Figure 12b,c the measures of coseismic ruptures from hand compass and tablet device are showed whereas Figure 12d displays the direction of fault scarp attitude obtained from DSM analysis.
Comparing the three rose diagrams, we observe that the coseismic ruptures mostly strike in the same direction of the scarp generated from the ancient earthquakes even if, in a few cases, they show oblique directions. The fact that the coseismic ruptures are localized on the long-term fault scarp suggests a preferential growth of the central part of the fault during each seismic event.
The three rose diagrams of Figure 12b-d, reporting on the PTP attitudes measured with the different methods, show a substantial agreement (particularly the b,c ones) but also a certain dispersion. We interpret the latter as due to the remarkable differences in the number of acquired data. In fact, the major deviations occur when the hand compass and Fieldmove collected data are compared with data extracted from virtual outcrops. The 30 October coseismic ruptures were not measured from DSM because the aerophotogrammetric image resolution was insufficient to detect them. A lower elevation flight would have been necessary, especially in the areas of maximum slip, but unfortunately, when this high-precision mission was planned, the area had been erased by agricultural activities, hampering the acquisition of new images useful for making these measurements.

Accuracy and Precision
The integration of images acquired from a GPS/GNSS Drone has allowed placing of the virtual outcrop in its geographical position, with some limitations in terms of absolute accuracy. For most of the structural geology analysis, which did not need very-high accuracy in terms of geographical positioning, the described method can be considered satisfactory.
It is emphasized that this approach has to be considered as an integration to the "traditional" structural geological analysis. From the previous sections, it is evident that, in the two sample areas, the results obtained from aerophotogrammetrical processing and direct field measurements are comparable and that their precision is good. The maximum error measured along the fault scarps was close to 1 cm in the first area (CAB), and around 1-3 cm in the PTP area.
It is also to be considered that many sites, which may be potentially be studied using the proposed approach, are unreachable with bulky and heavy instrumentation.
In our case studies, the low performance of the GPS installed on the drone allowed correct positioning in a geographical system, but without a centimetric or millimetric accuracy. In any case, the precision of the height, width, and length of the virtual outcrop was satisfactory, thanks to the

Accuracy and Precision
The integration of images acquired from a GPS/GNSS Drone has allowed placing of the virtual outcrop in its geographical position, with some limitations in terms of absolute accuracy. For most of the structural geology analysis, which did not need very-high accuracy in terms of geographical positioning, the described method can be considered satisfactory.
It is emphasized that this approach has to be considered as an integration to the "traditional" structural geological analysis. From the previous sections, it is evident that, in the two sample areas, the results obtained from aerophotogrammetrical processing and direct field measurements are comparable and that their precision is good. The maximum error measured along the fault scarps was close to 1 cm in the first area (CAB), and around 1-3 cm in the PTP area.
It is also to be considered that many sites, which may be potentially be studied using the proposed approach, are unreachable with bulky and heavy instrumentation.
In our case studies, the low performance of the GPS installed on the drone allowed correct positioning in a geographical system, but without a centimetric or millimetric accuracy. In any case, the precision of the height, width, and length of the virtual outcrop was satisfactory, thanks to the correct use of caliber instruments. In conclusion, the results here obtained made it possible to create a valid and reliable model.

Discussion
The application of our working method to two study areas affected by coseismic surface faulting in 2016 Central Italy seismic sequence demonstrates that the virtual outcrop models represent an important tool for structural-geological and geomorphological research aimed at identifying and characterizing active tectonic structures.
Furthermore, comparing the information obtained from the morphological analysis of the fault scarp of CAB, with configuration of the coseismic surface faulting of the 2016 Central Italy seismic sequence, it is possible to make inferences on the rupturing history of the studied faults.
The good fit between the profile of the height of fault scarp and the 2016 coseismic slip profile (Figure 8b) suggests that the long-term fault scarp may have been formed as a result of several earthquakes, each causing a similar amount of surface displacement. It is also possible to infer for these events comparable values of magnitude.
In particular, taking into account: (i) the height of the entire fault scarp (ii) the amount of the 30 October 2016 coseismic slip, (iii) the geometry of the slope profiles also including the possible eroded free face, and (iv) the assumption that earthquakes of equal/similar magnitude generated equal/similar dislocations (compared to 2016 one), we hypothesize that at least five events are needed to reach the observed values of fault scarp height.
Previous paleoseismological works [16,49,50] have highlighted several seismic events, some of which caused the PTP reactivation, which occurred in the Pano Grande-Mt Vettore area. In particular, four events have been recognized in the last 8000 years, in addition to the earthquake of 2016. These four earthquakes, would have been occurred (from the oldest): (i) between IV and VI millennium BC, (ii) at the end of IV millennium BC, (iii) between II and III millennium BC, (iv) between the end of III and IV century AC (maybe in 270 AC). Furthermore, accepting the inferences, which implies that the 4.5 m outcropping fault scarp of the CAB was exhumed after the Last Glacial Maximum L.G.M. (~18.000 ky), a preliminary estimate of the slip rates, of 0.25 mm/y is obtained.
Of course, the analyzed fault scarps might have recorded a higher number of coseismic slip events, which could have been followed by erosional episodes in a longer geological time; thus, the above estimate must be considered purely indicative.
Several authors studied the causes/effects of the 2016 earthquakes from many points of view, as structural-geology, geophysics, seismology, paleoseismology, geomorphology, interferometry, geodesy, hydrogeology, engineering [15,31,32,[34][35][36]39,40,, but only a few authors have provided and elaborated data acquired through drones [92][93][94][95]. In addition, there are no author-produced image analyses of coseismic ruptures employing the techniques we propose here. Our results, obtained from the elaboration of high-resolution topography, fit well with the data published in Villani et al. [36], Brozzetti et al. [15], and Perouse et al. [95], acquired through traditional or digital mapping techniques. At the same time, the present work has improved the details of the surveyed geological features, some of which were not appreciable directly in the field; among this latter, the degradation and erosion of the fault plane as well as the tilting of the topographic surface, the dip-angle, and the off-fault width of the tilted area.
The here obtained results showed that the use of the drone-derived photogrammetry presents acceptable errors for all those structural-geological applications, also those that need high precision (near centimetric resolution), and that might be an integration to the traditional field survey.
In Figure 13, three types of DEMs with different resolutions (10 m, 5 m, and 1 cm) are compared. The significant image resolution improvement of the topographic model obtained in this work ( Figure 13c) is evident, as well as significant improvement of the geological interpretation, for example, in the correct positioning of tectonic structures.
High-resolution topography allows us to delineate with high precision the fault trace and in some conditions, such as in the CAB case, to identify the long term and recent kinematic indicators.
In cases where active faults displace post-LGM slopes, the applied procedure improves the estimates of the scarp height, thus helping to make inferences on the associated slip rates.
Moreover, improving the precision of the fault mapping (e.g., in Figure 13c) can, in turn, facilitate the identification of sites aimed at paleoseismological trenching.
Appl. Sci. 2020, 10, x FOR PEER REVIEW 24 of 30 In cases where active faults displace post-LGM slopes, the applied procedure improves the estimates of the scarp height, thus helping to make inferences on the associated slip rates.
Moreover, improving the precision of the fault mapping (e.g., in Figure 13c) can, in turn, facilitate the identification of sites aimed at paleoseismological trenching.

Conclusions
During routine geological fieldwork, faults are generally surveyed on topographic and geological maps using a traditional compass-clinometer or, when a high-resolution survey is needed, using a digital device (smartphone o tablet) with a dedicated application.
In this paper, we have shown that the use of Fieldmove app for digital devices integrated with the use of drone-acquired imagery is a performing combination, which speedily provides large sets of good-quality data, sensibly improving the topographic and geological models that are subsequently reconstructed.
The presented high-resolution aerial survey represents the first attempt to digitally reconstruct recent coseismic fault ruptures in variable geomorphological and outcrop conditions and to compare them with large published datasets collected through traditional and digital mapping.
In the study cases, which refer to two active splays of the Vettore-Bove Fault affected by surface faulting during the 2016 Central Italy seismic sequence, we reconstructed the fault traces, the height of the fault scarps, the amount of associated coseismic slip and its along-strike variations, with a precision that is much higher compared to previous literature reconstructions [15,29,36,37,96].
For all the aforesaid parameters, the estimated errors range within a few centimeters, a value that is well below the standards required by routine structural geological survey and is also acceptable for precision estimates of coseismic ground deformations.

Conclusions
During routine geological fieldwork, faults are generally surveyed on topographic and geological maps using a traditional compass-clinometer or, when a high-resolution survey is needed, using a digital device (smartphone o tablet) with a dedicated application.
In this paper, we have shown that the use of Fieldmove app for digital devices integrated with the use of drone-acquired imagery is a performing combination, which speedily provides large sets of good-quality data, sensibly improving the topographic and geological models that are subsequently reconstructed.
The presented high-resolution aerial survey represents the first attempt to digitally reconstruct recent coseismic fault ruptures in variable geomorphological and outcrop conditions and to compare them with large published datasets collected through traditional and digital mapping.
In the study cases, which refer to two active splays of the Vettore-Bove Fault affected by surface faulting during the 2016 Central Italy seismic sequence, we reconstructed the fault traces, the height of the fault scarps, the amount of associated coseismic slip and its along-strike variations, with a precision that is much higher compared to previous literature reconstructions [15,29,36,37,97].
For all the aforesaid parameters, the estimated errors range within a few centimeters, a value that is well below the standards required by routine structural geological survey and is also acceptable for precision estimates of coseismic ground deformations.
A complete workflow in which the entire procedure is described in detail is reported. It is divided into successive steps specifying all the necessary software and tools to be applied to obtain the topographic model of a study area.
Moreover, an assessment of the precision and applicability of point clouds derived by drone imagery is provided and also compared with the performances of the digital and analogic compass-clinometer.
Some further possible applications of the reconstructed models on the investigated active fault, f.i. slip rate estimate or reconstruction of the rupture history is described, suggesting possible correlations and integrations with the available paleoseismological data.
The results of this work highlight that photogrammetry can cover and improve the map resolution, where necessary, with low-costs compared to more expensive techniques like the LiDAR data acquisition, which are very costly and logistically complex to apply in many locations.
In other words, these methodologies can undoubtedly be a significant step forward in geological mapping as well as in structural and geomorphological research. They represent a field of work capable of remarkable development and perspectives in the near future.
Funding: This research received no external funding.