The March 2021 Damasi Earthquake Sequence, Central Greece: Reactivation Evidence across the Westward Propagating Tyrnavos Graben

: On 3 March 2021, a strong shallow earthquake affected northern Thessaly, Greece, with an epicenter close to Damasi village causing signiﬁcant destruction of many stone houses. In this contribution, we provide ﬁeldwork observations, satellite radar interferometry, mapping of the active faults exposed in the epicentral area, liquefactions and coseismic surface ruptures, and preliminary geomorphological analyses of the epicentral area. The geomorphological analysis is based on air photographs, digital surface models analysis, Real-Time Kinematik (RTK) measurements with Global Navigation Satellite System (GNSS) receivers, and data from UAV ﬂight campaigns. Although the seismotectonic setting of the area is complex and there is an apparent mismatch between ﬁeld and interferometric data, the results of our investigations suggest that at least three fault segments were reactivated by the major shocks of the March seismic sequence. These tectonic structureslikely represent the westward propagation of the Tyrnavos Graben, where newly formed and inherited low-angle faults interplay in a complex manner.


Introduction
The 2021 seismic sequence of Central Greece, called hereinafter the Damasi earthquake, began on the 3rd of March with an Mw 6.3 earthquake (magnitude from NOA). Its epicenter is located close to the village of Damasi. This earthquake caused the significant destruction of many stone houses in villages of the epicentral region, but fortunately, there were no casualties. A second earthquake (Mw 6.0) occurred on March 4th (magnitude from NOA) (Figure 1), while numerous aftershocks were recorded in the following days clustering progressively towards the NW, inducing further damage to buildings. The seismic cluster is tightly confined on the area of Damasi and Vlachogianni villages during the first 12 or more hours after the 3rd of March event and then after the 4th of March event expanded north-westwards for more than 25 km. In map view, the aftershocks form a 45 km-long and 18 km-wide zone, while their recorded depths range between ≈2 and 20 km, with the majority of them placed below 10 km (Figure 1c). Their focal mechanisms are compatible with the regional kinematic model indicating normal faulting. The cluster continues to show signs of activity for the interval of 4 months after the major March sequence (Figure 1c).
The seismically affected area we investigated represents a large sector of Northern Thessaly, characterized by lithologies belonging to the Pelagonian superterrane [1] and consisting of gneiss and schists Palaeozoic in age, Triassic recrystallized carbonates, and    [21] and references therein. I max = maximum macroseismic intensity; I TG = maximum macroseismic intensity in Tyrnavos Graben; TG = Tyrnavos Graben, sector = location of epicentral area with respect to TG; I TG = maximum intensity within TG (observed in group A and inferred in B-D); M m = macroseismic magnitude. The present contribution aims at describing the reactivation of the complex fault array that cross the Damasi earthquake epicentral area and the associated coseismic environmental effects of the sequence based on systematic field observations and satellite radar interferometry. Furthermore, considering the crustal scale Tyrnavos Graben, best studied east of the epicentral area of the Damasi earthquake sequence, we intend to provide new information on how the recent tectonic evolution of the Vlachogianni-Damasi region is correlated with the mapped Tyrnavos Graben. Indeed, we intend to provide new information on the recent tectonic evolution of the epicentral area. More seismological details are beyond the goals of this research, and we address the reader to more specific papers (e.g., [26,27]).The post event investigation includes mapping of the active faults exposed in the epicentral area, liquefaction features, and coseismic surface ruptures. We also present preliminary geomorphological analyses of the epicentral area, which are based on historical air photographs and digital surface model analysis for highlighting the most important active faults in the area. Real-Time Kinematik (RTK) measurements with Global Navigation Satellite System (GNSS) receivers and data from UAV flight campaigns ( Figure 2) were used to precisely constrain the coseismic deformation across reactivated faults.

Earthquakes
which are based on historical air photographs and digital surface model analysis for highlighting the most important active faults in the area. Real-Time Kinematik (RTK) measurements with Global Navigation Satellite System (GNSS) receivers and data from UAV flight campaigns ( Figure 2) were used to precisely constrain the coseismic deformation across reactivated faults.

Mapping of Fault Array and Documentation of Ground Failures
During field inspection, numerous environmental effects of the 3rd and 4th March 2021 earthquakes were mapped at numerous sites in a broad area between Tyrnavos town, Damasi and Verdikousa villages, and Elassona town. These effects primarily include coseismic ground ruptures ( Figure 2) and liquefaction failures ( Figure 3). Our observations were collected through field mapping over the seismically affected area, which is clearly defined by the SAR differential interferometry, while repeated SAR scenes processing, from the Sentinel-1 satellite, for pre-and post earthquake periods, provided more key evidence since the seismic sequence included two strong earthquakes and a moderate one.

Mapping of Fault Array and Documentation of Ground Failures
During field inspection, numerous environmental effects of the 3rd and 4th March 2021 earthquakes were mapped at numerous sites in a broad area between Tyrnavos town, Damasi and Verdikousa villages, and Elassona town. These effects primarily include coseismic ground ruptures ( Figure 2) and liquefaction failures ( Figure 3). Our observations were collected through field mapping over the seismically affected area, which is clearly defined by the SAR differential interferometry, while repeated SAR scenes processing, from the Sentinel-1 satellite, for pre-and post earthquake periods, provided more key evidence since the seismic sequence included two strong earthquakes and a moderate one.
During the fieldwork, we focused on areas characterized by significant clustering of secondary effects, like liquefaction phenomena and/or ground failures, where accurate mapping by UAV photogrammetric flights was performed ( Figure 2). Our flights followed the methodology developed by [28][29][30]. Our field surveys started on the morning of the 4th of March 2021 and lasted for almost three weeks. During the field campaign, we produced more than 30 orthophoto maps (300 m-long by 200 m-wide) recording the liquefaction features and the seismically induced surface ruptures. Concerning the latter, we recognized at least five fresh scarps associated with fracture opening, where we further conducted detailed morphological and structural analyses. data obtained from SLC Sentinel-1, ascending and descending orbits, were processed using Sentinel Application Platform (SNAP) developed by Brockmann Consult, Sky-Watch, and C-S. The characteristics of the interferometric pairs are displayed in Table 2.

Liquefaction Features
Among the secondary effects associated with the major shocks of the seismic sequence, the most prominent ones are probably represented by diffuse liquefaction phenomena. The associated liquefaction features mainly affected two areas: the first and the most important is along the Titarissios Valley, being a few kilometers away from the epicenter, and a second one close to the Piniada Valley, representing a reach of the Pinios River at a distance of more than 18 km south of the mainshock epicenter. In the current contribution, we will focus on the Titarissios Valley since its observed features are correlated with primary earthquake evidence. In particular, many sand blows with maximum diameters up to 30 m ( Figure 3a) and generally in the order of 10 m were observed within the epicentral area. The associated craters formed by the dewatering and sand ejection from the shallow subsoil are typically 0.3-0.5 m in diameter. The thickness of the sand volcano deposits was higher around the crater and gradually decreased radially, with a varied range of a few cm up to 50 cm. Sand volcanoes could be divided into symmetrical and asymmetric types. The formers are concentrated on flat areas, while the latter in areas with topographic irregularities (Figure 3b-d, respectively). The sand blows occurred either as isolate features or clusters (Figure 3a-d, respectively). Aligned volcanoes generally had a prevailing NW orientation, with some liquefaction craters showing NE-distribution direction.
Overall, two main types of liquefaction features were observed in the area between Pretori and Damasi villages, with most of them concentrated between Vlachogianni and Mesochori villages. Finally, sand blows consisted of different sand types, e.g., coarse dry at the lower part and wet fine on top (Figure 3d). Our detailed observations in these 'double' liquefaction deposits suggest that sand ejection was caused by both the mainshock (3 March 2021) and the largest aftershock (4 March 2021). Secondly, collapsed structures were mapped to be associated with dikes, where soft-sediment faults are intruded by dikes. This second type of structure seems to form close to the Titarissios riverbank and associate with lateral spreading or collapse due to consolidation or mobilization of an underlying liquefiable sand level(s).

SAR Interferometry of the Epicentral Area
SAR interferometry was established as a valuable technique for Earth deformation monitoring caused by earthquakes since 1992, when radar satellite data acquired by ERS-1 were successfully used to map the Landers earthquake in California, USA [31]. The aforementioned SAR interferometry was an inspiration to several scientists studying ground deformation caused by earthquakes using Synthetic Aperture Radar (SAR) satellite missions [32][33][34][35][36][37]. Over the years, new SAR satellite missions were launched to contribute to more detailed analyses and a better understanding of earthquake deformation. Sentinel-1 satellite constellation, developed by European Space Agency (ESA), opened up new possibilities through the increased number of observations, the systematic global acquisitions, the short revisit times, and the more stable orbits [37]. In that context, Sentinel-1 data are ideal for the postseismic deformation mapping, resulting from the occurrence of earthquakes on 3 March, 4 March, and 12 March, 2021. In the present study, data obtained from SLC Sentinel-1, ascending and descending orbits, were processed using Sentinel Application Platform (SNAP) developed by Brockmann Consult, SkyWatch, and C-S. The characteristics of the interferometric pairs are displayed in Table 2.
Independently from other research groups (e.g., [38]), we also analyzed SAR interferograms with the aim of better understanding the coseismic surface deformation. The results of our differential interferometric analyses are represented in Figure 4. In particular, the first Sentinel-1 ascending interferogram was created by images spanning the first seismic event between 25 February and 3 March, 2021 ( Figure 4a). Fringes are very dense, and a local linear loss of coherence is identified on an axis starting from the center of the interferogram and extending to the northwest. The second interferogram, generated by the Sentinel-1 images of 3 and 9 March 2021, contributed to the measurement of coseismic deformation produced by the 4 March event (Figure 4b). Interferometric fringes moved to the northwest, while a similar linear loss of coherence is detected. Unfortunately, the isolation of the coseismic deformation for the second event was only possible through ascending data processing. Besides, two additional Sentinel-1 interferograms were created to capture the deformation that occurred by both major events. The ascending and descending interferograms are in Figure 4c,d, respectively, where two areas of maximum deformation could be clearly observed. The deformation mapping of the third major shock (12 March) reveals the generation of another area of subsidence further northwest (Figure 4e,f). Overall, the quality of Sentinel-1 interferograms is remarkable, exhibiting ultrahigh coherence and low tropospheric disturbances. Concerning InSAR processing, we removed the topographic component using a Shuttle Radar Topography Mission (SRTM) 1 Arc-Second Global DEM, while phase filtering was implemented through an adaptive algorithm proposed by [39].

Coseismic and Cumulative Faulting Evidence
Overall, field data and the interferograms show that the causative faults of the Damasi seismic sequence occupy the westernmost sector of the Tyrnavos Graben [7] ( Figure 1) and probably represent the embryonic stage of the lateral propagation of the northern Thessalian basin. Indeed, these seismogenic structures were not on geological maps and/or their tectonic features were not classified as active due to poor morphological expression or ambiguous seismotectonic evidence. After the mainshock of the 3 rd of March and the major aftershock of the 4th of March, we focused our field investigation on the Tyrnavos (TF), Vlachogianni (VF), and Mesochori (MF) faults, as well as on other

Coseismic and Cumulative Faulting Evidence
Overall, field data and the interferograms show that the causative faults of the Damasi seismic sequence occupy the westernmost sector of the Tyrnavos Graben [7] (Figure 1) and probably represent the embryonic stage of the lateral propagation of the northern Thessalian basin. Indeed, these seismogenic structures were not on geological maps and/or their tectonic features were not classified as active due to poor morphological expression or ambiguous seismotectonic evidence. After the mainshock of the 3rd of March and the major aftershock of the 4th of March, we focused our field investigation on the Tyrnavos (TF), Vlachogianni (VF), and Mesochori (MF) faults, as well as on other tectonic structures that possibly played a role in the distribution of the coseismic deformation (Megalo Eleftherochori, MeF, Damasouli, DaF, Kalivia, KaF, faults; Figure 2). Fieldwork and morphotectonic analyses were devoted to recognizing possible reactivations and the role of these structures during the March 2021 seismic sequence, when this work was completed, although the seismicity remained active during April, May, and June 2021.The trace of all these faults locates within the InSAR fringes, which locally show some disturbances.
Based on the preliminary epicentral location of the mainshock (Figure 1), the first candidate as the causative fault was considered the WNW-ESE trending Tyrnavos Fault, which was thus promptly surveyed. However, except for minor surface ruptures associated with few millimeters of opening across two asphalted roads crossing N-S the valley north of the Damasi village (Figure 2), no further evidence was observed. In the meantime, the first DInSAR results confirmed the lack of significant displacement along the trace of and associated with the Tyrnavos Fault [38].
As concerns the NW-SE oriented tectonic structures affecting the epicentral area, the Vlachogianni Fault is certainly the most prominent (Figures 2-4). Although it is segmented at the surface, it has a possible total length of ca. 15 km. The northwest sector seems to split into a couple of branches and progressively loses any surface expression within the Quaternary alluvial plain sediments flooring the Potamia Basin.
The clearest evidence of recent activity was observed along the central sector of the VF, where the fault borders to the south an 8-9 km-long reach of the Titarissios Valley ( Figure 5). Here, the systematic post-event fieldwork supported by a UAV survey ( Figure 6) allowed us to document the occurrence of several surface ruptures associated with the 3 March event. The mapped cracks show vertical offsets up to 10 cm and a maximum opening of about 4 cm. The rupture could be followed for at least 1 km across farmed fields, progressively disappearing in loose Quaternary deposits or grasslands. From the DSM of the area derived from the UAV flights data, it was also possible to reconstruct several topographic profiles across the morphological feature emphasizing the presence of ca. 1 m-high cumulative scarp affecting the Late Pleistocene alluvial cones (Figures 7 and 8). Since no liquefaction or lateral spreading phenomena were associated with the ground rupture and considering the presence of a clear flexural scarp, we tentatively suggest that the observed surface features are somehow linked to, and representative of, the coseismic reactivation of a fault at depth during the Damasi earthquake.
The fresh ground ruptures run at the base of, and parallel to, a linear cumulative scarp where a series of triangular facets are well-exposed ( Figure 5) and document a long-lasting activity of these structures.
Towards the southeast, the VF crosses the Palaeozoic gneiss, where a 5 m-thick cataclastic zone was observed, documenting a superposed brittle behavior, possibly suggesting recent shallow reactivations. In this sector, fresh surface ruptures were also recognized at two locations associated with an array of open joints and small-scale rockfalls.
DSM of the area derived from the UAV flights data, it was also possible to reconstruct several topographic profiles across the morphological feature emphasizing the presence of ca. 1 m-high cumulative scarp affecting the Late Pleistocene alluvial cones (Figures 7  and 8). Since no liquefaction or lateral spreading phenomena were associated with the ground rupture and considering the presence of a clear flexural scarp, we tentatively suggest that the observed surface features are somehow linked to, and representative of, the coseismic reactivation of a fault at depth during the Damasi earthquake. The fresh ground ruptures run at the base of, and parallel to, a linear cumulative scarp where a series of triangular facets are well-exposed ( Figure 5) and document a long-lasting activity of these structures.  At one of these locations, a local place called Bara Damasiou (Figure 2), sheep shepherd Vlioras Panagiotis observed luminous aerial phenomena that appeared at a distance of less than 100 m from the VF during the main earthquake event. Similar witnesses were recorded by our team relative to waves temporarily affecting the ground surface.
The Vlachogianni Fault was also mapped eastwards across the carbonate bedrock south of Damasi [7], where it loses any surface expression in correspondence with the N-S trending abandoned reach of the Titarissios Valley [13].
In the seismotectonic framework of the broader area, the trace of the VF is aligned with the active Larissa Fault well mapped on the other side of the valley [16]. The latter structure represents one of the major tectonic features of the whole Tyrnavos Graben [8,17] ( Figure 1).   At one of these locations, a local place called Bara Damasiou (Figure 2), sheep shepherd Vlioras Panagiotis observed luminous aerial phenomena that appeared at a distance of less than 100 m from the VF during the main earthquake event. Similar witnesses were recorded by our team relative to waves temporarily affecting the ground surface. The Vlachogianni Fault was also mapped eastwards across the carbonate bedrock south of Damasi [7],where it loses any surface expression in correspondence with the N-S trending abandoned reach of the Titarissios Valley [13].
In the seismotectonic framework of the broader area, the trace of the VF is aligned with the active Larissa Fault well mapped on the other side of the valley [16]. The latter Although the real cumulative displacement of the Vlachogianni Fault is difficult to estimate, a simple topographic analysis tentatively suggests a minimum value of 270 m. From borehole data drilled in the Potamia Basin (Figure 2), the thickness of the Pliocene-Quaternary sediment is about 180 m [40]. Accordingly, the cumulative displacement of the VF is possibly as much as 450 m. This total displacement is likely the result of two deformational phases: the Pliocene-Early Pleistocene and the Late Pleistocene-Present. However, the amount of displacement associated to the two extensional phases and their proportion are unknown.
Probably the most important surface rupture in terms of lateral continuity and amount of throw and opening was mapped along the northern side of the Titarissios Valley. On this side of the river, fresh ruptures were mapped, with a cumulative length of ca. 5 km. The observed displacement vectors document a south-dipping fault plane with normal kinematics. Throw values across this rupture are up to 28 cm, and openings are up to 10 cm (Figure 9). We refer to this newly formed and mapped structure as the Mesochori Fault (MF). Since these surface ruptures are close to the Mesochori village more than five oral witnesses confirm the correlation of this surface feature with the 3 March mainshock. Probably the most important surface rupture in terms of lateral continuity and amount of throw and opening was mapped along the northern side of the Titarissios Valley. On this side of the river, fresh ruptures were mapped, with a cumulative length of ca. 5 km. The observed displacement vectors document a south-dipping fault plane with normal kinematics. Throw values across this rupture are up to 28 cm, and openings are up to 10 cm (Figure 9). We refer to this newly formed and mapped structure as the Mesochori Fault (MF). Since these surface ruptures are close to the Mesochori village more than five oral witnesses confirm the correlation of this surface feature with the 3 March mainshock. The flexural surface scarp was also mapped through a systematic UAV flight campaign focusing on the sector with the best-preserved scarp (Figure 10a), where we excavated two palaeoseismological trenches, whose results will be presented in a separate paper. Based on the UAV flight campaign, we prepared several detailed topographic profiles to better investigate the distribution of the surface displacement; for simplicity, we present in this work only eight of them. Examples are shown in Figure 10b, suggesting a cumulative scarp height in the order of 0.9 m. The flexural surface scarp was also mapped through a systematic UAV flight campaign focusing on the sector with the best-preserved scarp (Figure 10a), where we excavated two palaeoseismological trenches, whose results will be presented in a separate paper. Based on the UAV flight campaign, we prepared several detailed topographic profiles to better investigate the distribution of the surface displacement; for simplicity, we present in this work only eight of them. Examples are shown in Figure 10b, suggesting a cumulative scarp height in the order of 0.9 m. Northwest of the Vlachogianni Fault tip, the E-W trending Ambelia Fault together with the antithetic Magoula Fault (AmF and MaF in Figure 2, respectively) were tentatively suggested as possibly active [7]. However, no field evidence of coseismic reactivation was observed during our post event survey.
In contrast, we posed attention to some N-S oriented faults affecting the area, which undoubtedly represent inherited structures within the Pelagonian basement [41] but possibly played (and could continue to play) a role in the evolution of the Tyrnavos Graben.  Considering its parallelism and its proximity (less than 2 km) with the Vlachogianni Fault and its antithetic behavior, the MF represents a secondary tectonic structure, likely with an accommodation role relative to the north-dipping VF. Figure 2, respectively) were tentatively suggested as possibly active [7]. However, no field evidence of coseismic reactivation was observed during our post event survey.

Northwest of the Vlachogianni Fault tip, the E-W trending Ambelia Fault together with the antithetic Magoula Fault (AmF and MaF in
In contrast, we posed attention to some N-S oriented faults affecting the area, which undoubtedly represent inherited structures within the Pelagonian basement [41] but possibly played (and could continue to play) a role in the evolution of the Tyrnavos Graben.
The Megalo Eleftherochori Fault, MeF, runs W of the homonymous village and is characterized by a brittle-ductile shear zone (Figures 2 and 11a). This shear zone was likely active during the late Alpine stages [41]  The Megalo Eleftherochori Fault, MeF, runs W of the homonymous village and is characterized by a brittle-ductile shear zone (Figure 2 and Figure 11a). This shear zone was likely active during the late Alpine stages [41] (i.e., Eocene-Miocene; for N-S trending faults by the Verdikousa village). The MeF includes a well-developed, 5-m-thick cataclastic zone with hematite concentration in a meter-thick fault core. The cataclastic zone suggests post-Alpine tectonic activity, and it was mapped along the bottom of a stream that runs parallel to the fault zone and drains into the Smoliotikos River ( Figure  2). The stream is narrow in the south and gets wide in the north, probably in a relationship with the fluvial geomorphology and river developed along the fault. MeF is characterized by an east-facing scarp dipping less than 40° juxtaposing the Hercynian Pieria Granitoid Complex. The fault scarp becomes progressively smoother northwards, losing its prominent geomorphic expression in correspondence with the Smoliotikos River. It has a possible cumulative throw in the order of 150 m. Reddish rocks represent cataclasis in calcareous rocks, and whitish rocks represent gneissic cataclasites. Carbonate rocks are exposed in the DF hanging-wall block (ca) and gneisses (gn) in its footwall block. Photo is taken looking south.

North of the Smoliotikos River is the Kalivia Fault, KaF, which borders the Potamia
Basin to the west (Figure 2). The KaF scarp is characterized by mountain front sinuosity index >3, and thus, it could be considered as an eroded, probably inactive, fault. It is composed of minor segments and has a total throw in the order of 50 m. The south tip of the KaF is near its intersection with the Smoliotikos River, while the northern fault tip is difficult to recognize since it probably underlies post-Alpine sediments of the Potami-aBasin.
During the fieldwork, we also investigated the east-dipping Damasouli Fault (DaF; Figure 11b, Figure 12 and Figure 13). Although the trace of the fault north of the Vlachogianni Fault has relatively poor morphological expression, its southern part is instead well-marked for at least 2 km. In this sector, the fault is characterized by a cataclastic zone (Figure 12), where the fault rocks bear dip-slip kinematic indicators ( Figure  13) documenting the uplift of the Palaeozoic schist-gneiss (hanging-wall) relative to the Triassic marbles (footwall). These kinematic data show clear evidence of inversion tectonics since this contact was originally a reverse fault [2,8].
Along with the well-exposed DaF, a series of small-scale landslides were recognized (Figure 12), and their density is about six landslides per square kilometer. At least two of these gravitational phenomena were triggered by the seismic sequence (Figure 12b,c), while open cracks and diffuse block toppling also developed ( Figure 13). Reddish rocks represent cataclasis in calcareous rocks, and whitish rocks represent gneissic cataclasites. Carbonate rocks are exposed in the DF hanging-wall block (ca) and gneisses (gn) in its footwall block. Photo is taken looking south.

North of the Smoliotikos River is the Kalivia Fault, KaF, which borders the Potamia
Basin to the west (Figure 2). The KaF scarp is characterized by mountain front sinuosity index > 3, and thus, it could be considered as an eroded, probably inactive, fault. It is composed of minor segments and has a total throw in the order of 50 m. The south tip of the KaF is near its intersection with the Smoliotikos River, while the northern fault tip is difficult to recognize since it probably underlies post-Alpine sediments of the PotamiaBasin.
During the fieldwork, we also investigated the east-dipping Damasouli Fault (DaF; Figures 11b, 12 and 13). Although the trace of the fault north of the Vlachogianni Fault has relatively poor morphological expression, its southern part is instead well-marked for at least 2 km. In this sector, the fault is characterized by a cataclastic zone (Figure 12), where the fault rocks bear dip-slip kinematic indicators (Figure 13) documenting the uplift of the Palaeozoic schist-gneiss (hanging-wall) relative to the Triassic marbles (footwall). These kinematic data show clear evidence of inversion tectonics since this contact was originally a reverse fault [2,8].
Along with the well-exposed DaF, a series of small-scale landslides were recognized (Figure 12), and their density is about six landslides per square kilometer. At least two of these gravitational phenomena were triggered by the seismic sequence (Figure 12b,c), while open cracks and diffuse block toppling also developed ( Figure 13).
Tectonic geomorphology provides a unique opportunity to investigate, through the analysis of landforms, the signature of the tectonic processes on landscapes over a period spanning the late Holocene to early Pleistocene, or even late Pliocene. Accordingly, we apply facets analysis and mountain front and river sinuosity patterns to infer the occurrence of intermediate-and long-term deformation in the study area. Tectonic geomorphology provides a unique opportunity to investigate, through the analysis of landforms, the signature of the tectonic processes on landscapes over a period spanning the late Holocene to early Pleistocene, or even late Pliocene. Accordingly, we apply facets analysis and mountain front and river sinuosity patterns to infer the occurrence of intermediate-and long-term deformation in the study area. Google Earth imageries used to determine the presence of morphotectonic features along the faults, like remarkable topographic breaks or steps ( Figure 14). In this regard, both VF and MeF produce prominent fault scarps where morphometric analyses can be applied. For example, to evaluate the dissection of the mountain front, we estimated the Pf index for both faults. Google Earth imageries used to determine the presence of morphotectonic features along the faults, like remarkable topographic breaks or steps ( Figure 14). In this regard, both VF and MeF produce prominent fault scarps where morphometric analyses can be applied. For example, to evaluate the dissection of the mountain front, we estimated the Pf index for both faults.  Figure 15).
Also, along the VF mountain front, triangular facets are present occasionally in the northwest, as clearly observed on 1960 air photos (1:15,000 scale). The steepest facets are found along the central part in correspondence of the ground ruptures formed due to the March event. The Pf index for the VF is 87% (Figure 15). Triangular shaped facets, which generally form by erosion of fault-bounded mountain ranges, are arguably one of the most prominent geomorphic features on active normal fault scarps ( [18,42]). This evidence indicates that the VF had a recent (Late Quaternary) activity, likely characterized by distinct tectonic pulses as suggested by the higher (and older) triangular facets.  Figure 15).
Also, along the VF mountain front, triangular facets are present occasionally in the northwest, as clearly observed on 1960 air photos (1:15,000 scale). The steepest facets are found along the central part in correspondence of the ground ruptures formed due to the March event. The Pf index for the VF is 87% (Figure 15). Triangular shaped facets, which generally form by erosion of fault-bounded mountain ranges, are arguably one of the most prominent geomorphic features on active normal fault scarps [18,42]. This evidence indicates that the VF had a recent (Late Quaternary) activity, likely characterized by distinct tectonic pulses as suggested by the higher (and older) triangular facets.
Concerning the MeF, though it shows some faceted spurs, its degree of recent activity is questionable. Similarly, the erosion across Kalivia Fault trace is prominent, and the overall tectonic geomorphology across the western border of the Potamia Basin suggest these are likely inactive structures.
No triangular facets were observed in the footwall of the Mesochori Fault, nor was a marked bedrock scarp. The lack of such geomorphic evidence and of detailed morphotectonic investigations ( Figure 10) is likely the primary reason this faultwas never mapped before the Damasi earthquake sequence.
Titarissios River (from its original southwards flow across the Piniada Valley to its final destination, the Karditsa basin) towards the Larissa Plain [12]. Notwithstanding, the secondary role of the Mesochori Fault certainly contributed to the structural control by laterally constraining a ca. 10 km-long reach of the Titarissios River. Along this valley, the river sinuosity has changed from 1945 to 2019 by increasing from 1.23 to 1.32 ( Figure 16); this could reflect a possible change in sediment supply or some possible tilting of the valley floor [43]. It was recently proposed that the Late Quaternary regional hydrography was strongly influenced by the Vlachogianni, Larissa, and Tyrnavos faults (Figure 1). Although with different roles, all these tectonic structures contributed to the diversion of the Titarissios River (from its original southwards flow across the Piniada Valley to its final destination, the Karditsa basin) towards the Larissa Plain [12]. Notwithstanding, the secondary role of the Mesochori Fault certainly contributed to the structural control by laterally constraining a ca. 10 km-long reach of the Titarissios River. Along this valley, the river sinuosity has changed from 1945 to 2019 by increasing from 1.23 to 1.32 ( Figure 16); this could reflect a possible change in sediment supply or some possible tilting of the valley floor [43].

Discussion
Analysis of differential interferograms certainly contributed to the rapid and detailed mapping of the ground deformation pattern of the March 3 rd mainshock and its major aftershocks (Figure 4). At a first glance, the satellite approach suggests a mainly blind sliding structure [26]. However, the immediate post-event fieldwork observations with the support of drone surveys carried out in key areas documented that other tectonic structures were also reactivated to produce observable morphotectonic features. In particular, detailed field survey investigations provide evidence that deformation in the epicentral area is associated with an array of previously mapped normal faults considered as possibly active [7], though not included in the Greek database of seismogenic sources (GreDaSS; [44]). Also, the fieldwork allowed the recognition of new structures and confirmed their activity; among them are the Vlachogianni (VF) and Mesochori (MF) faults. Indeed, these tectonic structures show geomorphic features attesting to the geologically ongoing deformation; for example, they maintain straight mountain fronts, form well preserved triangular facets, and probably control the sinuosity of a central reach of the Titarissios River. In line with these observations and complementary to the overall picture are the dense network of liquefaction features, the minor rockfalls along these fault traces, and especially, the coseismic ground ruptures (Figures 2, 3, 6 and 8-13).
Similar partially contradicting results between DInSAR analyses and field evidence in seismogenic areas characterized by complex geological and tectonic settings are not exceptional [45][46][47]. In particular, the loss of coherence of the interferograms across areas covered by a significant thickness of loose sediments, as it occurs within the Titarissios Valley, clearly obscures the true pattern of the fringes. In the Thessalian case, if the amount of surface displacement on the antithetic VF and MF was comparable, as it seems to be confirmed by the field observations (Figures 7 and 10), the fringes outside the narrow Titarissios Valley graben should be not markedly displaced.
On the other hand, DInSAR results suggest that a significant amount of the coseismic slip occurred on a low-angle blind fault (e.g., [26]). To explain and combine all the available field and satellite observations, we suggest the occurrence of a complex tectonic structure within the uppermost part of the crust. The Vlachogianni Fault represents a steeply dipping shallow segment that reaches the Earth's surface as a splay of a low-angle normal fault at depth. If this is the case, the VF could have caused widespread

Discussion
Analysis of differential interferograms certainly contributed to the rapid and detailed mapping of the ground deformation pattern of the March 3rd mainshock and its major aftershocks (Figure 4). At a first glance, the satellite approach suggests a mainly blind sliding structure [26]. However, the immediate post-event fieldwork observations with the support of drone surveys carried out in key areas documented that other tectonic structures were also reactivated to produce observable morphotectonic features. In particular, detailed field survey investigations provide evidence that deformation in the epicentral area is associated with an array of previously mapped normal faults considered as possibly active [7], though not included in the Greece database of seismogenic sources (GreDaSS; [44]). Also, the fieldwork allowed the recognition of new structures and confirmed their activity; among them are the Vlachogianni (VF) and Mesochori (MF) faults. Indeed, these tectonic structures show geomorphic features attesting to the geologically ongoing deformation; for example, they maintain straight mountain fronts, form well preserved triangular facets, and probably control the sinuosity of a central reach of the Titarissios River. In line with these observations and complementary to the overall picture are the dense network of liquefaction features, the minor rockfalls along these fault traces, and especially, the coseismic ground ruptures (Figures 2, 3, 6 and 8-13).
Similar partially contradicting results between DInSAR analyses and field evidence in seismogenic areas characterized by complex geological and tectonic settings are not exceptional [45][46][47]. In particular, the loss of coherence of the interferograms across areas covered by a significant thickness of loose sediments, as it occurs within the Titarissios Valley, clearly obscures the true pattern of the fringes. In the Thessalian case, if the amount of surface displacement on the antithetic VF and MF was comparable, as it seems to be confirmed by the field observations (Figures 7 and 10), the fringes outside the narrow Titarissios Valley graben should be not markedly displaced.
On the other hand, DInSAR results suggest that a significant amount of the coseismic slip occurred on a low-angle blind fault (e.g., [26]). To explain and combine all the available field and satellite observations, we suggest the occurrence of a complex tectonic structure within the uppermost part of the crust. The Vlachogianni Fault represents a steeply dipping shallow segment that reaches the Earth's surface as a splay of a low-angle normal fault at depth. If this is the case, the VF could have caused widespread subsidence on both its hanging-wall and footwall blocks (e.g., [48,49]). In this geometric-kinematic frame, the Mesochori Fault represents a major antithetic splay of the lowangle VF segment. In this regard, the palaeoseismological results could possibly provide evidence of whether coseismic reactivations comparable to the March 2021 Damasi event occurred in the recent past along the MF. Further investigations are in progress and will likely shed light on this issue.
During the fieldwork, we mapped an array of cracks along the Damasouli Fault (DaF) and triangular facets along the Megalo Eleftherochori Fault (MeF) as well, both characterized by an N-S trend. A similar trend is also defined for the Kalivia Fault ( Figure 2). These three structures are assumed as inherited ones, but it is tentatively considered that they could have played a secondary role during seismogenesis. These N-S trending faults possibly induced partitioning of the deformation or halted the rupture process across the dominating NNE-dipping structures; for example, the Vlachogianni Fault (VF).

Concluding Remarks
With documentation completed for (i) the recent activity of at least three faults and (ii) the clear westwards migration of the seismicity as emphasized in the interferogram analyses (e.g., [38] and this study; Figure 4), we can sum up with the following major conclusions: (1) This study demonstrates the presence of a complex continuous fault array characterizing the epicentral area of the Damasi earthquake. In the epicenter, the fault array includes reactivated NNE to NE-or SSW to SW-dipping faults, and N-S trending inherited structures likely play a secondary role in the seismogenesis. (2) The faults with a morphological expression within the area trend WNW-ESE, and are characterized by linear fault scarps and well-exposed triangular facets, indicating long-term deformation. The Titarissios River sinuosity possibly reflects short term deformation before the recent seismicity. (3) The documented recent activity of these faults confirms that the Tyrnavos Graben was representing a seismic gap [7] in Central Greece and suggests that the tectonic basin is still growing and propagating westwards. Accordingly, the specific role of the Vlachogianni (VF) and Mesochori (MF) Faults was previously underestimated.