Concurrent deformation processes in the Matese massif area (Central-Southern Apennines, Italy)

Journal Pre-proof Concurrent deformation processes in the Matese massif area (Central-Southern Apennines, Italy) A. Esposito, A. Galvani, V. Sepe, S. Atzori, G. Brandi, E. Cubellis, P. De Martino, M. Dolce, A. Massucci, F. Obrizzo, G. Pietrantonio, F. Riguzzi, U. Tammaro

PII:

S0040-1951(19)30349-X

DOI:

https://doi.org/10.1016/j.tecto.2019.228234

Reference:

TECTO 228234

To appear in: Received Date:

7 May 2019

Revised Date:

15 October 2019

Accepted Date:

20 October 2019

Please cite this article as: Esposito A, Galvani A, Sepe V, Atzori S, Brandi G, Cubellis E, De Martino P, Dolce M, Massucci A, Obrizzo F, Pietrantonio G, Riguzzi F, Tammaro U, Concurrent deformation processes in the Matese massif area (Central-Southern Apennines, Italy), Tectonophysics (2019), doi: https://doi.org/10.1016/j.tecto.2019.228234

This is a PDF file of an article that has undergone enhancements after acceptance, such as the addition of a cover page and metadata, and formatting for readability, but it is not yet the definitive version of record. This version will undergo additional copyediting, typesetting and review before it is published in its final form, but we are providing this version to give early visibility of the article. Please note that, during the production process, errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain. © 2019 Published by Elsevier.

Concurrent deformation processes in the Matese massif area (Central-Southern Apennines, Italy) Esposito A.*, Galvani A.*, Sepe V.*, Atzori S. *, Brandi G.**, Cubellis E.**, De Martino P.**, Dolce M.**, Massucci A.*, Obrizzo F.**, Pietrantonio G.*, Riguzzi F.*, Tammaro U.**

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*Istituto Nazionale di Geofisica e Vulcanologia – Osservatorio Nazionale Terremoti, Roma ** Istituto Nazionale di Geofisica e Vulcanologia – Osservatorio Vesuviano, Napoli

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Highlights  Interseismic GPS velocity field for monitoring of the Apennine

The extension rate does not follow the topographic height of the Apennine.

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A tensile source has been modelled for the 29 December 2013 earthquake.

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Sharing of the SAGnet GPS archive.

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Abstract

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We investigated the interseismic GPS velocity field across the transition zone between Central and Southern Apennine comprising the Meta–Mainarde-Venafro

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and Alto Molise–Sannio-Matese mounts. The kinematic field obtained by combining GPS network solutions is based on data collected by the unpublished episodic

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campaigns carried out on Southern Apennine Geodetic network (SAGNet from 2000 to 2013), IGM95 network (Surace, 1997; Giuliani et al., 2009 from 1994 to 2007) and continuous GPS stations. The data collected after the 29 December 2013 earthquake (Mw 5.0) until early 2014 allowed estimating displacements at 15 SAGNet stations.

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The extension rate computed across the Matese massif along an anti-Apennine profile is 2.00.2 mm/yr. The interseismic velocities projected along the profile show that the maximum extension does not follow the topographic high of the Apennines but is shifted toward the eastern outer belt. No significant GPS deformation corresponding to inner faults systems of the Matese massif is detected. Taking into account our results and other geophysical data, we propose a conceptual model, which identifies the 2013-2014 seismic sequence as not due to

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an extensional deformation style usual along the Apennine chain. In fact, we have measured too large “coseismic” displacements, that could be explained as the result of tectonic regional stress, CO2 -rich fluid migration and elastic loading of water in

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the karst Matese massif. We recognized a tensile source as model of dislocation of 2013-2014 earthquakes. It represents a simplification of a main fault system and

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fracture zone affecting the Matese massif. The dislocation along NE-dipping North

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Matese Fault System (NMFS) could be the driving mechanism of the recent seismic sequences.

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Moreover, to the first time the SAGnet GPS data collected from 1994 to 2014, are share and available to the scientific community in the open access data archive.

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Keywords: GPS networks, geodetic strain rate, Matese massif, Central-Southern

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Apennines.

1. Introduction

The strain of the lithosphere is produced by separate complex geodynamic processes operating anywhere from the shallow crust to the uppermost mantle. In

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general, the strain estimation takes into account processes such as fault loading, viscous deformation along the brittle-ductile transition zone, post-seismic response, fluid intrusions, phases of groundwater recharge/discharge, atmospheric loading, etc. (England and Jackson, 1989; Thatcher, 1995). In order to evaluate and separate the concurrent contributions to the strain due to each single process, continuous monitoring of an area is required for long periods of time. The investigated area hosts a complex portion of the Apennine chain characterized

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by several faults systems. In the past, the area was struck by destructive earthquakes of intensity I≥IX MCS, occurring in 1349, 1456, 1688 and 1805. More recently, some lower magnitude seismic sequences occurred in 1997-1998 (MD =

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4.1), 2001 (MD = 3.3), 2005 (MD = 3.3), 2013-2014 (MW = 5.0) and 2016 (Mw = 4.3) (Cubellis et al., 1995, 2005; Milano et al., 1999, 2005, 2008; Rovida et al., 2016;

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Convertito et al., 2014; 2016; Galli et al., 2017; Moretti et al. 2017).

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Recent GPS studies have estimated that this sector of the Apennine chain undergoes to an extension rate of about 4-5 mm/yr, suggesting a partitioning of deformation due to different seismogenic structures (Giuliani et al., 2009; Boncio et

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al., 2016; Cowie et al., 2017). Moreover, GPS measurements can be used to study co-seismic displacements even in case of moderate earthquakes (Ganas et al.

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2013; Serpelloni et al., 2012).

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Here we present the results obtained through the SAGNet (Southern Apennine Geodetic Network, Sepe et al., 2009) and the densification of the GPS permanent network (Devoti et al., 2017) which allowed to estimate with more detail the interseismic velocity field from the linear interpolation of the coordinate time series in the time span 2002-2013 and the interseismic strain rate. This velocity field is combined with the velocity field published by Giuliani et al. (2009).

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We attempt to estimate the “coseismic” displacements due to the earthquake of 29 December 2013 from three episodic time series has been done by using the interseismic velocities to interpolate site positions just before the earthquake occurrence. The geodetic data discussed in the light of other geophysical and geological evidence put constraints on i) active interseismic deformation, ii) the role of active faults, iii) the influence of deep fluid, diffuse CO2 and rainfall release as trigger of the Matese 2013 sequence.

2.1. Geological and seismological framework

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2. Material and Methods

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The Apennine is an East-verging chain developed in the Cenozoic as the

accretionary wedge of the southwest-dipping subduction of the Adriatic plate. An

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active extension NE-SW and a general uplift affect the Apennines (e.g. Devoti et al., 2011). In the last decade several studies recognized the crucial role of rich CO2 fluid

Improta et al., 2014).

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circulation as a trigger of seismicity (Ventura et al., 2007; Di Luccio et al., 2010;

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The area under investigation is located in a split sector of the Apennines chain, corresponding to the transition zone between the central Apennines, the Meta-

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Mainarde - Venafro Mountains, and the northern portion of the southern Apennines, comprising the Alto Molise – Sannio - Matese Mounts (Fig. 1). In a relatively small

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area a puzzle of stratigraphic succession outcrops is identified: slope and by-pass margin deposits, carbonate units succession and terrigenous. Two main fault systems are recognized with NW- and NNE-trending (Di Bucci et al., 2002, 2005, Milano et al., 2002, 2008). Recent paleo-seismological and quaternary geology studies associated some NWtrending active faults to historical destructive earthquakes (Bousquet et al.,1993; 4

Galadini & Galli, 2000; Di Bucci et al., 2002, Galli & Galadini, 2003; Galli & Naso, 2009; Galli et al., 2017). The Matese massif (Fig. 1 and 2) is characterized by several principal faults: the Northern Matese fault system (NMFS), NW-trending and NE-dipping, bordering the Bojano-Isernia basin. Along the Bojano basin the portion of NMFS is named Bojano Basin fault (BBF). This structure was responsible of the 1456 and 1805 events (Galli & Galadini, 2003; Galli et al., 2017). Moving toward SE, near Venafro village, the

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Aquae Iulie fault (AIF, NW-trending, SW dipping) has been recognized as active and associated with the 1349 earthquake (Galli & Naso, 2009).

In the inner massif, a secondary SW-dipping fault system is known as the Matese

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Lake fault (MLF), which borders the northern side of the homonymous lake and the San Gregorio Fault (SGF), and the Castello Matese Fault (CMF). Finally, the SW-

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dipping normal fault Piedimonte Matese (PFM) borders the massif toward the

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Volturno Basin, and the San Pietro Infine fault (SPIF) borders the Venafro Mounts (Ferranti et al., 2015; Boncio et al., 2016).

In the past, the area was struck by destructive earthquakes (I≥IX MCS) separated

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by long periods of relative quiescence (Fig.1). The major events occurred in 1349, 1456, 1688 and 1805. Nowadays, seismic measurements show that this portion of

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the Apennines is affected by low magnitude events (M≤3), without evidence of a

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preferred occurrence alignment. The larger earthquakes are often superimposed to low magnitude seismic events, like the ones that occurred after the mainshocks of 1997-98, 2001, 2005, 2013-2014 and 2014-2016 (Milano et al., 2008; Fracassi and Milano, 2014; Ferranti et al., 2015; Convertito et al., 2014, 2016; Di Luccio et al., 2018).

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In 2013, December 29, the Matese massif was hit by a Mw 5.0 earthquake followed by intense seismic activity (Convertito et al., 2016). A second earthquake occurred on 2014, January 20 (Mw 4.2). A low-level seismic activity continued until February 2014. From the sequence beginning, more than 350 events were recorded, confined in a finger-like cluster located between 10 and 25 km depth, with very few events between 5-10 km depth (Di Luccio et al., 2018).

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2.2. GPS data and velocity solution The SAGNet is a non-permanent GPS network covering an area of about 100 km2 consisting of 65 sites distributed across Lazio, Campania, Abruzzo and Molise

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regions, with a mean inter-distance of about 7 km (Fig. 1) (Sepe et al., 2009). The

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network was planned and realized starting from 1994 as part of the European Project "Earthquakes prediction in tectonic active areas using space techniques” in

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collaboration with the Navigation Institute of the University of Stuttgart. (Luongo et al. 1996; Cubellis et al 1995). Since 2000 the Istituto Nazionale di Geofisica e

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Vulcanologia (INGV) has expanded the network to the actual configuration. In this paper we share for the first time the archive of the SAGNet network where

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data from 1994 to 2014 are collected. The data can be retrieved via anonymous FTP at the following link ftp://ftp.ingv.it/pro/SAGNet.

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The analyzed dataset consists of observations coming both from part of the SAGNet and the permanent GPS networks available in the area in time span 2000 to 2013 until the earthquake of December 29 (Fig. 3); the SAGnet data are from 18 GPS stations. The sampling rate was 30s and the observing windows from 12 to 24 hours, for at least 2 complete (24 hours) observation sessions, and three or more campaigns.

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Immediately after the December 29, 2013 earthquake a subset of 15 SAGNet benchmarks was reoccupied collecting data from 30 December 2013 to 4 April 2014. The continuous GPS data were provided by the CGPS networks located in the central and southern Apennines region. These stations are maintained by various Institutions and Agencies, INGV (RING network (Avallone et al., 2010); ASI (Italian Space Agency); Leica Geosystems (ItalPos network). Data processing has been

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performed by the Bernese sw v.5.0 (Beutler et al., 2007), following the scheme described in Devoti et al., 2017, obtaining separate velocity fields for CGPS and the campaign surveyed sites.

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The two velocity fields and the velocity solution published in Giuliani et al. (2009) were combined using in a least-square sense, following the procedure described in

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ITRF2008 reference frame.

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Devoti et al., 2017, obtaining a unique combined velocity solution expressed in the

The normal matrix was formed from the three independent velocity solutions and was inverted to estimate the unified velocity field. As the covariance matrix is usually

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known apart from a constant multiplier, we also estimated solution-scale factors together with the combined velocity solution. This ensured that the individual χ2 of

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each velocity solution was equally balanced (individual solutions do not prevail in the

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combination process) and the total χ2 is close to unity (realistic errors). The obtained combined velocity field represents a weighted velocity average that takes into account the correlation matrices of the three solutions.

3. Results We first take into account the interseismic velocity field (i.e. excluding data after the

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2013 seismic event) (Table1). Fig. 2 shows the combined velocities with respect to a fixed Adriatic plate. The Adriatic Eulerian pole was computed minimizing horizontal velocities of 11 stations located in the Adriatic sector of the studied area (1532, 1541, FRES, FOGG, LARI, LESE, SMRA, SPCI, TRIV, CROC, MELA) with a least-square inversion (Table 2). The velocity field shows a clear pattern toward SW confirming the extension style across the Apennine chain. The velocities increase from Adriatic to Tyrrhenian

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coast, defining the Adriatic domain as a belt 50 to 70 Km wide. Around the Matese massif the velocity vectors display a small clockwise rotation from S-trend to SW-trend with similar magnitude (~1.5 mm/yr). Along the western

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border of the massif, in the Volturno Valley and Campania plain, the velocities show a clear SW-trend.

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We projected the velocities along a NE-SW oriented profile, parallel to the average

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directions of the velocity vectors, approximately normal to the main fault systems and including the epicenter of the 2013 December earthquake (Fig. 4a). The projection, including 32 24 sites, show a gradual increase of velocity proceeding

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from NE to SW, with an average value of 0.40.2mm/yr between the Adriatic coast

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hill and Sannio Mounts (“Adriatic domain”) and of -2.40.2mm/yr from Bojano basin and Campania Plain (“Tyrrhenian domain”). The location of the transition between

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the two velocity domains corresponds to the western flank of Sannio Mounts. The velocity difference, of 2.00.3 mm/yr, takes place in a narrow belt (<10 Km). Between the Matese massif and the Campania plain the velocity varies smoothly. No significant deformation rate is highlighted in the Matese massif, although most of the GPS sites and tectonic structures are placed here.

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We have analyzed the horizontal strain rate tensor from the horizontal velocities and their uncertainties, due to the lack of vertical velocities, assuming a uniform strain rate field. The method applies a distance weighted approach on a regular spaced grid and interpolates the strain rates from sparse velocity measurements (Shen et al., 2007). Figure 5 shows the extension rate which reaches the maximum areal value (in red) out of the Matese massif. We also attempted to estimate the coseismic deformation related to the December

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29, 2013 event. The time series of 15 non-permanent stations (Table 3) shows significant offsets. The horizontal components are reported in Fig. 6.

The offsets were estimated from GPS time series by interpolating station positions

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at earthquake epoch using the estimated interseismic velocities of each site. The horizontal coseismic displacement field shows a sub-radial trend. Larger

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displacements are present in the NE portion of the Matese massif: RMAN moved

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toward N by about 3 cm, RORA, BOIA, BARA, CAMC, SEPI and GURE moved NEwards between 0.7 and 2 cm. These main displacements are on average perpendicular to the North Matese Fault System NW-trend that border the karstic

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massif. The permanent site ALIF, SACR, LNGN, VAGA; PTRJ (the last three

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located within the massif) do not show displacements.

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4. Discussion

4.1- Interseismic data

The puzzle of geophysical frame of Apennine chain as an extension style deformation, seismicity distribution, normal faulting, uplift, degassing is driven to Wdipping subduction and eastward progression of the back-arc basin-accretionary wedge-foredeep complex. The retreating of the subduction hinge has been 9

interpreted as due to the push generated by the eastward wedge mantle flow (Doglioni, 1991) and the spreading of the Tyrrhenian Basin (Luongo et al., 1991; Milano et al., 1994). The processes ascribable to delamination processes are active (De Astis et al., 2006; Improta et al, 2014; Di Luccio et al, 2018). A portion of the seismicity is due to dynamics of the eastward underlying mantle wedge flow located at a depth of 20 to 40 Km (Ventura et a., 2007; Improta et al, 2014). The deformation across the Apennine chain is therefore due to several contributions:

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from fault loading, decoupling between lithosphere and asthenosphere, viscous deformation along the shear zone into the crust, to historical earthquakes, fluid intrusions, and phases of groundwater recharge/discharge.

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Giuliani et al. (2009) estimated 4-5 mm/yr extension accumulated on NMFS and AIF.

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and those estimated in this work.

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Here, we use and show all the available velocities: those from Giuliani at al. (2009)

To compare our result with those from Giuliani et al. (2009), we considered two profiles traversing the southern Apennines with the corresponding velocity

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projections (Figs. 2 and 4). The profile b, crossing Venafro and Alto Molise Mounts (Fig. 4b), drawn and described in Giuliani et al., 2009, and augmented with the new

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CGPS and SAGNet network shows here a velocity difference of 1.90.3 mm/yr

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between the Tyrrhenian and Adriatic domains separated by the Alto Molise Mounts. The velocities in both profiles (Figs. 3a and 3b) appear quasi-steady inside each tectonic domain, Tyrrhenian and Adriatic. The extent of the two domains is 80 and 60 km respectively. A narrow ramp (< 10 Km) characterizes the transient between the velocities of the two domains in profile 3a, while along the profile 3b the available dataset does not allow to define with more details the distance interval of

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the velocity transition between the two domains. Therefore, our increased detail allows to evidence that the velocities change in a narrow band, and the highest values of strain rate is accumulated there. The projected velocities on profile 3a display a variation of 2.00.3 mm/yr on about a 10 Km interval that correspond to a strain-rate of (20030) x10-9yr-1. Profile 3b shows the same variation of velocities on a distance of about 15 Km, and the strain rate is (13020) x10--9yr-1). These values are comparable with those from previous

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studies along the Apennine chain (Devoti et. 2011; Palano et al., 2011; D’Agostino, 2014) if uncertainties are taken into account.

Finally, we explored in detail the small variations of velocities inside the Tyrrhenian

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domain by considering a second order velocity pattern. The estimated strain rate is 10-15x10-9yr-1. This value represents is smaller of the average uncertainty value on

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the strain rate, for this reason we consider the estimated strain rate as not

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significant. Moreover, no clear correlation is observed between this velocity gradient and the inner fault systems of the Matese massif.

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The maximum relative geodetic extension does not follow the maximum topography chain but the transient is shifted toward the outer belt. The range of transient

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deformation, along the two profiles, suggests that the strain is accumulating at shallow depth (8-15 Km) along the western flank of Alto Molise and Sannio Mounts.

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The driving mechanism could be a creeping dislocation along the antithetical normal NMFS where the ongoing activity has been recognized also by recent 1997-98 and 2014-2016 seismic sequences and by paleoseismological investigations (Galli et al., 2017). To understand the interactions between competing sources of deformation, we focus our results under the light of other geophysical data (Fig.4).

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(I)

The diffuse CO2 degassing area in the Sannio - Matese area corresponds

roughly with the GPS transient between the two domains. The diffuse deep CO2 degassing area is expanding in the western portion of the Apennine until the boundary with the foreland region. The CO2 flux affects the inner and axial portion of the Apennine chain (Chiodini et al, 2004; Ventura et al., 2007). Recent study (Ascione et al., 2018) shows that the maximum flux is located along western portion of PMF fault system. The recent seismicity (1981-2016) shows that most events occurred in the

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(II)

eastern Tyrrhenian domain are located at depths <15 km in the overriding plate. Deeper earthquakes (20-30 Km) are generally located east of the outer belt,

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corresponding to the Adriatic crust where the CO2 flux decreases (Ventura et al., 2007). The deep seismic sequence 2013-2014 represents a peculiar swarm

Tomographic studies show a complex crustal southern Apennine structure

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(III)

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because it is located in the axial belt.

(Bisio et al., 2004; Improta et al., 2014; Di Stefano & Ciaccio, 2014) with a pronounced heterogeneity. In particular, the heterogeneity is located beneath the

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Matese massif. Below 9 km, a lower Vp is present, probably representing the ending of the low-Vp region encircling the Neapolitan volcanic district (Improta et al., 2014).

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Negative anomaly of Vp/Vs in the middle crust has been interpreted as a thermal-

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fluid anomaly caused by the upwelling of the hot Tyrrhenian mantle wedge beneath the Apennines (Chiarabba & Chiodini, 2013).

4.2 “Co-seismic” data The GPS displacements observed after 29 December 2013 earthquake have shown a NE-trending of sub-radial distribution around the Matese massif (Fig. 6).

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Seismological analysis on 2013-2014 Matese sequence have shown some peculiar features: i) the rupture velocity is lower than other Italian normal fault earthquake (ii) the rupture length is shorter than the theoretical predicted for a Mw5 iii) the vertical clustered seismicity distribution; iv) a subcircular-shaped attenuation zone is around the hypocentral area (Fig. 4a). These last seismological data have suggested that the 2013-2014 sequence could be due to a pulse of deep magma within the lower crust from the South Apennine mantle wedge (Convertito et al., 2016; Di Luccio et

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al., 2018). The overpressure of rich fluid of CO2 may have triggered the earthquake controlling the nucleation, reactivation of normal faults, and development of a mesh of fault-fractures (Sibson, 2000; Di Luccio et al. 2018). The migration of pressurized

generate the pattern of displacements.

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volumes CO2-rich fluid due to a vertical pulse of magma could have contributed to

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We have attempted to model the estimated GPS displacements using a simple

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tensile source in elastic, homogeneous and isotropic half-space (Okada, 1985). We have defined the computational domain considering the source free of positioning. The coordinates used are that of Mw 5.0 mainshock. The height a.s.l. of GPS

topography.

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stations was also considered in the inversion, in order to minimize the effects of

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For the retrieval of the source parameters left free (Table 4) we used a non-linear

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inversion algorithm based on the Levenberg–Marquardt least-square approach (Levenberg 1944; Marquardt 1963) modified with multiple restarts to better identify the global minimum of the cost function. We tried to invert the GPS data using the source parameters available on http://terremoti.ingv.it/event/2874261 assumed uniform slip. The results do not show a good match. We inverted the GPS data considering a to tensile source opening; the modelled results are show in Table 4

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and Fig. 6. The displacements predicted by this model are significantly in better agreement with the observed data, especially in the north-eastern and central sectors of the massif. Opening value as calculated has a good reliable if estimated as P using the relation (Gudmundsson, 1999; Schultz, 1995):

DP =

W ×E

(

2L 1- n 2

)

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where W is the modelled open, E is the Young’s modulus of crystalline basement, L is the length of the modelled faults and  is Poisson’s ratio.

Assuming that the static Young’s modulus of the crystalline basement is E=50 GPa

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(Schulz, 1995) and = 0.25 (Schultz, 1995), we obtained an increase fluid pressure

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of 13 6.9 MPa as responsible for part of GPS displacements. The order of magnitude of this value, with its uncertainties, is comparable with the pressure

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required to activate crack opening and shear failure as suggest in Di Luccio et al. (2018).

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Recent studies have shown that the process of loading and circulation water into karst aquifers is able to produce significant deformation (Devoti et al., 2015; Silverii

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et al., 2016 2018; Devoti et al. 2018) due to annual, seasonal and daily signals. We have analyzed the data of five hydrological stations close to the Matese massif

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to understand if there were significant rainfalls before the seismic event (Fig. 7, data from http://www.protezionecivile.molise.it/centro-funzionale/la-rete-meteo-idropluviometrica.html; http://centrofunzionale.regione.campania.it). During December 2013, the daily amount of rainfall shows significant events on 1, 2 and 26 December, in particular, the Campitello Matese station, located in the center of massif, recorded about 120 mm of rain just 3 days before the event. 14

These data could suggest that a portion of the "co-seismic" deformation recorded by GPS can be induced by the rainfall events as reported by Devoti et al. (2015) and Devoti et al. (2018) where extreme rainfall events in fractured limestone with fractures parallel to the tectonic structures can induce significant horizontal deformations of the order of several mm. Further data are needed to investigate in detail this hypothesis.

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5. CONCLUSION The combined GPS data collected in the time span 2002-2013 by the networks

SAGNet and CGPS allow us to obtain a detailed horizontal velocity field. We have

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detected two GPS velocities domains: Tyrrhenian and Adriatic domains.

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The extension rate (2 mm/yr) estimated across this boundary is consistent with values known in Central Apennine by other studies (Devoti et al. 2011; Serpelloni et

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al., 2005; Galvani et al., 2012), while is lower than the value of 4-5 mm/yr reported by Giuliani et al., (2009). Our data display an extension rate and size of transient

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signals mostly constrained thanks to the SAGNet and the new CGPS sites. We observed that the maximum of extension rate does not follow the topographic

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high of the chain but is shifted toward the eastern outer belt. The tip of the creeping dislocation is located at a depth ranging between 10 and 15

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km along the NMFS-BBF associated with the Apulian sedimentary layers (Improta et al., 2014). NMFS-BBF striking NW-SE tectonic structure represents an important kinematic juncture, which is affected by a large strain rate between 130 and 200 x10-9yr-1. Historical and recent earthquakes are generated by the NMFS-BBF (Galli & Naso, 2009; Galli et al., 2017; Milano et al., 2005).

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No significant GPS deformation corresponding to inner faults systems of the Matese massif is detected. The GPS velocities appear relatively steady there. We have observed that the GPS transient follows roughly the CO2 degassing into the overriding accretionary prism enclosed by NMFS-BBF, and follows roughly the boundary between Tyrrhenian and Adriatic plate (Di Stefano & Ciaccio, 2014). Geochemical investigations evidence the importance of permeability of the Matese massif and its crucial role concerning the circulation of deep fluids or mineralized

not due at a usual deformation of extensional style.

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water. On the basis of the observations we suggest that the 2013-2014 sequence is

Moreover, the observed displacements recorded after the mainshock of December

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29, 2013 could be explained by a NW-trend tensile source where the main

deformation is toward NE. The tensile source is a simplification of the networks of

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fracture and fault systems where the regional stress and pressurized deep fluid are

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acting. Rupture processes are favored when fluid overpressure occurs an additional effect due hypothesized magma pulse to the 29 December (Di Luccio et al., 2018). Our data suggest that GPS displacements contain the contribution of CO2 fluids and

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rainfall and water infiltration paths.

The SAGNet GPS data archive will allow the integration of this data with other GPS

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networks, and will contribute to improve the assessment of seismic hazard.

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The dense SAGnet network has shown how it is possible to obtain a detailed velocities field useful for the study of hazard scenarios. Other not permanent networks have been fundamentals to study the coseismic effects (Anzidei et al., 2009). We think that our results even in combination with other independent data, can support further studies for the assessment of tectonic hazard of this active region of Apennine chain.

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Funding: This work was supported by INGV and DPCS1-C1 - 2012-2021

Author contributions: V. S. proposed the study and designed the SAGNet network. F.O. planned the initial geodetic network related to European Project "Earthquakes prediction in tectonic active areas using space techniques". V.S., A.G., G.B., P.D.M,

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M.D., F.O., U.T. and A.M collected GPS data during surveys. E.C. contributed to historical seismicity. A.G. and P.D.M analyzed the GPS data and, together with G.P. and F.R., planned the combination of GPS networks. A.G. and G.P. wrote

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methodological paragraphs. S.A. inverted GPS data to modelled the source. A.E.

Declaration of interests

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discussions from all the Authors.

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wrote the manuscript, coordinates and provided the interpretation with inputs and

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☒ The authors declare that they have no known competing financial interests or personal relationships that could have appeared to influence the work reported in this paper.

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☐The authors declare the following financial interests/personal relationships which may be considered as potential competing interests:

Acknowledgments: R. Devoti, F. Di Luccio; G. Ventura, R. Di Stefano and L. Improta for useful discussions and suggestions. D. Winterhalter for patient revised of manuscript. Beatriz Briuzela for support. D. Becker, Navigation Institute - University of Stuttgart for GPS surveys from 1994 to 1996. We thank Prof. A. Ganas and anonymous review for the constructive comments to improve the manuscript.

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deformation. J. Geophys. Res. 100, 3885–3894. Ventura G., Cinti F. R., Di Luccio F., Pino N. A., 2007. Mantle wedge dynamics versus crustal seismicity in the Apennines (Italy). Geochem. Geophys. Geosyst. 8, Q02013, doi:10.1029/2006GC001421.

Data and material availability:

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ftp://ftp.ingv.it/pro/SAGNet

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Figure caption

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Fig. 1 - GPS networks, crustal seismicity and quaternary fault sistems. Black triangles CGPS, red triangles SAGnet stations, green triangles Other networks. Seismicity with magnitude larger 2. The colored dots indicate the most significant seismic relocated sequences from 2013 to 2016 (Di Luccio et al., 2018). The 2013-2014 as purple and the 2014-2016 as blue. Grey and black dots indicate seismic sequence from ISIDE database (http://iside.rm.it). Black Square represents Historical Heartquakes from http://emidius.mi.ingv.it/CPTI15-DBMI15/. Yellow Star indicates the mainshocks of 201312-29. Quaternary Fault System (red lines) SPIF - San Pietro Infine Fault (Boncio et al., 2016); PMF - Piedimonte Matese Fault (Boncio et al., 2016, Ferranti et al., 2015); SGF San Gregorio Fault (Ferranti et al., 2015); MLF - Matese Lake Fault (Boncio et al., 2016); AIF - Aquae Iuliae Fault (Galli e Naso, 2009);NMFS - North Matese Fault System (Ferranti et al., 2015, Galli e Naso, 2009, Galli e Galadini, 2003, Di Bucci et al., 2002). Dashed red line ORL - Ortona Roccamonfina Lineament.

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Fig. 2 - GPS velocity field with respect to a non-moving Adriatic plate. Black arrows CGPS, red arrows SAGnet station, green arrows Other networks. Velocity ellipses represent 1sigma confidence error regions. Yellow Star indicate the mainshocks of 2013-12-29. Dashed black lines show the traces of the velocity profiles reported in Fig. 4

Fig. 3 – SAGnet archive and data analysis time span

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Fig. 4 - GPS velocities profiles. Black triangles CGPSstations. Red triangles SAGnet stations. Green triangles Other networks stations. Orange line extension along “a” profile. Green dashed line CO2 flux modified from Ventura et al. (2007) and Ascioni et al. (2018). Colored dots crustal seismicity sequence M>2 from 2013 to 2016 by http://iside.rm.ingv.it 2013-2014 as purple and the 2014-2016 as blue seismic sequences. Yellow Star the mainshock of 2013-12-29. Geological section modified from Roure et al., (1991).

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Fig. 5- Extension-rate map obtained from an interpolation of the velocity field.

Fig.6– Best fitting of GPS displacements. Observed data: Red arrows SAGnet stations. Black arrows CGPS. Modelled data: blue arrows. Yellow Star: the mainshocks of 2013-1229. Light blue triangles: hydrological sites

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Fig. 7– Histogram monthly rainfall

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Table 1 - Velocity field dataset of the SAGNet and of the surrounding continuous GPS stations shown in Figure 2 Hei (m)

East mm/yr

sigE mm/yr

North mm/yr

sigN mm/yr

Up mm/yr

sigUp mm/yr

Delta-T (years)

41.3270 40.9309 41.1097 41.5461 41.5604 41.0281 41.1947 41.5977 41.9844 41.2811 41.9735 41.5131 41.0670 41.0728 41.5995 41.8104 41.5005 42.0469 41.7060 41.3712 41.1461 41.0469 41.9549 42.1644 41.0312 42.1243 42.0111 41.7174 41.2234 41.3643 41.7035 41.3975 41.4068 42.0479 41.7404 41.7666 41.4154 42.1104 41.8696

167.7 921.2 554.2 1004.7 739.0 1066.3 142.4 904.4 849.7 117.4 404.7 470.8 404.4 499.9 550.7 434.7 1069.7 816.5 163.0 1072.6 375.6 100.8 729.2 287.6 714.6 571.9 280.6 850.4 588.3 1113.1 1018.0 847.1 100.6 474.1 244.5 599.4 784.8 209.8 1045.8

-1.1 -2.2 -2.4 -0.6 -0.4 -1.7 -2.8 -0.5 -1.6 -1.2 -0.2 -0.5 -1.7 -1.8 -1.1 -0.2 -0.5 1.0 -1.6 -0.9 -2.6 -1.9 -0.7 -1.8 -1.9 0.6 0.2 -2.7 -1.4 -1.0 -0.8 -2.6 -2.2 -0.3 0.1 0.5 -2.8 0.1 -1.3

0.8 0.8 1.2 0.5 0.8 0.5 0.9 0.6 1.1 0.7 0.5 1.0 0.1 0.5 0.8 0.6 1.4 0.8 0.8 0.5 0.6 0.9 1.0 1.2 1.0 0.6 1.2 0.9 0.6 0.6 0.5 0.5 1.3 0.6 0.7 0.5 0.5 0.6 0.3

-0.9 -0.4 -1.0 -0.1 -0.4 -0.1 -1.1 -0.3 0.0 -2.7 0.1 -0.1 -0.9 -0.7 1.1 0.5 -1.7 -0.1 -0.3 0.6 -1.7 -0.9 -1.0 0.8 -1.7 1.1 -0.2 -1.8 -0.9 -1.0 -0.5 -1.0 -1.0 0.0 0.1 0.2 -1.6 -0.4 -0.9

0.6 0.6 0.9 0.4 0.6 0.4 0.7 0.4 2.2 0.5 0.4 0.7 0.2 0.3 0.7 0.5 2.0 0.6 0.5 0.4 0.4 0.7 1.6 1.2 0.7 0.4 1.4 1.3 0.4 0.4 0.3 0.3 1.4 0.5 0.5 0.3 0.4 0.4 0.3

-2.0 0.9 0.8 0.3 1.7 1.0 -0.2 0.9 4.3 1.3 0.0 0.1 0.9 0.8 0.4 0.2 0.0 -2.9 -0.2 0.3 0.3 -0.3 0.3 0.4 0.8 0.2 -0.1 1.2 0.3 0.6 0.4 1.1 2.1 -2.8 -0.3 0.1 1.4 -1.6 3.0

1.8 1.7 2.6 1.1 1.7 1.2 2.0 1.3 4.3 1.5 1.1 2.2 0.3 1.0 1.9 1.4 3.6 1.7 1.6 1.2 1.3 1.9 3.4 3.0 2.2 1.3 3.3 2.9 1.2 1.3 1.0 1.0 2.9 1.4 1.5 1.0 1.2 1.3 0.8

5.3 5.5 3.9 8.8 5.9 8.1 4.9 7.4 10.8 6.1 8.3 4.5 -1.0 9.6 5.5 7.2 7.6 5.7 6.0 8.1 7.5 4.9 4.7 3.7 4.2 7.4 4.3 6.8 7.8 7.3 9.4 9.6 4.5 7.4 6.6 9.2 8.8 7.4 13.0

n/a

-1.2

0.8

0.9

0.0

0.4

6.0

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IGM 95 (from Giuliani et al. 2009) 1531 14.3890 41.9330

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lat ∞

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SITE lon ID ∞ CGPS located in figure 2 ALIF 14.3346 ANGE 15.1839 AV01 15.0827 BSSO 14.5940 CABA 14.6784 CAFE 15.2366 CARI 13.9742 CERA 14.0180 CVAL 13.8113 FORM 13.6994 FRES 14.6693 GATE 14.9099 GRO1 15.1009 GROT 15.0599 ISER 14.2355 LARI 14.9221 LNGN 14.2526 LPEL 14.1832 MELA 15.1271 MOCO 15.1586 MODR 13.8808 NICO 14.3274 OTRA 13.6459 PAGL 14.4981 PAOL 14.5675 PBRA 14.2285 PETC 14.8600 POFI 13.7119 PSB1 14.8107 PTRJ 14.5289 RNI2 14.1524 SACR 14.7058 SGL1 13.7655 SMRA 13.9241 SPCI 15.2595 TRIV 14.5502 VAGA 14.2343 VTRA 14.7079 VVLO 13.6232

-1.7

30

41.7880 41.7120 41.9220 41.7600 41.9650 41.7820 41.5420 41.4040 41.5870 41.4650 41.4380 41.5790 41.6950 41.6680 41.7090 41.1430

n/a n/a n/a n/a n/a n/a n/a n/a n/a n/a n/a n/a n/a n/a n/a n/a

0.7 -2.0 0.5 -0.2 0.7 -0.4 -1.3 -3.6 -1.7 -0.8 -2.7 -1.5 -1.6 -1.6 0.3 -4.6

0.7 0.9 0.8 1.2 1.1 1.4 0.7 1.2 0.8 0.9 1.0 0.7 1.1 0.9 0.8 1.0

-0.3 -1.2 0.6 -0.6 -0.9 0.2 -0.8 -2.7 -0.3 -0.9 0.1 -1.2 0.5 -0.9 0.3 -2.1

SAGNet BALA BARA BOIA CAMC CERM COAV CUSA ISCM LETI PIMA PRTL SGMA TELE LAGA MORC RMAN VAIR SCON

14.2732 14.5596 14.4699 14.5020 14.7371 14.1129 14.5023 14.2067 14.2526 14.3297 14.1432 14.3793 14.5267 14.4343 14.6042 14.3488 14.1007 14.0372

41.2900 41.5262 41.4678 41.4484 41.4569 41.6096 41.3420 41.6447 41.4538 41.3399 41.4151 41.3872 41.2225 41.4339 41.3549 41.4966 41.3599 41.7589

173.0 672.9 966.8 816.2 1129.8 615.5 556.8 802.4 1101.6 176.0 716.7 939.3 115.0 1678.2 1218.8 995.6 199.3 1300.3

-2.5 -0.9 -1.3 -0.4 -0.9 -1.0 -1.6 -1.0 -0.9 0.9 -1.0 -0.8 -1.2 -1.0 -2.1 -0.7 -2.4 -0.7

0.6 1.5 0.9 1.0 1.0 0.7 1.0 0.9 1.0 1.0 0.8 0.6 0.9 1.0 0.8 0.7 0.9 1.0

-1.5 -2.7 -2.9 -2.4 -0.5 -0.7 -1.7 -0.1 -1.8 -2.0 -1.3 -1.9 -1.8 -0.8 -1.8 -3.3 -2.0 -1.0

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0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

0.4 0.5 0.4 0.6 0.5 0.7 0.4 0.6 0.4 0.4 0.5 0.3 0.5 0.4 0.4 0.5

12.9 12.9 12.8 4.6 6.0 8.7 12.9 12.9 12.9 12.9 6.1 12.9 5.0 5.0 5.0 6.0

0.9 1.9 1.9 1.9 2.2 1.4 2.0 1.8 2.0 2.1 1.7 1.2 1.7 2.1 1.6 1.2 1.8 2.1

0.4 -1.0 -2.6 3.2 0.2 4.5 1.1 2.9 0.5 -4.0 2.1 -0.1 -2.2 -0.7 0.7 -0.4 2.7 8.7

1.9 4.4 3.8 3.8 4.4 2.8 3.9 3.5 4.0 4.2 3.3 2.4 3.5 4.1 3.1 2.5 3.5 4.2

10.4 3.4 10.3 12.6 10.3 10.3 10.4 10.4 10.2 10.2 10.7 12.3 10.3 10.2 12.5 12.3 10.3 10.2

Jo

ur

na

0.8 1.0 0.9 1.3 1.2 1.5 0.8 1.4 0.9 0.9 1.1 0.8 1.2 1.0 0.9 1.1

ro of

14.3060 14.1390 14.8150 14.7370 14.5340 14.5520 13.9370 13.8910 14.3260 14.3990 14.0330 14.1270 14.8320 14.9440 14.8000 13.8580

-p

1532 153X 1541 1542 1543 154X 1601 1602 1611 1612 1613 1614 CGUA CROC LESE MS01

31

Table 2 Adriatic Eulerian pole parameters Normalized χ2 1.58 rotation rate (deg/Myr) 0.40 ± 0.31 latitude (deg) 62.059N longitude (deg) -52.204 E semi-major axis of error ellipse (deg) 110.5 semi-minor axis of error ellipse (deg) 0.4 azimuth of semi-major axis (deg) -92.1

ro of

Table 3 - Horizontal coseismic displacements with 68% error ellipses East

E

North

N

Up

Up

ID

(m)

mm

mm

mm

mm

mm

mm

SAGNe t BALA 14.2732 41.2900

173.0

0.3

1.6

-1.2

1.9

60.2

7.5

BARA

14.5595 41.5262

672.9

3.0

2.3

18.5

2.5

6.5

10.0

BOIA

14.4699 41.4678

966.8

17.5

2.0

16.0

2.3

8.4

9.2

CAMC 14.5020 41.4484

816.2

2.4

3.5

14.1

4.4

-27.1

17.5

CES1

14.6195 41.2861

923.5

-2.2

4.6

3.4

5.5

1.5

22.0

CUSA

14.5023 41.3420

556.8

10.2

3.6

-6.3

4.4

-9.4

17.7

GURE

14.5617 41.4448

744.4

6.1

2.1

4.1

2.5

15.5

10.2

LETI

14.2526 41.4538

1101.6

2.8

2.9

-4.3

3.4

8.0

13.5

MORC 14.6042 41.3550

1218.8

10.1

3.2

2.4

3.9

-15.7

15.4

MTRD 14.1848 41.5223

659.6

-8.4

3.8

-4.0

4.1

-52.8

18.2

re

lP

na

lat

14.3297 41.3399

176.0

2.3

3.3

-13.2

3.8

37.7

15.6

RMAN 14.3487 41.4965

995.6

0.2

2.0

32.7

2.4

31.5

9.2

RORA

14.1195 41.5285

477.7

10.2

3.4

17.7

4.0

-31.7

16.1

SEPI

14.6181 41.4294

607.5

13.6

4.3

18.6

4.9

-37.5

22.3

SGMA 14.3793 41.3872

939.3

2.2

2.0

-6.9

2.4

4.4

9.5

Jo

CGPS

ur

PIMA

lon

-p

Hei

SITE

ALIF

14.3346 41.3270

167.7

0.0

1.0

-2.5

1.0

4.8

3.5

LNGN

14.2526 41.5005

1069.7

-0.3

1.0

2.7

1.0

7.3

3.5

PTRJ

14.5289 41.3643

1113.1

-0.5

1.0

-1.5

1.0

0.0

3.5

SACR

14.7058 41.3975

847.1

-1.7

1.0

4.1

1.0

5.3

3.5

VAGA

14.2343 41.4154

784.8

-0.2

1.0

0.7

1.0

5.2

3.5

32

Table 4 - *the UTM coordinates refer to the source center, **the depth is the vertical depth of the top edge of the fault Width

Depth

Dip

Strike

East

North

Opening

m

m

m

deg,

deg,

m

m

m

5000

3000

8000**

66

280

452300*

4583300*

1.3

Jo

ur

na

lP

re

-p

ro of

Length

33