Abstract
In this study, an updated crustal velocity field for the Greece area was estimated using a time series analysis that covers a duration of 16 years (2001–2016) from 227 Global Navigation Satellite System (GNSS) permanent stations. The GPS processing was carried out using GNSS Analysis software at MIT (GAMIT) and the velocity field expressed with respect to Eurasian plate. For the time series analysis, we applied a robust Median Interannual Difference Adjusted for Skewness trend estimator to mitigate the effects of discontinuities due to geophysical phenomena on the estimation of geodetic velocities and their uncertainties. The main earthquake events that occurred in the GPS time series analysis in the study area are analyzed, providing the coseismic displacements in the permanent GNSS stations. We also compare our geodetic velocities with five previous publications, where we found consistency at the mm/year level, leading to reliable results for the geodynamic behavior of the Greek area, providing a dense velocity field.
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Introduction
The southeastern Mediterranean region, particularly Greek territory, is one of the world’s most earthquakeprone areas, with intense and complex geodynamic behavior. The Aegean Sea and its surrounding region are frequently referred to as a "natural laboratory of geophysics," due to a wide range of deformation mechanisms found in a relatively small geographical area. Since the advent of space geodesy, the tectonics of Greece have been extensively researched using both campaign acquired and continuous GPS data. The last decades the GNSS technique was a very important tool for studying the kinematics in plate boundaries, coseismic displacements, interseismic and postseismic deformation. The growth of international/regional GNSS tracking networks plays a key role that allows for better estimations about the crustal deformation. The earlier geodetic studies have been carried out since the late 1980s, using GPS campaign measurements to estimate the strain rates of the Aegean Sea on a large spatial scale or over long timescales. The first measurement campaigns are based on Satellite Laser Ranging (SLR) technique at six sites within the Aegean region since 1986 as part of WEGENER/MEDLAS network (Noomen et al. 1996; Plag et al. 1998) and GPS campaign type of observations. Most previous studies focus on tectonically active areas such as the Ionian Sea (Kahle et al. 1995; Rossikopoulos et al. 1998; Hollenstein et al. 2006; Ganas et al. 2013), the central Greece (Clarke et al. 1998; Chousianitis et al. 2013) and at the Gulf of Corinth (Briole et al. 2000; Avallone et al. 2004; Lazos et al. 2020), which is one of the most active rift within the Aegean region.
Methodology
This section begins with the GPS data analysis, where we specify the processing strategy that we follow in order to estimate the loosely constrained position solution. We then describe the methodology of the reference frame definition, providing the postfit statistics of the reference frame realization. Finally, the main seismic events that have an effect on our GPS time series analysis are represented, giving the estimated coseismic displacements.
Geodetic data analysis
We analyzed the GPS data of a dense GNSS permanent network of 227 European GNSS stations, among them 186 sites located in Greece, 10 in Bulgaria and 7 in Romania and 24 are part of the International GNSS Service (IGS) network. The geographic distribution of Greek GNSS permanent stations is illustrated in Fig. 1. More specific about the Greek GNSS network, 77 to HxGN SmartNet Greece operated by the Metrica SA (https://www.metrica.gr), 46 to Hellenic Position System (HEPOS, https://www.hepos.gr), 21 to the National Observatory of Athens (NOA) with 1 of them is in the contribution with National and Kapodistrian University of Athens (NKUA) known as NOANET (Ganas et al. 2008; Chousianitis et al. 2021), 18 to Dionysos Satellite Observatory (http://dionysos.survey.ntua.gr) of School of Rural, Surveying and Geoinformatics Engineering in cooperation with British Centre for the Observation and Modelling of Earthquakes, Volcanoes and Tectonics (DSO/COMET), 5 to HermesNet (Fotiou et al. 2009) managed by Department of Geodesy and Surveying (DGS) of the School of Rural and Surveying Engineering of Aristotle University of Thessaloniki (https://www.users.auth.gr/cpik), 5 to Corinth Rift Laboratory (CRL, http://crlab.eu), 1 station belongs to Centre National d'Etudes Spatiales (CNES), 1 to Institut National des Sciences de l'Univers (INSU/ENS), 6 to PPGNet (https://www.pecny.cz/CzechGeo/ppgnet) joint network of Geodetic Observatory Pecny—Research Institute of Geodesy, Topography and Cartography, PatrasCharles University (RIGTC GOP), 1 to Technological Educational Institute of Serres, 1 to Technical University of Crete and 4 to EarthScope (1 are with NOA).
The GPS data was processed for the time period 2001–2016, using GAMIT/GLOBK software release 10.7 (Herring et al. 2018aa; Herring et al. 2018b). We analyze daily RINEX data in a threestep approach to estimate station position, using doubledifferencing techniques to eliminate satellite and receiver clock errors. To enhance computation efficiency and consider the GNSS network geometry, the station distribution scheme was optimized into five separate subnetworks. The GNSS stations in each subnetwork are determined every day, based on station availability, and are chosen by geographic location to minimize station baseline lengths, which improves integer phase ambiguity resolution. Particularly, we select to divide the GNSS network following two criteria: (a) to minimize the baseline length between the stations and (b) to availability of the GNSS stations. Some of the most common issues that occurs on geodetic network design concern on:

Reference frame definition through the estimation of position coordinates on fiducial sites of the geodetic network.

The network geometry, ensuring the optimal observation selection.

The definition of weights in observations, as formed in the weight matrix.

The densification of local GNSS network, starting with fundamental control networks, i.e., IGS Permanent network.
The location of the 24 IGS and 5 Greek European Permanent Network (EPN) stations is shown in Fig. 2, where used for reference frame definition. These stations coordinates and geodetic velocities are precisely determined by international services such as IERS and IGS and used to connect the five local individual subnetworks (see Fig. 3).
As a first step of GPS data processing, a weighted least squares algorithm was used to estimate the station position and satellite orbit parameters, imposing proper constraints to a priori station position coordinates at the level of \(0.05\mathrm{ m}\) to aid phase ambiguity resolution. Integer phase ambiguities are generally well resolved in all the subnetwork solutions, with greater than 94% in wide lane and greater than \(90\%\) in narrow lane of ambiguities are resolved, based on Dong and Bock (1989) methodology.
Figure 4 shows the time series of the percentage of resolved phase ambiguities, in narrow lane for each subnetwork. Notably, the ambiguity resolution for the NOANET (see Fig. 4e) exhibits a lower level in the early years of its processing, primarily attributed to the limited number of GNSS stations available. It is important to emphasize that the solution generated using the IGS precise orbits which become available, with a latency of 12–18 days, where the orbital parameters are adjusted in 24 h arcs. Then loosely constrained solutions from each individual subnetwork were combined into daily, providing a single fullnetwork solution using GLOBK. The reference frame realization was implemented on ITRF2014 (Altamimi et al. 2016) using as fiducial points 24 IGS stations (see Fig. 2), which are located in the surrounding area, in European plate. These sites selected consider the optimal geographic distribution of the GNSS network, the completeness of the observations, and the contribution of these GNSS stations to IGS network. Most of these sites are colocation with other satellite techniques (VLBI, SLR, DORIS).
The GAMIT software uses the LC or L3 ionospherefree linear combination of GPS phase observables by applying a doubledifferencing technique to eliminate phase biases related to drifts in the satellite and receiver clock oscillators (Fotiou and Pikridas 2012). Tropospheric refraction significantly affects the high performance of GPS position estimations with impact mostly on height component, to reduce it we use the GPT2 model for a priori atmospheric parameters (Lagler et al. 2013) and Vienna Mapping Functions 1 (VMF1) grids (Boehm et al. 2006). VMF1 includes the meteorological coefficients as derived from gridded reanalysis of European Centre for MediumRange Weather, improving the Zenith Wet Delay (ZWD) estimations. The residual zenith wet delays were adjusted at 2 h intervals using piecewise linear function with process noise uncertainty constraint of \(20 \mathrm{mm}/\sqrt{\mathrm{hr}}\), gradients also estimated in the same interval with a priori constraint of \(10 \mathrm{mm}\) at \(10^\circ\) elevation angle. Tidal effects such as solid Earth tides, ocean loading, pole tide, atmospheric loading, and geocenter motion can significantly bias the position estimations and consequently velocity estimation in GNSS stations. To minimize these influences of temporal changes that can be driven to unrealistic, we comply the international recommendations following the IERS Conventions 2003 (McCarthy and Petit 2004). Most predominant tidal forces in semiannual and annual periods are modeled in the GPS data analysis. The Ocean tide effect can be well calculated using the ocean tide model that can provide by Chalmers University of Technology due to the web service (http://holt.oso.chalmers.se/loading). In our analysis, for ocean tide loading effects we apply the FES2004 model (Lyard et al. 2006), including corrections for center of mass motion. Regarding nontidal atmospheric loading component, we applied the methodology that is described by Tregoning and van Dam (2005).
There are two types of antenna phase center calibration models, the absolute and the relative model provided by NOAA’s National Geodetic Survey (NGS). IGS absolute phase center variations models (IGS08_1930.atx) for satellite and groundbased GNSS antennas are adopted, improving the position estimations and reducing the systematic errors on long intercontinental baselines that they have found in the relative phase center variation (PCV) model. It must be noted that in short baselines, the relative PCV model do not have negative impact on position estimations. Below, we provide the most important processing models that we adopt in our strategy (listed in Table 1), including the atmospheric delay and mapping functions, tide, and tidal loading models. Aside from the applied models, we document the principal processing parameters that we use following the IGS/EPN recommendations.
Reference frame definition
The geodetic network adjustment was carried out following the sequential least squares approach, applying the stacking of normal equations (Dermanis and Fotiou 1992). The estimated parameters are independent of each other and have been derived by imposing loosely constraints to stations coordinates, orbital solutions and earth orientation parameters (EOP). The observation equations for the \(k=\mathrm{1,2},\dots\) GNSS subnetworks are written as:
or, in more general notation:
where \({\mathbf{x}}\) is the vector of unknown parameter improvements, not only the station coordinates, and \({\mathbf{A}}\) is the matrix of given coefficients with full rank, as called design matrix and with \(mathbf{v}\) the vector of observational errors. Here, \(\mathrm{C}\) is the covariance matrix for each \(k\) subnetwork, where the positivedefinite weight matrix is expressed as \(\mathbf{P}={\mathbf{C}}^{1}\) for the \(\mathbf{b}_{k}\) observation vector.
We assume that each observation series was independent between them, and the observation errors \(\mathbf{v}\) were characterized as normal random errors following the Gaussian or normal distribution.
The normal equation matrix for each \(k\) independent series \(\left(i=\mathrm{1,2},\dots k\right)\) becomes:
which can also be written in a more analytic form for each \(k\) independent series:
where the solution of the normal equations is:
Equivalent can be expressed as:
respectively, as:
The observation equation can be expressed using the linearized form of the pseudoobservations, for all the parameters at the epoch \(\mathrm{t}\) as:
where \({\mathbf {b}}_{t}\) is the vector of the differences between the observations and the a priori values, \({\mathbf{A}}_{t}\) is the design matrix, which contains the partial derivatives of each observation with respect to each parameter, and \({\mathbf {x}}_{t}\) is the estimated unknown parameters with \(E\left\{ {\mathbf {v}_{t} } \right\} = 0\), \(E\left\{ {\mathbf {v}_{t}\mathbf {v}_{t}^{T} } \right\} =\mathbf {V}_{t}\), \(E\left\{ {\mathbf {v}_{t} \mathbf {v}_{t + 1}^{T} } \right\} = 0\).
For the reference frame definition, we use a 7parameter Helmert transformation (HT), where the resulting geocentric coordinates of the GNSS sites are transformed to an a priori reference frame (i.e., ITRFyy), using fiducial control points in the central European plate. Minimum constraint conditions are based on the assumption that there are two reference frames, where the geocentric coordinates of each \(i\) station are known. Helmert transformation (HT) is a key tool that relates to reference frame definition and its parameter estimates may be affected by the network distribution, with the magnitude of these being an indication of the consistency between the solutions. Figure 5 shows the HT residuals in topocentric coordinate system and the postfit RMS.
The a posteriori RMS error of the 7parameteres Helmert transformation is \(1.8 \pm 0.7 \mathrm{mm}\), and these statistical values of the reference frame definitions maintain the consistency with the ITRF2014 solutions.
Preanalysis of the time series
It is well known that the appearance of discontinuities in the position time series has a significant impact on the estimation of geophysical signals. They typically result from changes in the equipment of permanent reference stations or from geophysical phenomena (e.g., seismic phenomena), which cause significant changes in position that are spatially correlated with nearby stations. To mitigate this effect, GPS data are often filtered and processed to remove or correct for discontinuities. This can involve removing or adjusting data that are known to be affected by instrument errors or other artificial sources of discontinuity or using mathematical models to correct for discontinuities caused by natural events. We preanalyzed the GNSS observations using an automated algorithm for the quality check of RINEX files, to ensure the performance of the tracking of each constellation for the GNSS stations. Also, we search for antenna offsets due to equipment changes that have an impact to height estimation. Various previous studies have shown that twothirds of the discontinuities are caused by known factors such as geophysical sources (e.g., earthquake displacements), nongeophysical sources (e.g., equipment changes), and unknown factors (e.g., upgrading the receiver firmware or changing the antenna position). The remaining onethird of the sources that cause discontinuities in the position time series are unknown, potentially humaninduced, and related to changes in the GNSS data processing strategy or processing parameters such as the cutoff angle (Gazeaux et al. 2013).
To eliminate the effects in time series discontinuities due to (i) earthquake events and (ii) antenna/equipment changes, we use a Heaviside step function, where we separate the time series. In GPS data analysis, we have the choice to include these discontinuities initially in data processing step, as break offsets from each site in specific time or to include it on the next step of GPS time series analysis. Many previous studies focus on discontinuities detection methodology, providing an easyautomated algorithmic processes. In our analysis we use the findoffset program of the Hector software (Bos et al. 2013) to search for potential offset positions and estimate their sizes. In Fig. 6, we depict the peak ground velocity (PGV) as retrieved from United States Geological Survey (USGS) ShakeMap System (Worden and Wald 2016) and the GNSS sites that were available during the seismic event. Peak ground velocity (PGV) is a measure of the maximum velocity of ground motion (cm per second) caused by an earthquake event (EQ). It is used to evaluate the intensity of ground shaking and potential damage to structures. We should note that the most discontinuities are detected on the vertical component related to equipment changes and more especially with antenna changes. On the other hand, the estimated offsets due to coseismic displacements have in the most cases effect on horizontal component and depend on the nature of the fault which gives the EQ event. Herring et al. (2016) proposed the empirical formula that approximates the radius of influence of an earthquake, where \(d\) is the influenced radius from the EQ event in \(Km\).
Blewitt et al. (2018) propose an empirical formula that helps in identify the potential time series discontinuities caused by earthquake events, using a distance threshold which is calculated by the simple formula:
where \({M}_{W}\) is the magnitude of the earthquake and the distance \(r\) between the epicenter and the GNSS site expressed in km. It is essential to emphasize that (11) and (12) are exclusively utilized during the initial phase of earthquake offset detection in the GPS data preprocessing level, wherein they are properly integrated into the baseline solution processing step.
During the study period, 8 earthquake events had an impact and were detected on GPS position time series (see supplementary material), are those of Methoni 2008 February 14, Movri 2008 June 8, Efpalion 2010 January, Cephalonia 2014 January and February, Samothraki 2014 May 24, and Lefkada 2015 November 17. In Table 2, we describe in detail the most earthquake events that they have an impact on GNSS stations as recognized by daily position monitoring, with moment magnitude greater than \(5.3{ M}_{w}\). Also, Table 3 describes the coseismic displacements in topocentric coordinate system (east, north, up), as calculated for the mean position for approximately 10 days before and after the main seismic event, in nearly to the epicenter GNSS stations. The uncertainties of coseismic displacements are estimated for each component before and after the main shock by applying the law of error propagation to the uncertainties of the coordinates.
It is essential to specifically mention that Fig. 6a provides an encompassing view, incorporating four distinct earthquake events in Methoni, Movri, and Efpalion (2010/01/18, 2010/01/22). The Cephalonia doublet, comprising two earthquake events with magnitudes.
\({M}_{w}=6.1\) and \({M}_{w}=6.0\), is illustrated in Fig. 6b as a unified depiction of the coseismic displacements and the PGV values.
The postseismic effects, particularly for significant events, can persist over several years due to the extended relaxation time. As a result, these effects tend to smoothen over time and can become challenging to differentiate from the longterm velocity. In the Greek area, many studies focus on postseismic deformation using GNSS stations and InSAR techniques, which are occurred after strong earthquake events as in the case of 2015 Lefkada \(({M}_{w}=6.5)\) earthquake (Vallianatos and Sakkas 2021). In this study, we do not examine the postseismic deformation in GNSS site due to the larger events.
Geodetic GPS time series analysis
It was already known from previous studies that GNSS time series contain tectonic and nontectonic signals that we need to minimize due to the purposes of our research. Nontectonic signals refer to a variety of sources of movement or deformation of the Earth’s surface that are not directly related to plate tectonics or other geodynamic processes. These signals can include a range of natural and anthropogenic effects, such as atmospheric effects, ocean tides, and humaninduced subsidence. Besides, it is crucial to consider the presence of spatially correlated signals arising from two primary sources: commonmode signals (CMS) and commonmode errors (CME). Commonmode signals are associated with largescale processes, encompassing phenomena like solid Earth displacements, ocean and atmosphere effects, and satellite orbit mismodeling. These processes contribute to the emergence of correlated signals in the GNSS data. Conversely, commonmode errors stem from inaccuracies in processing, including mismodeling of displacements induced by various factors like solid Earth, ocean, and atmosphere, along with the occurrence of draconitic signals. By understanding and addressing both nontectonic signals and spatially correlated signals, we can refine our analysis and ensure the accuracy of our research finding.
To estimate the geodetic velocities and their realistic uncertainties from the daily position time series, we applied the robust Median Interannual Difference Adjusted for Skewness (MIDAS) trend estimator (Blewitt et al. 2016), which avoids detecting step discontinuities. MIDAS algorithm provides the most accurate estimations about the geodetic velocities and their uncertainties, as verified to blind tests on synthetic data (Gazeaux et al. 2013). MIDAS is a variant of the Theil‐Sen median trend estimator, which a nonparametric method for estimating the slope of a linear trend in a dataset. It was based on the median of the slopes of all possible pairs of data points in the dataset, rather than the mean of the slopes as in traditional linear regression. The median of slopes between pairs of data of the ordinary TheilSen estimator can be expressed as: \(\widehat{v}={\mathrm{median}}_{j>1}\left(\frac{{x}_{j}{x}_{i}}{{t}_{j}{t}_{i}}\right)\), where coordinate \({x}_{i}\) is sampled at time \({t}_{i}\). In particular, this process involves ordering the computation of the median trend using slopes from all selected data pairs and selecting the median as the estimated rate for the entire dataset. Additionally, the median absolute deviation (MAD) is calculated and multiplied by a constant 1.4826 to determine the standard deviation of the rates \(\sigma =1.4826\times MAD\), assuming that the differences between the rates and the median follow a Gaussian distribution. The velocity uncertainty is rescaled by \(1.2533/\sqrt{N}\), where \({\rm N}\) is the number of individual rates calculated within the program. The differences between the MIDAS and a simple linear regression model are very close in the level of \(1 \pm 1\mathrm{ mm}/\mathrm{yr}\) on GNSS stations without discontinuities on their position time series. We do, however, note the greater differences found on GNSS sites which are located in Santorini Island (NOMI, KERA), with differences greater to \(18\mathrm{ mm}/\mathrm{yr}\) on horizontal and \(8\mathrm{ mm}/\mathrm{yr}\) on vertical component, due to the inflation observed during the Santorini unrest of 2011–2012 that caused nonlinear ground motion as also observed in previous studies using GPS and InSAR (Papoutsis et al. 2013).
The geodetic velocities are expressed to the European Terrestrial Reference Frame 2000 (ETRF2000), which is an implementation of the European Terrestrial Reference System of 1989 (ETRS89), following the transformation formula (Altamimi 2018) to link ETRF89 to the ITRS for station velocities:
where \(\dot{X}_{{{\text{ETRF}}_{{{\text{yy}}}} }}^{i} , \dot{X}_{{{\text{ITRFyy}}}}^{i}\) is the 3D vectors of geodetic velocities in \(yy\) reference frame realizations, on ITRS and ETRS89 respectively. \(X_{{{\text{ITRFyy}}}}^{i}\) denotes the 3D position vector with respect to \({\text{ITRFyy}}\). The rotation rate parameters, \(\dot{R}x_{{{\text{yy}}}} , \dot{R}y_{{{\text{yy}}}} , \dot{R}z_{{{\text{yy}}}}\) about each axis of a (clockwise) Cartesian system, are the three components of the Eurasia Euler vector (or angular velocity) expressed in the \({\text{ITRFyy}}\).
Results and discussion
This section starts by describing the geodetic velocity field in Greece, using a longterm GPS time series analysis. Then, we evaluate our results with previously published studies, proving a more dense and accurate velocity field that can be used for a plethora of geodetic and geophysical studies.
Greek geodetic velocity field
The estimated horizontal velocities and their uncertainties with respect to Eurasia are shown in Fig. 7. The final geodetic velocity includes 215 GNSS stations out of a total of 227 initial process locations, with the exclusion of 12 sites due to a small time span of data availability. Velocities with respect to Eurasia plate selected because they can provide a clear view of the geophysical processes being performed on the crustal earth in Greek area. The role of the GPS velocities is very important on a plenty of geodetic applications as the semikinematic reference frame realization and for geophysical applications, providing the true deformation field. In semikinematic datum, the knowledge of the deformation is crucial from the timedepending transformation formula between the observed/measurement epoch and the reference epoch where the datum is referred (Bitharis et al. 2019). For the scope of geophysics, the velocity field has enabled extensive research into the accumulation of strain, plate coupling, and transient motion in various subduction zone configurations, as well as the examination of the relative significance of the various processes occurring within a subduction zone.
As a result, the northern part of Greece is more consistent to the stable European plate, with small horizontal velocities with mean magnitude less than subcentimeter. The velocities at the southern part of Greece are systematically greater than those that occurred in the northern part. Aegean Sea and more especially Crete Island are moving away from the most stable part of Europe with southwest direction and value of about \(3.2\mathrm{ cm}/\mathrm{yr}.\) We find a simple pattern with the magnitude and orientation of the velocity field, which confirms the role of the tectonic settings in the region, as the Hellenic Trench, the North Anatolian Fault (NAF), and the Cephalonia–Lefkada Transform Fault Zone (CLTFZ) in the central Ionian. The Aegean Sea and the southern part of Greece move westward along the bounding strikeslip faults, with primary tectonic setting the prolongation of the North Anatolian Fault (NAF), which controls the geodynamic evolution of region.
The vertical velocities and their uncertainties over the Greek territory are illustrated in Fig. 8. In contrast with the horizontal velocities, the vertical component does not show any predominant pattern. The magnitude is considerably smaller than the velocities in the horizontal component due to the geodynamic behavior in Greece.
The GPS vertical velocities are a very interesting product in sealevel applications and can be used as a correction term in vertical land motion (VLM) providing the absolute sealevel rise. The sealevel rise can be estimated using tide gauge records, which measure the change in sea level over time at a specific location in coast. However, tide gauge records are often limited in their spatial coverage and can be affected by local factors such as land subsidence or uplift. Satellite altimetry is another method for measuring sealevel change, which uses radar or laser instruments to measure the height of the sea surface from space. However, satellite altimetry data are affected by errors such as signal penetration through the atmosphere and ocean waves, and it is limited in the temporal resolution. By using GPS vertical velocities as a correction term, it is possible to correct for the effects of VLM on the measurements made by tide gauges or satellite altimetry, which can improve the accuracy of the sealevel rise estimates. Measuring and analyzing GPS vertical velocities is a challenging task that poses several limitations. These limitations include signal errors, spatial and temporal resolution, network density, processing techniques, and noise and outliers. To overcome these limitations, we need a longlasting time series (beyond 8 years), to minimize the impact of transient and seasonal signals on vertical geodetic velocities estimates as described by Masson et al. (2019). In Fig. 9, the dispersions on the horizontal and vertical components are illustrated.
It was interesting to notice that the uncertainties in vertical component were about three times larger in comparison with each horizontal component, due to seasonal effects that have mainly impact on vertical direction as known sources of tidal effects, surface mass distributions from the atmosphere, oceans, snow, and soil moisture. That reflects the larger uncertainties on the vertical component than the horizontal plain, with mean value \(0.6 \mathrm{mm}/\mathrm{yr}\) and \(0.4 \mathrm{mm}/\mathrm{yr},\) respectively.
Comparison with previous selected solutions
In this section, we perform a validation and quality assurance by comparing our estimated geodetic velocities with those obtained from previous studies. This comparison serves to verify the reliability of our analysis and ensure the consistency among the solutions and robustness of velocity field. We select previously published velocity solutions with the precondition that the various datasets complement one another. In the frame of EPN, three related Working Groups (WGs) provide geodetic velocities: European Dense Velocities Working Group (Chair: E. Brockmann), EPN Densification Working Group (Chair: A. Kenyeres), and Deformation Models Working Group (Chair: M. Lidberg). Since 2016, our research findings have been actively contributing to the European Dense Velocities Working Group and the Deformation Models Working Group, augmenting their efforts in understanding crustal movements and developing accurate geodetic velocity fields within the European region. The evaluation includes five velocity fields (England et al. 2016; Brockmann et al. 2019; Bitharis 2021; Briole et al. 2021; PiñaValdés et al. 2022), which are briefly described below. We conduct a comparative analysis by juxtaposing our results with those from previous studies that have employed diverse techniques in GNSS processing. Specifically, we consider studies that have utilized the precise point positioning (PPP) method and combined solutions derived from different processing schemas. By examining and contrasting these approaches, we aim to gain valuable insights into the strengths and limitations of our own methodology while enriching the understanding of geodetic phenomena in the context of various processing techniques.

GJI2021 This velocity solution was derived from Briole et al. (2021) and was carried out using PPP method. The coordinate time series of 282 permanent GNSS stations located in Greece and 47 in surrounding countries are calculated and analyzed. The studied period is 2000–2020, with mean time series length \(6.5\mathrm{ yr}\). The geodetic velocities and their uncertainties are given in ITRF2014, in topocentric coordinate system. In order to compare the velocities with the other studies, we use the official transformation parameters to express the geodetic velocities wrt European plate, in ETRF2000. We should note that in the GJI2021 dataset, the GNSS station (KRIN), located near the village of Krini, exhibits a distinct kinematic behavior compared to the dominant one in this area (see Fig. 10b). This deviation is attributed to an active landslide, as described by Briole et al. (2021). This assessment is further corroborated by Tsironi et al. (2022) through InSAR time series analysis, confirming that the observed displacement rate is a result of the active landslide in the area and is not linked to tectonic motion.

EUREFEDV This solution is provided from European Terrestrial Reference Frame (EUREF) Technical Working Group—European Dense Velocities (Brockmann et al. 2017), where more than 60,000 GNSS stations are included to dataset. The main scope of the TWG is to provide a dense velocity field in the European region, exploiting the existing velocity estimates provided by the contributing national agencies, following the simple “classical approach” combining the individual data sets using a HT model.

JGR2016 This study focuses on the Anatolian and Aegean regions providing the geodetic horizontal velocities at 346 GNSS sites (England et al. 2016). The final solution was performed as a combination of 24 previously published studies, with the selection criterion being the level of velocity uncertainties.

EPOSUGA The solution (doi: http://dx.doi.org/10.17178/GNSS.products.all) provides vertical and horizontal velocities with their respective uncertainties for 1092 GNSS stations, most of them located in metropolitan France and Italy as well as sparse information in UK, Scandinavia, Germany, Greece, and the Iberic peninsula. The velocity solution was processed using double difference with GAMIT software, and then, velocities were estimated through a statistical analysis of the position time series using the MIDAS software. The velocity field is given with respect to the stable Eurasian plate as defined by ITRF2014. The solution is provided through the European Plate Observing System (EPOS).

JGR2022 In this study, a 3D secular velocity field that covers Eurasia is presented, including 4.863 GNSS stations (PiñaValdés et al. 2022). The final velocity field is expressed in Eurasian fixed plate by combining 10 deferent datasets which all are aligned to EPN Densification (EPND) solution (Kenyeres et al. 2019) by applying a 6parameter HT model to provide a harmonized combined solution. This method followed because the 10 individual datasets were in different reference frames.
The geodetic velocity fields that we select to compare are given in Fig. 10, as expressed with respect to Eurasian fixed plate, in ETRF2000 reference frame. A more comprehensive analysis of the geodetic velocity comparison between common GNSS stations from our present study and previously published results reveals the critical role of reference frame realization in influencing the compatibility of geodetic velocities. Figure 10 presents the discrepancies in geodetic velocity fields as residuals between our current study and the published results, underscoring the significance of reference frame considerations for accurate assessments of geodetic velocity agreement. Systematic differences were observed between our present study and two solutions: GJI2021 solution (Briole et al. 2021) and JGR2016 solution (England et al. 2016). These differences were particularly prominent in the southern part of Greece. The velocity differences exhibited a consistent northeastern direction, with mean magnitudes of 1.4 mm/yr and 2.3 mm/yr in the horizontal plane for the two solutions, respectively. The discrepancies identified in our study fall within an acceptable range for longterm analyses of the geodetic velocity field, rendering them suitable for application in tectonic and geodetic studies. However, it should be noted that to achieve harmonization among various studies and create a synthetic/combined velocity field, the implementation of Helmert transformation formulas and crosscorrelation analysis is highly recommended. These techniques are essential for ensuring compatibility and coherence across different datasets, facilitating the creation of a unified and comprehensive geodetic velocity representation. The supplementary materials encompass the results pertaining to the residuals of horizontal velocity fields in Greece, facilitating a comparative examination between the findings of the current study, as derived from Bitharis (2021), and those of prior solutions.
In order to ensure the consistency of the velocity fields, we crosscompare the geodetic velocities between each study. As shown in Fig. 11, the differences of the horizontal velocities between the common GNSS sites for the selected previous studies are at the level of millimeter per year. Therefore, all previously published results are compatible with each other, providing reliable results of the geodynamic behavior in Greek area.
Conclusions
Our study involved the analysis of GPS data collected from a highly concentrated GNSS permanent network comprising of 227 European GNSS stations, of which 186 were geographically located within the territory of Greece, the processed data collected by research institutes, universities, and private companies. The derived results were used to produce a new high accurate velocity field taking into analysis procedure important seismic events. A high accurate velocity field was very important on timedepending transformation between the geodetic datum, providing a more stable reference frame which needed in many geodetic, cartographic, and cadastral purposes. Additionally, an expanded spatial and geographic coverage, along with a longtime span of daily GPS position time series, enables us to present a comprehensive view of temporal crustal deforming areas and strain rate fields. Furthermore, we have emphasized realistic uncertainty estimation to ensure the reliability of our results, employing robust trend estimators. A comparison of geodetic velocities with previous published studies indicates the agreement of our results, improving the understanding of the geodynamic processes, in a complex and highly active tectonic region, such as Greece. The dataset will be made available to a broad spectrum of users, comprising scientists engaged in the study of earthquakes and tectonics but also researchers involved in geodesy and cartography.
Data availability
Data are available from the corresponding author on reasonable request.
References
Altamimi Z, Rebischung P, Métivier L, Collilieux X (2016) ITRF2014: A new release of the international terrestrial reference frame modeling nonlinear station motions. J Geophys Res Solid Earth 121(8):6109–6131. https://doi.org/10.1002/2016JB013098
Altamimi Z (2018) Relationship and transformation between the international and the European terrestrial reference systems. EUREF technical note 1. Institut National de l’Information Géographique et
Avallone A, Briole P, AgatzaBalodimou AM, Billiris H, Charade O, Mitsakaki C, Veis G (2004) Analysis of eleven years of deformation measured by GPS in the Corinth rift laboratory area. Comptes Rendus Geosci 336(4–5):301–311
Bitharis S, Papadopoulos N, Pikridas C, Fotiou A, Rossikopoulos D, Kagiadakis V (2019) Assessing a new velocity field in Greece towards a new semikinematic datum. Surv Rev 51(368):450–459. https://doi.org/10.1080/00396265.2018.1479937
Bitharis S (2021) Study of the geodynamic field in Greece using modern satellite geodetic methods. PhD Thesis, School of Rural and Surveying Engineering, Aristotle University of Thessaloniki, Greece
Blewitt G, Kreemer C, Hammond WC, Gazeaux J (2016) MIDAS robust trend estimator for accurate GPS station velocities without step detection. J Geophys Res Solid Earth 121(3):2054–2068. https://doi.org/10.1002/2015JB012552
Blewitt G, Hammond WC, Kreemer C (2018) Harnessing the GPS data explosion for interdisciplinary science. Eos (Washington DC) 99(10.1029):485
Boehm J, Werl B, Schuh H (2006) Troposphere mapping functions for GPS and very long baseline interferometry from European centre for mediumrange weather forecasts operational analysis data. J Geophys Res Solid Earth. https://doi.org/10.1029/2005JB003629
Bos MS, Fernandes RMS, Williams SDP, Bastos L (2013) Fast error analysis of continuous GNSS observations with missing data. J Geod 87(4):351–360. https://doi.org/10.1007/s0019001206050
Briole P, Rigo A, LyonCaen H, Ruegg JC, Papazissi K, Mitsakaki C, Balodimou A, Veis G, Hatzfeld D, Deschamps A (2000) Active deformation of the Corinth rift, Greece: results from repeated global positioning system surveys between 1990 and 1995. J Geophys Res Solid Earth 105(B11):25605–25625. https://doi.org/10.1029/2000JB900148
Briole P, Ganas A, Elias P, Dimitrov D (2021) The GPS velocity field of the Aegean. New observations, contribution of the earthquakes, crustal blocks model. Geophys J Int 226(1):468–492
Brockmann E, Lutz S, Zurutuza J, Caporali A, Lidberg M, Völksen C, Sánchez L, Serpelloni E, Bitharis S, Pikridas C (2019) Towards a dense velocity field in Europe as a basis for maintaining the european reference frame. 27th IUGG Assembly, Montreal
Brockmann E, et al (2017) Towards an European dense velocities field. In: EUREF symposium 2017. Wroclaw Poland; 05/2017, pp 1–17
Chousianitis K, Ganas A, Gianniou M (2013) Kinematic interpretation of presentday crustal deformation in central Greece from continuous GPS measurements. J Geodyn 71:1–13. https://doi.org/10.1016/J.JOG.2013.06.004
Chousianitis K, Papanikolaou X, Drakatos G, Tselentis GA (2021) NOANET: a continuously operating GNSS network for solidearth sciences in Greece. Seismol Res Lett. https://doi.org/10.1785/0220200340
Clarke PJ et al (1998) Crustal strain in central Greece from repeated GPS measurements in the interval 1989–1997. Geophys J Int 135(1):195–214. https://doi.org/10.1046/j.1365246X.1998.00633.x
Deprez A, Socquet A, Walpersdorf A, Cotte N, Tarayoun A (2019) GNSS position and velocity solutions in Europe (data)
Dermanis A, Fotiou A (1992) Methods and application of observation adjustment. Ziti, Thessaloniki
Dong D, Bock Y (1989) Global positioning system network analysis with phase ambiguity resolution applied to crustal deformation studies in California. J Geophys Res 94(B4):3949–3966. https://doi.org/10.1029/JB094iB04p03949
England P, Houseman G, Nocquet JM (2016) Constraints from GPS measurements on the dynamics of deformation in Anatolia and the Aegean. J Geophys Res Solid Earth 121(12):8888–8916. https://doi.org/10.1002/2016JB013382
Fotiou A, Pikridas C (2012) GPS and geodetic applications. Ziti, Thessaloniki
Fotiou A, Pikridas C, Rossikopoulos D, Spatalas S, Tsioukas V, Katsougiannopoulos S (2009) The Hermes GNSS NtripCaster of AUTh. Bulletin of Geodesy and Geophysics, formerly Bollettino di Geodesia e Scienze Affini, 69(1)
Ganas A, Marinou A, Anastasiou D, Paradissis D, Papazissi K, Tzavaras P, Drakatos G (2013) GPSderived estimates of crustal deformation in the central and North Ionian Sea, Greece: 3 yr results from NOANET continuous network data. J Geodyn 67:62–71. https://doi.org/10.1016/j.jog.2012.05.010
Ganas A, Drakatos G, Rontogianni S, Tsimi C, Petrou P, Papanikolaou M, Argyrakis P, Boukouras K, Melis N, Stavrakakis G (2008) NOANET: the new permanent GPS network for Geodynamics in Greece, Geophys Res Abstr, Vol. 10, pp EGU2008A04380
Ganas A, Tsironi V, Kollia E, Delagas M, Tsimi C, Oikonomou A (2018) Recent upgrades of the NOA database of active faults in Greece (NOAFAULTs). In: 19th general assembly of WEGENER, September 2018, Grenoble, p 219400. https://doi.org/10.5281/zenodo.3483136
Gazeaux J et al (2013) Detecting offsets in GPS time series: first results from the detection of offsets in GPS experiment. J Geophys Res Solid Earth 118(5):2397–2407. https://doi.org/10.1002/jgrb.50152
Herring TA, Melbourne TI, Murray MH, Floyd MA, Szeliga WM, King RW, Phillips DA, Puskas CM, Santillan M, Wang L (2016) Plate boundary observatory and related networks: GPS data analysis methods and geodetic products. Rev Geophy 54(4):759–808. https://doi.org/10.1002/2016RG000529
Herring TA, King RW, Floyd MA, McClusky SC (2018a) GAMIT reference manual. Department of earth and planetary sciences, Massachusetts institute of technology, Cambridge, Massachusetts
Herring, TA, Floyd, MA, King, RW, McClusky, SC (2018b) Global Kalman filter VLBI and GPS Analysis Program, GLOBK Reference Manual, Release 10.6. Department of Earth, Atmospheric and Planetary Sciences, Massachusetts Institute of Technology, Cambridge, Massachusetts
Hollenstein C, Geiger A, Kahle HG, Veis G (2006) CGPS time series and trajectories of crustal motion along the West Hellenic Arc. Geophys J Int 164:182–191. https://doi.org/10.1111/j.1365246X.2005.02804.x
Kahle HG, Müller MV, Geiger A, Danuser G, Mueller S, Veis G, Billiris H, Paradissis D (1995) The strain field in northwestern Greece and the Ionian Islands: results inferred from GPS measurements. Tectonophysics 249(1–2):41–52. https://doi.org/10.1016/00401951(95)00042L
Kenyeres A et al (2019) Regional integration of longterm national dense GNSS network solutions. GPS Solut 23:122. https://doi.org/10.1007/s1029101909027
Lagler K, Schindelegger M, Böhm J, Krásná H, Nilsson T (2013) GPT2: empirical slant delay model for radio space geodetic techniques. Geophys Res Lett 40(6):1069–1073. https://doi.org/10.1002/grl.50288
Lazos I, Chatzipetros A, Pavlides S, Pikridas C, Bitharis S (2020) Tectonic crustal deformation of Corinth gulf, Greece, based on primary geodetic data. Acta Geodyn Geomater 17:413–424
Lyard F, Lefevre F, Letellier T, Francis O (2006) Modelling the global ocean tides: modern insights from FES2004. Ocean Dyn 56(5–6):394–415
Masson C, Mazzotti S, Vernant P (2019) Precision of continuous GPS velocities from statistical analysis of synthetic time series. Solid Earth 10(1):329–342. https://doi.org/10.5194/SE103292019
McCarthy DD, Petit G (2004) IERS conventions (2003). (IERS Technical Note, 32) Frankfurt am Main: Verlag des Bundesamts für Kartographie und Geodäsie
Noomen R, Springer TA, Ambrosius BAC, Herzberger K, Kuijper DC, Mets GJ, Overgaauw B, Wakker KF (1996) Crustal deformations in the Mediterranean area computed from SLR and GPS observations. J Geodyn 21(1):73–96. https://doi.org/10.1016/02643707(95)000151
Papoutsis I, Papanikolaou X, Floyd M, Ji KH, Kontoes C, Paradissis D, Zacharis V (2013) Mapping inflation at Santorini volcano, Greece, using GPS and InSAR. Geophys Res Lett 40:267–272. https://doi.org/10.1029/2012GL054137
PiñaValdés J, Socquet A, Beauval C, Doin MP, D’Agostino N, Shen ZK (2022) 3D GNSS velocity field sheds light on the deformation mechanisms in Europe: effects of the vertical crustal motion on the distribution of seismicity. J Geophys Res Solid Earth 127(6):2021023451. https://doi.org/10.1029/2021JB023451
Plag HP, Ambrosius B, Baker TF, Beutler G, Bianco G, Blewitt G, Boucher C, Davis JL, Degnan JJ, Johansson JM, Kahle HG, Kumkova I, Marson I, Mueller S, Pavlis EC, Pearlman MR, Richter B, Spakman W, Tatevian SK, Tomasi P, Wilson P, Zerbini S (1998) Scientific objectives of current and future WEGENER activities. Tectonophysics 294(3–4):177–223. https://doi.org/10.1016/S00401951(98)001000
Rossikopoulos D, Fotiou A, Livieratos E, Baldi P (1998) A rigorous analysis of GPS data to detect crustal deformations. Application in the area of the Ionian Sea. Tectonophysics 294(3–4):271–280. https://doi.org/10.1016/S00401951(98)00105X
Tregoning P, van Dam T (2005) Atmospheric pressure loading corrections applied to GPS data at the observation level. Geophys Res Lett 32:L22310. https://doi.org/10.1029/2005GL024104
Tsironi V, Ganas A, Karamitros I, Efstathiou E, Koukouvelas I, Sokos E (2022) Kinematics of active landslides in Achaia (Peloponnese, Greece) through InSAR time series analysis and relation to rainfall patterns. https://doi.org/10.3390/rs14040844
Vallianatos F, Sakkas V (2021) Multiscale postseismic deformation based on cGNSS time series following the 2015 Lefkas (W. Greece) Mw6.5 earthquake. Appl Sci 11(11):4817
Wessel P, Smith WHF, Scharroo R, Luis J, Wobbe F (2013) Generic mapping tools: improved version released. EOS Trans Am Geophys Union 94(45):409–410. https://doi.org/10.1002/2013EO450001
Worden CB, Wald DJ (2016) ShakeMap manual online technical manual user’s guide and software guide. US Geol Surv. https://doi.org/10.5066/F7D21VPQ
Acknowledgements
We gratefully acknowledge permission to use GNSS data from the METRICA S.A., the National Cadastre and Mapping Agency S.A of Greece, the National Observatory of Athens, and the Dionysos Satellite Observatory of NTUA. The authors would like to thank the editor and the two anonymous reviewers for their invaluable contributions in improving the quality of this paper. The figures were created by using the Generic Mapping Tools (Wessel et al. 2013). The publication of the article in OA mode was financially supported by HEALLink.
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SB and CP devised the main conceptual ideas, performed the research, analyzed the data, and wrote the paper, and AF and DR gave helpful discussion on data analysis and network adjustment. All authors reviewed the manuscript.
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Bitharis, S., Pikridas, C., Fotiou, A. et al. GPS data analysis and geodetic velocity field investigation in Greece, 2001–2016. GPS Solut 28, 16 (2024). https://doi.org/10.1007/s10291023015498
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DOI: https://doi.org/10.1007/s10291023015498