# Modelling the Velocity Field in a Regular Grid in the Area of Poland on the Basis of the Velocities of European Permanent Stations

## Abstract

The paper presents the results of testing the various methods of permanent stations’ velocity residua interpolation in a regular grid, which constitutes a continuous model of the velocity field in the territory of Poland. Three packages of software were used in the research from the point of view of interpolation: GMT (*The Generic Mapping Tools*), Surfer and ArcGIS. The following methods were tested in the softwares: the *Nearest Neighbor, Triangulation* (TIN), *Spline Interpolation*, *Surface*, *Inverse Distance to a Power*, *Minimum Curvature* and *Kriging*. The presented research used the absolute velocities’ values expressed in the ITRF2005 reference frame and the intraplate velocities related to the NUVEL model of over 300 permanent reference stations of the EPN and ASG-EUPOS networks covering the area of Europe. Interpolation for the area of Poland was done using data from the whole area of Europe to make the results at the borders of the interpolation area reliable. As a result of this research, an optimum method of such data interpolation was developed. All the mentioned methods were tested for being local or global, for the possibility to compute errors of the interpolated values, for explicitness and fidelity of the interpolation functions or the smoothing mode. In the authors’ opinion, the best data interpolation method is Kriging with the linear semivariogram model run in the Surfer programme because it allows for the computation of errors in the interpolated values and it is a global method (it distorts the results in the least way). Alternately, it is acceptable to use the Minimum Curvature method. Empirical analysis of the interpolation results obtained by means of the two methods showed that the results are identical. The tests were conducted using the intraplate velocities of the European sites. Statistics in the form of computing the minimum, maximum and mean values of the interpolated North and East components of the velocity residuum were prepared for all the tested methods, and each of the resulting continuous velocity fields was visualized by means of the GMT programme. The interpolated components of the velocities and their residua are presented in the form of tables and bar diagrams.

### Keywords

Velocity field interpolation GPS ASG-EUPOS EPN## 1 Introduction

The velocities of the Eurasian plate are described in the area of Europe by means of the permanent station velocities. These sites constitute a so-called velocity model. Interpolation of these discrete points to the remaining areas not covered by the measurement points for the continuous velocity model seems to be an important issue. Such a model will be created in this study for the area of Poland using the velocities obtained from the permanent stations located in Europe, which record the observations from the Global Positioning System (GPS). Worth pointing out is the fact that several of the softwares tested in this research are the black boxes. Therefore the authors compared only the results of a few methods of velocity interpolations rather than concentrating on the algorithms, in an attempt to find the one most appropriate to the present geological situation. The geological situation of the area of Poland, that is, how each of the structures behaves, was a kind of verification of an applied method of interpolation.

The velocities of Central Europe have been determined since the 1990s by means of the epoch campaigns. The GPS campaigns CEGRN (Central European GPS Geodynamic Reference Network—1994, 1995, 1996, 1997, 1999, 2001) were designed to investigate the intraplate velocities of the region between the Baltic Sea and the Mediterranean Sea (Becker*et al.*2002; Rogowski and Hefty1998). In the period of 11 years, eight CERGOP GPS observation campaigns were executed. The velocity vectors were determined for stations which participated in GPS observation campaigns in 1994–2005 (Klek and Rogowski2006). Several Local Analysis Centres (LAC) took part in the processing aimed at the estimation of the velocities of the permanent and other occupied sites based on the time series of coordinates (Bogusz*et al.*2002). From that time, several permanent sites were established. The velocities determined from the long-span time series of coordinates are becoming more and more reliable, but there is still a limited number of factors which can diminish this reliability. Some of them could be real, geophysical effects (Bogusz*et al.*2011, 2012a), however some may be the artefacts of the satellite system itself. Among the possible mechanisms Penna and Stewart (2003) showed how non-modelled analysis errors in tidal frequencies in the diurnal and semi-diurnal bands can be efficiently aliased to longer periods. Dong*et al.* (2002) conducted a breakdown by the different origins of the oscillations in the GPS observations into three groups related to real and artificial effects. A similar analysis concerning daily solutions was presented by Ray*et al.* (2008). They focused on the non-linear residuals generated in the ITRF2005 combination from weekly combined global frames produced by IGS (International GNSS Service). The Polish Ground-Based Augmentation System (GBAS) ASG-EUPOS has been operating since 2008. As a part of the European project EUPOS, it conducts permanent analyses for stability in position changes for geodynamical studies as well as for the realisation of the ETRS89 reference system (Figurski*et al.*2010). Additionally, we should remember that the vertical changes in Central Europe are on the order of single millimetres per year, which corresponds to the accuracy of their determination. The known models of recent vertical movements of the Earth's crust surface in the area of Poland were processed to make the verification on the basis of independent (satellite) measurements. The model was created using the satellite data and it was confronted with earlier (levelling) models. Some differences in the analysed models have been noticed, which indicates the defect of reference distinctly resulting from sea level variability (Kontny and Bogusz2012).

Interpolation of unknown values on the area among the measured points may be realised by means of at least several methods. The most commonly known techniques include: the Moving Average, Thiessen’s polygons, Triangulation (TIN), Kriging and Spline. Kreemer*et al.* (2003) made a global model of both velocities and strain rates. They performed a least-squares fitting between the model and observed geodetic velocities as well as modelled and observed geological strain rates. The modelled data were interpolated over a spherical Earth using *bi*-*cubic Bessel splines* whereas the observed data contained 3,000 velocity values. Kreemer*et al.* (1998) used the earthquake strain rates derived from 74 events to estimate a long-term velocity field for the zone between the North American and Pacific plates. The velocity field was estimated for two proposed kinematic models: the first implied the presence of a micro-plate and the other a transform deformation zone (pseudo-plate). The authors obtained the velocity field by the inversion of the earthquake strain rates. Beavan and Haines (2001) derived continuous horizontal velocity and strain fields from 362 GPS stations distributed across New Zealand. The velocity field model was interpolated with the bi-cubic spline functions defined within a curvilinear grid that covered the New Zealand area and was extended into the Australian and Pacific plates. Holt*et al.* (2000) obtained a velocity field by joint inversion of strain rates of over 230 GPS stations’ velocities. They performed a Kostrov summation of fault slip rates and in this way inferred strain rates within the area of Asia. They then fitted the strain rates with a continuous velocity field using bilinear spline interpolation. Kierulf*et al.* (2012) obtained the continuous velocity field for Norway. They interpolated the velocities from 140 GNSS stations with the means of Kriging interpolation and the use of the GIA forward model. The authors stated that the statistical interpolation method gave better results inside the analysed network while the geophysical model estimated the velocities better on the edge of the network. Majdanski (2012), using data from POLONAISE’97, CELEBRATION 2000 and SUDETES 2003 experiments, made a 3D model of the velocity distribution in the crust and upper mantle by the interpolation of 2D models and over 30 profiles. He compared the different interpolation techniques and concluded that Kriging is precise enough to model the tectonic events on the area of Poland.

## 2 Plate Kinematic Models for Calculating the Intraplate Velocities

*ω*for each plate

*p*is estimated from (Altamimi

*et al.*2007; Drewes2009):

*X*

_{l}is a point’s velocity vector and

*X*

_{i}is a position vector for each point.

*v*

_{n}and

*v*

_{e}of the velocity vector can be described by (Hefty2007):

The Euler parameters for different plate motion models

Model | \( \varphi_{E} \left[ {^{ \circ } } \right] \) | \( \lambda_{E} \left[ {^{ \circ } } \right] \) | \( \omega \left[ {{ \circ \mathord{\left/ {\vphantom { \circ {M\alpha }}} \right. \kern-0pt} {Ma }}} \right] \) |
---|---|---|---|

APKIM2005 (IGN) | 53.4 | 264.3 | 0.259 |

APKIM2005 (DGFI) | 54.5 | 262.9 | 0.258 |

NNR NUVEL-1A | 50.6 | 247.7 | 0.234 |

ITRF2005 | 56.330 | 264.021 | 0.261 |

## 3 Data

The Polish Active Geodetic Network (ASG-EUPOS) is the multifunctional precise satellite positioning system established by the Head Office of Geodesy and Cartography in 2008. The adjusted network consists of over 130 Polish foreign incorporated sites.

A project concerning the construction of modules of support and development of the ASG-EUPOS system was started in 2010 (Figurski*et al.*2011). One of the tasks is to construct a geodynamic module for interpreting the results of processing satellite observations for contemporary research of the Earth’s dynamics in the area of Central Europe. A key issue of this module is to develop a continuous model of velocities based on measurements from permanent stations. The studies made so far concerned horizontal (Bogusz*et al.*2012b) and vertical velocity fields (Kontny and Bogusz2012) in a discrete form.

*et al.*2007) and normal equations from the EPN (EUREF Permanent Network) and ASG-EUPOS (more than 300 GNSS sites presented in Fig. 3) sites. The detailed description was given in the paper by Bogusz

*et al.*(2012b).

The correct determination of the intraplate velocities is doubtful when based upon using various models of plate motion. In our studies we have used the NUVEL-1A-NNR geological model (De Mets*et al.*1990) for calculating the residua of velocities expressed in the ITRF2005 reference frame (International Terrestrial Reference Frame) (Altamimi*et al.*2007).

The statistics of the ASG-EUPOS permanent stations’ velocity residua for the NUVEL model

\( v_{N}^{NUVEL} \) (mm/year) | \( v_{N}^{NUVEL}\) (mm/year) | |
---|---|---|

Maximum value | 4.40 | 1.20 |

Minimum value | −0.60 | −2.60 |

Mean value | 2.17 | −0.98 |

## 4 The Tested Software

Three packages of software were tested within the research: GMT (The Generic Mapping Tools), Golden Software’s Surfer package and ArcGIS. GMT (Wessel and Smith1998) is free software for computation results visualising in a wide range of projections and for various kinds of results processing, e.g. filtering or interpolating. GMT is also equipped with a vast free GIS database, e.g. coastlines, rivers or state borders. The software saves the produced maps in the PostScript (PS) or the Encapsulated PostScript (EPS) formats according to the user’s command input from the command line level. It also enables the user to write scripts and automate the tasks run by the software (Wessel and Smith2011). Golden Software’s Surfer package (license number: Golden Software’s Surfer package 10.0, WIG WAT, nr WS-113545-ta4t) is a programme developed for visualising data; therefore it is often used for creating maps and terrain surface modelling. A wide set of embedded interpolation algorithms enables us to select an optimum one for the input data set (Golden Software, Version 10.0). ArcGIS (license number: ESRI_SENTINEL_KEY = 3712999727004) is a software designed for creating, editing, browsing and analysing geographic information in the form of maps and data organised in tables. The programme enables the user to analyse data from the point of view of e.g. their spatial distribution or relations between them. GIS software is now not only a tool for the visualisation of the calculations, but also allows for advanced statistical analysis of phenomena in relation to their location on the Earth’s surface (Burrough2001; Burrough and Mc Donnell1998; Johnston*et al.*, 2001).

The analysis of various interpolation methods and programmes is carried out to determine the range of the possible solutions. The analyses of vertical velocities of the Earth’s crust on the area of Poland conducted by Kowalczyk (2009) indicated the significance of this problem.

## 5 The Investigated Interpolation Methods

- (a)
in the GMT programme: the Nearest Neighbor method, the Triangulation method (TIN) and the Surface method;

- (b)
in the Surfer programme: the Minimum Curvature method, Inverse Distance to a Power and Kriging;

- (c)
in the ArcGIS programme: Spline Interpolation method and the Kriging method and the most appropriate semi-variogram model was selected.

Selection of the optimum interpolation method should depend on: the explicitness of the interpolation algorithms, complexity and time needed for completing interpolation within the specific programme, and the capability to compute the errors of the interpolated values. Worth pointing out is the fact that in the described study the computed errors are not based on the errors of velocity vectors determined by the GNSS observations, but are rather the evidence of the efficiency of the selected interpolation method.

Some of the tested methods have an inexplicit interpolation function. When a selected method is implicit we cannot say for sure how it really works. It is very important to know how the algorithm calculates the interpolated values or their errors to compare it with other tested methods. Some of the described methods are popular ones, so we can suppose that the algorithm looks a certain way. The other ones are not well known and it is hard to say if their way of calculation is appropriate to our goal (how they treat the velocities and the distances between given points and the interpolation nodes), thus their efficiency can only be estimated by comparing the results.

### 5.1 The Minimum Curvature Method

### 5.2 The Kriging Method

_{i}and the values v

_{i}in the data points:

\( {\text{A = }}\left[ {\begin{array}{*{20}c} {\gamma (d_{ 1 , 1} )} & {\gamma ( {\text{d}}_{ 1 , 2} )} & \ldots & {\gamma (d_{ 1 ,N} )} & 1\\ {\gamma (d_{ 2 , 1} )} & {\gamma ( {\text{d}}_{ 2 , 2} )} & \ldots & {\gamma (d_{ 2 ,N} )} & 1\\ \ldots & \ldots & \ldots & \ldots & \ldots \\ {\gamma (d_{N , 1} )} & {\gamma ( {\text{d}}_{N , 2} )} & \ldots & {\gamma (d_{N,N} )} & 1\\ 1& 1& \ldots & 1& 0\\ \end{array} } \right] \) is a matrix of semivariances depending on the distance between the data points,

\( \lambda\, {=}\left[ {\begin{array}{*{20}c} {\lambda_{ 1} } \\ {\lambda_{ 2} } \\ \ldots \\ {\lambda_{N} } \\ \psi \\ \end{array} } \right] \) is a vector of weights and *ψ* is a Lagrange multiplier,

\( {\text{b = }}\left[ {\begin{array}{*{20}c} {\gamma (d_{\text{i,1}} )} \\ {\gamma (d_{\text{i,2}} )} \\ \ldots \\ {\gamma (d_{{{\text{i,}}N}} )} \\ 1\\ \end{array} } \right] \) is a vector of the semivariances depending on the distance between the interpolated point and the measurements. In this work, the stationarity of the input data was assumed. The semivariance function γ(d_{i}) is adjusted based on empirical semivariance values calculated from the input data.

In the Surfer programme the Kriging method is realised by defining a model of the semivariogram that best adjusts to the location of the processed data. A semivariogram is a statistically-based, quantitative description of a surface’s roughness. It is a function of a separation vector: this includes both distance and direction, or Δx and Δy. The variogram function yields the mean dissimilarity between points separated by the specified vector (dissimilarity is measured by the squared difference in the *Z* values) (Golden Software).

The Length (A) parameter defines how rapidly the variogram components change with the increasing separation distance. The Length (A) parameter for a variogram component is used to scale the physical separation distance. [Δx Δy] is the separation vector (in map coordinates).

- Δ
_{int} an interpolation error,

*v*_{int}residuum of the interpolated velocity,

*v*_{meas}measurement result

The Kriging method has an inexplicit interpolation function but the Surfer programme computes the errors of the interpolated values, which is a significant advantage of the method (Fig. 9).

#### 5.2.1 The Development of the Kriging Model

The Kriging method has the capability to generalise and predict trends in velocities, and thereby remove the local effects that are not related to the tectonic movements. The sensitivity of the method tested in ArcGIS depends on its parameters that were input at several steps of the modelling. In the development phase of empirically selecting the appropriate semivariogram, the optimum interval (lag size) and the maximum distance (number of lags) for which the semivariance is computed have to be selected.

*N*is the number of samples, V(x

_{i}) and V(x

_{i+h}) are the measured values at a distance of h. The theoretical model of the semivariogram that fits the empirical data the best has been selected on the basis of a cross-validation procedure, which allows one to evaluate how accurately the model is able to determine the approximated values (Webster and Olivier2007). Several models of semivariogram have been tested and the adjustment was assessed by three statistics:

- the mean error ME:$$ {\text{ME = }}\frac{ 1}{N} \times \sum\limits_{\text{i = 1}}^{N} {\left( {V (x_{\text{i}} )- \widehat{V} (x_{\text{i}} )} \right)} $$(12)
- the mean squared error MSE:$$ {\text{MSE = }}\frac{ 1}{N} \times \sum\limits_{\text{i = 1}}^{N} {\left( {V (x_{\text{i}} )- \widehat{V} (x_{\text{i}} )} \right)^{ 2} } $$(13)
- the mean squared deviation ratio MSDR:$$ {\text{MSDR = }}\frac{ 1}{N} \times \sum\limits_{\text{i = 1}}^{N} {\frac{{\left( {V ( {\text{x}}_{\text{i}} )- \widehat{V} (x_{\text{i}} )} \right)^{ 2} }}{{\widehat{\sigma }^{ 2} (x_{\text{i}} )}}} $$(14)

Cross-validation numerical results (North component—V_{N})

Model | Mean error (mm/year) | Root mean squared error (mm/year) | Root mean squared deviation ratio |
---|---|---|---|

Gaussian | −0.015 | 0.708 | 1.095 |

Spherical | −0.015 | 0.713 | 1.097 |

Exponential | −0.015 | 0.718 | 1.101 |

Cross-validation numerical results (East component—V_{E})

Model | Mean error [mm/year] | Root mean squared error [mm/year] | Root mean squared deviation ratio |
---|---|---|---|

Gaussian | −0.002 | 0.696 | 1.118 |

Spherical | −0.015 | 0.709 | 1.131 |

Exponential | −0.011 | 0.725 | 1.170 |

mean error is close to zero (−0.015 mm/year for the N component and −0.002 mm/year for the E component),

root mean squared error is the smallest (0.708 mm/year for the N component and 0.696 mm/year for the E component),

root mean squared deviation ratio is close to one (1.095 for the N component and 1.118 for E component).

*C*

_{0}is a nugget value,

*C*is a sill,

*h*is the lag and a is the range.

*V*

_{N}(Figs. 10, 11) and

*V*

_{E}(Figs. 12, 13) components are shown in direction of the minimum and maximum ranges. In the corners of the figures the pie charts of the empirical semivariance in square cells that are one lag wide have been placed. The pie charts show changes of empirical semivariance values with regard to the direction, which justifies the use of the anisotropic model. The applied model of anisotropy is a zonal variant, for which semivariograms for the specific directions have different ranges. The ellipses show the range in the model in a given direction.

Semivariogram parameters (*C*_{0}—nugget value, *C*—partial sill, h—lag, and a—range (minimum, maximum)) for the *V*_{N} component are *C*_{0} = 0.362 mm/year, C = 0.256 mm/year, *h* = 55 km, a is from 324 to 440 km respectively. For the *V*_{E} component parameters take the following values: *C*_{0} = 0.316 mm/year, C = 0.334 mm/year, *h* = 55 km and a ranges from 324 to 440 km.

##### 5.2.1.1 The North Component *V*_{N}

For the *V*_{N} component of the velocity, the semivariances change in a smaller range in the direction of NW–SE (Fig. 10) while there is a significant increase in the perpendicular direction (Fig. 11). The values of the semivariances are calculated using the points located inside the ellipse of the semi-axes of 440 km and 324 km divided into 8 sectors. The azimuth of the longer axis of the ellipse is 164°.

##### 5.2.1.2 The East Component *V*_{E}

For the *V*_{E} component of the velocity, the semivariances change in a smaller range in the direction of NE-SW (Fig. 12) while there is a significant increase in the perpendicular direction (Fig. 13). The values of the semivariances are calculated using the points inside the ellipse of the semi-axes of 440 km and 324 km divided into 8 sectors. The azimuth of the longer axis of the ellipse is 52°.

Application of the anisotropy model enables the better fitting of the model to the data. It takes into consideration the differentiation of the velocity with respect to both the distance and direction.

The directions of the ellipses coincide with the directions of the velocity gradients. For the *V*_{N} component, the longer axis of the ellipse (A = 164°) coincides with the direction of the smaller gradient, and the shorter one coincides with the direction of the greater gradient. It is similar for the *V*_{E} component while the longer axis’ azimuth is 52°.

It is worth mentioning that the azimuths of the ellipses agree with the location of the faults in the T–T (Teisseyre-Tornquist) Zone (approx. azimuth is 132°) and the respective perpendicular directions. It is probable that they will coincide with the main deformations that will be determined in the area of Poland.

_{N}decrease in the North-East direction (the South-West part of Poland moves slower than the North-East one) whereas the V

_{E}components increase in the South-East direction (the North-West part of Poland moves slower than the South-East one).

The differences among the results in modelling were found by analysing the distances between the isolines. In the anisotropic model the distances decrease. The greater gradient appeared in the main directions, and the interpolated points were calculated in these directions with the use of the weights (customised to the specifics of the phenomenon) that differed from the ones that were used in the isotropic model.

### 5.3 The Spline Interpolation Method

The Spline Interpolation method is a minimum curvature function, which passes through all data points with the accuracy of their mean errors. In the data points the function’s curvature has the minimum value, while the course of the function between the points is close to linear. All data points have their influence on the value of the interpolated point. Each station is involved in determining the vectors “a” of the function’s coefficients described by Eq. (18) separately for each component. The number of the coefficients is equal to the number of stations. The closest stations have the greatest impact on the value of the interpolated point and the effect decreases logarithmically. In this model, the isotropy of the input data was assumed.

*n*,*e*horizontal coordinates of the interpolated point;

- N
_{i}, E_{i} horizontal coordinates of the i-th permanent station.

_{i}were determined from solutions of the system equations with the following conditions:

*a*

_{i}were obtained separately for

*V*

_{N}and

*V*

_{E}from the following equation:

*a*vector of the function parameters,

*A*matrix of the coefficients,

*f*vector of the permanent stations’ velocities.

*a*

_{i}parameters is calculated using the following equation:

*V*, the error propagation law is used:

## 6 Comparison of Results

Comparison of interpolation results

Component of the velocity residuum [mm/year] | Method of interpolation | ||||||||
---|---|---|---|---|---|---|---|---|---|

Data | Nearest neighbor | Triangulation | Minimum Curvature | Inverse distance to a power | Kriging | Surface | Spline | ||

N | MN | −1.0 | −1.0 | 0.0 | 0.1 | 0.5 | 0.2 | −0.1 | −0.2 |

MAX | 4.1 | 4.1 | 3.9 | 4.7 | 4.0 | 3.8 | 4.0 | 3.9 | |

MEAN | 1.8 | 1.8 | 1.8 | 2.2 | 1.8 | 1.8 | 1.7 | 1.7 | |

E | MN | −3.5 | −3.5 | −3.2 | −2.7 | −3.3 | −3.2 | −4.2 | −3.5 |

MAX | 0.9 | 0.9 | 0.2 | 1.2 | 0.0 | 0.4 | 0.5 | 0.9 | |

MEAN | −1.1 | −1.1 | −1.1 | −0.9 | −1.1 | −1.1 | −1.1 | −1.2 |

The differences between all the results obtained by means of the tested interpolation methods and the data are at the level of a few tenths of mm/year. The Nearest Neighbor method was rejected by the authors despite the fact that the interpolation results are very similar to the measurement data. Its disadvantage is locality—it does not take into consideration the spatial variability of the discussed phenomenon—and discontinuity—the nearest measurement data have the greatest impact on the interpolated nodes without taking the farther stations into consideration. The disadvantage of the Triangulation method is the fact that the interpolation results depend only on three measurement data. Therefore, this method will not be used for interpolation in the creation of the continuous model of the velocity field. The Inverse Distance to a Power method does not take into consideration, as the Nearest Neighbor method does, the spatial variability of the discussed phenomenon. Interpolation by means of the Kriging method, due to connecting points of similar values, perfectly displays the spatial variability of the investigated phenomenon. Additionally, it enables the computation of the errors of the interpolated values, which makes it the optimum method for the interpolation of investigated observations for the continuous model of the velocity field. Interpolation by means of the Surface method yields results similar to the measurement data. Despite this, it has not been selected by the authors as the optimum method for interpolating the velocity residua of permanent stations in the area of Poland because changing the values of its parameters does not result in changes in the interpolated values. The Spline method interpolates the velocity residua for the continuous model perfectly adjusting to the measurement data. Additionally, the ArcGIS software enables one to compute the errors of the interpolated values which, due to this feature of the method, are minimum. However, the method has a disadvantage—it does not take into consideration the spatial variability of the investigated phenomenon—the measurement datum closest to the interpolated node has the greatest impact on the interpolated value.

The measurement data are marked in red, the interpolation results using the Kriging method are marked in green, and the interpolation results using the Minimum Curvature method are marked in blue. The indicated errors concern the interpolation using the Kriging method.

## 7 Summary

All the previous research on obtaining the continuous velocity field applied Kriging or Delaunay triangulation to the different GPS data sets. Grenerczy (2003) created the continuous velocity plate field based on data from regional networks, for the whole period of each station activity. The following networks were considered in the studies: CEGRN (the Central European GPS Geodynamic Reference Network), CRODYN (the Croatian and Slovene Geodynamic Network), HGRN (the Hungarian GPS Geodynamic Reference Network), IGS (The International GNSS Service) and SAGET (Satellite Geodynamic Traverses). The continuous velocity field was created by interpolating data for the whole region of Central Europe with two interpolation methods: Kriging and Delaunay triangulation with linear interpolation. Both methods gave similar effects. The obtained intraplate velocity values ranged from 0.1 up to 5 mm/year depending on the region of interpolation. The produced GPS-derived contour map of crustal velocity magnitudes in Central Europe was in very good agreement with the earthquake activity map. Grenerczy (2004) described the accuracy of GPS network assumption in the Hungarian area and made the new method of analysis independent of the scale coefficient between frames. Linear regression and its errors were checked on a few baselines of the HGRN network. Statistical tests were made and their results were favourable with respect to values, correlation and standard deviations of estimated parameters. A velocity map based on the reference station data was made, without making any unnecessary transformations, just minimising the velocities on the stable part of the European plate, using seven stations. Based on the map of velocities, the map of the continuous velocity field was made by interpolating velocities via the Kriging method with the nugget effect. Hefty (2007) demonstrated a method of combining regional and local velocity fields into a homogenous system consistent with the ITRF2000 and then reduced for the APKIM2000 model. The described horizontal velocities resulted from seven various regional and local analyses of 192 GPS sites by means of epoch campaigns and permanent observations from the region of Central Europe, Adriatic region and the Balkan Peninsula. Several characteristic blocks with significant horizontal velocity trends for the Central and Southeastern Europe were proved. The two remarkable movements oriented northwards and southwards were shown with the magnitude of 3÷5 mm/year for the Adriatic region and 3 mm/year for the Southern Carpathian Mountains and Eastern part of the Balkan Peninsula. The results of the interpolation were presented in 2° × 1° and 1° × 0.5° grids with 2σ error ellipses.

This research concerned testing seven methods for the interpolation of the intraplate velocities by means of three programmes. The Nearest Neighbor, Triangulation and Surface methods were tested by means of the free GMT programme. The GMT programme does not enable one to compute the errors of the interpolated values, and its interpolation algorithms are inexplicit. The Minimum Curvature, Inverse Distance to a Power and Kriging methods were tested by means of the Surfer programme. Surfer’s interpolation algorithms are also inexplicit. The possibility of computing errors of the interpolated values is available only for the Kriging method. Data processing using the discussed software is neither complicated nor a time-consuming task. Selection of the optimum interpolation method should be dependent on the explicitness of the interpolation function and on the capability to determine the errors of the interpolated values. The Spline method was tested using the ArcGIS software. It yielded values of interpolated intraplate velocities similar to the Kriging method. However, the errors in the interpolation nodes were much smaller because this method perfectly adjusts to the measurement data which is its disadvantage—it does not take into consideration the spatial distribution of the investigated phenomenon. Statistics in the form of maximum, minimum and mean values of the velocity residuum components were prepared for the measurement data and for all interpolation methods. The Kriging Function was selected to be used for modelling the continuous velocity field in the area of Poland on the basis of the analyses and conducted tests. In the authors’ opinion, Kriging is the best method of modelling velocity residua to obtain trends of the investigated phenomenon. This method is immune to local disturbances of the velocity field. The difference between the arithmetic mean of the components of velocity residua computed from the measurement data and those interpolated by means of the Kriging method is at the level of hundredth of a millimeter/y. Interpolation by means of the Green* i* in the GMT programme yields almost identical results as Kriging, and the values of the interpolated intraplate velocities with respect to the NUVEL model using Spline Functions proved compatibility in independent investigations with interpolated values using the Kriging Functions at the level of 1 mm/year. The Minimum Curvature method may alternately be applied for the Kriging method. Empirical analysis of the results proved that both methods yield identical results for appropriate density of measurement data. The impact of the small intraplate velocity at one site (DRWP) is observed in all results of the tested interpolation methods. Anomalous directions of velocity residua at some of the permanent stations cause differences from the North-East trend of the velocity residua vectors. This occurs on a greater or a smaller area depending on the characteristics of the tested interpolation method.

## Notes

### Acknowledgments

We gratefully acknowledge Dr. Mariusz Figurski for providing velocities. This research is supported by the Polish Ministry of Science and Higher Education, grant No. 0960/R/T02/2010/10.

### References

- Altamimi, Z., Collilieux, X., Legrand, J., Garayt, B., Boucher, C. (2007),
*ITRF2005: A new release of the International Terrestrial Reference Frame based on time series of station positions and Earth Orientation Parameters*. J. Geophys. Res., 2007, nr 112.Google Scholar - Beavan, J., Haines, J. (2001),
*Contemporary horizontal velocity and strain rate fields of the Pacific*-*Australian plate boundary zone through New Zealand*. Journal of Geophysical Research, vol.*106*, no. B1, pp. 741–770, January 10, 2001.Google Scholar - Becker, M., Cristea, E., Figurski, M., Gerhatova, L., Grenerczy, G., Hefty, J., Kenyeres, A., Liwosz, T., Stangl, G. (2002),
*Central European intraplate velocities from CEGRN campaigns*. Reports on Geodesy No. 1(*61*), 2002, pp. 83–92.Google Scholar - Bogusz, J., Figurski, M., Kontny, B., Grzempowski, P. (2012a),
*Horizontal velocity field derived from EPN and ASG*-*EUPOS satellite data on the example of south*-*western part of Poland*. Acta Geodynamica et Geomaterialia, v.*9*, No. 3 (*167*), 2012, pp. 349–357.Google Scholar - Bogusz, J., Figurski, M., Kontny, B., Grzempowski, P. (2012b),
*Unmodelled effects in the horizontal velocity fields: ASG*-*EUPOS case study*. Artificial Satellites—Vol.*47*, No. 2—2012 doi:10.2478/v10018-012-0014-x, pp. 67–79. - Bogusz, J., Figurski, M., Kroszczyński, K., Szafranek, K. (2011),
*Investigation of environmental influences to the precise GNNS solutions*. Acta Geodynamica et Geomaterialia, vol.*8*, No. 1 (161), 2011, pp. 5–15.Google Scholar - Bogusz, J., Figurski, M., Kruczyk, M., Kujawa, L., Kurka, W., Liwosz, T., Pfeil, M., Rogowski, J.B. (2002),
*Activities of Astro*-*Geodetic Observatory in Jozefoslaw in the frame of IGS and EUREF*. Advances in Space Research, Vol.*30*, No. 2, 2002, pp. 351–356.Google Scholar - Burrough, P. A. (1986).
*Principles of Geographical Information Systems for Land Resources Assessment*. New York: Oxford University Press.Google Scholar - Burrough, P., McDonnell, R. (1998),
*Principles of Geographical Information Systems*. Oxford University Press, Oxford.Google Scholar - Burrough, P.A. (2001),
*GIS and geostatistics: Essential partners for spatial analysis*. Environmental and Ecological Statistics*8*, pp. 361–377.Google Scholar - Dach, R., Hugentobler, U., Fridez, S. and Meindl, M. (eds.) (2007),
*Bernese GPS software version 5.0*. Astronomical Institute, the University of Bern.Google Scholar - De Mets, C., Gordon, R.G., Argus, D.F., Stein, S. (1990),
*Current plate motion*. Geophysical Journal International, 1990, no 101, pp. 425–478.Google Scholar - Dong, D., Fang, P., Bock, Y., Cheng, M. K., Miyazaki, S. (2002),
*Anatomy of apparent seasonal variations from GPS*-*derived site position time series*. J. Geophys. Res. 107(B4):2075. doi:10.1029/2001JB000573. - Drewes, H. (2009),
*Geodetic The Actual Plate Kinematic and Crustal Deformation Model APKIM2005 as Basis for Non-Rotating ITRF*. Geodetic Reference Frames, Springer-Verlag Heidelberg.Google Scholar - Figurski, M., Bogusz, J., Bosy, J., Kontny, B., Krankowski, A., Wielgosz, P. (2011), "
*ASG*+"*: project for improving Polish multifunctional precise satellite positioning system*. Reports on Geodesy, No. 2 (*91*) 2011, pp. 51–58.Google Scholar - Figurski, M., Szafranek, K., Bogusz, J., Kamiński, P. (2010),
*Investigation on stability of mountainous EUPOS sites’ coordinates*. Acta Geodynamica et Geomaterialia, Vol.*7*, No. 3 (*159*), 2010, pp. 263–274.Google Scholar - Grenerczy, G. (2003),
*Kinematics between the Adriatic and the Eurasian Plate Interior: further Constraints from CEGRN and Local Space Geodetic Data*. Reports on Geodesy, No. 1. (*64*), pp. 65–74, 2003.Google Scholar - Grenerczy, G. (2004),
*The Motion of Adria and its Effects on the Pannonian Basin: Report of CERGPOP*-*2/Environment WP10.3*. Reports on Geodesy No. 2. (*69*), pp. 73–80, 2004.Google Scholar - Hefty, J. (2007),
*Geo*-*kinematics of central and south*-*east Europe resulting from combination of various regional GPS velocity fields*. Acta Geodyn. Geomater., Vol.*4*, No. 4 (*148*), pp. 173–189, 2007.Google Scholar - Holt, W.E., Chamot-Rooke, N., Le Pichon, X., Haines, A.J., Shen-Tu, B., Ren, J. (2000),
*Velocity field in Asia inferred from Quaternary fault slip rates and Global Positioning System observations*. Journal of Geophysical Research, vol.*105*, no. B8, pp. 19,185–19,209, August 10, 2000.Google Scholar - Johnston, K., Ver Hoef, J. M., Krivoruchko, K., Lucas, N. (2001),
*Using ArcGIS Geostatistical Analyst*. ESRI.Google Scholar - Kierulf, H.P., Ouassou, M., Simpson, M.J.R., Vestøl, O. (2012),
*A continuous velocity field for Norway*. Journal of Geodesy, November 2012, doi:10.1007/s00190-012-0603-2. - Klek, M., Rogowski, J. B. (2006),
*Determination of deformations of the central Europe from CERGOP GPS observations campaigns*. Reports on Geodesy No. 1 (*76*), 2006, pp. 55–60.Google Scholar - Kontny, B., Bogusz, J. (2012),
*Models of vertical movements of the earth crust surface in the area of Poland derived from levelling and GNSS data*. Acta Geodynamica et Geomaterialia, v.*9*, No. 3(*167*), 2012.Google Scholar - Kowalczyk, K. (2009),
*Interpolation of vertical crustal movements using the Surfer 8.0. The result depends on the method*(in Polish), Magazyn Geoinformacyjny, 8 (*171*).Google Scholar - Kreemer, C., Govers, R., Furlong, K.P., Holt, W.E. (1998),
*Plate boundary deformation between the Pacific and North America in the Explorer region*. Tectonophysics 293 (1998), pp. 225–238.Google Scholar - Kreemer, C., Holt, W.E, Haines, A.J. (2003),
*An integrated global model of present*-*day plate motions and plate boundary deformation*. Geophysical Journal International. Volume*154*, Issue 1, pp. 8–34, July 2003.Google Scholar - Majdanski, M. (2012),
*The Structure of the Crust in TESZ Area by Kriging Interpolation*. Acta Geophysica, Volume:*60*, Issue: 1, pp. 59–75. doi:10.2478/s11600-011-0058-5. Published: February 2012. - McBratney, A. B., Webster, R. (1986),
*Choosing Functions for Semi*-*variograms of Soil Properties and Fitting Them to Sampling Estimates*. Journal of Soil Science*37*, pp. 617–639.Google Scholar - Osada, E. (1995),
*Spline*-*Transformation of coordinates in GIS*. Geo-Informations-Systeme, Heft 4, Wichmann, Karlsruhe.Google Scholar - Penna, N. T., Stewart, M. P. (2003),
*Aliased tidal signatures in continuous GPS height time series*. Geophys. Res. Lett. 30(23):2184. doi:10.1029/2003GL018828. - Ray, J., Altamimi, Z., Collilieux, X., van Dam, T. (2008),
*Anomalous harmonics in the spectra of GPS position estimates*. GPS Solut (2008) 12:55–64. doi:10.1007/s10291-007-0067-7. - Rogowski, J., Hefty, J. (1998),
*Final Report of the CERGOP Study Group CSG*-*3*<*CERGOP Reference Frame*>. Reports on Geodesy No. 10 (40), 1998, Proceedings of the 9th CEI CERGOP Working Conference Wettzell, Germany 5–7 May 1998, pp. 169–194.Google Scholar - Webster, R., Olivier, M.A. (2007),
*Geostatistics for Environmental Scientist*. Wiley & Son, Ltd;Google Scholar - Wessel, P., Smith, W. (2011),
*The Generic Mapping Tools A Map*-*making Tutorial*. Version 4.5.7.Google Scholar - Wessel, P., Smith, W.H.F. (1998),
*New, improved version of the Generic Mapping Tools*. Released, EOS Trans. AGU, 79, 579.Google Scholar - Zhang, J., Yao, N. (2008),
*The Geostatistical Framework for Spatial Prediction*, Geo-spatial Information Science 11(*3*): pp. 180s–185.Google Scholar

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