The area of Poland covers a complicated contact between Precambrian Europe to the northeast and Phanerozoic terranes to the southwest (Fig. 1). The Trans-European Suture Zone (TESZ) between them is a major crustal-scale feature, which appears to be a deep-seated boundary reaching down to a depth of at least 200 km (e.g., Zielhuis and Nolet 1994; Schweitzer 1995; Wilde-Piórko et al. 2009). In Poland, the southwestern edge of the East European Craton (or the paleocontinent Baltica) is fault-bounded by the Teisseyre-Tornquist Zone (TTZ) which is continued in Scandinavia along the Sorgenfrei-Tornquist Zone (STZ). The structure and evolution of this area are still important tectonic problems in Europe north of the Alps (e.g., Dadlez 1982; Ziegler 1990; Pożaryski et al. 1992; Berthelsen 1998; Pharaoh 1999; Winchester and PACE TMR Network Team 2002; Winchester et al. 2002). In southern Poland, the younger Carpathian arc is an interrelated component of the Mediterranean arc basin, a complex, collisional environment between the European and Adriatic plates, which involved a variety of micro-continents and oceanic areas (e.g., Golonka et al. 2003).

Fig. 1
figure 1

Tectonic sketch of pre-Permian Central Europe in contact with the East European Platform, Variscides, and Alpine orogen. The blue frame shows the location of the study area in Poland. Compiled mainly from: Pożaryski and Dembowski (1983), Ziegler (1990), Winchester et al. (2002), Narkiewicz et al. (2011), Cymerman (2007), and Skridlaitė et al. (2006). Ard.-Rhen. M. Ardenno-Rhenish Massif, BT Baltic Terrane, FSS Fennoscandia–Sarmatia Suture, HCM Holy Cross Mountains, MB Małopolska Block, MLSZ Mid-Lithuanian Suture Zone, MSFTB Moravian-Silesian Fold-and-Thrust Belt, PLT Polish-Latvian Terrane, PM Pomerania Massif, RFH Ringkobing-Fyn High, STZ Sorgenfrei-Tornquist Zone, Thor S. Thor Suture, TTZ Teisseyre-Tornquist Zone, USB Upper Silesian Block, VA Voronezh Anteclise, VDF Variscan Deformation Front

The sedimentary cover of the EEC in northern Poland is rather thin, being only 0.3–1 km thick in the region of the Mazury-Belarus anteclize, but increases southwestwards to 7–8 km along the EEC margin. In the TESZ, the sedimentary layer attains a thickness of up to 9–12 km. The Variscan domain is characterized by a 1- to 2-km-thick sedimentary cover, while the Carpathians are characterized by very thick sediments of up to c. 20 km (e.g., Guterch and Grad 2006). For this reason, the basement in the TESZ and in the Carpathians is not reached by boreholes, so its depth is available only from geophysical investigations, mostly from seismic profiling. In particular, seismic velocities in the basement could be used for discrimination between the crystalline and consolidated types of the crust. According to Dadlez (2006) and Dadlez et al. (2005), the crystalline crust is considered to consist of highly deformed metamorphic and igneous rocks, characteristic of Precambrian platforms. By contrast, the consolidated crust is composed of highly deformed but not necessarily metamorphosed sedimentary and subordinate igneous rocks, characteristic of the Paleozoic platform. The aim of this paper is to find the geometry of the seismic basement, its velocity, as well as the relationship between the crystalline basement, the consolidated basement, and the sedimentary cover in Poland.

Geological and geophysical context

Despite the ongoing discussion about the sedimentary cover and its basement in Poland, there is no consent between geologists on the tectonic subdivision and their structural interpretation. An example of such a discordance could be illustrated for geological cross sections through the Trans-European Suture Zone (TESZ) in Poland, between the East European Platform (EEP) and the West European Platform (WEP), as shown in Fig. 2. The same geological cross section along line AA′ (Fig. 2a) is interpreted in a different way by Karnkowski (2008) and Żelaźniewicz et al. (2011). Two tectonic subdivisions (Fig. 2b) differ both in the sedimentary cover and in the basement. Another geological regional subdivision of the Polish Lowlands was proposed by Narkiewicz and Dadlez (2008). The subdivision by Żelaźniewicz et al. (2011) was commented on and criticized by Narkiewicz (2012), and the discussion still seems to be far from finalized.

Fig. 2
figure 2

Geological and seismic cross sections trough of the Trans-European Suture Zone (TESZ) in Poland between the East European Platform (EEP) and West European Platform (WEP). a Location map of seismic profiles. b Geological cross section along line AA′ with two tectonic subdivisions by Karnkowski (2008) and Żelaźniewicz et al. (2011). c, d Seismic sections beneath profiles 1-VI-66, M-7, and P4. Note basement velocity differentiation: about 6.1 km/s for the EEP and about 5.8 km/s for the WEP. Basement in the TESZ area is not reached by boreholes (see dashed pink lines at depth of 5 km), so its depth and velocity is available only from seismic profiles. FSB Fore-Sudetic Block, K-P Synclinorium Kościerzyna-Puławy Synclinorium, MPA Mid-Polish Anticlinorium, NSS North-Sudetic Synclinorium, Sz-M Synclinorium Szczecin-Miechów Synclinorium, WEP West European Platform, WS Western Sudetes, Compilation from Karnkowski (2008), Żelaźniewicz et al. (2011), and Grad et al. (1991, 2003a, b)

Seismic cross sections for profiles M-7, 1-VI-66, and P4, all close to line AA′, are shown in Fig. 2c, d. The sedimentary cover along the geological cross section (Fig. 2b) and seismic cross section along the P4 profile (Fig. 2d) show similar sequences of layers, including complicated Permian (Zechstein) salt diapirs and salt pillows in the TESZ (Krzywiec 2006a, b; Mazur et al. 2005). However, the major structural features of the seismic profiles are the basement depth and its velocity differentiation: c. 6.1 km/s for the EEP and c. 5.8 km/s for the WEP (Grad et al. 1991, 2003a, b). Differentiation of the basement is also observed in the complicated pattern of the Bouguer anomalies, the irregular pattern of the magnetic anomalies, electromagnetic properties, and the heat flow. All of these observations will be discussed at the end of the paper, together with the tectonic subdivisions of the area of Poland.


In the area of Poland, the depth of the basement and its structure was studied using different methods and surveying techniques including deep geological boreholes, seismic refraction and reflection profiles, magnetic, gravity, and magnetotelluric measurements. Using these data, multiple studies regarding the basement depth were carried out and all such available studies are used in this paper and collectively displayed in Fig. 3. All map grids in this paper are recalculated to the same resolution of 0.02° (longitude) by 0.01° (latitude). That corresponds to semi-rectangular cells: 1112 m by 1281 m for northern Poland and 1112 m by 1459 m for southern Poland. Using grids with the same resolution allows for a simple manipulation and the performing of mathematical operations between multiple grids. All maps presented in this section are in the Lambert conic projection centered on 19.25°E. All grid calculations are performed for the rectangular area: 13.8–24.5°E, 48.7–55.0°N.

Fig. 3
figure 3

The database for the basement depth and velocity in the area of Poland. a Basement depth from boreholes limited to 4.5 km depth (Małolepszy 2005; see text for more explanation); white color shows area with no data. b Depth of the seismic basement in northeastern Poland (Skorupa 1974) and depth of the basement (high-conductivity layer) from magnetotelluric investigations in Carpathians in southern Poland (Stefaniuk and Klityński 2007). c Basement depth beneath seismic refraction profiles; for each point along the profiles, a mask of 20 km radius was used to plot the basement depth; the white color shows an area with no refraction data. d Data coverage from all sources; colors correspond to a number of data sources available at a given location and the white color shows places with no data. e Averaged and interpolated basement depth from all available sources. f Interpolated P-wave velocity of the uppermost basement from seismic refraction profiles; the dotted line ellipse shows the area of anomalous velocity (anisotropy) discussed in the text. The data in the map c are from modern seismic refraction experiments/profiles: POLONAISE’97: Guterch et al. (1999); profile P1—Jansen et al. (1999); profile P2—Janik et al. (2002); profile P3—Środa and POLONAISE Working Group 1999 (1999); profile P4—Grad et al. (2003a, b); profile P5—Czuba et al. (2001); CELEBRATION 2000: Guterch et al. (2003): profiles CEL01 and CEL04—Środa et al. (2006); profile CEL02—Malinowski et al. (2005); profile CEL03—Janik et al. (2005); profile CEL05—Grad et al. (2006); profile CEL10—Grad et al. (2009); profiles CEL06, CEL11, CEL12, CEL13, CEL14, CEL21, CEL22, CEL23—Janik et al. (2009); SUDETES 2003: Grad et al. (2003a, b); profile S01—Grad et al. (2008); profiles S02, S03, S06—Majdański et al. (2006); OTHRER profiles: LT-2, LT-4, LT-5—Grad et al. (2005); profile LT-7—Guterch et al. (1994); profiles M-7, M-9—Grad et al. (1991); profile TTZ—Grad et al. (1999); profile PANCAKE—Starostenko et al. (2013); profile 1-VI-66—Grad et al. (1990)

The complete basement depth map of the East European Craton in northeastern Poland was created by Skorupa (1974). This study covered an area of the EEC where the thickness of sediments is only 0.3–1 km thick in the region of the Mazury-Belarus anteclize, mostly less than 4 km, and reaches c. 10 km on the edge of the East European Craton (see Fig. 3b, NE Poland). The study was based on data from geological boreholes and the set of regional seismic refraction profiles available at that time. In our elaboration, a corresponding mask for this map is calculated as having value 1 where data are available and value 0 elsewhere. This map covers 42.1 % of the area of Poland.

A second basement depth map was compiled, based on geological boreholes data, using maps from the geological atlas of horizontal cuttings (Kotański 1997; Piotrowska et al. 2005; Małolepszy 2005; Nita et al. 2007; The compiled map was prepared down to 6 km depths, but knowing that borehole surveying has a limited range (due to the small amount of deep wells) only depths down to 4.5 km are considered in this paper. A proper mask for this map is calculated as having value 1 where data are available and the basement depth is shallower than 4.5 km, and value 0 elsewhere. This map (Fig. 3a) covers 58.3 % of the area of Poland.

Most of the Carpathian basement is not reached by boreholes. The use of the magnetotelluric method allowed for a study of the area where sediments are very thick—up to c. 25 km. In magnetotelluric soundings, the basement is identified as a high-resistivity (low-conductivity) layer. The map of such a “basement” was prepared for the Carpathians using data form magnetotelluric soundings and boreholes by Stefaniuk and Klityński (2007). A proper mask for this map is calculated as having value 1 where data are available and value 0 elsewhere. This map is shown in Fig. 3b (southern Poland) and covers 6.6 % of the area of Poland.

Combined together, these three maps (Fig. 3a, b) cover 75.9 % of the area of Poland, but do not provide data about the basement depth in central Poland—in the area of the Trans-European Suture Zone (TESZ). The goal of this paper is to provide full knowledge of the basement depth for the whole area of Poland. To achieve this, the data set is supplemented by 32 models from deep seismic refraction profiles. The area of Poland is very well covered with modern seismic refraction profiles from multiple experiments, which are detailed in the figure caption of Fig. 3 with corresponding references.

For each profile, detailed 2D models of seismic velocities are analyzed in 1000 m (horizontal) by 100 m (vertical) resolution. Each model grid cell contains information about the P-wave seismic velocity and the layer number. The layer number allows tracking of geological layers for the profile. Additionally, the exact geographical locations of grid columns along the profile path are calculated. For each profile, the layer numbers corresponding to the basement are noted, allowing us to derive the basement depth for a certain location along the profile path.

The processing of all profiles provides a data set which includes latitude, longitude, basement depth, and P-wave velocity of the uppermost basement. This distinct distribution of points is later interpolated to a grid using GMT 5.1.1 surface command (Wessel and Smith 1991, 1998) with both interior and boundary tension parameters set to 0.5, and the convergence limit set to 0.01. Additionally, a grid mask is calculated as having value 1 in grid cells, within 20 km from any data point along the profile, and value 0 in other cases. A basement depth map calculated from seismic refraction profiles with an overlaying mask is shown in Fig. 3c. This map covers 72.3 % of the area of Poland.

The resulting seismic basement map is created by combining the basement map created from seismic refraction profiles data with three additional basement depth maps available for parts of Poland. Figure 3d shows the data availability map (sum of four masks mentioned above). 94.3 % of the area of Poland is covered by at least one data source, 66.9 % is covered by at least two data sources, and 19.0 % is covered by at least three data sources. Finally, a combined basement map is obtained by averaging all four maps within the area of their availability and interpolating within gaps using the GMT 5.1.1 surface command with both interior and boundary tension parameters set to 0.5, and convergence limit set to 0.01. The resulting interpolated map covers 100 % of the area of Poland and is shown in Fig. 3e.

Apart from the basement depth, the analysis of seismic refraction profiles provides the P-wave velocity of the uppermost basement. Figure 3f shows the result of interpolation of these data to a full grid. One issue is identified regarding the velocity map—in Fig. 3f it is marked by ellipse. In southern Poland, one of the profiles (CEL14) provides P-wave velocities much higher than for the other profiles around it, which are located nearly perpendicular to it. This is identified as the result of anisotropy in seismic velocities in this area (Środa 2006), and for further analysis P-wave velocities for profile CEL14 are reduced by 6 %. After applying this change to the data sets, the P-wave map is recalculated.

Both basement depth and P-wave velocity of the uppermost basement maps are filtered using the GMT 5.1.1 grdfilter command for geographic grids with spherical distance calculation. A simple boxcar filter is used, where all weights are equal giving a mean value from a given radius (filter width)—in this case 30 km. The final interpolated maps are presented in Fig. 4.

Fig. 4
figure 4

The basement depth and P-wave velocity of the uppermost basement in the area of Poland. a Final basement depth map filtered with 30-km-radius boxcar filter. b Final P-wave velocity map of the uppermost basement filtered with a 30-km-radius boxcar filter. For abbreviations see Fig. 1

Seismic basement: results

The main features of the basement depth map in Poland (Fig. 4a) are a deep trough in the TESZ and a deep basement in the Carpathians. The depth difference of the basement over the area reaches up to 20 km. In the EEC, the change in the basement depth is smooth, increasing from c. 1 km in the northeast to c. 10 km toward the southwest at the margin of the craton. This smooth shape could be due to the Earth’s surface erosion, “polishing” the rocks’ trough for a million years from the Precambrian onward. As a result, the basement depth of the EEC does not show any distinct correlation with crystalline massifs and domains. To the southwest of the Variscan deformation front, the depth of the Paleozoic basement of the WEP is increasing from c. 1 km in the southwest to c. 10 km toward the TESZ in the northeast. The basement below the Carpathians is deepening toward the south and reaches up to 20 km in depth. In the Polish Carpathians, a deeper basement was found in the eastern part, the border of which roughly follows c. 21°E longitude. The triangle-shape area between EEC, WEP, and Carpathians is characterized by a 2- to 5-km-deep basement.

This study is not the first one to provide a basement depth map for the area of Poland; however, it is the first to be dedicated to this region and prepared in such detail. The high-resolution basement depth map from this paper is compared to three other maps of lower resolution: one global map (Laske and Masters 1997) and two regional maps (Molinari and Morelli 2011; Tesauro et al. 2008). For a comparison of these maps and the map from our study, all are filtered and interpolated with the same 50-km boxcar filter (Fig. 5).

Fig. 5
figure 5

Comparison of our basement depth with previous models for the area of Poland. a Final basement depth map filtered with 50-km-radius boxcar filter. b Difference between final basement map and global basement depth by Laske and Masters (1997). c Difference between final basement map and basement depth by Molinari and Morelli (2011). d Difference between final basement map and basement depth by Tesauro et al. (2008)

Laske and Masters (1997) provide a global model of sediments’ thickness with a resolution of 0.5° by 0.5°. The thickness of sediments is provided and for a comparison with our basement depth, a Digital Elevation Model (Michalak 2004) has to be included. The difference between the map from this study and the map by Laske and Masters (1997) is shown in Fig. 5b. Molinari and Morelli (2011) provide a crustal model for the European Plate (EPcrust) with a resolution of 0.5° by 0.5°, from which the thickness of sediments is taken. For a comparison with our basement depth, a Digital Elevation Model (Michalak 2004) has to be included to reduce the thickness to depth in relation to the sea level. The difference between the map from this study and the map by Molinari and Morelli (2011) is shown in Fig. 5c. Tesauro et al. (2008) provide a crustal model for Western and Central Europe and surroundings with 0.25° by 0.25° resolution from which the basement depth is taken for comparison. The difference between the map from this study and the map by Tesauro et al. (2008) is shown in Fig. 5d.

The comparison of our basement map with previously published maps shows many similarities, particularly for the EEC and the WEP. For these areas, differences are in the order of 1 km only for the Laske and Masters (1997) map, and of up to 3 km for the Molinari and Morelli (2011) and the Tesauro et al. (2008) maps. Much larger differences are observed in the TESZ, particularly in NW Poland, and in the Carpathians, particularly in their eastern part. For these areas, differences are larger for the Laske and Masters (1997) map, being up to 6–9 km, while for the Molinari and Morelli (2011) and the Tesauro et al. (2008) maps, the difference is in the order of 4–6 km. A recently published basement depth map for the Central European Basin System (Scheck-Wenderoth and Maystrenko 2013) also shows similar basement pattern in the TESZ area in NW Poland.

Complementary to the basement depth map is the P-wave velocity map of the uppermost basement (Fig. 4b). Velocities Vp > 6 km/s are observed in the EEC, north of the TTZ. However, this cratonic area is not homogeneous. Two distinct boundaries in velocity are marked in Fig. 4b by dashed lines that delineate the Fennoscandia–Sarmatia Suture (FSS) and the Mid-Lithuanian suture zone (MLSZ). The FSS is a suture between two once autonomous crustal segments/megablocks—Fennoscandia and Sarmatia (e.g., Bogdanova et al. 2006, 2008). The second boundary, SW–NE trending belt date from the initial assembly of this part of Baltica by terrane accretion, and is a feature that has been interpreted as the Mid-Lithuanian suture zone (MLSZ; e.g., Skridlaite and Motuza 2001; Skridlaitė et al. 2006). In the area of Lithuania, the MLSZ is 30–40 km wide and its continuation follows the border between Baltic terrane and Polish-Latvian terrane in the area of Poland (Cymerman 2007). The belt between the MLSZ and the FSS is characterized by significantly lower velocities of the uppermost basement. In northeastern Poland, along the state border, the relatively small areas with high P-wave velocities were found. They are interpreted as high-velocity magmatic intrusions beneath profile P4 and beneath the profile P5. Unfortunately, both intrusions are crossed only by one single profile, thus their size and shape could not be determined from these profiles alone. These intrusions are known as anorthosite bodies of Suwałki and Kętrzyn within the Paleoproterozoic (1.50–1.56 Ga) Mazury granitoid complex. The youngest magmatic Neoproterozoic–Paleozoic rocks in the region are intrusions of alkaline rocks (e.g., Tajno intrusion; Ryka 1984); however, they were not crossed by any of the profile. Accordingly they are not visible in the velocity map.

Southwest of the TTZ, velocities of the uppermost basement are significantly lower, being Vp < 6 km/s. Only in southern Poland, in the corner between the Variscan deformation front and the Carpathians, velocities Vp > 6 km/s are observed, in the area of the Upper Silesian Block (USB in Fig. 1).

The P-wave velocity data set consists of 10,804 values extracted from 2D seismic models. Velocity versus depth relations calculated separately for Precambrian, Cadomian, Caledonian, and Variscan basement (see Fig. 7e for location) are shown in Fig. 6. Black lines show a linear fit, wide gray bands show the standard deviation, and fit coefficients are given in Table 1. On average, the Precambrian basement is characterized by velocities that are c. 0.2 km/s higher then for other areas. The velocity gradient for the Precambrian, Cadomian, and Variscan basements is positive, and for each kilometer depth, the velocity increases by 9–11 m/s. An exception is the Caledonian basement for which velocity on average decreases by c. 13 m/s for each kilometer depth. However, this decrease could be artificial as in the depth range of 6000–10,000 m velocities are higher, similar to cratonic, while in the depth range of 10,000–13,000 m velocities are lower, similar to the WEP basement. This could indicate that the Caledonian basement represents a transition at domain between the EEC and the WEP, without a characteristic velocity of its own.

Fig. 6
figure 6

Velocity versus depth relations for P-wave velocities in the uppermost basement calculated separately for Precambrian, Cadomian, Caledonian, and Variscan basements (see Fig. 7e for location). Black dots show velocities taken from 2D seismic refraction profiles (see Fig. 3c for profiles location), black lines show linear fit and wide gray bands show standard deviation. Fit coefficients are given in Table 1

Table 1 Velocity–depth relations for basement in Poland, V(z) = a + bz [m/s], z—depth [m] n—number of velocity samples


Apart from a complex seismic structure, the area of Poland is also associated with significant gravimetric, magnetic, electromagnetic, and heat flow anomalies (Fig. 7). The anomalies indicate major changes of the basement structure and correlate with those evident from seismic data.

Fig. 7
figure 7

Summary of geophysical characteristics of the basement in Poland. a Slope of the basement calculated for the basement map presented in this paper (Fig. 4a); slope values are in degree from horizontal. b Bouguer gravity anomaly map of Poland, displayed as harmonic relief image illuminated from NW (Wybraniec 1999). c Magnetic anomaly map of Poland illuminated from SE (Wybraniec 1999; Petecki et al. 2003; Królikowski 2006). d Heat flow map (Karwasiecka and Bruszewska 1997; Majorowicz et al. 2003); white dots show location of wells with temperature logs. e Map of basement consolidation ages of Poland (Karnkowski 2008). f Position of the TTZ in Poland according to various authors: 1 after Pożaryski et al. (1992), 2 after Dadlez (1982), 3 after Narkiewicz et al. (2011), 4 magnetic line, southern margin of the EEC (Pomeranian Massif) after Królikowski (2006), 5 basement borders after Karnkowski (2008)

The Bouguer anomaly values (Fig. 7b; Królikowski and Petecki 1995; Wybraniec 1999; Bielik et al. 2006) display values as low as −60 mGal over the TESZ. However, the northeasternmost portion of this gravity minimum overlays an intrabasement feature of the EEC. The adjacent Paleozoic terranes to the southwest and the EEC to the northeast are characterized by near-zero to positive gravity anomalies of up to +20 and +10 mGal, respectively. In the Carpathians, Bouguer anomalies reach values of about −80 mGal.

The magnetic anomalies within the TESZ and in the Carpathians (Fig. 7c; Wybraniec 1999; Petecki et al. 2003) are subdued (±100 nT), which may result from the deeply buried magnetic basement. In contrast, the EEC magnetic anomalies vary at short wavelengths from 1500 to +1500 nT and correlate well with tectonic features and intrusions.

The area of the Pomeranian part of TESZ is characterized by relatively low velocities of the uppermost basement (Vp ~ 5.85 km/s), and correlates well with the location of pronounced sub-horizontal conductor found by the electromagnetic studies (Ernst et al. 2008; Jóźwiak 2013). The conductor has a resistivity as low as 2 Ωm, and is interpreted as Silurian–Cambrian metasediments. Its enhanced conductivity may be caused either by electronic conductors (graphite, alum shale) within Caledonian formations initially rich in coal facies, or by saline fluids (crustal brines) located most likely in the vicinity of deep fault systems (Ernst et al. 2008).

Heat flow variations in the area of Poland (Fig. 7d; Karwasiecka and Bruszewska 1997; Majorowicz et al. 2003) indicate a major change in the thermal regime. In general, the TESZ separates a “cold” EEC area with a low heat flow of c. 40 mW/m2 to the northeast from a “hot” area with a higher heat flow of 40–70 mW/m2 in the Paleozoic terranes and Carpathians to the southwest.

The morphology of the geophysical fields, shown in these three maps, coincides in general with the tectonic structure in Poland and has a clear lineation in the NW–SE direction. According to Karnkowski (2008), four principal types of basement structure can be distinguished in the area of Poland: the EEC basement in the northeast, the Caledonian (TESZ) southwest of the EEC edge, the Variscan in SE Poland, and Cadomian basement in the south (Fig. 7e). These features coincide with the map of the basement slope calculated from our basement map (Fig. 7a). Slope values are shown in degree up from horizontal. A small slope is characteristic for the whole area of the EEC, the WEP, and the Cadomian basement. In this map, the TTZ follows the southern edge of the EEC with a slope of 8–12o. The northern edge of the WEP, corresponding to the Variscan deformation front (see Fig. 1), is bounded by a zone with a significant slope of 10–15o. The steepest slope of the basement is observed below the Carpathians, particularly their eastern part, where the basement slope reaches a value of up to c. 20o.

The TTZ in Poland, interpreted as the edge of the EEC, is a NW–SE trending feature. However, its position differs in details according to different authors (Fig. 7f): Dadlez (1982), Pożaryski et al. (1992), Karnkowski (2008), and Narkiewicz et al. (2011). This variation in location may reach up to 50 km. Additionally, the magnetic line bordering the southern margin of the EEC (Pomeranian Massif) after Królikowski (2006) is shown in Fig. 7f.

In an attempt to interpret basement lithologies for the EEC and the WEP based on P-wave velocities (Fig. 6), we have inferred the most plausible lithologies for the uppermost basement by a comparison with global laboratory data for various rock assemblages (Christensen and Mooney 1995). Lithological candidates for the EEC and the WEP basement are shown in Fig. 8. As a reference temperature, we used temperature–depth curves for low, average, and high heat flow thermal regimes (Fig. 8a; Christensen and Mooney 1995). In the upper 10 km of the crust, the published temperature–depth curve for the EEC lies close to the average one (Majorowicz et al. 2003), whereas for the Saxothuringian area the temperature–depth curve lies close to the high heat flow curve (Čermák 1995). The high heat flow curve also fits the temperatures measured directly in the KTB borehole down to a depth of about 9100 m (Emmermann and Lauterjung 1997). Near identical to the low thermal regime curve is the temperature for the central part of the Fennoscandian Shield (Kukkonen et al. 2003). The temperature curve of the WEP in southwest Poland (Majorowicz et al. 2003) is higher even then the high regime curve, and is close to curve D according to Lachenbruch and Sass (1977). Thus, for our comparison between seismic and laboratory data, we used the “hot” regime for the WEP and the “average” regime for the EEC.

Fig. 8
figure 8

a Temperature–depth curves for three heat flow provinces: low, average, and high (Christensen and Mooney 1995). For comparison, dashed curves show the temperature–depth for the Saxothuringian area (Sax; Čermák 1995), Western European Platform (WEP) in southwest Poland, East European Craton (EEC) in northeast Poland (Majorowicz et al. 2003), and for the central part of the Fennoscandian Shield (FSh; Kukkonen et al. 2003). Thick gray line extending to about 10 km shows measured temperature in KTB borehole (Emmermann and Lauterjung 1997). b Comparison of the linear fit of Vp velocities in the uppermost basement in Poland (gray lines) with laboratory data for chosen rocks (Christensen and Mooney 1995): BAS basalt and QTZ quartzite for high-temperature regime of the WEP, and BGN biotite/tonalite/gneiss, GGN granite/gneiss, GRA granite/granodiorite, PHY phyllite and SLT slate for average-temperature regime of the EEP

In Fig. 8b, laboratory data for a high-temperature regime are shown for various rock assemblages. The observed velocities in the WEP basement are close to basalt and quartzite, particularly for the depth range of 10–15 km. Granite/gneiss and biotite/tonalite/gneiss have higher velocities. On the other hand, gneisses are actually the most common lithology exposed in that area (e.g., Mueller 1995), and borehole data from the basement of the Wolsztyn-Leszno High show the occurrence of phyllites.

The relatively low-velocity basement of the TESZ can be interpreted as an extensive pile of low-grade metasediments (e.g., metagraywackes). Alternatively, it may also represent a gneiss complex, if intense NW–SE-oriented anisotropy is assumed consistent with the regional geological context (Jarosiński and Dąbrowski 2006; Środa 2006). Anisotropy has not been taken into account in Fig. 8a, but it should be noted that according to Christensen and Mooney (1995), anisotropy can reach values ranging from 1 to 5 % (e.g., granite/granodiorite, granite/gneiss, basalt, metagraywacke, quartzite) to 10–20 % (e.g., phyllite, slate, amphibolite) in basement rocks.

Close to the margin of the EEC, there is no direct information about the type of rocks and the age of the basement. However, in the northeastern EEC, drill holes have provided considerable information about the Precambrian basement (Ryka 1984; Skridlaite and Motuza 2001). Accordingly, the Palaeoproterozoic crystalline basement of the EEC is mostly composed of granulites, migmatites, anorthosites, and granite/gneisses (e.g., Ryka 1984; Skridlaite and Motuza 2001).


In Poland, the basement in the TESZ and the Carpathians is not reached by boreholes, so its depth and velocity are available only from seismic profiles and can be inferred indirectly by a joint integration of geophysical data. Using all available data, a basement depth map and the distribution of seismic P-wave velocity in the uppermost basement for the area of Poland were created.

The new results of this paper, regarding the seismic basement in the area of Poland, are displayed in three maps: the basement depth map (Fig. 4a), the P-wave velocity map of the uppermost basement (Fig. 4b), and the map of the basement slope (Fig. 7a).

The basement depth map is compared with three basement maps published earlier: global by Laske and Masters (1997), European crustal model EPcrust by Molinari and Morelli (2011), and crustal model for Western and Central Europe by Tesauro et al. (2008). The comparison shows many similarities, particularly for the EEC and the WEP (Fig. 5). In the TESZ in NW Poland, large differences of up to 6–9 km could be explained by another discrimination between the crystalline (Precambrian) and consolidated (Paleozoic) types of crust. Two types of crust are reflected in basement velocities: velocities Vp > 6 km/s are observed in the EEC, north of the TTZ, while southwest of the TTZ velocities of the uppermost basement are significantly lower, being Vp < 6 km/s. The continuation of the structures to the northwest is discussed for the Central European Basin System (Scheck-Wenderoth and Maystrenko 2013) and the Danish area and surroundings (Lassen and Thybo 2012).

Differences of basement velocities for the EEC and the WEP correspond to the density differentiation of both provinces. The EEC basement density of 2.71–2.75 g/cm3 was modeled across the Skagerrak Graben (Lassen and Thybo 2012). In NW Poland, Królikowski and Petecki (2002) obtained a 2D density model along the LT-7 profile with basement values of 2.68 g/cm3 for WEP and 2.82 g/cm3 for EEP. Similar values were applied by Maystrenko and Scheck-Wenderoth (2013) in a 3D density model of the Central European Basin System and adjacent areas: 2.79–2.83 g/cm3 for EEC basement, 2.67 g/cm3 for Variscan granitoids, and 2.79 g/cm3 for Variscan upper crust.

Slightly smaller basement densities were found in Poland in the eastern portion of EEC. The top part of the crystalline Precambrian basement has excellent density evidence thanks to a number of sampled boreholes, deeply penetrating the crystalline basement. Only these boreholes, which penetrate the crystalline basement into depths of at least several tens of meters, were recognized as representative ones, because of the weathering of the surface of the crystalline basement in ancient times and some other processes leading to a decrease in the density at several meters depths. The top of the Precambrian basement represents the “granitoid type” which consists mostly of gneisses, with an average density of 2.72 g/cm3 (Krysiński et al. 2009). Similar basement density values, c. 2.75 g/cm3, were found from 2D gravity modeling along the seismic profile POLCRUST-01 in SE Poland (Narkiewicz et al. 2015). A constant density of 2.70 g/cm3, corresponding to rocks in the top of the crystalline complex of old cratons, was assigned to rocks of the crystalline basement of the EEC in SE Poland by Grabowska and Bojdys (2001).

The map of the basement slope (Fig. 7a) shows two significant features running in NW–SE directions through central Poland: the northern one could be related to the edge of the EEC, while the southern one to the Variscan deformation front (see Fig. 1). The edge of the EEC in Poland, the Teisseyre-Tornquist Zone (TTZ), continues in SW Scandinavia as the Sorgenfrei-Tornquist Zone (STZ). This boundary between Baltica and Phanerozoic Europe is well visible in the basement, Moho depth, as well as in lithospheric thickness (e.g., Lassen and Thybo 2012; Scheck-Wenderoth and Maystrenko 2013; Grad et al. 2009, 2014; Knapmeyer-Endrun et al. 2014; Wilde-Piórko et al. 2010; Puziewicz et al. 2006; Gregersen et al. 2002; Geissler et al. 2010). The gravity modeling suggests a very small density value in the uppermost mantle 3.11 g/cm3 below the younger area of WEP, while for the older area of EEC, it is 3.3 g/cm3 (e.g., Krysiński et al. 2009).

The position of the TTZ in Poland differs according to different geological and geophysical interpretations (Fig. 7f). As suggested by Karnkowski (2008), the tectonic sub-division in the area of Poland should be done at three levels: sub-Cenozoic, sub-Permian, and at the crystalline/consolidated basement. Within these levels, the range of tectonic units could be different. The edge of the EEC in the basement level is relatively clear and defines the southwestern range of the craton. However, another criterion in the continental scale could be one more—crustal criterion, e.g., range of the high velocity lower crust beneath EEC (Grad et al. 2002, 2003a, b, 2008).

Finally, the map of seismic basement depth and basement P-wave velocity map in the area of Poland will be an important contribution to the digital 3D seismic model of the crust and uppermost mantle. Together with detailed data about geometry and velocities in the sedimentary cover (Grad and Polkowski 2012; Polkowski and Grad 2015), and a huge set of regional seismic refraction profiles, they permit for the creation of a detailed model for seismic local, regional, and global studies (Malinowski et al. 2013; Grad et al. 2015).

The basement depth and uppermost basement P-wave velocity maps for the area of Poland, filtered with 30-km-radius boxcar filter, as shown in Fig. 4, can be found in digital form at: