- Email: [email protected]
Movement tendencies of the West Carpathians in the Quaternary
Tectonophysics, 29 (1975) 369-375 @ Elsevier Scientific Publishing Company, Amsterdam - Printed in The Netherlands
MOVEMENT TENDENCIES QUATERNARY
OF THE WEST CARPATHIANS
369
IN THE
J. KVITKOVIC Geographical Institute, Slovak Academy
of Sciences, Bratislava (C.S.S.R.)
(Revised version accepted July 25, 1975)
ABSTRACT Kvitkovi??, J., 1975. Movement tendencies of the West Carpathians in the Quaternary. In: N. Pavoni and R. Green (Editors), Recent Crustal Movements. Tectonophysics, 29 (l-4): 369-375. Characteristic features of the West Carpathians belonging to the system of young Alpine mountain ranges are the contrasts in relief. The compilation of the Map of the Movement Tendencies of the West Carpathians in the Quaternary is based especially on the relief-erosive dissection intensity, on the river terraces, and on the thickness of the Quaternary sediments. The morphographical maps, especially the hypsographic map, the map of mean gradient angle, and that of relief energy were very valuable basic materials. In the resulting map the individual morphostructures are divided into seven groups with different movement intensities. The total amplitude of the Quaternary movements in the West Carpathians attains 300-500 m at least. From the viewpoint of present movements, it is necessary to remark that the morphostructures of highmountain regions with values >+1.5 mm per year are lifted up most intensively, while the morphostructural units of the by-Carpathian depressions sink unevenly with a maximum value of -5.3 mm per year. The total present rate of movement of the earth’s crust in the West Carpathians attains about 7 mm per year. INTRODUCTION
In recent years, within the study of neotectonics and recent movements of the earth’s crust, great attention has been paid to the processes occurring both in the crust and the upper mantle. The result of these processes, of course, in interaction with exogenic processes, is the present-day relief. Thus, on the relief analysis, geomorphologists can contribute greatly in elucidating the endogenic processes mainly as to the neotectonic period. FUNDAMENTAL CARPATHIANS
FEATURES
IN THE DEVELOPMENT
IN THE NEOTECTONIC
OF RELIEF
IN THE WEST
STAGE
A characteristic feature of the morphology of the West Carpathians is their inner dissection, the alternation in short distances of two antagonis-
370
tic forms, the mountain groups and the intermountain basins incised between them. The West Carpathians as a megaform arose successively as late as the neotectonic development stage - i.e. in the Late Tortonian to the Quaternary. As to their relief, several levelling phases occurred in this stage, interrupted by intensive vertical movements as evidenced by the remnants of a few old denudation surfaces preserved in the individual mountain ranges. According to Mazur (1964, 1965), the oldest levelled surface - the top level - arose in the Late Tortonian and in the Sarmatian. Its deformation occurred during the Attican phase of movements. Whereas, for example, in the area of the Klenova in the Male Karpaty this surface is situated at heights of 500-550 m, in the Bumbier area in the Nizke Tatry it rises as high as 2,000 m. The further levelling surface (middle mountain level) was built in the Pannonian. Regionally its spread is considerable. Its development was interrupted in the Rhodanian phase of movements in the Middle Pliocene, when the surface mentioned was broken and unevenly uplifted. By these uneven movements, horsts, arch horsts and eventually grabens were built, from which, in the course of further development, the present-day morphostructures were formed. The deformations of the Pannonian surface attain values of about 1,500 m in the area of eastern Slovakia (Karnis and KvitkoviZ, 1970). In the Late Pliocene, along greater rivers, the third levelled surface the river level - was spreading also in the basins and on the foothills of mountain ranges. In the course of the Quaternary, the river level has been cut and on its slopes five to six river terraces arose. In the mountain ranges the river terraces are found above the present-day river beds at relative heights of 50-150 m, while in the lowlands on the fringes of the Carpathians, they submerge under the Young Quaternary alluvia. It can be seen that in the course of the whole neotectonic development of the Carpathians, the contrast of the relief increased and the orographical units were formed successively. REGIONAL
DIFFERENTIATION
OF INTENSITY
OF THE QUATERNARY
MOVE-
MENTS
From the study of recent movements of the earth’s crust by repeated levellings in the U.S.S.R., as well as from knowledge of the world’s literature, Meshcheryakov (1969) deduced that the recent movements have a general distribution over almost the whole of the earth’s surface. In the literature it is frequently emphasized that neotectonic and also the recent movements are closely related. Starting from this knowledge, and on the basis of attainments in the study of levelled surfaces, river terraces, thickness of the Quaternary sediments and vertical dissection of respective relief types, we can determine the basic movement tendencies of a given territory in the Quaternary period. In compiling the present map of the movement tendencies of the West C.arpathians in the Quaternary (Fig. l), exist-
371
372
ing morphographical maps have also been taken into consideration: the hypsometric map, that of relief energy (Mazur, 1962; Mazur and Maztirova, 1965) and the map of mean gradient angle (Kvitkovic, 1973). From the viewpoint of results the maps mentioned, although compiled by different methods, show a high degree of correlation with contemporary morphostructures. Gerassimov (1969) and Von Gaertner (1969) in particular have recently expressed the rationality and usefulness of these methods in studying the young movements of the earth’s crust as well as the recent. relief. As mentioned, in the Middle Pliocene and Quaternary in the Carpathian area morphostructural units were formed as follows: by-Carpathian lowlands, middle mountains and high mountains, separated from one another by intermountain basins. According to morphographical criteria resulting especially from the map of relief energy, the individual morphostructures are divided into the following seven groups, the distribution of which is represented on the accompanying map. (1) Regions of lowlands, which are noted in the course of the Quaternary for strongly differentiated subsidences, and where the Quaternary sediments, which are predominantly of a fluvial nature, attain a thickness of 10 to over 300 m. The relief energy attains values of O-30 m. (2) Regions of slightly differentiated uplifts (both lowlands and basin hilly lands belong here). The relief energy attains here values of 31---lo0 m. (3) Regions of moderately strong uplifts (lower low-mountains). Here the relief energy attains values of 101-180 m. (4) Regions of mean strong uplifts (higher low-mountains). In this type the relief energy attains values of 181-310 m. (5) Regions of considerably strong uplifts (lower uplands). The relief energy attains values of 311-370 m. (6) Regions of strong uplifts (higher uplands). Here the relief energy attains values of 371-640 m. (7) Regions of extremely strong uplifts (high mountains). Here the relief energy attains values of 641 m and more. The map mentioned represents a fairly telling picture of the geographical distribution of positive or negative trends, as well as of the intensity of the Quaternary movements, which is important also for the study of recent movements of the earth’s crust. Of the West Carpathians, the Vysoke Tatry, Zapadne Tatry, Nizke Tatry and other mountain ranges with glacial or alm relief were most uplifted. Besides glaciation erosion in the high mountains, further morphological evidence for the Quaternary movements can be given in the form of unbalanced gradient curves, convergence of terraces along the streams, occurrence of facetted slopes, antecedent behavior, occurrence of subsequent valleys and so on. Similar evidence can be stated from the area of middle mountains. Of the lowlands, the Podunajska Niiina subsided and also at present continues to subside most intensively, and the thickness of the Quater-
373
nary sediments attains over 300 m in its central parts. The differentiated subsidences of the Zahorski, Podunajska, and Vychodoslovenska Niiinas, as well as the considerable thickness of the Quaternary sediments, are deduced from the lack of river terraces, from the changes in river patterns, buried sand dunes, peats, and from the occurrence of earthquakes as well as from the results of repeated levellings. Further evidence for occurrence of the Quaternary movements is provided by the study of the periglacial alluvial cones of intermountain basins and foothill areas. As to the quantitative determination of these movements for the individual morphostructures, this is relatively difficult, because appropriate studies on the subject are still only at an early stage. LuknilS (1959,1973) ascribes to the Young Pliocene to Quaternary uplifts in the Vysoke Tatry values of 300-400 m. At the same time with the uplifts denudation processes are also taking place, which are of a considerably lesser intensity and which lead to the lowering of the surface. Luknig (1973) states that in the course of the Holocene Epoch the Tatran ridges were lowered in average by 5 m, which is probably an extreme value for the whole West Carpathian area. According to present knowledge, the total amplitude of the Quaternary movements of the West Carpathian area attains a value at least of 300-500 m, which for a relatively short time period of about 1.5 million years corresponds to a fairly high rate of movement. The movement tendencies of the individual morphostructures, and eventually of the morphostructural groups, have a close relation to geological processes occurring in the earth’s crust. Above all, high positive anomalies of heat flows are noted for intensively differentiated subsidences of the lowlands and of the Liar Basin. This fact points to active deep processes under the depressions mentioned and at the same time it demonstrates their contemporary tectonic activity. Further it is necessary to mention the fault disturbances, which reflect in the morphology, and especially the disturbances which also manifest themselves today. These have been indicated on the map both on the basis of findings by geologico-morphological methods as well as by means of repeated levellings. Recent disturbances manifest themselves especially at the fringes of the lowlands, the sub-Tatran and Hornad faults, the faults at the fringes of both the Fatras, as well as the disturbances along the contact between the Slovenske Rudohorie and the basins (KvitkoviE and Vanko, 1972) are also active. These statements are also confirmed to a considerable degree by the distribution of the epicentres of earthquakes (Karnik et al., 1957). The presented Map of the Movement Tendencies of the West Carpathians in the Quaternary, in comparison with the knowledge of presentday movements of the earth’s crust (gained by means of geodetic methods), shows a considerable correlation of these movements. For instance, our
374
high-mountain areas, which were lifted up extremely strongly in the Quaternary, are lifting up even today with an intensity +1.5 mm per year and more. The movements in the by-Carpathian lowlands are suggested, e.g., by Quaternary sediments up to 300 m thick. In the lowlands, subsidences with a maximum value of --5.3 mm per year also occur at the present (KvitkoviE and Vanko, 1972). At the same time the value mentioned represents the strongest subsidence of an area within the whole country and it is situated between Gbelce and Sttirovo in the eastern part of the Danube Lowland. Finally, the middle-mountain areas are lifting up differentially, attaining values of about 1 mm per year (Kvitkovii: and Vanko, 1971,1972; VyskoEil, 1972; Kopecky and VyskoZil, 1972).
CONCLUSION
The tectonic processes played a very important role in forming the present-day relief of the West Carpathians in the course of Younger Neogene and Quaternary. In this contribution, the Quaternary tectonics is emphasized, the knowledge of which is necessary in studying recent movements. From the presented map it results that respective morphostructures with different movement tendencies are separated from one another by disturbances which were active in the Pleistocene and eventually also today. Further, it may be inferred that in the West Carpathian area differentiated movements in the mountain ranges have unambiguously positive values, while in the lowlands subsidences with a considerable intensity prevailed. An intermediate category of movements between the subsiding lowlands and the uplifting mountain ranges is represented by intermountain basins, especially those with Flysch filling. The total amplitude of the Quaternary movements in the Carpathian area attains 300-500 m. The amplitude of present-day movements attains 7 mm per year.
REFERENCES Gerassimov, I.P., 1969. Geomorphological expression of neotectonics. Mouvements modernes, volcanisme et seismes sur les continents et les fonds oceaniques. Pour le VIII Congr’es de I’INQUA Paris, 1969. Nauka, Moscow, pp. 40-46. Karnik, V., Michal, E. and MolnCr, A., 1957. Erdbebe_nkatalog der Tschechoslowakei bis zum Jahre 1956. Price Geofysikilniho ustavu CSAV, 69: 411-598. KarniS, J. and KvitkoviE, J., 1970. An Outline of the Geomorphological Conditions of Eastern Slovakia. SNP, Bratislava, 220 pp. Kopecky, A. and VyskoEil, P., 1972. Recent earth’s surface movements in Czechoslovakia established by geodetic measurements. V&tn. U&Ted. Ustavu geol., 47 (3): 129-139. KvitkoviE, J., 1973. Karte des mittleren Hangwinkels der Westkarpaten. Maszstab 1: 500 000. Archiv des Geographischen Institutes der SAV, Bratislava.
375 KvitkoviE, J. and Vanko, J., 1971. Studium der rezenten Erdkrustenbewegungen auf dem Gebiet der Slowakei. Geograficky Easopis, XXIII (2): 124-132. Kvitkovic’, J. and Vanko, J., 1972. Recent crustal movements in the region of eastern Slovakia. GeografickJi &sopis, XXIV (2): 151-163. Luknili, M., 1959. Relief und die Zerlegung quartarer Formationen in der Hohen Tatra und in ihrem Vorland. Geologicky sb., X (1): 233-268. Luknig, M., 1973. Relief der Hohen Tatra und ihr Vorland. Verlag SAV, Bratislava, 375 pp. Maziir, E., 1962. Hypsometrische Karte der Slowakei. Maszstab 1 : 500 000. Archiv des Geographischen Institutes SAV, Bratislava. Mazur, E., 1964. Intermountain basins - a characteristic element in the relief of Slovakia. Geograficky Easopis, XVI (2): 105-126. Mazur, E., 1965. Major features of the West Carpathians in Slovakia as a result of young tectonic movements. In: Geomorphological Problems of the Carpathians. Slovak Academy of Sciences, Bratislava, pp. 9-53. Maztir, E. and Mazdrova, V., 1965. Karte der Reliefenergie der Slowakei und ihre Anwendung bei der geographischen Rayonierung. Geografickgi casopis, XVII (1): 3-18. Meshcheryakov, Yu.A., 1969. Map of contemporary crustal movements in Europe and its relation of the neotectonic maps. Mouvements modernes, volcanisme et seismes sur les continents et les fonds oceaniques. Pour le VIII Congres de 1’ INQUA Paris, 1969, Nauka, Moscow, pp. 28-34. Von Gaertner, H.R., 1969. Some considerations concerning compilation of neotectonic map of Europe. Mouvements modernes, volcanisme et seismes sur les continents et les fonds oceaniques. Pour le VIII Congres de 1’ INQUA Paris, 1969. Nauka, Moscow, pp. 38-39. Vyskocil, P., 1972. Basic tendency of the recent vertical earth’s crust movements on the territory of Czechoslovakia. Geodeticky a kartografickf obzor, 18 (9): 239-244.
MOVEMENT TENDENCIES QUATERNARY
OF THE WEST CARPATHIANS
369
IN THE
J. KVITKOVIC Geographical Institute, Slovak Academy
of Sciences, Bratislava (C.S.S.R.)
(Revised version accepted July 25, 1975)
ABSTRACT Kvitkovi??, J., 1975. Movement tendencies of the West Carpathians in the Quaternary. In: N. Pavoni and R. Green (Editors), Recent Crustal Movements. Tectonophysics, 29 (l-4): 369-375. Characteristic features of the West Carpathians belonging to the system of young Alpine mountain ranges are the contrasts in relief. The compilation of the Map of the Movement Tendencies of the West Carpathians in the Quaternary is based especially on the relief-erosive dissection intensity, on the river terraces, and on the thickness of the Quaternary sediments. The morphographical maps, especially the hypsographic map, the map of mean gradient angle, and that of relief energy were very valuable basic materials. In the resulting map the individual morphostructures are divided into seven groups with different movement intensities. The total amplitude of the Quaternary movements in the West Carpathians attains 300-500 m at least. From the viewpoint of present movements, it is necessary to remark that the morphostructures of highmountain regions with values >+1.5 mm per year are lifted up most intensively, while the morphostructural units of the by-Carpathian depressions sink unevenly with a maximum value of -5.3 mm per year. The total present rate of movement of the earth’s crust in the West Carpathians attains about 7 mm per year. INTRODUCTION
In recent years, within the study of neotectonics and recent movements of the earth’s crust, great attention has been paid to the processes occurring both in the crust and the upper mantle. The result of these processes, of course, in interaction with exogenic processes, is the present-day relief. Thus, on the relief analysis, geomorphologists can contribute greatly in elucidating the endogenic processes mainly as to the neotectonic period. FUNDAMENTAL CARPATHIANS
FEATURES
IN THE DEVELOPMENT
IN THE NEOTECTONIC
OF RELIEF
IN THE WEST
STAGE
A characteristic feature of the morphology of the West Carpathians is their inner dissection, the alternation in short distances of two antagonis-
370
tic forms, the mountain groups and the intermountain basins incised between them. The West Carpathians as a megaform arose successively as late as the neotectonic development stage - i.e. in the Late Tortonian to the Quaternary. As to their relief, several levelling phases occurred in this stage, interrupted by intensive vertical movements as evidenced by the remnants of a few old denudation surfaces preserved in the individual mountain ranges. According to Mazur (1964, 1965), the oldest levelled surface - the top level - arose in the Late Tortonian and in the Sarmatian. Its deformation occurred during the Attican phase of movements. Whereas, for example, in the area of the Klenova in the Male Karpaty this surface is situated at heights of 500-550 m, in the Bumbier area in the Nizke Tatry it rises as high as 2,000 m. The further levelling surface (middle mountain level) was built in the Pannonian. Regionally its spread is considerable. Its development was interrupted in the Rhodanian phase of movements in the Middle Pliocene, when the surface mentioned was broken and unevenly uplifted. By these uneven movements, horsts, arch horsts and eventually grabens were built, from which, in the course of further development, the present-day morphostructures were formed. The deformations of the Pannonian surface attain values of about 1,500 m in the area of eastern Slovakia (Karnis and KvitkoviZ, 1970). In the Late Pliocene, along greater rivers, the third levelled surface the river level - was spreading also in the basins and on the foothills of mountain ranges. In the course of the Quaternary, the river level has been cut and on its slopes five to six river terraces arose. In the mountain ranges the river terraces are found above the present-day river beds at relative heights of 50-150 m, while in the lowlands on the fringes of the Carpathians, they submerge under the Young Quaternary alluvia. It can be seen that in the course of the whole neotectonic development of the Carpathians, the contrast of the relief increased and the orographical units were formed successively. REGIONAL
DIFFERENTIATION
OF INTENSITY
OF THE QUATERNARY
MOVE-
MENTS
From the study of recent movements of the earth’s crust by repeated levellings in the U.S.S.R., as well as from knowledge of the world’s literature, Meshcheryakov (1969) deduced that the recent movements have a general distribution over almost the whole of the earth’s surface. In the literature it is frequently emphasized that neotectonic and also the recent movements are closely related. Starting from this knowledge, and on the basis of attainments in the study of levelled surfaces, river terraces, thickness of the Quaternary sediments and vertical dissection of respective relief types, we can determine the basic movement tendencies of a given territory in the Quaternary period. In compiling the present map of the movement tendencies of the West C.arpathians in the Quaternary (Fig. l), exist-
371
372
ing morphographical maps have also been taken into consideration: the hypsometric map, that of relief energy (Mazur, 1962; Mazur and Maztirova, 1965) and the map of mean gradient angle (Kvitkovic, 1973). From the viewpoint of results the maps mentioned, although compiled by different methods, show a high degree of correlation with contemporary morphostructures. Gerassimov (1969) and Von Gaertner (1969) in particular have recently expressed the rationality and usefulness of these methods in studying the young movements of the earth’s crust as well as the recent. relief. As mentioned, in the Middle Pliocene and Quaternary in the Carpathian area morphostructural units were formed as follows: by-Carpathian lowlands, middle mountains and high mountains, separated from one another by intermountain basins. According to morphographical criteria resulting especially from the map of relief energy, the individual morphostructures are divided into the following seven groups, the distribution of which is represented on the accompanying map. (1) Regions of lowlands, which are noted in the course of the Quaternary for strongly differentiated subsidences, and where the Quaternary sediments, which are predominantly of a fluvial nature, attain a thickness of 10 to over 300 m. The relief energy attains values of O-30 m. (2) Regions of slightly differentiated uplifts (both lowlands and basin hilly lands belong here). The relief energy attains here values of 31---lo0 m. (3) Regions of moderately strong uplifts (lower low-mountains). Here the relief energy attains values of 101-180 m. (4) Regions of mean strong uplifts (higher low-mountains). In this type the relief energy attains values of 181-310 m. (5) Regions of considerably strong uplifts (lower uplands). The relief energy attains values of 311-370 m. (6) Regions of strong uplifts (higher uplands). Here the relief energy attains values of 371-640 m. (7) Regions of extremely strong uplifts (high mountains). Here the relief energy attains values of 641 m and more. The map mentioned represents a fairly telling picture of the geographical distribution of positive or negative trends, as well as of the intensity of the Quaternary movements, which is important also for the study of recent movements of the earth’s crust. Of the West Carpathians, the Vysoke Tatry, Zapadne Tatry, Nizke Tatry and other mountain ranges with glacial or alm relief were most uplifted. Besides glaciation erosion in the high mountains, further morphological evidence for the Quaternary movements can be given in the form of unbalanced gradient curves, convergence of terraces along the streams, occurrence of facetted slopes, antecedent behavior, occurrence of subsequent valleys and so on. Similar evidence can be stated from the area of middle mountains. Of the lowlands, the Podunajska Niiina subsided and also at present continues to subside most intensively, and the thickness of the Quater-
373
nary sediments attains over 300 m in its central parts. The differentiated subsidences of the Zahorski, Podunajska, and Vychodoslovenska Niiinas, as well as the considerable thickness of the Quaternary sediments, are deduced from the lack of river terraces, from the changes in river patterns, buried sand dunes, peats, and from the occurrence of earthquakes as well as from the results of repeated levellings. Further evidence for occurrence of the Quaternary movements is provided by the study of the periglacial alluvial cones of intermountain basins and foothill areas. As to the quantitative determination of these movements for the individual morphostructures, this is relatively difficult, because appropriate studies on the subject are still only at an early stage. LuknilS (1959,1973) ascribes to the Young Pliocene to Quaternary uplifts in the Vysoke Tatry values of 300-400 m. At the same time with the uplifts denudation processes are also taking place, which are of a considerably lesser intensity and which lead to the lowering of the surface. Luknig (1973) states that in the course of the Holocene Epoch the Tatran ridges were lowered in average by 5 m, which is probably an extreme value for the whole West Carpathian area. According to present knowledge, the total amplitude of the Quaternary movements of the West Carpathian area attains a value at least of 300-500 m, which for a relatively short time period of about 1.5 million years corresponds to a fairly high rate of movement. The movement tendencies of the individual morphostructures, and eventually of the morphostructural groups, have a close relation to geological processes occurring in the earth’s crust. Above all, high positive anomalies of heat flows are noted for intensively differentiated subsidences of the lowlands and of the Liar Basin. This fact points to active deep processes under the depressions mentioned and at the same time it demonstrates their contemporary tectonic activity. Further it is necessary to mention the fault disturbances, which reflect in the morphology, and especially the disturbances which also manifest themselves today. These have been indicated on the map both on the basis of findings by geologico-morphological methods as well as by means of repeated levellings. Recent disturbances manifest themselves especially at the fringes of the lowlands, the sub-Tatran and Hornad faults, the faults at the fringes of both the Fatras, as well as the disturbances along the contact between the Slovenske Rudohorie and the basins (KvitkoviE and Vanko, 1972) are also active. These statements are also confirmed to a considerable degree by the distribution of the epicentres of earthquakes (Karnik et al., 1957). The presented Map of the Movement Tendencies of the West Carpathians in the Quaternary, in comparison with the knowledge of presentday movements of the earth’s crust (gained by means of geodetic methods), shows a considerable correlation of these movements. For instance, our
374
high-mountain areas, which were lifted up extremely strongly in the Quaternary, are lifting up even today with an intensity +1.5 mm per year and more. The movements in the by-Carpathian lowlands are suggested, e.g., by Quaternary sediments up to 300 m thick. In the lowlands, subsidences with a maximum value of --5.3 mm per year also occur at the present (KvitkoviE and Vanko, 1972). At the same time the value mentioned represents the strongest subsidence of an area within the whole country and it is situated between Gbelce and Sttirovo in the eastern part of the Danube Lowland. Finally, the middle-mountain areas are lifting up differentially, attaining values of about 1 mm per year (Kvitkovii: and Vanko, 1971,1972; VyskoEil, 1972; Kopecky and VyskoZil, 1972).
CONCLUSION
The tectonic processes played a very important role in forming the present-day relief of the West Carpathians in the course of Younger Neogene and Quaternary. In this contribution, the Quaternary tectonics is emphasized, the knowledge of which is necessary in studying recent movements. From the presented map it results that respective morphostructures with different movement tendencies are separated from one another by disturbances which were active in the Pleistocene and eventually also today. Further, it may be inferred that in the West Carpathian area differentiated movements in the mountain ranges have unambiguously positive values, while in the lowlands subsidences with a considerable intensity prevailed. An intermediate category of movements between the subsiding lowlands and the uplifting mountain ranges is represented by intermountain basins, especially those with Flysch filling. The total amplitude of the Quaternary movements in the Carpathian area attains 300-500 m. The amplitude of present-day movements attains 7 mm per year.
REFERENCES Gerassimov, I.P., 1969. Geomorphological expression of neotectonics. Mouvements modernes, volcanisme et seismes sur les continents et les fonds oceaniques. Pour le VIII Congr’es de I’INQUA Paris, 1969. Nauka, Moscow, pp. 40-46. Karnik, V., Michal, E. and MolnCr, A., 1957. Erdbebe_nkatalog der Tschechoslowakei bis zum Jahre 1956. Price Geofysikilniho ustavu CSAV, 69: 411-598. KarniS, J. and KvitkoviE, J., 1970. An Outline of the Geomorphological Conditions of Eastern Slovakia. SNP, Bratislava, 220 pp. Kopecky, A. and VyskoEil, P., 1972. Recent earth’s surface movements in Czechoslovakia established by geodetic measurements. V&tn. U&Ted. Ustavu geol., 47 (3): 129-139. KvitkoviE, J., 1973. Karte des mittleren Hangwinkels der Westkarpaten. Maszstab 1: 500 000. Archiv des Geographischen Institutes der SAV, Bratislava.
375 KvitkoviE, J. and Vanko, J., 1971. Studium der rezenten Erdkrustenbewegungen auf dem Gebiet der Slowakei. Geograficky Easopis, XXIII (2): 124-132. Kvitkovic’, J. and Vanko, J., 1972. Recent crustal movements in the region of eastern Slovakia. GeografickJi &sopis, XXIV (2): 151-163. Luknili, M., 1959. Relief und die Zerlegung quartarer Formationen in der Hohen Tatra und in ihrem Vorland. Geologicky sb., X (1): 233-268. Luknig, M., 1973. Relief der Hohen Tatra und ihr Vorland. Verlag SAV, Bratislava, 375 pp. Maziir, E., 1962. Hypsometrische Karte der Slowakei. Maszstab 1 : 500 000. Archiv des Geographischen Institutes SAV, Bratislava. Mazur, E., 1964. Intermountain basins - a characteristic element in the relief of Slovakia. Geograficky Easopis, XVI (2): 105-126. Mazur, E., 1965. Major features of the West Carpathians in Slovakia as a result of young tectonic movements. In: Geomorphological Problems of the Carpathians. Slovak Academy of Sciences, Bratislava, pp. 9-53. Maztir, E. and Mazdrova, V., 1965. Karte der Reliefenergie der Slowakei und ihre Anwendung bei der geographischen Rayonierung. Geografickgi casopis, XVII (1): 3-18. Meshcheryakov, Yu.A., 1969. Map of contemporary crustal movements in Europe and its relation of the neotectonic maps. Mouvements modernes, volcanisme et seismes sur les continents et les fonds oceaniques. Pour le VIII Congres de 1’ INQUA Paris, 1969, Nauka, Moscow, pp. 28-34. Von Gaertner, H.R., 1969. Some considerations concerning compilation of neotectonic map of Europe. Mouvements modernes, volcanisme et seismes sur les continents et les fonds oceaniques. Pour le VIII Congres de 1’ INQUA Paris, 1969. Nauka, Moscow, pp. 38-39. Vyskocil, P., 1972. Basic tendency of the recent vertical earth’s crust movements on the territory of Czechoslovakia. Geodeticky a kartografickf obzor, 18 (9): 239-244.