Neotectonic movements in the carpathians

Tectonophysics, 104 (1984) 195-204 Elsevier Science Publishers B.V., Amsterdam - Printed in The Netherlands

195

Letter Section Neotectonic

movements

in the Carpathians

WITOLD ZUCHIEWICZ I~stitate of Geological Krakbw (Poland)

Sciences,

(Received April 25,1983;

J~ie~lo~ian

Uniuersity,

2A ~~eand~

Str., 30-063

revised version accepted December 7, 1983)

ABSTRACT Zuchiewicz, W., 1984. 195-204.

Neotectonic

movements in the Carpathians. Tectonophysics,

104:

This article discusses the main results of neotectonic investigations in the Polish Carpathians. Longitudinal elevations and isolated blocks have been uplifted at different rates, ranging from 0.05 to 0.3 mmfyr. Intramontane basins and longitudinal depressions reveal subsidence attaining 0.12 mm&r. Presentday velocities of vertical movements attain 3 mm annually while the contemporary thrusting of the Carpathians onto their foreland is from 2 to 6 mm/yr. Four Quaternary episodes of increased tectonic activity have been distinguished: at the Pliocene-Pleistocene boundary, in the Early Pleistocene, before the MatuyamaBrunhes boundary and during the Holsteinian Interglacial. The latter is thought to be the most prominent.

INTRODUCTION

According to Miirner (1978), neotectonic movements have no real boundary back in time, They include all time-scales of movement: from seismic, Holocene, Pleistocene up to Pliocene ones. It is widely accepted that the time of the beginning of the “neotectonic stage” was different in various parts of the world. In the U.S.A., Japan, Western Europe and Romania the lower limit of neotectonics is usually put at the Pliocene-Pleistocene boundary (Stille, 1955; Pannekoek, 1960) or in the Early Pliocene (Kaizuka, 1975). In Czechoslovakia, however, the neotectonic stage is thought to comprise Neogene~ua~rn~ movements (Ivan and Zeman, 1974). Nikolaev (1982) proposes placing the beginning of neotectonics in Southern Asia in the Eocene. In the Balkan Mts. these movements are considered to have begun in Sarmatian times (Jaranoff, 1963), whereas in the U.S.S.R. they are confined to the period that began after the cessation of folding in the Alpides (Gofshtein, 1964; Astakhov, 1971). Riihle (1976) and KvitkoviE and PlanEar (1975) relate the beginning of neotectonics in the Carpathians to the Upper Badenian. The movements assigned to Late Sarmatian, Pliocene and Quatemary 0040-1951/84/$03.00

0 1984 Elsevier Science Publishers B.V.

196

times can characterize the neotectonic stage of the development of the Carpathians (Wojcik and Zuchiewicz, 1979). It was the time when Carpathian morphology was being formed. Tectonic mobility during this period is thought to have produced large-scale upward of the Flysch Carpathians (Klimaszewski, 1966) and/or differential faulting (Bashenina et al., 1969). These processes began in Middle Badenian times (Kvitkovic, 1978). STATE

OF KNOWLEDGE

Extensive reviews concerning previous neotectonic investigations in the West Carpathians were published by a number of geologists (Klimaszewski, 1966; Starkel, 1972; Henkiel, 1977-1978, KvitkoviE, 1978). Drainage patterns and main geomorphic units were confined to transverse and longitudinal undulations of the orogen (Teisseyre, 1921, 1928; Klimaszewski, 1965; Starkel, 1972), as well as to deep-reaching tectonic structures (Henkiel, 1975; Starkel, 1976; Zuchiewicz, 1981). Many authors dealt with planation surfaces and the relationships between their deformations and the distribution of tectonic depressions and elevations (Klimaszewski, 1965; Starkel, 1972, 1975; Baumgart-Kotarba et al., 1976; Henkiel, 1977-1978). Among a number of neotectonic maps hitherto prepared for the Carpathian arc, that by Kopecky (1972) should be mentioned, as it represents the morphostructural differentiation of the Slovak Carpathians. This zonality was, however, based mainly on hypsometric criteria. NEOTECTONIC

STRUCTURES

The varying thickness of the flysch deposits in the Outer Carpathians, being related to transverse elevations and depressions within the substratum, reflects the prolongation of foreland structures under the Carpathian orogen (Figs. 1 and 2). The distribution of these blocks determines the existence of neotectonic structures, while the amplitudes and intensity of Plio-Quaternary movements seem to relate to the orientation of deep-reaching faults (Henkiel, 1975; Zuchiewicz, 1981). Areas which have been uplifted during the whole Quaternary comprise axes of longitudinal elevations whereas large depressions are associated with the lower courses of Carpathian rivers and with intramontane troughs. AMPLITUDES

Studies on planation surfaces (Klimaszewski, 1948, 1972; Gofshtein, 1964, 1979; Cys, 1966; Starkel, 1969, 1972; Mazur, and CinEura, 1975) have shown that during the Moldavian, Attican, Rhone and Valachian phases, erosional dissection of the West Carpathians was from 280 to 400 m and rose within the East Carpathians up to 820-1000 m. The greatest deformations characterized the Attican and Rhone phases, when the dissection of the West Carpathians was from 60 to 90 m in the west to 120-200 m in

197

the east and 200-300 m in the south. Similar figures for the East Carpathians were up to 250-400 m. The remaining phases showed much smaller amount of uplift.

400km

Fig. 1. Schematic structural division of the Carpathians (partly after Royden et al., 1982). 1 = molasse deposits, 2 = Outer Carpathians, 3 = Inner Carpathians, 4 = area shown in Fig. 2. BM -Bohemian Massif, E - East European Platform, EA - Eastern Alps, SA - Southern Alps, PA - peri-Adriatic line, WC - West Carpathians, EC - East Carpathians, SC South Carpathians, Vr - Vrancea Region, A - Apuseni Mountains, M - Moesia, PB Pannonian Basin, DA - Dinsric Alps, V - Vardar Zone.

Fig. 2. Sketch of deep crustal elements of the Polish Carpathians. 1 = Carpathian overthrust, 2 = fractures within the Carpathian substratum, 3 = Pieniny Klippen Belt, 4 = axis of negative gravimetric anomaly, 5 = southern border of the Epivariscan Platform, 6 = epicentres of earthquakes, 7 = earthquakes recorded on the Polish territory of epicentres situated in the Slovak Carpathians.

198

The total amount of Neogene subsidence in the Polish Internal Carpathians attained 900-1600 m (Watycha, 1976). This subsidence was accompanied by simultaneous uplift of the surrounding mountain ranges, from 200 to 550 m (Zuchiewicz, 1980). The degree of Quaternary uplift is different in various parts of the Carpathian arc and ranges from 80 to 150 m in the Polish (Starkel, 1969) and from 100 to 150 m in the East Carpathians (Gofshtein, 1979) to 320 m in the Vrancea Region and even 400-900 m in the South Carpathians (Popp, 1980). The Pannonian Basin reveals simultaneous subsidence, of up to 370650 m, including 170-250 m during the past 0.9 Ma (Ronai, 1981). This tendency was disturbed in the Holocene by uplift movements of isolated blocks thereby forming the basin (Joo et al., 1981). According to Slovak geologists (Kvitkoviti and Vanko, 1972; Kvitkovic, 1975), the amplitude of Quatemary uplift in the West Carpathians is 300-500 m. RATES

The whole Carpathian arc seems to reveal a transverse zonality of distribution and intensity of vertical movements, dependent on a block-type tectonic pattern (Somov, 1974). Axes of longitudinal elevations have shown varying rates of Quatemary upheaval, from 0.06 to 0.3 mm/yr. These figures are greater in the Holocene within axial parts of mountain ranges and diminish or change their sign along the mountain margins. Intramontane basins and longitudinal depressions have been subsiding at a rate of -0.05 to -0.12 mm/yr. These areas include intramontane troughs filled with thick Neogene and Quaternary sediments. The changing intensity of vertical movements led to deformations of terrace levels. These deformations seem frequently to be related to reactivated Tertiary faults and fold axes. According to KvitkoviE (1975, 1978), the present-day intensity of the West Carpathian uplift exceeds +1.5 mm/yr, whereas the rate of subsidence within adjoining lowlands is -5.3 mm annually. The most recent geodetic relevellings (Job et al., 1981) reveal intensive uplift in the eastern part of the Outer Carpathians of up to +3 mm/yr. There is also some evidence pointing to the presence of contemporary horizontal movements, observed in the northwestern (VyskoEiI, 1979, 1982) and northeastern (Liszkowski, 1975) parts of the flysch Carpathians. Annual rates of these movements are l-l.5 mm in the West and 2-6 mm in the East Carpathians (Somov and Kuznetsova, 1975). NEOTECTONIC

PHASES

On the basis of a morphostructural and neotectonic analysis, it is possible to distinguish several tectonic episodes (phases s.l.), running diachronically along the Alpine chain. The age of these episodes correlated with 1.8, 0.9,

199

0.5 and 0.3 Ma B.P. in the Alps, 0.9 Ma in the Central West Carpathians, 1.8 and 0.9 Ma in the East Carpathians, 1.8 and 0.7 Ma in the East Carpathian Foredeep, 0.9, 0.4 and 0.03 Ma in the Caucasus (Fig. 3). The above ages coincide reasonably with those described by Kukla (1932), namely: 3.0,2.0, 1.6,0.8 and 0.4 Ma B.P.

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According to Lukina (1982), neotectonic phases in the East Carpathians manifested themselves at the end of the Pliocene, at the EopleistoceneEarly Pleistocene boundary, at the decline of the Early Pleistocene, and in the Middle and Late Pleistocene, as well as during Holocene times.

200 Within the Pannonian Basin two Plio-Pleistocene phases have been distinguished (Ronai, 1981): Valachian and Pasadenian. The Pasadenian itself consists of three subphases: the Danube (2-0.9 Ma B.P.), Koros (0.9-0.4 Ma) and Tisza (0.4-0.01 Ma). The fastest subsidence is thought to have developed during the Danube subphase. According to hitherto published papers and the author’s own investigations in the West Carpathians, there are indications of four Quaternary episodes showing increased tectonic activity: (1) At the Pliocene-Pleistocene boundary an uplift of the Central West Carpathians, as well as the East and South Carpathians, took place (HarEar, 1975). In the Pannonian Basin the Late Valachian phase was then active (Pecsi, 1976). There occurred changes in the river network along the contact between the Carpathians and the Bohemian Massif (Zeman, 1979). Longitudinal elevations of the flysch Carpathians were also uplifted (Starkel, 1972; Zuchiewicz, 1982) while intramontane troughs underwent subsidence (Klimaszewski, 1967). Within the North Polish Lowland, the Malopolanian movements are reported to have begun (Baraniecka, 1975). (2) During the Early Quaternary times the main phase of uplift in the Alps is reported to have operated (Winkler-Hermaden, 1955); this was connected with the onset of Pasadenian movements. Meanwhile, the Romanian Carpathians (Popp, 1980) and Stara Planina Mts. (Kanev, 1965) were rising up and the Pannonian Basin was being lowered by the Danube movements (Ronai, 1981). The same applies to intramontane depressions within the Polish Carpathians (Niedzielski, 1971). (3) Another stage of increased tectonic activity relates to a period preceding the Matuyama-Brunhes boundary (Sibrava, 1980). In the Bohemian Massif it was a period of the Drahany neovolcanic and neotectonic phase (Sibrava and Havlizek, 1980), while in the Pannonian Lowland the Koros negative movements prevailed (Banacky et al., 1965; Pecsi, 1976; Ronai, 1981). These movements led to changes in the river pattern and caused disturbances in terrace profiles of the Slovak rivers (HarEar, 1975; Vass, 1979). (4) The last main tectonic phase, which embraced practically the whole of Europe, manifested itself during the Holsteinian (Mindel-Riss). Axial parts of mountain ranges were then uplifted (Riihle, 1976; Banacky, 1978) and, in the Romanian Carpathians, new fold structures began to develop (Starkel, 1969). Intramontane troughs suffered strong subsidence and 1972; Pecsi, faulting (Banackjr et al., 1965; LukniH, 1959; Ksiazkiewicz, 1976; Zuchiewicz, 1981). In the Pannonian Basin this tectonic episode coincided with the decline of the Kijrijs subphase (Ronai, 1981). It was ak& the time when the uplift of the Alps took place (Winkler-Hermaden, 1955; Genieser, 1962) and was connected with the so-called Ortenau phase. The North Polish Lowland was then affected by the Masovian phase (Baraniecka, 1975). After the above phase had ceased, there occurred a number of minor tectonic episodes although their intensity and extent were much Smaller (Eemian, Late Glacial, Holocene).

201

The greatest intensity and importance phase connected with the Holsteinian.

should, therefore,

be applied to the

FUTURE TASKS

A number of problems associated with main directions of neotectonic investigations within the Carpathians have to be resolved in the nearest future: (1) A detailed geomorpholo~c~ map of the Carpathians is needed, with special reference to absolute chronology of forms and deposits. (2) Thorough studies should be made of river terraces and deformations of their longitudinal profiles, together with quantitative analyses of the impact of climatic factors upon river erosion. (3) Studies are required on mesostructures, especially joints. Not every joint system in the Carpathian flysch is associated with folding and the following nappe thrusting. Some of the joints may relate to younger episodes of deformation. (4) The role of isostatic rebound in the Carpathian Foothills after the retreat of the Scandinavian icesheet and the melting of mountain glaciers should be studied. (5) Geodetic repeated me~uremen~ need to be made aiming at the precise reconstruction of the pattern of vertical and horizontal movements.

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204 Wojcik, A. and Zuchiewicz, W., 1979. The present state of studies on the neotectonics of the West Carpathians. Przegl. Geol., 8: 458-461. Zeman, J., 1979. Dynamics of the crustal block structure of the Bohemian Massif. In: J. Vanek (Editor), Geodynamic Investigations in Czechoslovakia. Veda, Bratislava. Zuchiewicz, W., 1980. Young tectonic movements and morphology of the Pieniny Mts. (Polish West Carpathians). Ann. Sot. Geol. Pol., 50: 263-300. Zuchiewicz, W., 1981. The Late Neogene-Quaternary tectonics of the Polish West Carpathians. Bull. INQUA, Neotect. Comm., 4: 57-59. Zuchiewicz, W., 1982. A contribution to the study of neotectonic movements of the Polish Carpathians. Bull. INQUA, Neotect. Comm., 5: 10-19.