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The Vegetational History of Local Flora and Evidences of Human Activities Recorded in the Pollen Diagram from Side Regetovka, Ne Slovakia

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The Vegetational History of Local Flora and Evidences of Human Activities Recorded in the Pollen Diagram from Side Regetovka, Ne Slovakia Acta Palaeobot. 35 (2): 253-274, 1995 THE VEGETATIONAL HISTORY OF LOCAL FLORA AND EVIDENCES OF HUMAN ACTIVITIES RECORDED IN THE POLLEN DIAGRAM FROM SIDE REGETOVKA, NE SLOVAKIA AGNIESZKA WACNIK W. Szafer Institute of Botany, Polish Academy of Sciences, Lubicz 46, 31-512 Krakow, Poland ABSTRACT. Material for this palynological study comes from a fen at the village Regetovka (Slovakian part of the Low Beskids). Five samples of deposit were radiocarbon dated. The results of pollen analysis were used to reconstruct the successional changes in the plant cover during the Middle and Younger Atlantic, the Sub-Boreal and Sub-Atlantic. Five pollen assemblage zones (PAZ) have been distinguished in the diagram. The record of man's economic activity on the vegetation have been observed from the samples before 6700 BP through the whole profile, but with variable intensity (four settlement phases). KEY WORDS: palynology, Holocene, NE Slovakia, Low Beskids, pollen assemblage zones (PAZ), human impact INTRODUCTION The Low Beskids with the adjoining area of deposits, to reconstruct vegetational history, to the Jaslo-Sanok Depression have repeatedly find the moment of first appearence of agricul­ attracted attention of both palaeobotanists ture in this area, to analyse the disturbances and archaeologists. A number of palynological in the primary plant cover under the influence studies on changes occurring in the plant com­ of settlement and to refer the phases of the in­ munities with time has been published since tensification of agricultural activity to the cul­ the thirties: Roztoki (Szafer & Jaron 1935), tural changes in the study area. Cergowa Gora (Wi~ckowski & Szczepanek 1963), Besko (Koperowa 1970), K~pa (Gerlach et al. 1972), Szymbark (Gil et al. 1974), Jasiel GENERAL CHARACTERISTICS OF (Szczepanek 1987), Roztoki (Harmata 1987, NATURAL ENVIRONMENT IN THE 1995 a, b) and Tarnowiec (Harmata 1987, 1995 LOW BESKIDS LOCATION, RELIEF a, b). AND GEOLOGICAL STRUCTURE This study was designed to widen our knowledge on vegetation history of the Slova­ The Low Beskids are the easternmost part kian part of the Low Beskids poorly explored of the West Carpathians. They bridge the east­ so far. An investigation has been carried out as ern and western ranges of the Beskids. The a part of the interdisciplinary programme: Low Beskids occupy an area of 1 789 km and "First agricultural and stock-breeding farmers extend as a 20-30 km-wide belt for about 100 on both sides of the Low Beskids", carred out km. Their relief is characteristic of low moun­ chiefly by archaeologists at cooperation be­ tains rising to an altitude of 500-850 m, ex­ tween the Institute of History of Material Cul­ ceptionally even above 1000 m, eg. Busov ture, Polish Academy of Sciences (at present (1010 m), the highest segment elevation in the the Institute of Archaeology and Ethnology, Slovakian territory, and Lackowa (1001 m) on Polish Academy of Sciences) in Warsaw and the Polish side (Adamczyk & Gerlach 1983). the Institute of Archaeology, SAScs in Nitra in They form the lowest and narrowest segment 1991 (Machnik & Macala 1992). of the Carpathian arch, begining at the Tylicz The purposes of the present work have been Pass (683 m) in the west, being it boundary to recognized the stratigraphy of organogenic with the Nowy Sqcz Beskids (Radziejowa 254 1265 m), and extends tu the Lupk6w Pass (640 cation of roads or railway lines is worth men­ m), which in the east separates the Low Be­ tioning here (Adamczyk & Gerlach 1983). skids from the Bieszczady Mts. (Tarnica 1348 m). The Beskid hills decreasedistinctly in alti­ Soils tude towards the north and the south. The lo­ weslying bottoms of the river valleys in the Acid and leached brown soils, brown soils areas of the Jaslo-Sanok Depression and of and lessive soils, pararendzinas, podzolic soils Ci~zkowice Foot-hills on the northern side, proper, hydrogenic, initial and other soils have and in the Ondava and Labeorc Uplands on mainly developed in the study area in connec­ the southern side lie at an altitude of 200-300 tion with the differentiated land relief (Swi~s m. This region is characterized by the NW-SE 1982). The floors of valleys are usualy lined course of the main ridges and hills (Adamczyk with clay-dust soils on sands and gravels. The & Gerlach 1983). In the eastern part the rid­ flat-topped ridges moderately high and low ges form more district and longer ranges than foothills, sloping down towards the valleys are in the western part, where typical are small covered by clay-loam soils with a low propor­ groups of mountains scattered like islands or tion of skeletal elements. On steep portions of very short ranges of variable course. the slopes of montains and high foot-hills clay­ The Low Beskids are a watershed range. stone, more rarely clay soils occur (Adamczyk The main drainage areas from the rivers Biala & Gerlach 1983). Dunajcowa, Ropa with S~k6wka, Wisloka, The soils show a broad range of depths, pro­ Jasiolka, Wislok, Oslawa and on the southern portions of skeletal parts and moisture. They side the rivers Topla with its tributaries are generaly poor in phosphorus, somewhat Kamenec, Svierzovka and Rusucka Voda, On­ richer in potassium, contain either consider­ dava with Kapisovka and Lubomirka, and La­ able or only trace amounts of calcium, the rock borec with Vydranka. The hydrological regime outcrops and slope weathering waste are of the rivers and streams is characterized by usually rich in calcium, hence, the xerothermic the greatest flow during the spring thaw and and calciphilous vegetation is much more fre­ the smallest in autumn. The geological sub­ quently grouped in lower positions than in stratum of the Low Beskids shows a high de­ higher parts of valleys or on summits (Swi~s gree of folding and fissuring (Starkel 1972). 1982). On the basis of differences in the appearance, arrangement and nature of these forms, and Differentiation of climatic elements their geological structure five main geomor­ phological units have been distinguished: the The situation and the diverse nature of re­ Gryb6w Mts., Magura Range, Dukla Beskids, lief of the Low Beskids exert an influence upon Ryman6w Beskids and the Jasliska-Wislok­ the individual features of climatic conditions. Komancza Depression (Adamczyk & Gerlach This region constitutes a climatic boundary be­ 1983). The various morphogenetic processes tween the West and the East Carpathians, occur in the area of the Low Beskids, such as which has also been confirmed by geobotanical mechanical denudation (landslide, soil creep, studies of this area (Swi~s 1982). solifluction), deflation and chemical denuda­ Two climatic zones have been distinguished tion (dissolution, leaching). It is a classical re­ in the Low Beskids: a moderately warm and gion of gravitational movements, the most humid zone and a moderately cool and humid characteristic of which are the landslides. one. In river valleys and depressions the Their origin conditioned by a suitable inclina­ moderately warm zone reaches up to 460 m tion of rock layers in the substratum and by a.s.l. and on convex form to 620 m a.s.l. It is the occurrence of impermeable shales under­ characterized by the mean annual tempera­ lying the porous rocks. Typical of this part of ture exceeding 6° C. The moderately cool zone the flysch Carpathians is also the process of extends above the foregoing altitudes and the reactivation of landslides resulting in the oc­ mean annual temperature is below 6° Chere. currence of landlises varying in age in close The annual precipitation ranges from 600 to neighbourhood to each other. The anthro­ 900 mm. The number of days with snow cover pogenic influence on the formation of same is from 81 at Dukla to 99 at Wislok Wielki and landslides, brought about by the improper lo- its maximum thickness fluctuates from 73 cm 255 at Ryman6w to 113 cm at Koma:Jicza tum incane) with grey alder, sycamore maple (Adamczyk & Gerlach 1983). The climate of or ash and a small addition of hornbeam, the Low Beskids is more continental than that aspen and willow. The largest areas is occu­ of the West Carpathians and as consequence pied by the Carpathian beech forests (Dentario the vegetation season begins about 7-9 days glandulosae-Fagetum) with beech, fir and sy­ later but the first phases of spring develop­ camore maple. On the rocky bends the stands ment are shorter (ObrEi)bska-Starklowa 1983). of Phyllitido-Aceretum occur with the domi­ The whole vegetation season lasts from 215 nant sycamore maple accompanied by beech, days in low-lying places to 182 days on sum­ elm and ash. Large areas in the western part mits (Hess 1965). of the Low Beskids are occupied by fertile fir The Low Beskids are characterized by the forest of the order Fagetalia and poorer fir considerable prevalence of southerly winds forests from the alliance Vaccinio-Piceion. Acid (50%) over northerlies (20%) and easterly and beech wood (Luzulo-Fagetum), dominated by westerly winds (15% either).The occurence of beech with contribution of fir, occurs very rare­ the foehn winds from south called the Dukla ly on flats and on ridges (Fabianowski & Rut­ or Ryman6w winds, is of particular signific­ kowski 1983). The most common forest associ­ ance (Hess et al. 1978). These strong winds ations are Dryopterido dilatatae-Abietetum, (more than lOm/sec) or very strong winds occurring in different sub-association on the (more than 15m/sec) persist from one to sev­ fertile moist slopes of brook ravines or up to eral days. In the foot-hill zone (Szymbark) the the summits of hills, and Vaccinio myrtilli­ number of days with foehn makes 16% of the Abietetum, occupying most frequently the year days, falling chiefly in the period of No­ flats, more rarely the slopes.
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