Volcanic Soils of the High Börzsöny and Their Relationship with Geomorphological Conditions 227 Hungarian Geographical Bulletin 58 (4) (2009) pp. 227–242 Volcanic soils of the High Börzsöny and their relationship with geomorphological conditions Madarász, Balázs1–Jakab, Gergely1 Abstract Heretofore very litt le research has been done on a specifi c soil type in Hungary called „erubáz”, which develops on volcanic rocks. Its largest uniform and unbroken spot is located in the central part of Börzsöny Mountains (High Börzsöny). It is assumed that in reality this spot extends beyond its contours indicated in the soil map of the area. The main objective of the research project was to carry out a detailed analysis of this soil type and to identify its subtypes and varieties. A large scale soil mapping (1:25 000) and geomorphological mapping (1:10 000) was performed in order to determine the spatial distribution of the subtypes and varieties and to investigate the relationship between the territorial extension and geomorphological position. The sampling network was set aft er a thorough study of environmental conditions (e.g. relief, botanical conditions etc.). 38 soil profi les and 115 boring samples were taken by Pürckhauer auger because of the signifi cant inhomogeneity of the studied area. Our former studies (Madarász, B. 2009) revealed that two varieties of the s-called ‘erubáz’ soil, i.e. the brown and the black erubáz can be distin- guished in the study area. Black erubáz soils occur on narrow ridges with high elevations as described in the classical defi nition by P. Stefanovits. Aft er a few 10 meters from the crest of the ridges downslope they will be replaced by the brown erubáz. The latt er can be found on the top of the ridges and on their slopes as well whilst the black erubáz appears only above 700 m a.s.l. except one smaller spot. The occurrence of the brown erubáz is controlled by soil climatic conditions. It develops mainly where enough moisture and heat are available for the decomposition of organic material but they are not suffi cient and the geomorphic position is not suitable for the development of forest soils. Keywords: erubáz soil, High Börzsöny study area, DEM, sampling, laboratory analyses Introduction One of the most ignored and less studied soil types in Hungary is the so called erubáz or fekete nyirok (black, wet soil), a special soil type developed on volcanic rocks. The main reason for this negligence is the fact that this soil occurs in small patches dispersed in the hilly regions of the country, which 1 Geographical Research Institute, Hungarian Academy of Sciences. H-1112 Budapest, Budaörsi út 45. E-mail: madaraszb@mtafk i.hu, jakabg@mtafk i.hu 228 are outside the scope of agriculture. Because of its inferior role in agricultural mass-production and small areal extent, only the forestries and some vine- yards are interested in studying these soils. In the 1950’s Stefanovits, P. dealt also with soil types of no major agricultural importance so that his investigations included the forest soils, too. Consequently, the erubáz soil was also included in his genetic soil clas- sifi cation system as an independent soil type (Stefanovits, P. 1951, 1956, 1959; Stefanovits, P.–Szűcs, L. 1961). Since then very litt le has been done and very few data were assembled on this soil type (Góczán, L. 1968, 1970; Néráth, M. 1997; Szendrei, G. 1998; Barczi, A. 2000; Fehér, O. et al. 2006; Fehér, O. 2007). Recently a detailed characterisation of the erubáz soils was provided by Madarász, B. (2009). The surface occurrence of the erubáz soil can be estimated on the basis of the 1:100,000 scale agrotopographic map of Hungary. According to this map most of the volcanic landscapes are covered by ‘brown forest soils with clay illuviation’ (luvisols) and ‘brown earth’ (cambisols), since these soil types are typical under the climatic conditions of Hungary. The areal extension of the erubáz soil is limited to the Börzsöny–Visegrád Mountains and to the basaltic mesas of the Tapolca Basin, covering an area of 44 km2 altogether, with the larg- est spot in the High Börzsöny. However, erubáz soils may occur on considerably larger areas than suggested by the agrotopographic map, only their tiny spots dispersed in a mosaic-like patt ern are impossible to visualize at this scale. During the last half-century several soil maps were prepared on the High Börzsöny area. First of these was the 1:200,000 scale genetic soil map prepared by Stefanovits, P. and Szűcs, L. (1961). The above mentioned agro- topographic map was published in 1982. In this map two soil types are shown within the study area, i.e. the ‘brown forest soils with clay illuviation’ (luvi- sol) and the erubáz, the latt er with the largest areal extension in the country. Láng, S. (1955) in his book entitled “Physical geography of the Mátra and the Börzsöny” modifi ed the version of the Stefanovits–Szűcs map already available in 1954. Járó, Z. (1978) published in his study a special soil map (1:200,000), where ranker soil covers almost 95% of the area. This must be treated with reservations as rankers are ‘shallow soils aff ected by the par- ent material’ developed on massive silicate rocks, but not on volcanic rocks, provided that the soil type developed on volcanites is the erubáz itself. The above mentioned maps are small-scale ones as no large-scale soil mapping was conducted in the Börzsöny Mountain so far which could provide detailed information of the areal extension and properties of the erubáz soil. The present paper is aimed to report about a detailed fi eld and labora- tory analysis of this scarcely known soil type. In the Hungarian genetic soil classifi cation system only the erubáz soil type exists, no sub-types and varieties have been specifi ed. However, it became obvious at the beginning of the study 229 that this soil type is far from being uniform as it is suggested by its classical defi nition. The large scale geomorphic mapping (1:10,000) and soil mapping (1:25,000) carried out by the authors in the High Börzsöny study area were aimed to understand the soil types of this area bett er, to describe the erubáz soil, to identify its sub-types, to learn more about the geomorphological posi- tion and to reveal the areal extension and appearance. The study area Topography and landscape evolution The Börzsöny Mountains belong to the inner-Carpathian volcanic chain having mid-Miocene origin. It is the third largest volcanic region of Hungary, con- taining three topographic micro-regions. The major part of the study area is located in the Central (High) Börzsöny micro-region and some areas close to its boundary belong to the foothills of the Börzsöny (Marosi, S.–Somogyi, S. (eds.) 1990). The calc-alcaline intermediary volcanism in the High Börzsöny (16.5– 13.5 Ma) produced block-and-ash-fl ows and lava fl ows mostly of pyroxene andesite (Pantó Gy. 1970; Balla Z. 1978; Karátson D. 1997, 2007). The study area (45.9 km2) includes the highest part of the central caldera rim (Karátson, D. 2007) together with its inner slopes of easterly aspect and with the outer slopes of westerly aspect. The study area has a radial valley network. As a result of the Pleistocene periglacial landscape evolution the slopes above 500 m asl. are mainly covered by rock debris, stones and are disrupted by cryoplanation steps (Szabó J. 1996). Physical weathering by frost destroyed more the lava strata of bedded lava rocks, while erosion carved tower-like rock formations of the more resistant block-and-ash-fl ow deposits (e.g. Katalin-szikla, Szabó-kövek). The caldera rim, i.e. the Nagy-Hideg-hegy–Csóványos–Magosfa range of 800–900 m altitude forms the central part of the study area. The altitude of the study area ranges between 275 and 939 m (Fig. 1). It is poorly dissected, with a frequent occurrence of steep slopes and rock debris fi elds. Slopes are steeper than 25% on ca. 80% of the area and 35% on its 54%, (Figs 2 and 3). The relative relief decreases towards the boundaries of the study area from 350–370 m/km2 to 100–150 m/km2 (Kertész Á. 1976, 1978). Most of the slopes are exposed to west – north-west and to east–south-east (Fig. 3). Climate Climate is of primary importance in determining the conditions of soil forma- tion. The study area belongs to the cool-wet climate type, where the annual 230 Figure 1. TIN digital elevation model of the High Börzsöny study area, (m). Abbreviations: NH = Nagy-Hideg-hegy, Cs = Csóványos; M = Magosfa 231 Figure 2. Slope gradient map of the High Börzsöny study area, (%). Abbreviations see in Figure 1. 232 mean temperature remains below 8–8.5 °C. The winter is long and cold and frost is always possible except in summer. The annual mean precipitation is 800 mm, which can be even more in the peak areas. Most of the precipitation arrives at the beginning of summer (May–June), while the second part of the summer is drier and more sunny (Péczely, Gy., 1978; Láng, S., 1955). The number of days with snow cover varies between 60–80 and 100–120 days in the lower and higher regions, respectively. Average thickness of the snow cover is 30–50 cm. The aridity index is 0.82–0.90 (Marosi, S.–Somogyi, S. (eds.) 1990) Figure 3. Slope gradient (A) and slope aspect (B) frequency histograms of the High Börzsöny study area 233 Vegetation and land use The High Börzsöny is almost uninhabited; therefore the vegetation is still almost in a natural state in most of the area. 97% of the study area is forested. The vegetation is montane and submontane beech, forests developed on slope- debris and on rock surfaces, whereas clearings are covered by meadows and rock shrubs (Fekete, G.–Varga, Z., 2006). Part of the andesite rock-fi elds still is not forested; the growth of the trees is hindered by debris thickness and by the lack of moisture. On the thinner rock-debris, slope-debris forests and acidophilous forests have developed, the former mainly mixed with lime, ash and maple species, the latt er mostly with beech, oak (Quercus petraea), some sorb and birch (Kárpáti Z. 1952). The most important locations of erubáz soils, like e.g. at the top levels on the caldera rim, are covered by ash (Fraxinus excelsior) (Photo 1). In the opinion of some experts this is of anthropogenic origin, in other words, the consequence of improper forestry policy of the distant past. The beech has considerable bearing only every 7–10 years, while the ash has seeds more frequently. The young ash tree requires light and presumably sunny habi- Photo 1. Ash (Fraxinus excelsior) trees before sprouting on the caldera rim between Csóványos and Nagy-Hideg-hegy 234 tat, while the young beech grows well in the shadow. Herbivore big game likes young ash, but it consumes the beech only if nothing bett er is available. Accordingly, if a beech forest was cut in a period when the number of wild- game was low, the forest of saplings in this area was ash instead of beech. In other opinions the stretch of ash in beech forests is a natural process on drier areas with a shallow soil (Király, G. et al. 2008). Methods As a first step of the soil mapping 1:10,000 topographic maps and the 1:50,000 geological map (Korpás L.–Csillagné Teplánszky E. 1999) were used to establish the network of sampling sites. The main objective of the mapping was the identifi cation of the extension and geomorphic position of the areas covered by erubáz soils. Altogether 38 soil profi les were excavated and 115 Pürckhauer-type auger samplings were performed. For sampling the princi- ples of soil mapping were applied (Szabolcs, I. 1966; Buzás, I. 1988, 1993). The FAO (1990) standard was used for the description of soil profi les. The genetic soil horizons were named and characterized on the basis of Szodfridt, I. (1993) and Stefanovits, P. et al. (1999). 1:10,000 topographic maps were used as a basis of geomorpological mapping. The methodology and the legend of Pécsi, M. (1963, 1991) were ap- plied for the mapping procedure. Analysis of the soil samples was carried out in the laboratory of the Geographical Research Institute, in accordance with the certifi ed standards. CaCO3 content of the soil was measured using Scheibler’s gas-volumetric method (Buzás, I. 1988). Inorganic carbon content was leached by the de- calcifi cation method developed in the Institute. Organic carbon content was measured using Tekmar Dohrmann Apollo 9000 NDIR spectrometer. Humus content of the soils was determined by the equation of Stefanovits, P. et al. (1999): Humus% = TOC% × 1,72. The determination of the pH value (pH(H2O); pH(KCl)) was performed with the potentiometric method (Buzás, I. 1993; MSZ- 08-0206/2-1978). The colour of the samples was identifi ed by the Munsell colour scale under dry and wet soil conditions. Bulk density was measured on undisturbed samples of known volume, by drying in oven (Buzás, I. 1988, 1993). Aft er the disintegration of the aggregates the mechanical composi- tion of the samples was determined using Fritsch Analysett e Microtech 22 laser diff raction particle size analyzer. Mineralogical and clay-mineralogi- cal analyses of the soils were performed applying X-ray diff raction method in the Geochemical Research Institute of the Hungarian Academy of Sciences by means of a PHILIPS PW 1710 equipment. 235 For map compilation and graphics as well as for area measurements the ESRI Arc View 3.3 was applied. ESRI Arc View 3.3 and Surfer 8 soft wares were used for Digital Elevation Model construction. Results Evaluation of the soil map Soil mapping is a diffi cult task in landscapes with dissected topography. However, based on fi eld observation and laboratory analyses the relation- ship between topography and soil types can be identifi ed thus facilitating the mapping procedure. The 1:10,000 scale geomorphological map provided a good and essential basis for the mapping, i.e. some soil types, like the erubáz soil occur mostly in typical geomorphic positions, on top levels, ridges and on steep slopes of southerly exposure (Fig. 4). In addition to this land mosaics can aff ect soil evolution processes (Szalai, Z. 2008; Szalai, Z.–Németh, T. 2008). Parent materials are usually andesite lava and andesite block-and-ash- fl ow deposits. Their mineralogical, physical and chemical compositions are widely varied. Where the climate is moderately wet diff erent associations of deciduous forests have developed and soil climate can be described as udic or mesic (Wernstedt, F.L. 1983). Genetic soil types of the High Börzsöny study area Below a short description is given about all soil types occurring in the High Börzsöny area. Their detailed description except for the erubáz soils is not provided here. Skeletal soils (Lithosols) A considerable area is occupied by stony skeletal soils (Fig. 5), especially where soil erosion is an important factor, so that products of weathering are removed from the slope immediately aft er their formation. They can be found on nar- row ridges, small hilltops and on steep slopes. On the inner slopes of the caldera rim rock-debris slopes are encountered frequently as a consequence of Pleistocene periglacial frost riving. Soil formation in these areas is in its incipient phase. The thickness of the soil cover is less than 10 cm. Soil patches alternate with rocky spots. Rock fragment proportion may reach 70–90%. These soils can 236 Figure 4. Geomorphological map of the High Börzsöny study area (1:10,000). Abbreviations see in Figure 1 237 Figure 5. Soil map of the High Börzsöny study area (1:25,000). Abbreviations see in Figure 1. 238 be considered as thin erubáz-like soils, where the soil thickness could not reach the adequate depth. Spots of skeletal and erubáz soils occur in a mosaic-like patt ern. Skeletal soils occur in areas with similar geomorphological position. Shallow soils infl uenced by the parent material Erubáz is the most widespread soil type of the study area (Fig. 5). Its humus content is very varied as a consequence of diff ering conditions of organic material decomposition. This diversity is the result of humidity, temperature and pH diff erences. According to the detailed studies of Madarász, B. (2009) the distinction of two sub-types, i.e. brown and black erubáz is necessary. The humus content of brown erubáz rarely exceeds 4% while that of black erubáz, exposed to extreme soil climatic conditions may reach 10%. The wet colour of the latt er (10YR 2/2, 10YR 2/1) and the dry colour (10YR 2/2, 10YR 3/2) refer to dark brown or black colours. The brown sub-type is dark greyish-brown when dry (10 YR 4/2, 4/3, 5/3) and very dark greyish-brown or dark brown in wet state (10 YR 3/2, 3/3). Scatt ered spots of black erubáz can be found on the highest levels of the study area, on the hilltops and ridges reaching the altitude of 750–915 m asl. The size of their area rarely exceeds 100 m2. They vary with spots of stony skeletal soils (Figs 4 and 5). The geomorphological survey revealed that potential areas of the oc- currence of erubáz soils are very restricted in the study area. The fairly nar- row ridges are only rarely interrupted by slope terraces. Hilltop areas and erosional inselbergs are not predominant, steep slopes dissected by rock fi elds prevail. According to the geomorphological sketch of the area the percentage suitability of the landforms for the development of erubáz soils is as follows: 1% hilltop areas, 1.5% erosional inselbergs, 8.3% intervalley ridges and 2.9% slope terraces. In spite of this percentage values erubáz soils can be found only on 1.1% of the study area. Brown erubáz soil shows a signifi cantly larger territorial extension. It may develop practically everywhere from the hilltops to the valley sides as its occurrence is not associated with special landforms or slope exposures. In locations where the specifi c conditions of the forma- tion of black erubáz are not fulfi lled, i.e. biological decomposition hindered by winter freezing and summer drought (Madarász, B. 2009), brown erubáz soils have developed. Their spatial appearance is less mosaic-like than that of the black erubáz forming large continuous soil patches. Brown erubáz soils can be re- garded as a transition from black erubáz towards the ‘brown forest soils with clay illuviation’, the diff erentiation of soil horizons however cannot be ob- served yet. 239 The erubáz soils of the Börzsöny Hills have a slightly acidic pH and their N supply is favourable. Their structure has a granular character and in dry state it is dusty frequently. The average depth of the profi les is 43 cm. They have usually a loamy or sometimes a clayey-loamy texture. The organic material and the clay minerals form a strongly bonded humic horizon. Characteristic clay minerals are caolinite (15–30%), illite (10–20%) and smectite (5–10%). Although severe desiccation of the soil under a forest occur only rarely in the presence of a considerable amount of smectite 1–2 cm wide fi ssures may develop. There is an abundance in opal and christobalit and goethit is also a major component. Calcium is the most important exchangeable cation. Their saturation is low and no CaCO3 is present in the soil of the study area (Madarász, B. 2009). According to the classical description the vegetation cover developed on erubáz soils consists of scarce and degenerated specimens. Our fi eld studies do not support this statement. At some locations on shallow soils with tran- sitional character towards skeletal soils the forest was degenerated while in most areas covered by erubáz soils well developed oak and beech forests were found. Nevertheless, vegetation is usually determined by the anthropogenic activities and their intensity. ‘Brown forest soils with clay illuviation’ (Luvisols) As a consequence of topographic and climate conditions subtypes of the ‘brown forest soils with clay illuviation’ are the most widespread soil types of the study area. Their profi les are best developed on gentle slopes and slope terraces. On steeper slopes their profi le as a rule is truncated. They occur mostly at altitudes under 600 m asl. as a consequence of slope steepness and dissected topography. (Figs 4 and 5). Slope debris soils The eroded material is accumulated mainly in the valleys. Its thickness may reach several meters. Accordingly, slope debris soils can be found at lower elevations on the valley fl oors. Their presence is considerable only in the wid- ened valley fl oors at the border of the study area (Figs 4 and 5). Conclusions In the course of the large-scale soil mapping in the High Börzsöny study area the following soil types were identifi ed: skeletal soils, brown forest soils 240 with clay illuviation, slope-debris soils and erubáz soils (aff ected by parent material). Two subtypes of the erubáz soil are described as the black and the brown erubáz. Black erubáz soils occur on high and narrow ridges, in accordance with the classical defi nition of Stefanovits. Their development is associated with specifi c soil-climatic and topographic conditions, namely to the zone of biological decomposition hindered by severe winter freezing and summer dry- ing. They are present only in a few 10 meters width on the ridges, along the slopes they are replaced by brown erubáz soils. Except for one small patch the black erubáz soil appears above 700 m asl. At the same time the brown erubáz soil may occur everywhere on lower ridges and slopes. 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