The hot spring deposits near Magyarkút and their paleobotanical analysis : (Börzsöny Mountains, Hungary) 3 Hungarian Geographical Bulletin 59 (1) (2010) pp. 3–16. The hot spring deposits near Magyarkút and their paleobotanical analysis (Börzsöny Mountains, Hungary) Hably, Lilla1–Schweitzer, Ferenc2–Szeberényi, József 3 Abstract The clarifi cation of the location and origin of the siliceous-calcareous deposits north of Magyarkút can lead to noteworthy conclusions in connection with the geological evolu- tion in the environment of the Szokolya Basin. Utilizing the already available bibliography, this research separated the discussed deposits from the other types of sediments detectable in their environment. The presence of the siliceous-calcareous deposits on the south-eastern edge of the Börzsöny, near the set- tlement of Magyarkút was already partly known. Nevertheless, the lately found terrestrial plant fossils provided novel knowledge. According to the researches based on geomorphological and paleobotanical meth- ods, the study assumes that a hot spring activity of postvolcanic origin took place in a time interval during the Middle to Late Miocene, in a subtropical environment. Besides the al- ready known calcareous spring deposits embedded into the diatomaceous environment, in the side of the Szalamandrás Hill rocks of presumably terrestrial origin were also recognised and described based on the fl ora present in them. Completing the former knowledge, the study can claim, that among the hot spring deposits of Magyarkút, the terrestrial deposits of Szalamandrás Hill can defi nitely be separated from the rock complex of limnic origin – the latt er being similar to the spring deposits of the Szokolya Basin. The fl ora remnants prove or specify the chronological results of earlier researches regarding the Middle to Late Miocene age of the deposits. Keywords: siliceous-calcareous deposits, geyserite, paleobotanical evidence, Podocarpium podocarpum Introduction The investigation of sediments on the south-eastern margin of the Börzsöny Mountains dates back to more than one hundred years. Former studies fre- 1 DsC., Head of department, Department of Botany, Hungarian Natural History Museum, H-1088. Baross utca 13. E-mail: hably@bot.nhmus.hu 2 DSc, Geographical Research Institute, Hungarian Academy of Sciences, H-1112 Budapest, Budaörsi út 45. E-mail: schweitf@mtafk i.hu 3 PhD., Geographical Research Institute, Hungarian Academy of Sciences, H-1112 Budapest, Budaörsi út 45. E-mail: szeber@mtafk i.hu 4 quently mentioned the sediments covering volcanites near the sett lement Magyarkút, even though their names and their proposed origin oft en proved to be highly diff erent and contradictory. The most recent references defi ne them as a sediment complex produced both by volcanic and non-volcanic processes (Karátson, D. 2002, 2007). However, the sedimentary complex still lacks an adequate description. From the really varied deposits near Magyarkút sequences of calcar- eous-siliceous deposits were selected for more detailed analysis, which are signifi cantly diff erent from all other sequences of the area. Composition and morphology of their bedrock outcrops refer to postvolcanic activity. The fos- silized plant remnants found here are of exceptional importance for dating. This study aims at the structural description of the rocks, the identifi - cation of the plant remnants found in the calcareous spring deposits, fi nally dating and reconstruction of the conditions of their formation. The calcareous spring-deposits at Magyarkút are referred to in several instances in literature. The earliest reference is writt en by Böckh, H. (1899), who mentioned the formations only peripherally: „Let me refer to those travertine and siliceous deposits, which can be found around Verőcze (near Magyarkút) and in the Puncz Trench (Szokolya Basin). They are the most closely connected to the underlying andesite breccia and tuff s. Superimposing the lignite seams the tuff breccia layers change into extremely fi ne tuff s, in some places the transition into sandy, marly, siliceous and calcareous layers is almost undetectable.…” Böckh was the fi rst to realize the importance of calcareous and sili- ceous deposits, and unambiguously associated them with the neighbouring volcanic products. In his geological study about the Börzsöny Mountains, Ferenczi, I. (1935) mentioned the deposits of the small stream extending upwards the western slope of Borbély Hill (located south-east of Magyarkút). He describes a so-called “andesite agglomerate”, the grain size of which gradually decreases from the bott om of the stream upwards, and is covered by rounded andesite gravel and fi nally by “travertine, geyserite and opaline spring-products” in the higher regions. These spring-products are to be found in the line of the gully on Borbély Hill. They represent the southernmost, mainly fragmented sec- tion of the occurrences near Magyarkút, and are identical with the samples taken from the bedrock. According to Ferenczi’s description, in this section the sediment covers agglomerate with a thickness of 50–60 metres. The sedi- ment was identifi ed as „a fresh-water sediment group composed of diatomaceous shale, geyserite, chalcedony, and produced by postvolcanic activities”. Báldi, T.–Kókai, J. (1970) mentioned the area of Magyarkút in relation to the dating of the andesite-volcanic activity in the Börzsöny. Their study highlighted the role of limnic/marine calcareous cover deposits fi lling the 5 Szokolya Basin, and briefl y mentioned the sporadically present travertines in the diatomaceous succession at Magyarkút, primarily on Borbély Hill. Authors supposed that the limnic formations at Magyarkút can be corre- lated with those of the Szokolya Basin, which were considered to be Lower Badenian. Based on morphological characteristics and the records of airborne magnetic surveys and in accordance with the fi ndings of Jámbor, Á.–Moldvay, L.–Rónai, A. (1982), a geological map was constructed. Its explanatory text claims that “based on their outcrop the presence of diatomite, geyserite and travertine at Magyarkút can be classifi ed as part of the Tortonian (Badenian)”, i.e. the Rákos Limestone Formation. There is Ól Hill on the northern side of Szokolya Basin (Figure 1). Nagy, B. (1983) found here siliceous sediments containing limonite. In his opinion, these are hot spring deposits. In conclusion, the calcareous spring deposits near Magyarkút were found at the turn of the 19th and 20th centuries and referred to as „geyserite” and „travertine” up until the 1980’s. Many studies connected them to the de- posits of the Szokolya Basin. More detailed analyses were not carried out in the last two decades of the last century; moreover, the deposits neither were considered during the mapping of the area (Korpás, L.–Csillag-Teplánszky, E. 1999), nor for the reconstruction of the geological evolution of the Börzsöny Mountains (Korpás, L. ed. 1998). Description of the study area The hot spring deposits, as earlier described, can be found near the sett lement Magyarkút (Figure 1). The sett lement of Magyarkút is located on the south-eastern margin of the Börzsöny Mts., on a widening of a valley bott om, where the Keskeny- Bükk Stream fl ows into the Les Stream (Figure 2). The eastern and southern margins of the area of 8 km2 represented on the terrain model is marked by the curved crest of the Keskeny-Bükk–Csapás Hill–Magas Hill–Borbély Hill ridge, while the northern margin is indicated by the andesitic Kis-Kő Hill and by the Nagyhársas formed by Oligocene deposits. The most signifi cant occurrences in the area are undeniably repre- sented by the rocks found in the hillside of the Szalamandrás Hill. These rocks enclosed paleobotanical rests, with the help of which a dating of good accuracy can be carried out. During a fi eld trip 35 samples were taken from the rocks near Szalamandrás Hill, out of which 27 contained fl ora residues. The paleobotanical analysis was carried out by Hably, L. in the Department of Botany, Hungarian Natural History Museum. 6 Fig. 1. Magyarkút and environs 7 Fi g. 2 . S ur ro un di ng o f M ag ya rk út o n th e D ig ita l E le va tio n M od el 8 Although previous researchers (Böckh, H. 1899; Ferenczi, I. 1935; Báldi, T.–Kókai, J. 1970) described several occurrences in the inner side of the crest of the Keskeny-Bükk-Borbély Hill, the present study discusses the deposits on the side of the Szalamandrás Hill exclusively. This is the very place where the paleobotanical rarities to be introduced later on were revealed. This locality represents by all means a novelty, since there were no other fi ndings of similar quality and condition detected nearby. The Szalamandrás Hill (243 m) is one of the elevations prepared by weathering of the slope gently descending towards the stream valley fl anked by the Keskeny-Bükk–Borbély Hill’s ridge (Figure 2). From the north and the west, it is bordered by the Keskeny-Bükk Stream, while its southern and east- ern borders are marked by the line of steep gullies. In the southern and western side of the Szalamandrás Hill a signifi cant amount of hot spring deposits can be detected (Figure 3). These calcareous spring deposits directly superimpose the andesite weathering products of gravel-sand size. The bedrock outcrops on the surface can be primarily related to the terrain at 210–230 m above sea level, where several, clearly isolated, porous, hollow limestone blocks are present (Figure 3 (1); photos 2–3), presumably marking the sites where water of springs issued. Stratifi ed calcareous spring deposits can be found at several places near the bedrock blocks (Figure 3 (2); photos 4–5). The two rock types frequently occur together, developing from each other. Thus the porous calcareous spring deposits undoubtedly emerge from a stratifi ed environment of rocks. One can assume that the once operating springs could develop the whole formation. Stratifi ed calcareous material precipitated from stagnant water or from water pouring down along the sides of the cones and accumulating in the area between them. Description of the rocks The samples taken from the surface outcrops appear in their natural occur- rence as moss-grown, greyish-white or dark-grey, hard, resistant rocks. The colour of their fresh fracture is generally beige-, greyish-, yellowish-white. As the eff ect of hammering, they give a siliceous scent frequently accompanied by sparks, which is due to silicifi cation of the limestone. In many cases quartz and calcite also occur as inclusions. Regarding their structure massive, porous and stratifi ed rocks can be distinguished. The weathered surface is greyish-white (1), at some places having traces referring to corrosion (Photo 1). The fresh fracture features a mixture of light-brown to beige and darker brown patches (2). The irregularly-shaped, in some cases angular cavities are fi lled out by white calcite crystals (3). 9 Fi g. 3 . C al ca re ou s s pr in g de po si ts o n th e Sz al am an dr ás H ill . – 1 = Po ro us sp ri ng d ep os it ro ck s; 2 = st ra tifi e d ro ck s; 3 = de br is ; 4 = lo ca lit y o f fl o ra a nd fa un a 10 There are 0.5 mm wide, 2–5 mm long, curved, narrow holes fi lled out by white calcite crystals. The rock oft en contains quartz as inclusion, and is chipping with sharp rims (4). Porous-structured rocks can be recognised in the hillside of the Szalamandrás Hill (photos 2, 3a and 3b). Their weathered surface is greyish-white, the fresh fracture is white or beige-white. The layers of the rocks are built up from 0.5 mm thin sheets (Photo 3b, (1)), and construct a complex structure, in which the components of irregularly twisting layers look similar to a „crumpled wet sheet of paper”. The thickness of the layers varies between 1 and 5 mm. There are smaller and larger cavities within the rocks, ranging also between 1 and 5 mm in size (Photo 3a, (1)), the inner side of which is sometimes covered by calcite crystals. The rock is chipping, and breaks along angular rims. Photo 1. Massive calcareous spring deposit. – 1 = surface; 2 = fresh fracture; 3 = calcite crystal; 4 = sharp rims Photo 2. In situ occurrence of a 3 m high, porous spring deposit on the slope of the Szalamandrás Hill Photo 3a. Porous spring deposits. – 1 = cavities in the rock Photo 3b. Enlarged picture of porous spring deposits. – 1 = 0.5 mm thin sheets 11 In the case of stratifi ed rocks, various kinds of occurrences are possi- ble, and are to be found in the side of Szalamandrás Hill, north of the gully of Medve-kút and of Hosszú gully. They are detectable always near the massive or porous rocks, in some cases they alternate with the latt er. Their decomposi- tion surface is white, sometimes with a yellowish-greyish tint. A special variety of it can be characterized by wispy layers thinner than 0.5 mm (Photo 4). Generally grey and white layers alternate. There are at every 4–5 mm regularly repeating, very thin, rusty brown layers (1) which probably refer to the periodical activity of the hot spring. The rock does not break up along the layers, the latt er cannot be separated from each other by a chisel (Photo 4a). The illustrated rocks of alternating layers are continuously develop- ing on the surface of the porous-structured rocks. Based on the outlook of the stratifi ed deposit, it could be the precipitation from some kind of water run- ning down on an uneven surface (Photo 4b); here the rock can be split along the layers by a chisel. The layers are wavy, rough surfaces (2). The other variety of stratifi ed rocks involves much more rougher, even 0.5–1 cm thick layers (Photo 5). Though the paper-thin, uneven surface of strati- Photo 4a. Microstratifi ed spring deposit, con- tinuously developing on the surface of the po- rous rock, on the side of the Szalamandrás Hill (243 m). – 1= rusty brown layers Photo 4b. Microstratified spring deposit. – 1= rusty brown layers; 2= wavy, rough surfaces of the layers Photo 5. Macrostratifi ed spring deposit 12 fi cation frequently occurs in this case as well, it can be defi nitely separated from the above described version, since the rocks can easily be taken apart. Oft en plant remnants, sometimes even calcareous snails can be found among the layers (pictures 6, 7). Regarding the number and preservation of the fi nds, the plant remnants have a greater signifi cance in this case. The fossils include mainly silicifi ed stems or carbonized remnants of leaves (Photo 6). The veins are visible even to the naked eye, in some cases the material of the leaves was preserved as well. The material of such conserved leaves is always extremely crumbling and poorly preserved. These remnants could be found exclusively in white coloured layers. Paleobotanical description Pteridophyta „Pteris” oeningensis Unger, F. (Photos 8, 9). 1847 Pteris oeningensis Unger, F., Unger, F. 124 p. Pl. 37, fi gures 6, 7. 1855 Pteris oeningensis Unger, F., Heer, O. 39 p. Pl. 12, Figure 5. (a-i) – Öningen. 1990 Pteris oeningensis Unger, F., Kovar- Eder, J.–Krainer, B. 18 p. Pl. 1, figures 7–10, Pl. 3. Figure 7. – Wörth bei Kirchberg/ Raab. 1998 Pteris oeningensis Unger, F., Krenn, H. 174 p. Pl. 1, Figure 3. 2004 Pteris oeningensis Unger, F., Kovar- Eder, J. 165 p. Pl. 1, fi gures 1–3. – Mataschen Pteris oeningensis Unger, F., Meller, B. and Hably, L. – Gratkorn, in progress. Description: Only 1.2–1.3 cm small fractions of the secondary wings of the leaf blade are preserved. The length of the sec- ondary winglets varies between 0.2–0.8 cm, their width is between 0.1–0.2 cm, their size decreases towards the leaf apex section of the wings. Their location alternates on the spur. The wings grow narrow in the rounded leaf apex; their basis section broadens out, and joins the petiole as well as partly the other wings. There is a strong midrib in the middle of the blade, which has a dense vein system. The winglets have a smooth edge. Photo 7. Silicifi ed gastropod Photo 6. Fossilized fern remnant 13 The majority of the plant remnants in the quarry belong to this species. More than 20 frac- tions were found, which were originally parts of the leaf apex or the middle section of the sec- ondary winglets. In some cases, the rims of the winglets were fos- silized turned up, and the leaf seems to be narrower than its ac- tual size is. The occurrence of the species was recorded at numerous Austrian Late Miocene quarries, at several places it is accompanied by Podocarpium podocarpum. Its oc- currence refers to autochthonous environment on the one hand, and to wet habitat on the other. Leguminosae Podocarpium podocarpum (Braun, A.) Herendeen, P.S. (Photo 10) 1992a Podogonium knorrii (Braun, A.) Heer, O.; Herendeen, P.S., 4 p. fi gures 1–5. 1992b Podocarpium podocarpum (Braun, A.) Herendeen, P.S. 732 p. 1995 Podogonium knorrii (Braun, A.) Heer, O., Erdei, B. 1995. 15 p. fi gures 10, 11. 2004 Podocarpium podocar- pum (Braun, A.) Herendeen, P.S., Kovar-Eder, J.–Kvaček, Z.– Ströbitzer-Hermann, M. 2004. 74 p. Pl. 9. fi gures 8–11. Description: The length of the leafl ets varies between 2.2–2.4 cm, their width ranges between 0.8–1.0 cm. They are oval-shaped, the leaf base is slightly asymmetric, and the leaf apex is sharp. The vein Photo 8. „Pteris” oeningensis Unger, F.; leaf apex of the secondary winglet Photo 9. „Pteris” oeningensis Unger, F.; medial section of the secondary winglet Photo 10. Podocarpium podocar- pum (Braun, A.) Herendeen, P.S. leafl et 14 system is brochidodrom, camptodrom. The midrib is strong, the secondary veins are thin but dense, they run nearly parallel, and fi nally join each other noose-like near the rim of the leafl et. A basal vein starts from the petiole – exclusively on one side –, which can be followed till the lower third-half of the layer. The leafl et has a smooth edge. The quarry involved three leafl ets of this subtropical species of tree. It fi rst oc- curred in Central Europe in the Carpathian (Magyaregregy; Hably, L. 2002; Parschlug; Kovar-Eder, J. et al. 2004), later became dominant in the Sarmatian, and was an important element of almost every Sarmatian quarry (Hably, L. 1992). Like many other Sarmatian components, it also disappeared from the Pannonian Basin during the Pannonian, and did not return in the Pliocene, not even to places, where other dominant Sarmatian species, e.g. the Quercus kubinyii, Zelkova zelkovifolia occurred in the Pliocene of Gérce and Pula (Hably, L.–Kvaček, Z. 1997). It became an additional component of a reasonably rich fl ora in the Carpathian, while it frequently accompanied the principal or characteristic species of Quercus kubinyii, Zelkova zelkovifolia, „Parrotia” pristina in the Sarmatian. It can be found as a member of a subtropical fl ora-complex at every of its known quarries. Ulmaceae cf. Ulmus sp. (Photo 11) Description: The length of the leaf is 2.6 cm, its width takes about 1.5 cm. Its base, leaf apex and edge are fragmented. The vein system is craspedodrom. The secondary veins leave the strong midrib in acute angle, at some places branch out in a Y–shape. Only a single fragmented print was found at the quarry. Based on the low amount of taxonomic characteristics, it could be a leaf of an elm tree, which was quite widespread together with the various species of the Neogene edaphic associations. It was gener- ally located in the grove forests of the high fl ood area. It most frequently occurred only as an additional component, the dominant stock of the Ulmus braunii is known from the Sarmatian, and Pliocene. Monocotyledonae gen. et sp. – 2 small frag- ments (Photo 12) Description: The fragments are somewhat longer than 1 cm, their width is 0.7–0.8 cm. They have a dense system of fi ne veins, run- ning parallel. Only two small fragments are known from the quarry. According to the parallel vein system, they can be the mem- bers of this class. Their occurrence refers to autochthonous environment on the one hand, and to a neighbouring wet habitat on the other.Photo 11. cf. Ulmus sp.; leaf 15 Conclusions Based on the quite scant fl ora remnants, one can assume the presence of an edaphic association strongly related to water: the monocotyledons and the ferns could be located in the direct neighbourhood of water, the elm-trees were in the high fl ood area, while the Podocarpium podocarpum forest could be found somewhat further apart, supposedly accompanied by other species, which were not fossilized. The Podocarpium can be detected in the Carpathian Basin from the Carpathian to the Sarmatian, therefore, the age of the quarry can be between the Middle and Late Miocene. Regarding its climatic requirements, this species provides the most amount of information as well, since its known occurrences all prove a subtropical climate. REFERENCES Báldi, T. and Kókai, J. 1970. A kismarosi tufi t faunája és a börzsönyi andezitvulkánosság kora. (The fauna of the tuffi te at Kismaros and the age of the andesite volcanic activ- ity in the Börzsöny Hills.) 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Hably, L. and Kvaček, Z. 1997. Early Pliocene plant megafossils from the volcanic area in West Hungary. Studia Naturalia 10: 5–151. Heer, O. 1855. Die tertiäre Flora der Schweiz I. Winterthur, J. Wuster-Comp. 118 p. Herendeen, P.S. 1992a. A reevaluation of the fossil genus Podogonium Heer, O. In Advances in Legume Systematics, Part 4. The Fossil Record 3–18. Eds. Herendeen, P.S. and Dilcher, D.L. Kew, Royal Botanic Gardens. Herendeen, P.S. 1992b. Podocarpium podocarpum comb. nov., the correct name for Podogonium knorrii Heer, O. nom. illegit. (fossil Fabaceae). Taxon 41: 731–736. Jámbor, Á., Moldvay, L. and Rónai, A. 1982. Magyarázó Magyarország 200 000-es földtani térképsorozatához (Explanatory notes to the geological map series of Hungary). L-34–II. Budapest, MÁFI (Hungarian Institute of Geology), 358 p. Karátson, D. 1997. Vulkáni működés és kalderakérdés a Börzsönyben. (Volcanic activity and the caldera issue in the Börzsöny Mountains.) Földrajzi Közlemények 121. (3–4): 151–172. 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