10 research outputs found
Szermonostor faragott kőanyagának geológiai vizsgálata és származása
Archeological excavations at the monastery of Szermonostor started in 1970 under the supervision of Ottó Trogmayer followed later by other archeologists including Ferenc Horváth and Katalin Vályi. These works used the most up to date methodologies and tools providing thorough documentation of features and artefacts. The lithic material, which is the subject of this study was handed over to us for analysis by Katalin Vályi. Based on our results the studied building stones were of outstanding quality and must derive from quarries of the Buda, Pilis, Gerecse Hills. The stones were transported to the site on the Danube and the Tisza Rivers. Although the majority of the stones come from the mentioned areas, some specimens have proveniences in the eastern and western parts of the Balaton Highlands. The order of description of the studied samples followed that of successive geological ages from the Permian to the Pleistocene. Processing marks and alterations were also noted and described
A DĂ©lkelet-Alföld Ă©s Szeged Ă©pĂtĹ‘-, dĂszĂtĹ‘-, használati köveinek erdĂ©lyi geolĂłgiai vonatkozásai a kora nĂ©pvándorlás kortĂłl a török korig
The lowlands of the Great Hungarian Plain (GHP) are generally lacking easily reachable outcropping natural rocks suitable for construction, decorative purposes or the preparation of various household commodities. The best resources meeting the QC requirements are mainly found in Southern Transylvania. These rocks range from marbles, schists, quartzites, the prevailing Upper Cretaceous „BĂłzes" type sandstones, Miocene oolithic limestones and fine-grained sandstones. Flint and salt also belong to this group. The best transportation route was offered by the Maros River itself. Numerous Early Avar cemeteries found along the Maros valley and the SE GHP yielded various type of stones used. Detailed archeometric analysis of theses stones from the largest Early Avar Age cemetery near MakĂł, representing the first settling generation brought interesting results. As these groups most likely used the rocks that they encountered during the course of their migration into the basin preceding 568 A.D., they must record the route itself too, which is so far unsettled in Hungarian archeology. The majority of the stones come from rocks found in SE Transylvania in the southern rim of the Transylvanian Mid-Mountain along the Maros valley. In addition, the northern half of the Southern Carpathians, the NW, SE and S part of the Transylvanian Basin. According to this, the route of migration out of Bulgaria must have led through SE Transylvania. Building and decorative stones of similar types and origin for the medieval castle of Szeged, the Downtown church as well as numerous temples and monasteries in the SE Great Hungarian Plains indicate the sustainment of these geological, economic links till the 17th century. Az Alföld termĂ©szetes kövekben szegĂ©ny vidĂ©kĂ©n Ăłriási szerepe volt más tájakrĂłl származĂł kĹ‘zeteknek. A legközelebb minĹ‘sĂ©gileg is elfogadhatĂł források fĹ‘kĂ©nt DĂ©l-ErdĂ©lyben vannak. Ezek a márványoktĂłl, a csillámpalákon, kvarcitokon, a domináns felsĹ‘-krĂ©ta „bĂłzesi" homokköveken át a miocĂ©n ikrás mĂ©szkövekig Ă©s homokkövekig terjednek. Ide tartozik a tűzkĹ‘ Ă©s a sĂł. A szállĂtáshoz a legĂ©sszerűbb megoldást a Maros biztosĂtotta. A nĂ©pvándorláskorban a DK-Alföldön számos kora avar temetĹ‘bĹ‘l kerĂĽlt elĹ‘ kĹ‘anyag. Az egĂ©sz tĂ©rsĂ©g legnagyobb elsĹ‘ generáciĂłs kora avar temetĹ‘je MakĂł-MikĂłcsa mellett találhatĂł, mely kĹ‘eszközeinek vizsgálata Ăşj Ă©rdekes eredmĂ©nyeket hozott. Mivel 568-as megĂ©rkezĂ©sĂĽket megelĹ‘zĹ‘en a vándorlás során Ă©rintett terĂĽletek kĹ‘zeteinek anyagát minden bizonnyal hasznosĂtották, Ăgy ezek vizsgálata az egykori migráciĂłs Ăştvonalakra is fĂ©nyt derĂthet, melyet eddig a magyar rĂ©gĂ©szet csak feltĂ©telezni vĂ©lt. Az eszközök kĹ‘zetanyagának többsĂ©ge egyĂ©rtelműen DK-ErdĂ©lyi származásĂş, az ErdĂ©lyi-közĂ©phegysĂ©g dĂ©li, Maros-menti, a DĂ©li-Kárpátok Ă©szaki Ă©s az ErdĂ©lyi-medence dĂ©li, Ă©szaknyugati Ă©s dĂ©lkeleti rĂ©szĂ©re korlátozĂłdik. Ăgy feltĂ©telezhetĹ‘, hogy a vizsgált közössĂ©g BulgáriábĂłl ErdĂ©lyen keresztĂĽl vándorolt be a Kárpát-medencĂ©be. A közĂ©pkori szegedi vár az AlsĂłvárosi templom Ă©s számos DKalföldi monostor, templom Ă©pĂtĹ‘ Ă©s dĂszĂtĹ‘kövei között is hasonlĂł elterjedĂ©si terĂĽletrĹ‘l származĂł kĹ‘zettĂpusok voltak azonosĂthatĂłak, mutatva a terĂĽletek fontos geolĂłgiai, gazdasági kapcsolatát egĂ©szen a XVII századig
A Tihanyi FormáciĂł a Balaton környĂ©kĂ©n: tĂpusszelvĂ©ny, kĂ©pzĹ‘dĂ©si körĂĽlmĂ©nyek, rĂ©tegtani jellemzĂ©s.
Revisiting the Tihany, Fehérpart section, overviewing archive data, comparison with successions of nearby wells,
well-logs, stratigraphic data and results of the high-resolution seismic surveys on Lake Balaton resulted a coherent picture on the depositional environment, age, stratigraphic correlation and palaeogeographic connections of the Tihany Formation. In addition to former analyses of grain-size distributions, carbonate and clay content, the sedimentary structures were investigated, a pilot study of gamma-ray measurements on the field was carried out and several orders of cyclicity were demonstrated. Besides previous palaeontological studies new fossils were collected, determined and magnetic polarity of the rocks were measured. The Tihany, Fehérpart section is correlated with the Spiniferites tihanyensis dinoflagellate, the MN11 micromammal and the Limnocardium decorum sublittoral mollusc biozones. It shows normal magnetic polarity. It is underlain by open lacustrine, reverse polarity shales of the Congeria
praerhomboidea zone, and is overlain by layers indicative of the Prosodacnomya zone. The latter is well definied by the
radiometric age (7.9 Ma) of the overlying volcano sedimentary suite. Therefore the Fehérpart section was deposited either 8.1–8.0 Ma (C4An.2n) or 8.3–8.2 Ma (C4Ar.1n chron) ago.
The Tihany Formation was deposited in a variety of palaeoenvironments related to deltas entering Lake Pannon. It is built up of parasequences, i.e. shallowing up successions from below wave base to lake level generated by sediment accumulation. Parasequences were formed on the delta front or in inter-distributary bays to delta-plain swamps and distributary channels. Beyond the high frequency lake-level and partly autocyclic environmental fluctuations, most likely climatically induced fourth-order lake-level changes of about 15–30 m amplitude occurred, resulting in minor transgressions followed by repeated progradation of deltaic lobes.
Although the Tihany (as well as the very alike SomlĂł) Formation is found along the rim of the hills currently, during its origin it was deposited in the same way as the Ăšjfalu Formation known only from the subsurface of deep basins. The dynamics of deltaic settings feeding to Lake Pannon can be understood by studying the Tihany Formation in outcrops.
The only difference among the two formations might be in the number of overlying delta cycles and their thickness. Both
numbers were determined by rate of subsidence smaller at basement highs where Tihany Formation accumulated than at
basin areas where Ăšjfalu Formation was definied. It is suggested here to include Tihany (and SomlĂł) beds as members of the Ăšjfalu Formation.
Fourth-order sequence boundaries were recognized between the overlying progradational deltaic bodies. In the vicinity of Tihany no evidences of lake-level drops were revealed, but elsewhere small incised-valley fills point to minor
lake-level drops. Overall regression interrupted by transgressive events continued on the study area until the shelf edge of Lake Pannon shifted as far to the south as 50-60 km, i.e. at about 8 Ma ago. Since then flooding events became rare and small in amplitude, then the area became a terrestrial plain. Fluvial deposits are not known from the direct vicinity, but travertines formed in small freshwater ponds fed by karst springs. The transition from lacustrine to terrestrial palaeoenvironments is part of the overall normal regression as a result of high sediment input to Lake Pannon. Large incised valleys or other evidences of recurring terrestrial conditions which could be related to third-order sequence boundaries mappable all over the Pannonian Basin were identified neither in Tihany nor in Ăšjfalu Formations
A DĂ©lkelet-Alföld Ă©s Szeged Ă©pĂtĹ‘-, dĂszĂtĹ‘-, használati köveinek erdĂ©lyi vonatkozásai a kora nĂ©pvándorlás kortĂłl a török korig
The lowlands of the Great Hungarian Plain (GHP) are generally lacking easily reachable outcropping natural rocks suitable for construction, decorative purposes or the preparation of various household commodities. The best resources meeting the QC requirements are mainly found in Southern Transylvania. These rocks range from marbles, schists, quartzites, the prevailing Upper Cretaceous „BĂłzes" type sandstones, Miocene oolithic limestones and fine-grained sandstones. Flint and salt also belong to this group. The best transportation route was offered by the Maros River itself. Numerous Early Avar cemeteries found along the Maros valley and the SE GHP yielded various type of stones used. Detailed archeometric analysis of theses stones from the largest Early Avar Age cemetery near MakĂł, representing the first settling generation brought interesting results. As these groups most likely used the rocks that they encountered during the course of their migration into the basin preceding 568 A.D., they must record the route itself too, which is so far unsettled in Hungarian archeology. The majority of the stones come from rocks found in SE Transylvania in the southern rim of the Transylvanian Mid-Mountain along the Maros valley. In addition, the northern half of the Southern Carpathians, the NW, SE and S part of the Transylvanian Basin. According to this, the route of migration out of Bulgaria must have led through SE Transylvania. Building and decorative stones of similar types and origin for the medieval castle of Szeged, the Downtown church as well as numerous temples and monasteries in the SE Great Hungarian Plains indicate the sustainment of these geological, economic links till the 17th century. Az Alföld termĂ©szetes kövekben szegĂ©ny vidĂ©kĂ©n Ăłriási szerepe volt más tájakrĂłl származĂł kĹ‘zeteknek. A legközelebb minĹ‘sĂ©gileg is elfogadhatĂł források fĹ‘kĂ©nt DĂ©l-ErdĂ©lyben vannak. Ezek a márványoktĂłl, a csillámpalákon, kvarcitokon, a domináns felsĹ‘-krĂ©ta „bĂłzesi" homokköveken át a miocĂ©n ikrás mĂ©szkövekig Ă©s homokkövekig terjednek. Ide tartozik a tűzkĹ‘ Ă©s a sĂł. A szállĂtáshoz a legĂ©sszerűbb megoldást a Maros biztosĂtotta. A nĂ©pvándorláskorban a DK-Alföldön számos kora avar temetĹ‘bĹ‘l kerĂĽlt elĹ‘ kĹ‘anyag. Az egĂ©sz tĂ©rsĂ©g legnagyobb elsĹ‘ generáciĂłs kora avar temetĹ‘je MakĂł-MikĂłcsa mellett találhatĂł, mely kĹ‘eszközeinek vizsgálata Ăşj Ă©rdekes eredmĂ©nyeket hozott. Mivel 568-as megĂ©rkezĂ©sĂĽket megelĹ‘zĹ‘en a vándorlás során Ă©rintett terĂĽletek kĹ‘zeteinek anyagát minden bizonnyal hasznosĂtották, Ăgy ezek vizsgálata az egykori migráciĂłs Ăştvonalakra is fĂ©nyt derĂthet, melyet eddig a magyar rĂ©gĂ©szet csak feltĂ©telezni vĂ©lt. Az eszközök kĹ‘zetanyagának többsĂ©ge egyĂ©rtelműen DK-ErdĂ©lyi származásĂş, az ErdĂ©lyi-közĂ©phegysĂ©g dĂ©li, Maros-menti, a DĂ©li-Kárpátok Ă©szaki Ă©s az ErdĂ©lyi-medence dĂ©li, Ă©szaknyugati Ă©s dĂ©lkeleti rĂ©szĂ©re korlátozĂłdik. Ăgy feltĂ©telezhetĹ‘, hogy a vizsgált közössĂ©g BulgáriábĂłl ErdĂ©lyen keresztĂĽl vándorolt be a Kárpát-medencĂ©be. A közĂ©pkori szegedi vár az AlsĂłvárosi templom Ă©s számos DKalföldi monostor, templom Ă©pĂtĹ‘ Ă©s dĂszĂtĹ‘kövei között is hasonlĂł elterjedĂ©si terĂĽletrĹ‘l származĂł kĹ‘zettĂpusok voltak azonosĂthatĂłak, mutatva a terĂĽletek fontos geolĂłgiai, gazdasági kapcsolatát egĂ©szen a XVII századig