| Mátra | |
|---|---|
 View of the mountain fromMátraderecske | |
| Highest point | |
| Peak | Kékes |
| Elevation | 1,014 m (3,327 ft) |
| Geography | |
 Location of Mátra (red) within physical subdivisions of Hungary | |
| Country | |
| Range coordinates | 47°52′N20°00′E / 47.867°N 20.000°E /47.867; 20.000 |
| Parent range | North Hungarian Mountains,Western Carpathians |
| Geology | |
| Rock type | Vulcanic |
TheMátra[ˈmaːtrɒ] (Slovak:Matra) is amountain range in northernHungary, between thetownsGyöngyös andEger. The country's highest peak,Kékestető (1014 m), belongs to this mountain range.
The formation of the Mátra is closely related to the formation of theNorth Hungarian Mountains and theCarpathians. Formations formed before the volcanism in theMiocene, are located primarily on the steep northern side of the Mátra. The reason for this is, that after the volcanism, the entire mountain range tilted southward due to thesubsidence of the trench extending south of the Mátra andBükk. The southern, more gentle part was buried by youngsediments, while on the northern side steep slopes were formed by landslides during thePleistocene.
The crystalline basement of the mountain range occurs as inclusions in volcanic rocks. Excluding these, the oldest formations are located along the fault system called theDarnó line, which runs northeast-southwest through the Eastern Mátra. The name of thethrow is given by theDarnó Hill rising betweenRecsk andSirok, whereTriassiclimestone,radiolarite andshale, as well asMiddle Pedimentary basalt pillow lavas, and in some placesOedic (Permian) limestone blocks are found.
In many places at the northern foot of the Mátra,Eocene volcanic and carbonate layers are deposited on theMesozoic formations; most of them are known from drilling, but they also surface north of the Eastern Mátra. These rocks can be linked to thePeriadriatic volcanism, which took place in the southern foreland of theAlps. They were brought to their present location by horizontal tectonic movements, so they have nothing to do with the real Mátra volcanism. This period is also represented by the igneous intrusion (intrusion rock body), to which theRecskskarn ore formation is also related.
The characteristic sediments of theOligocene age (Budamarl,Tardclay,Kiscellclay) cover the foot of the Mátra in places several hundred meters thick. Their layers are the source rocks of spring waters rich incarbon dioxide andhydrogen sulfide – thecsevices. In some places, tuff and tuffite layers are deposited in theKiscellclay, but these could not be the products of the Mátra volcano, but of a more distant volcano. Above the Kiscell clay, glauconiticsandstone,Parádschlieren andconglomerate layers dating from the beginning of the Miocene can be found; the latter is the bed of Miocene volcanic rocks in most places.
The main mass of the Mátra is formed by a several hundred-meter-thick layered volcanic rock mass consisting of an alternation of Middle Miocene (Badenian)pyroxeneandesite, andesitetuff and volcanicagglomerate. The driving force of the volcanic activity was the juxtaposition of the tworock plates that make up theCarpathian Basin region, theAlcapa and theTisza-Dacia. The migration of the cohesive, rotatingtectonic plates was not accompanied bysubduction (subduction) but by expansion processes: during these periods, thecalcium-richmagma could reach the surface. Theinner-Carpathian calc-alkaline volcanism, which began about 21 million years ago, in the first part of the Miocene, lasted until thePleistocene. The Mátra formed 13-18 million years ago as part of a series of events that are also significant in the geological history of ourEuropean continent.
The explosive, "acidic" volcanism rocks known as the introductory stage of Miocene volcanism are also found here. Of thepyroclastics classified under the collective name of lower, middle and upperrhyolite tuff, the middle one was identified in the Mátra. Its local variant was calledTardacitetuff due to its relatively lowersilicon content, the exact age of which is unknown; its formation time may be between 15-18 million years. It occurs asignimbrite deposited partly on land and partly under water up to an altitude of 500-600 meters in both the western and eastern parts. Since it is also found in relatively higher areas, it is certain that it played a fundamental role in the formation of the structure of the mountain range. The most likely scenario is that it was a series of violent and prolonged eruptions that ended with a caldera rupture. Another possibility is that the tilting of the Mátra towards the south caused the prominent geographical position of the tuff rock massif.
Theandesite lava blanket, which also determines the present-day landforms of the Mátra, was formed at about the same time as the formation of theTardacitetuff or 1-2 million years later, during the Miocene intermediate volcanism. The formation of andesite, i.e. magma with a medium SiO2-content, can be linked to plate subduction; the high volatile content of the plate subducting from the surface flows upwards and saturates themantle part above it. The melting point of the mantle material decreases with the process also calledmantle metasomatosis, so magma can form more easily. The melt formed at this time is still basaltic in composition, but by the time it reaches the surface through complicated magma mixing and differentiation (separation) processes, it becomes increasingly andesitic in nature. Andesitic lava – compared to rhyolite-dacite – is less violent, and instead of explosive, it comes to light during effusive eruptions, which do not involve caldera formation. In such cases – as in the case of Mátra – large-area lava sheets are more typical.
With the end of andesite volcanism,diatomaceous earth (diatomite) and thenlimestone were deposited in the basin betweenGyöngyöspata andSzurdokpüspöki, and at the end of the Miocene volcanism, some smallerrhyolite volcanoes were still active on the southern edge of the mountain range (one of the remains is the swelling cone of Kis-hegy at Gyöngyössolymos).[1]
The Mátra is part of theNorth Hungarian Mountains and belongs by origin to the largest young volcanic zone of Europe. It is situated between the valleys of the River Tarna and RiverZagyva. The Mátra divided into the Western Mátra, Central Mátra and the Eastern Mátra. The highest point of the Western Mátra is Muzsla (805 m). The Central Mátra consists of the plateau of Mátrabérc (Mátra Ridge) and the groups of the volcanic cones ofGalya-tető (964 m) andKékes (1014 m). Steep, rugged slopes, screes, talus slopes and slides alternate with one another, covered with closed beech forests. Gentler slopes and parallel valleys flow down to the south, the largest of which is the so-called Nagy-völgy ("Great valley"). The 'main entrance' to the Mátra was formed in parallel with the valley of Nagy-patak ("Great stream"), ranging from Mátrafüred to Mátraháza. From the vineyard-covered landscape of the foot of the Mátra travellers can arrive at the wooded mountains in a flash. To the east, after the steep escarpment of the 898-meter-high Sas-kő ("Eagle stone"), the 650–750-meter-high peaks of the Eastern Mátra follow one another. The northern part of the mountain range is calledMátralába ("the Mátra's feet"). This is a hilly area covered with 250–400-meter-high small volcanic cones, with mostly cultivated arable lands.
| West-Hungarian Borderland |  | |
|---|---|---|
| Little Hungarian Plain | ||
| Transdanubia | ||
| Transdanubian Mountains | ||
| Transdanubian Hills | ||
| North Hungarian Mountains | ||
| Great Hungarian Plain | ||
| International | |
|---|---|
| National | |
| Other | |
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