The Úrkút Manganese Ore Formation is a Jurassic geologic formation in Hungary. It covers the Early Toarcian stage of the Early Jurassic, and it is one of the main regional units linked to the Toarcian Anoxic Events.[2][3] Different fossils heve been recovered on the locations, including marine life such as Ammonites Fish and terrestrial fossils, such as Palynomorphs and fossil wood.[4][5][6][7] Úrkút (17´38'E and 47´05'N) and Eplény (17´55'E and 47´12'N) are the main deposits of the Formation.[1] Are related to the Bakony Range, an ancient massif that was uplifted gradually and exposed to a long period of erosion, where the deposits of Úrkút appear to be a basin inclined gently to the north, while the highest point to the south is the basalt mass of Kab Mountain. Eplény region consists of a broad N-S trending open valley between fiat-topped, small hills.[1][8]
| Úrkút Manganese Ore Formation | |
|---|---|
| Stratigraphic range: Toarcian ~ | |
 Ancient karst formation in an abandoned manganite quarry in Úrkút | |
| Type | Geological formation |
| Unit of | Úrkút Basin |
| Underlies | Épleny Limestone Formation |
| Overlies | Isztimér Formation |
| Thickness | 15 m (49 ft) |
| Lithology | |
| Primary | Manganese |
| Other | Rhodochrosite |
| Location | |
| Region | Central Mountains of Transdanubia |
| Country |  Hungary |
| Extent | ~12 km (7.5 mi) by 4–6 km (2.5–3.7 mi) |
| Type section | |
| Named for | Úrkút |
| Named by | Drubina-Szabo[1] |
| Year defined | 1959 |
  Úrkút Manganese Ore Formation (Hungary) | |
Geology
editThe Urkut Area is part of the Bakony Tectonic Block, with the abundant presence of faults dividing the region into several segments.[1] The terrain where the Manganese Ore is developed is characterised by a high fracturation, where the Jurassic beds and shale lent themselves readily to deformation, with minor folds, faults and shear zones.[9] During the geological evolution of the Bakony range a series of principal fractures were active repeatedly, yielding to vertical as well as horizontal forces that ultimately produced the structural make-up controlling the present topographic configuration of the area.[9] The Jurassic sediments, along the other Mesozoic aged strata were deposited in a branch of a Geosyncline, connected with the Alpine coeval biota.[1] On the Triassic-Jurassic boundary Kimmerian movements take place, as evidenced by the change observed on the texture of the local Calcareous sediments, interpreted as a gradual rising of the sea bottom.[9] To the end of the Lower Jurassic, on the Toarcian, there are several records of another series of pulses from Kimmerian movements, that resulted in partial emergence, which dates the beginning of Karst development on the Csirda Mountain. However, marine sedimentation continued over most of the region and the sea became more widespread.[1] On this time a global sea transgression occur, where on the Úrkút basin shallow-water sediments accumulated near the margins, and with progressive deepening of the sea bottom until the end of late Liassic time, sediments of correspondingly deeper water were deposited.[1] Due to a cut-off of water circulation there were a series of changes on the local development of the basin, which led to the accumulation of the manganese minerals.[1]
The Éplény Area shows a structure and geological development with minor differences from those of Úrkút, being considered overall identical. However, it suffered minor deformation during the late Kimmerian movements, and instead of the Austrian movements, the Subhercynian and Laramide movements produced important structures. After the Pyrenean and Savian movements, the Éplény area started to sink slowly and to receive marine sediments, emerging later on the Middle Miocene.[1] The manganese ore group of beds appears in an absolutely different way according to evolution in Eplény, where while in Úrkút 4 beds can be divided, in Eplény, the 3 beds appear usually with sharp boundary, in reduced thickness.[10]
Stratigraphy
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The oldest formations on the Úrkút basin are referred to the Upper Triassic Dolomite range and the Dachstein Limestone of Raetian age. After the deposition of the Triassic rocks a series of Jurassic strata successions have overlain the older deposits, with its lowermost contact found on the uppermost strata of the own Dachstein Limestone, developing a lower Liassic sequence that is a white, yellowish-gray or pink, dense Limestone resembling that of the Dachstein.[1] Over it, there is a series of younger liassic strata and a Crinoid-Brachiopod and Rhynchonellatan bearing reddish Limestone, that resembles the Sinemurian Hierlatz Limestone of the Csárda Mountain, that is the last unit under the coeval Manganese deposits from there. Late Pliensbachian strata is composed by nodular and cherty red limestone with abundant ammonites and brachiopods, that belong to the Isztimér Formation.[11] On the uppermost Pliensbachian strata there is a series of beds that consists of greenish-gray limestone and marl, which also contain crinoids and brachiopods, being the last unit under the Manganese Ore.[1] The Upper Liassic (Toarcian) sequence is composed mostly by the Úrkút Manganese and the Éplény Limestone (Late Toarcian-Aalenian), and starts with thick-bedded, gray, Radiolaria-bearing, argillaceous marl containing several intercalations of manganese carbonate, or rarely, manganese oxides, with the top of the sequence being a brown to purple nodular Limestone with light green spots.[1] Middle Jurassic overlaying these deposits, being mostly a series of cherty Marlstone containing the genus Posidonomya and several types of Radiolaria.[12] The Late Jurassic strata is vanished locally, with the Cretaceous sedimentation starting with several continental beds with Bauxite and accompanying Laterites.[1] Finally, on the Tertiary, the Lower Eocene continental clay and bauxite are overlain by gray carbonaceous clay and sandstone, with the Jurassic beds and manganiferous beds eroded.[1]
Lithology
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The Manganese Ore is the main component of the formation, and its distinctive characteristic element.[13] The Úrkút Manganese ores occur on marine sedimentary rocks composed mainly of bioclastic Limestone, radiolarian Clay Marlstone, and dark-gray to Black Shale. The Origin of the Local Manganese Ores based on the presence of siliceous manganese ores and antauthigenic Silica points to the volcanogenic-sedimentary origin of this Mn-ore deposits[14] Manganese nodules are widely distributed in the area in Jurassic rocks, mainly on the Lower Jurassic, but younger nodules also occur.[13] The Black Shale with Mn-carbonate get its maximum deposition on the Toarcian, concretely during the Tenuicostatum–Falciferum Ammonite zones in the coeval Sachrang Formation, Strubberg Formation and Allgäu Formation in the Northern Calcareous Alps and the Eastern Alps (Austria, Germany and Switzerland), while Úrkút and related deposits were the regional equivalent in the Transdanubian Range.[13] There are other deposits with Shale and associated Mn particles on contemporaneous oxic deposits occur that formed under similar environmental conditions.[15] The Úrkút Manganese deposit has been investigated geologically, mineralogically and chemically.[16] It has several properties, including very fine grain size (~ 1 μm), an enrichment of metals over a geologically very short time (-500 thousand years). Both Metals and the Manganese have been related with local hydrothermal vent systems, where the metal enrichment was a result of microbial activity.[17] There are at least three types of Manganese deposits that occur close in proximity. The first, those with cherty Fe–Mn-oxide ore, developed on the margins of the much larger carbonate ore body, whose origin has been related with proximal fracture systems, being composed by varicolored metalliferous Claystone. Other type includes the so-called Csárda-hill, where it is very cherty and iron-rich, and is suggested as originated from a low-temperature fluid flow along an associated fracture zone. This deposit is associated with sedimentary dykes, filled with red Lime-Mudstone, varicoloured Claystone, carbonate debris, or Mn oxides. The last type is the Black Shale-hosted Mn-carbonate, considered a distal ore-forming environment, where the Mn-carbonate proto-ore sediment accumulated. A hydrothermal/exhalative source of metals may have contributed to the formation of the deposits of Black Shale.[18]
There is a rhodochrosite ore, composed of laminated gray, green, brown, and black sections, and is associated with a diagenetic origin.[19] Rhodochrosite concretions with fish and plant fossils are common on the strata, composed by Mn-bearing Calcite with traces of hydroxyl-apatite, kutnohorite, smectite, quartz, feldspar, barite, pyrite, and quartz-cristobalite.[19] Mineralized sections do not contain fossils or traces of benthic fauna, and contain only rarely fish remnants, planktonic organisms as well as silicified, manganized, or coalified plant fragments.[20]
Celadonite and smectite, especially the first, had particular importance for understanding the genesis of the Úrkút manganese ore.[21] Celadonite and nontronite indicate paleo-oxygen level variations in the environment. There are well-crystallised celadonite occurrences that was formed by primary precipitation, differing from the known celadonite occurrences in that it is not found in direct association with submarine basic volcanic rocks, although being any evidence for volcanic contribution to the local ore genesis.[22] The Smectite is also found on the lower Pliensbachian Limestone. Nearly every Sample on Úrkút contains interstratified Illite/smectite.[23]
The Rn220 and Rn222 concentration in the Úrkút Manganese Formation is anomalously high, and it causes health risk for the attendants of the Úrkút Manganese Mine, which is considered to be related to active fossil Biomat (bacterial action) which leads local minerals to adsorb different atoms or ions, whether they are radiogenic or not.[24]
Paleoenvironment
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Black Shale is present worldwide in the lower Toarcian, linked to the anoxic events that took place, in Úrkút locally related with deposits of Manganese Ore.[25] Being part of the Transdanubian Range, the Úrkút Manganese Ore was linked to the environmental evolution of the southern passive margin of the rifting Tethys Ocean.[9] After Hettangian drowning and Sinemurian-Pliensbachian extensional tectonics and subsidence, along with pelagic sedimentation and submarine topography, a pronounced horst developed over the local sea, with a depth on the Pliensbachian-Toarcian Basin of 600 m.[26] The environment of the Formation was linked to 2 settings: a series o pelagic basind, including the Zala Basin and the own Úrkút and Eplieny Basins, related to open marine conditions where bioturbation is scarce, but there is a great amount of planktonic organisms, associated with a suboxic to anoxic conditions.[25] Radiolarians, sponge spicules, crinoid ossicles, bivalves, gastropods, ammonites and fish were recovered as the main local biota, deposited on a 20–40 m basinal ore sequence.[25] The Other deposits come from the near emerged lands, that include the Gerecse Hills, Vértes Hills and the Bakony Hills, whose biota has been recovered on the formation by palynological analysis and fossil wood.[27]
More recent studies support the lack of any igneous event during Pliensbachian and Toarcian times in the Úrkút Basin.[23] The Smectite formation lacks igneous rocks, tuffs, or volcanic glasses.[23] Although, it can be due to changes in the fluctuation on the basin.[23] Observed Mn veins and their above-proposed formation mechanism do not eliminate the possibility of tectonically formed Neptunian dikes elsewhere in the basin, which could well fit in the local, general tectonic environment observed, for instance in Eplény.[9]
In this setting volcanism was the main local event, where eroded near basaltic sequences provided a metallic source for the ore, being channeled by suboxic waters to the Úrkút Basin.[25] The local tectonic activity created fractures and deep faults and there was a development of endogenic thermal effects, such as degassing and the release of solutions, along with the mixing of syngenetic ash falls that deposited Fe into the carbonate rocks.[28] The fine Volcanic material was altered on the Marine sediments. The local hydrothermal emanations in the deep fault zones, where bacterial activity caused the precipitation of large amounts of metal ions in the form of very fine-grained oxyhydroxides. Meanwhile, the accumulation of dead bacteria created a mass of very reactive organic matter. Under aerobic conditions, the action of the microbial oxidation led to the local accumulation of Mn oxides that ended being Ca-rhodochrosite, and supported Celadonite formation by mixing of geological fluids with seawater. It has been calculated 563 years for the duration of ore local formation based on an estimated 3 weeks for a microbial population growth cycle.[29]
The local manganese ore is, in reality, a Mn-ore series of stromatolite with a volcanic tuff component, that was later transformed by diagenetic processes.[28] The modern analog of this environment of the Úrkút Manganese Ore basinal deposits would be flourishing Prokaryotic bacteria colonies located in submarine vent systems, normally related with remnants of proto-rifts or failed rift systems on continental crust in a submarine environment. The local environments are interpreted as hydrothermal vent systems of cooler temperatures.[28]
Fossils
editBivalves
edit| Bivalvia | |||||
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| Genus | Species | Material | Location | Notes | Images |
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Úrkút quarry. |
A Clam, member of the family Inoceramidae inside Myalinida. Mistaken for other related genera on the deposit, it is among the most abundant local clams. Found associated with large Fe deposition. |
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Úrkút quarry. |
A Clam, type member of the family Solemyidae inside Solemyida. Benthic fauna found in the black slate. |
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Brachiopoda
editThe dominant group are the Terebratulids, while Strophomenids play a significant role.[31] While the Brachiopods and Gastropods are more abundant on the underlying Hiertlaz Formation, but also continuous on the Úrkút and Épleny quarries.[31] In the very rich fauna of the local seamount slope the orders Terebratulida and Rhynchonellida play an equally important role, but the basin areas are characterized by a low-diversity fauna dominated by large terebratulids.[31]
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| Genus | Species | Material | Location | Notes | Images |
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A Rhynchonellatan, member of the family Nucleatidae inside Terebratulida. Benthic fauna found in the black slate. |
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Gastropoda
edit| Gastropoda | |||||
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| Genus | Species | Material | Location | Notes | Images |
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A Sea Snail, member of the family Eucyclidae inside Seguenzioidea. Abundant on deposits with Terrigenous inputs |
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Cephalopoda
edit| Cephalopoda | |||||
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| Genus | Species | Material | Location | Notes | Images |
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An Ammonite, member of the family Phylloceratidae inside Phylloceratida. Was the main identified ammonite locally on Úrkút, and is related to great concentrations of Fe. |
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A Nautilidan, type member of the family Cenoceratidae. A well distributed genus between the Sinemurian-Toarcian, found on Germany, England, Austria, Italy, etc. |
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An Ammonite, type member of the family Dactylioceratidae inside Ammonitida. Related with specimens from Germany and Austria. |
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An Ammonite, member of the family Hildoceratidae inside Ammonitida. The most diverse, related with specimens from Germany and Austria, but also north Italy. |
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An Ammonite, type member of the family Lytoceratidae inside Ammonitida. Related with specimens from Germany and Austria. |
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An Ammonite, member of the family Hildoceratidae inside Ammonitida. The most abundant, linked with specimens from north Italy. |
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An Ammonite, member of the family Phylloceratidae inside Phylloceratida. It is based on more complete specimens than other local Ammonites. |
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Actinopterygii
edit| Actinopterygii | |||||
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| Genus | Species | Material | Location | Notes | Images |
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An Osteichthyes, type member of the family Caturidae inside Amiiformes. On the skull the operculum and the praeoperculum are long and close contact. There is a single epidural plate that connects to the dorsal extension of the vertebral body.[6] |
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An Osteichthyes, type member of the family Dapediidae inside Holostei. The Dapedium specimen from Úrkút is the first articulated Mesozoic fish body fossil from Hungary that is described in detail.[34] The preserved cranium reveals important characters, although species-level identification is hindered by suboptimal preservation of some diagnostic features.[34] |
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An Osteichthyes, member of the family Pycnodontiformes inside Neopterygii. It is located on the dorsal side, with the skull bones frontal and parietal are strongly intertwined it extends strongly towards the anterior end of the skull. It has an interoperculum larger than any other fish taxon. The posterior scales on the fossil is characterized by the appearance of a 2–3-pronged spike.[6] |
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An Osteichthyes, type member of the family Leptolepididae inside Teleostei. On the fracture surfaces of the Shale, many mica flakes can be observed, along with the enrichment of fossils, including this genus. The Most abundant fish genus recovered locally, probably formed large Schools. Is linked to the Toarcian biota of Germany and England. |
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Fungi
edit| Fungi | |||||
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| Genus | Species | Material | Location | Notes | Images |
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Uncertain types of plant parasite Fungi. It was impossible to identificate the specimens found. Spores located on the manganese ores had hyphal threads. Some fungal remains occurred on disorganized higher plant remains, being probably parasitic or saprophytic vegetations, occurring in direct ratio with the plant rest. |
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Fungal spores of uncertain assignation, probably Ophiostomatales. O. urkutensis is known only from Úrkút and related with Plant spores, probably being a parasitic fungus. |
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Palynology
edit| Palynology | |||||
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| Genus | Species | Material | Location | Notes | Images |
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Affinities with the family Gymnospermophyta inside Gymnospermae. Unclassified Gymnosperm spores |
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Affinities with the family Bennettitales inside Spermatopsida. Medium to large sized Cycad-like flora pollen. |
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Affinities with both Sciadopityaceae and Miroviaceae in the Pinopsida. This pollen's resemblance to extant Sciadopitys suggest that Miroviaceae may be an extinct lineage of Sciadopityaceae-like plants.[37] | ||
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Affinities with the family Cheirolepidiaceae inside Coniferales. Coniferous pollen related to dy and hot settings, abundant on the Toarcian Afro-Mediterranean realm. |
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Affinities with the family Pteridopsida inside Tracheobionta. Unclassified Fern Spores |
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Affinities with the family Pteridophyta inside Tracheobionta. Unclassified fern spores |
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Affinities with the family Pteridaceae inside Polypodiopsida. Fern spores related with large colonies on humid settings. |
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Affinities with the family Cheirolepidiaceae inside Coniferales. Coniferous pollen related to dy and hot settings, common along with Classopollis. |
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Affinities with the family Pteridophyta inside Tracheobionta. Unclassified fern apores |
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Affinities with the family Prasinophyceae inside Chloroplastida. Green Algae Cysts, related with oxygenated waters. |
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Affinities with the family Caytoniales inside Pteridospermatophyta. Pollen from large arboreal to arbustive ferns, related with tropical settings. |
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Affinities with the family Cyatheales inside Polypodiopsida. Tree Fern spores, related with humid environments. C. minor was first identified on the Úrkút deposits. |
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Affinities with the family Cycadales inside Cycadopsida. |
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Affinities with the family Matoniaceae inside Gleicheniales. Fern spores related with modern genera that grew forming large colonies in tropical locations. The great diversity suggest this fern grows on sections proximal to the seashore. |
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Affinities with the family Gymnospermophyta inside Gymnospermae. Unclassified Gymnosperm spores |
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Affinities with the family Gymnospermophyta inside Gymnospermae. Unclassified Gymnosperm spores |
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Affinities with the family Erdtmanithecales. Originally identified as pollen from possible early angiosperms, is now classified as coming from Erdtmanithecales and relative arbustive to arboreal flora. |
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Affinities with the family Ginkgoaceae inside Ginkgoopsida. Pollen that resembles the modern Ginko pollen. |
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Affinities with the family Lycopodiaceae inside Lycophyta. Lycopod Spores, related with low herbaceous flora found associated with humid environments. |
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Affinities with the family Goniodomaceae inside Dinophyceae. Green Algae Cysts, related with oxygenated waters. |
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Affinities with the family Pinidae inside Coniferales. Associated with Classiopollis on dry environments. |
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Affinities with the family Schizaeaceae inside Schizaeales. Herbaceous fern spores, linked to open humid environments |
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Affinities with the family Pteridopsida inside Tracheobionta. Unclassified Fern Spores |
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Affinities with the family Pteridopsida inside Tracheobionta. Unclassified Fern Spores. L. pflugii, L. transdanubicus and L. urkutensis where identified first on Úrkút. |
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Affinities with the family Lycopodiaceae inside Lycophyta. Lycopod Spores, related with low herbaceous flora found associated with humid environments. |
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Affinities with the family Marattiaceae inside Marattiopsida. Fern spores related with modern genera that grew forming large colonies in tropical locations. |
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An Acritarch, probably related with Chloroplastida. Possible organic matter from green algae. |
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Affinities with the family Magnoliophyta inside Cycadophytanae. Pollen similar of the modern angiosperm pollen. |
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Affinities with the family Bennettitales inside Spermatopsida. Originally identified as pollen from possible early Angiosperms, is now classified as coming from Bennetitales, that are closely related with the true flowering plants. As its name suggest, M. urkutiensis was first described on Úrkút. |
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Affinities with the family Lycopodiaceae inside Lycophyta. Lycopod Spores, related with low herbaceous flora found associated with humid environments. |
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Affinities with the family Bennettitales inside Spermatopsida. A Hygrophyte pollen, related with dry lowlands. |
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Affinities with the family Podocarpaceae inside Coniferales. Associated with Classiopollis on dry environments. |
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Affinities with the family Selaginellaceae inside Lycophyta. Herbaceous fern spores, linked to open humid environments |
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Affinities with the family Prasinophyceae inside Chloroplastida. Green Algae Cysts, related with oxygenated waters. |
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Affinities with the family Gymnospermophyta inside Gymnospermae. Unclassified Gymnosperm spores |
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Affinities with the family Pteridophyta inside Tracheobionta. Unclassified dern apores. P. circulus was identified first on Úrkút. |
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Affinities with the family Umkomasiaceae inside Corystospermaceae. Pollen from large arboreal to arbustive ferns, related with tropical settings. |
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Affinities with the family Lycopodiaceae inside Lycophyta. Lycopod Spores, related with low herbaceous flora found associated with humid environments. |
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Affinities with the family Sphagnaceae inside Bryophyta. Moss spores from humid settings. |
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Affinities with the family Cheirolepidiaceae inside Coniferales. Coniferous pollen related to dy and hot settings. |
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Affinities with the Bryophyta inside Embryophyta. Moss Spores from humid settings. |
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Affinities with the family Pteridophyta inside Tracheobionta. |
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Affinities with the family Filicopsida inside Tracheobionta. Unclassified Fern Spores. T. verrucatus was identified first on Úrkút. |
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Affinities with the family Caytoniales inside Gymnospermae. Pollen similar of the modern angiosperm pollen. |
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Affinities with the family Pteridophyta inside Tracheobionta. Unclassified Fern Spores. |
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Affinities with the family Prasinophyceae inside Chloroplastida. Green Algae Cysts, related with oxygenated waters. |
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Affinities with the family Pteridophyta inside Tracheobionta. Unclassified Fern Spores. T. transdanubicus was identified first on Úrkút. |
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Affinities with the family Schizaeaceae inside Schizaeales. Herbaceous fern spores, linked to open humid environments |
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Affinities with the family Caytoniales inside Gymnospermae. Unclassified Gymnosperm spores |
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Fossil Wood
edit| Wood | |||||
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| Genus | Species | Material | Location | Notes | Images |
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Affinities with the family Araucariaceae inside Coniferales. Assigned to Dadoxylon agathiforme, Agathoxylon mecsekense, Araucarioxylon resiniferum, Brachyoxylon sp., Dadoxylon sp. and Baieroxylon sp.[42] This Genus represent the most diverse wood found locally, with several assigned specimens of poor preservation, but that can confidently be referred to Agathoxylon.[39] |
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Affinities with the family Cupressaceae inside Coniferales. This wood, poorly preserved, was only briefly mentioned, and is more probably conspecific with Platyspiroxylon sp. 2.[39] |
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Affinities with the family Ginkgoaceae inside Ginkgoopsida. Shows radial pitting is of mixed type, mostly uniseriate, radial pits forming small or long chains; cross-fields are of araucarioid type. It is labelled "Eplény, kovasodott fatörzs" (Eplény, silicificd wood).[39] |
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Affinities with the family Podocarpaceae inside Coniferales. Can be related with Araucarioxylon sp. 5?.[39] |
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Affinities with the family Taxaceae inside Coniferales. Labelled "Platyspiroxylon parenchymatosum, P. Greguss, Úrkút, István akna".[39] |
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Affinities with the family Taxaceae inside Coniferales. Labelled 'Técsbányatelep, András akna, 6. szint, 7. réteg, fővágat" [Pécsbányatelep, András shaft, 6th. level, 7th layer, main gallery], the sample anatomy, with mixed pitting and taxodioid cross-fields, clearly points out the genus Prototaxodioxylon.[39] |
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Affinities with the family Gymnospermophyta, incertae sedis.[39] |
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Affinities with the family Cheirolepidiaceae inside Coniferales.[42] |
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Affinities with the family Cheirolepidiaceae inside Coniferales. It was at the first suggested to come from the Cretaceous period. Then was found to be from the Toarcian. The local fossil wood is impregnated in manganese, what can be a further evidence for hydrothermal source for the local metals.[41] The wood of Simplicioxylon hungaricum is widespread on the lias of Europe, from the Hettangian to the Mid-Aalenian.[41] |
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Affinities with the family Araucariaceae inside Coniferales. Unique of úrkút, has been synonymized with Agathoxylon, although some trunks have different symmetry. It was originally thought to come from Aptian clay (now Albian clay), although this partly silicified sample is probably reworked from Toarcian layers.[39] |
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References
edit- ^ a b c d e f g h i j k l m n Drubina-Szabo, M. (1959). "Manganese deposits of Hungary" (PDF). Economic Geology. 54 (6): 1078–1094. doi:10.2113/gsecongeo.54.6.1078. Retrieved 16 November 2024.
- ^ Jenkyns, Hugh C.; Géczy, Barnabas; Marshall, James D. (1991). "Jurassic Manganese Carbonates of Central Europe and the Early Toarcian Anoxic Event". The Journal of Geology. 99 (2): 137–149. doi:10.1086/629481. ISSN 0022-1376.
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