[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.

[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.

[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.

[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.

After the Pyrenean and Savian movements, the Éplény area started to sink slowly and to receive marine sediments, emerging later on the Middle Miocene.

[10] The oldest formations on the Úrkút basin are referred to the Upper Triassic Dolomite range and the Dachstein Limestone of Raetian age.

Late Pliensbachian strata is composed by nodular and cherty red limestone with abundant ammonites and brachiopods, that belong to the Isztimér Formation.

[12] The Late Jurassic strata is vanished locally, with the Cretaceous sedimentation starting with several continental beds with Bauxite and accompanying Laterites.

[13] The Úrkút Manganese ores occur on marine sedimentary rocks composed mainly of bioclastic Limestone, radiolarian Clay Marlstone, and dark-gray to Black Shale.

[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).

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.

[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.

[24] 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.

[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.

[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.

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.

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.

Originally identified as pollen from possible early angiosperms, is now classified as coming from Erdtmanithecales and relative arbustive to arboreal flora.

Herbaceous fern spores, linked to open humid environments Laevigatosporites[36] Affinities with the family Pteridopsida inside Tracheobionta.

Originally identified as pollen from possible early Angiosperms, is now classified as coming from Bennetitales, that are closely related with the true flowering plants.

Herbaceous fern spores, linked to open humid environments Pleurozonaria[36] Affinities with the family Prasinophyceae inside Chloroplastida.

Herbaceous fern spores, linked to open humid environments Vitreisporites[36][5] Affinities with the family Caytoniales inside Gymnospermae.

[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.

level, 7th layer, main gallery], the sample anatomy, with mixed pitting and taxodioid cross-fields, clearly points out the genus Prototaxodioxylon.