Marne di Monte Serrone

The Marne di Monte Serrone ("Monte Serrone Marl") is a geological formation in Italy, dating to roughly between 181 and 178 million years ago,[1][2] and covering the early and middle Toarcian stage of the Jurassic Period of central Italy.[1] It is the regional equivalent to the Toarcian units of Spain such as the Turmiel Formation, units in Montenegro, such as the Budoš Limestone and units like the Wazzant Formation and the Azilal Formation of Morocco.[3]

Marne di Monte Serrone
Stratigraphic range: Early-Mid Toarcian
~181–178 Ma
↓
Panoramic of Monte Serrone with the Jurassic in the background
TypeGeological formation
Sub-unitsValdorbia, Colle d´Orlando, Pale Vallone & Pozzale Sections
UnderliesRosso Ammonitico, Calcari e Marne a Posidonia & Calcari Diasprigni Formations
OverliesCorniola & Calcare Massicio Formations
Thickness64–80 m (210–262 ft)
Lithology
PrimaryCalcilutites & clay-rich greenish marls with calcareous lenses
OtherArgillaceous gray green marls with calcarenites alternated with marls
Location
Coordinates42°59′30.1″N 12°50′58.2″E
RegionUmbria
Country Italy
ExtentUmbria-Marche Basin
Type section
Named forMonte Serrone
Named byPialli
Year defined1969
Marne di Monte Serrone (Italy)

Description

The Marne di Monte Serrone was first defined by Pialli in 1969.[4]

The formation is characterised for be one of the most complete sections of the Toarcian paleobiographical strata around Europe.[5] It is also one of the best places on southern Europe where the strata shows the effects of the Lower Toarcian anoxic event (TAE). The formation also provides data about the changes after the Toarcian AE, with changes on the deposited micritic limestones and marls, what shows a local sedimentary response to the Toarcian climatic perturbation induced by the Vulcanism of the Southern Karoo-Ferrar that boiled the carbon cycle and change the mechanism of Earth climate. The dawn after the Toarcian AE is presented locally by changes on the environments, to more seashore to lagoonal ones.[6]

Depositional environment

The environment of the formation has been compared to the present on the Toarcian Betic Cordillera strata, with a corridor of pelagic environments with influence from emerged reliefs.[7] Other sections are related to nearby emerged lands, seashore deposits and even inland deposition, due to the changes in lithology (especially with the clay minerals kaolinite and smectite). Due to that, the main depositional layers of the formation are believed to come from an environment intermediate between pelagic and nearshore settings.[8]

Due to the influence of different depositional settings, the lithology of the formation was widely distributed, with changes on the mineralological composition. The clay Mineral assemblages, with the neritic sedimentation, expose a change on the deposition, as it can be seen on the Valdorbia Section, where on the Middle Toarcian the reduction of this minerals indicate a sea-level fall, with a change from a bathyal to a middle shelf environment. Additionally there is a record of changes on the fauna, specially bivalves that suggests a variable flow regime at the major wave base as a result of a storm event.[9]

Fossil content

The biota of the formation comprise mostly marine microinvertebrates and algae, with the presence of ammonites and abundant pollen in the Middle Toarcian sections. Nanoplankton is one of the most representative finds of the layers, appearing deposited with interruptions, probably due to changes on the oxygen content of the sea floor.[10] Phytoplankton includes abundant dinoflagellate cysts and acritarchs, specially the genus Micrhystridium. There registered a transgression on the sea level on the Lower Toarcian, with a rise, giving the Umbria-Marche Basin pelagic conditions, and a regression during the Middle Toarcian. Those changes implicate the disappearance of genera of dinoflagellates from the strata to be replaced with new ones.[11][12] Some dinoflagellate genera such as Mendicodinium are more abundant in the Marne di Monte Serrone than in any other unit discovered until 1997.[13]

Foraminiferal analysis had been done, revealing changes in the salinity, with Spirillina as the most abundant genus found, followed by Prodentalina, Eoguttulina, Lenticulina, Nodosaria, Lingulonodosaria and Pseudonodosaria.[14] Invertebrate remains are mainly brachiopods (Pseudokingena, Nannirhynchia and Lokutella, among others) and ammonites; Eodactylites, Pleuroceras, Canavaria, Trinacrioceras, Lioceratoides, and Praepolyplectus as predominant genera.[15]

Other marine fauna includes Holothuriidan Sclerites, unidentified crinoids, fragmentary asteroideans and fish teeth, similar to the genera Saurostomus and Dapedium.[16]

There are terrestrial fossils and sediments, specially clay. The main source area for the clay could have been the palaeosoils developed on the Carbonate Latium-Abruzzo Platform, although more recent studies prove a continental origin.[17] The Main fossils from terrestrial deposits are plant Pollen, mostly Pteridophyta spores and Circumpolles, and Palynomacerals.[18] The genera includes Leptolepidites (Lycopsida) spp., Trilites (Filicopsida) spp., Ischyosporites (Pteridopsida) spp. or Foveosporites (Selaginellaceae) spp. and others less abundant, such as the genus Callialasporites (Coniferales).

There is a curious reduction of the Cheirolepidiaceae genus Classopollis, abundant on coeval associations from northern Europe, Portugal, northeast Italy and Israel, as a possible effect of paleoclimatic changes.[19] In 2019 was recovered that Marne di Monte Serrone seashore section was part of the now lost continent of Greater Adria, with the confirmation of a continental origin for the plant matter, as was proposed in 1997.[20]

See also

References
  1. Baldanza, 1989
  2. Sabatino et al., 2009
  3. Monaco, 1994
  4. Pialli, 1969
  5. Palliani & Mattioli, 1994
  6. Satolli et al., 2018
  7. Nini et al., 1996
  8. Parisi et al., 1996
  9. Ortega Huertas et al., 1993
  10. Noël et al., 1993
  11. Palliani et al., 1998
  12. Palliani et al., 1999
  13. Palliani et al., 1997
  14. Rodríguez Tovar et al., 2016
  15. Bilotta et al., 2010
  16. Monaco et al., 1994
  17. Perilli et al., 2008
  18. Palliani & Riding, 1997
  19. Palliani, 1997
  20. Van Hinsbergen et al., 2019

Bibliography
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