Rya Formation

The Rya Formation (Swedish: Ryaformationen) is a geologic formation in Skåne County, southern Sweden. It is Early to early Middle Jurassic (early Sinemurian to late Aalenian) in age. The Rya Formation comprises siltstones, claystones, sandstones, mudstones and rare coal beds. The formation overlies the Höganäs Formation and is overlain by the Vilhelmsfält and Mariedal Formations.
The formation was deposited in the Höganäs and Øresund Basins that formed in the earliest Jurassic as part of the break-up of Pangea. The thick formation comprises four members, from base to top the Döshult, Pankarp, Katslösa and Rydebäck Members. The depositional environment of the formation ranges from continental to open marine.
The Rya Formation has provided fossils of a number of sharks, ammonites, bivalves and ichnofossils. Coalified wood occurs as scattered pieces up to long and indeterminate belemnites, echinoids, serpulids, ostracods and nodosariid foraminifera were also recorded in the formation. Iron ooids containing erratic boulders, called "Geschiebe" in German, attributed to the Rya Formation were found in Holstein, northern Germany.
Description.
The Rya Formation crops out in Colonus Shale Trough of western Scania.
The formation overlies the Höganäs Formation and is overlain by the Vilhelmsfält Formation in the Helsingborg area and by the Mariedal Formation in the area of Landskrona and Kävlinge. The Rya Formation is subdivided, from base to top, into the Döshult, Pankarp, Katslösa and Rydebäck Members. The formation is found in the Ängelholm, Helsingborg, Landskrona and Kävlinge areas. In southwest Skåne, the Rya Formation is missing or only
poorly developed. In the Øresund Basin between Sweden and Denmark, the formation is truncated by the Basal Middle Jurassic unconformity.
Erratic boulders, called "Geschiebe" in German, attributed to the Rya Formation and containing iron ooids were found in Holstein, northern Germany.
Subdivision.
The early Sinemurian Döshult Member (Swedish "Döshultsledet") comprises coarse-grained cross-layered sandstones and siltstones in the lower part, and is dominated by dark clays and marls rich in marine fossils in the upper part. The member is up to thick in the Ängelholm, Helsingborg and Landskrona areas. Presently, the basal part of this member is exposed at three localities in the Helsingborg area. These contain mineralogically and texturally mature, trough cross-bedded sandstones, commonly with herringbone structures showing north and south oriented paleocurrent directions. The occurrence of herringbone structures in well-sorted sand suggests high energy foreshore to subtidal marine depositional conditions for the lower part of the member. In an abandoned quarry in northwest Skåne (Gantofta brickpit in the Helsingborg area, outcrop very limited at present) the upper part of the Döshult Member commences with bioturbated marine nearshore sands, including burrows, as well as abundant marine invertebrate body fossils. This is followed by a bioturbated shelf mudstone with storm-deposited sand and silt intercalations (tempestites). A massive red mudstone with scarce marine body fossils and burrows follows, which is interpreted as having been deposited rapidly, in a low energy but oxidizing environment. The youngest part of the succession comprises siltstones and mudstones, with carbonate-rich beds, deposited in a shallow marine setting. Coaly detritus, muscovite, very small shells and shell fragments, and framboidal pyrite nodules (0.1–0.3 mm in diameter) are characteristic constituents of this member.
The dark mudstones of the Döshult Member are overlain by the Pankarp Member (Swedish "Pankarpsledet") with a sharp conglomeratic boundary. The late Sinemurian Pankarp Member has an estimated thickness of up to in the subsurface of the Ängelholm, Helsingborg and Landskrona areas. In the Kävlinge area, the thickness is about thick. In westernmost Skåne, the member has been observed in small diameter drill cores. There, the member is subdivided into a lower unit of variegated clays and shales, a middle, poorly sorted silty to sandy unit including a coal bed, and an upper monotonous mudstone unit which is silty and rich in organic matter at the base, and reddish–greenish at the top. It presents different coloration probably due to different degrees of oxidation of iron in the claystone. In the uppermost part of one core, the Pankarp Member comprises lenticular bedded heteroliths with "Planolites" burrows.
The late Sinemurian to early Pliensbachian Katslösa Member (Swedish "Katslösaledet") is mainly known from the subsurface in westernmost Skåne, and it has a thickness of in the Ängelholm, Helsingborg and Landskrona areas. In the Kävlinge area, the thickness is about . Sedimentological interpretations are mainly based on the results of petrographical studies of museum collections. The Katslösa Member yields a rich marine microfauna and macrofauna, and it is dominated by homogeneous mudstone deposited in a marine low-energy environment. Is composed mostly by marine green, brown and dark gray claystones and sandstones. Thin beds of matrix-rich quartz wackes are common. They are typically mineralogically mature but texturally highly immature with abundant angular sand grains. The matrix comprises organic matter, micrite, mica and clay minerals. In thin section, the sandstones show evidence of intense burrowing, which has obliterated depositional structures. Scattered berthierine ooids, as well as authigenic siderite crystals have been observed in the member.
The late Pliensbachian to late Aalenian Rydebäck Member (Swedish "Rydebäcksledet") is up to thick in the Ängelholm, Helsingborg and Landskrona areas. It is only known from subsurface material in westernmost Skåne, and sedimentological analysis is based on observations from two wells (Rydebäck–Fortuna-1 and -4). These layers were deposited in small bands during a sea regression, and consist of marine gray, black, green and reddish brown sand and siltstones. The member comprises a uniform succession of muddy arenites with a rich marine microfauna (mostly foraminifera), and represents deposition in an offshore low-energy environment. The sediments are strongly burrowed, which has caused an effective mixing of sand and mud, resulting in the forming of quartz wackes. The sand is quartz-rich, and grains are typically well rounded. Berthierine ooids are common constituents of the sediment.
Depositional environments.
Tethys Sea transgression entailed formation of fossil-bearing marine deposits in Skane, also associated with an increased tectonic activity. Deposition of the Rya Formation began with nearshore coarse clastics, and continued with offshore mudstones with tempestites (the Döshult Member), followed by offshore muddy sediments with a brief non-marine interval (the Pankarp Member), and ended with deposition of open marine low-energy deposits (Katslösa and Rydebäck Members). The marine Rya Formation shows an overall fining-upwards trend, and an up-section bathymetric deepening of the depositional environment. The depositional environment in western Skåne was either physically protected from the storm energy due to basin topography, or deposition in Skåne took place below storm wavebase. Berthierine ooids occur scattered in the Katslösa
Member and are increasingly abundant up-section in the Rydebäck Member. There is a possibility that iron ooid formation was promoted by precipitation of iron and silica from volcanic fluids rising up through the substrate, as has been reported from modern marine sediments offshore Indonesia. This hypothesis has emerged with the publication of age data for the volcanic rocks in Skåne, which now appear to be comparable in age to the prominent iron ooid-bearing deposits, i.e. the Rydebäck Member and the Röddinge Formation.
Age.
Based on foraminifers, ammonites and ostracods, the Döshult Member is dated to the early Sinemurian, the Pankarp Member to the late Sinemurian, the Katslösa Member to the late Sinemurian to early Pliensbachian and the Rydebäck Member to the late Pliensbachian to late Aalenian.
The formation is time-equivalent with the Röddinge Formation of the Vomb Trough, the Djupadal Formation in cental Skane and the Sorthat Formation of Denmark, with which it shares the "Spheripollenites"–"Leptolepidites" and "Callialasporites"–"Perinopollenites" Zones. The formation also correlates with the Fjerritslev Formation of the Danish Basin, and the Gassum Formation of the Øresund Basin. The storm-dominated, hummocky cross-stratified Hasle Formation on Bornholm is contemporaneous with the muddy Katslösa Member of the Rya Formation.
Basin history.
The basins where the Rya Formation was deposited form part of the Sorgenfrei-Tornquist Zone (STZ) of the Trans-European Suture Zone, the boundary between Baltica to the northeast and Peri-Gondwana to the southwest. The orogeny was active in the Late Ordovician, or approximately 445 million years ago.
At the Carboniferous-Permian boundary around 300 Ma, the area was influenced by the Skagerrak-Centered Large Igneous Province, another large igneous province stretching across the North Sea, the eponymous Skagerrak between Denmark and Sweden and to the northwest up to northern England and Scotland.
The basins of southern Sweden and eastern Denmark were formed during the latest Triassic and earliest Jurassic. During this time the Central Atlantic magmatic province (CAMP), with an estimated the largest igneous province in Earth's history, was formed to the present southwest of the Danish-Swedish realm. In the Skåne area, the Central Skåne Volcanic Province was active during the time of deposition of the Rya Formation, commencing around the Sinemurian-Pliensbachian boundary. The earliest magmatism was partly emplaced into and across pre-existing extensional basin structures. The first and the main volcanic phase of this volcanic province occurred in the Early Jurassic (late Sinemurian to Toarcian) at 191–178 Ma. Analysis of the volcanic rocks produced by this Jurassic volcanism suggests a continental Strombolian-type eruptive character close to the oceans of the Early Jurassic. No correlative pyroclastic beds have yet been identified in sedimentary basins surrounding central Skåne.
During deposition of the Rydebäck Member, the Toarcian turnover happened. This event at the Pliensbachian-Toarcian boundary characterized by widespread anoxic conditions globally, led to the extinction of various groups of flora and fauna. Taxa inhabiting the upper water column were unaffected by anoxia and included ammonites and belemnites. Epifaunal taxa adapted to low-oxygen conditions, such as the buchiids, posidoniids and inoceramids, flourished in the post-extinction environment during the survival interval.
Economic geology.
A study on the geothermal potential of reservoirs in the Øresund Basin published in 2018 by Erlström et al. gave results of the formation together with the Gassum and Höganäs Formations, giving the following characteristics of the three Early Jurassic formations:
A study published in the same year analyzing the CO2 storage potential of the Rya and Höganäs Formations concluded a storage capacity of 543 megatons of carbon dioxide.
The organic content of the Jurassic strata in Skåne is typically dominated by gas-prone kerogen (type III), which is below, or at the onset of, thermal maturity.
Paleoenvironment.
The sedimentological evolution of the Jurassic in southwestern Skåne, specially the Rya Formation, has provided depth diverse data about it´s different environments, specially on those samples recovered on the Höllviken-2 core and sidewall cores from the FFC-1 well. The unit was linked on all it´s sedimentological history with the main Fennoscandinavian land. The local succession in the Höllviken Halfgraben and Barsebäck Platform has measured continue during most of the Triassic and Early Jurassic times. Inte western part of the Höllviken Halfgraben during the Hettangian–Pliensbachian succession there is evidence of higher subsidence rate along the Öresund Fault, indicating tectonically controlled deposition and the presence of a submarine high at the west of this fault. In the east is the Skarup Platform, interpreted as a Jurassic high based on its incomplete or missing Rhaetian–Lower Jurassic strata, along redeposited spores and pollen in the Höllviken Halfgraben and increased sand output, that point to this zone as the major freshwater terrestrial source. This deposits shows several nearshore enviornments, from offshore marine environment probably below wave base on the sinemurian level, as proven by the presence of well cemented fine sand and 2 m thick clay dominated heterolites, that change to more marine influenced flaser bedded heterolites with some strongly bioturbated horizons and convolute beds in the Pliensbachian, and end in the Pliensbachian–Lower Toarcian with a sandy seashore setting with high energy lenticular beds. Some sections are suggested to be tidal flat zones and/or distal bar deltaic deposits.
Fossil content.
The formation has provided fossils of typically marine fauna. With the exception of a continental coal bed, the formation is marine in character. Shark teeth were reported from the Rydebäck Member. Apart from a few teeth of the hybodont "Hybodus reticulatus", the shark fauna from the Rya Formation is exclusively neoselachian.
Coalified wood occurs as scattered pieces up to long and indeterminate belemnites, echinoids, serpulids, ostracods and nodosariid foraminifera were also recorded in the formation.