Rya Formation

The Rya Formation crops out in Colonus Shale Trough of western Scania.Ahlberg et al., 2003, p.528

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.Ahlberg et al., 2003, p.530 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.Ahlberg et al., 2003, p.533 In the Øresund Basin between Sweden and Denmark, the formation is truncated by the Basal Middle Jurassic unconformity.Erlström et al., 2018, p.129

Erratic boulders, called Geschiebe in German, attributed to the Rya Formation and containing iron ooids were found in Holstein, northern Germany.Hinz-Schallreuter & Schallreuter, 2009, p.2

;Döshult Member

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.Andersson & Hybertsen, 2010-8-17 The member is up to {{convert|80|m|ft}} 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.

;Pankarp Member

The dark mudstones of the Döshult Member are overlain by the Pankarp Member (Swedish Pankarpsledet) with a sharp conglomeratic boundary.Frandsen & Surlyk, 2003, p.550 The late Sinemurian Pankarp Member has an estimated thickness of up to {{convert|70|m|ft}} in the subsurface of the Ängelholm, Helsingborg and Landskrona areas. In the Kävlinge area, the thickness is about {{convert|20|m|ft}} 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.

;Katslösa Member

File:Map of Rya Formation - Katslosa and Rydeback members - Scania.jpg

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 {{convert|30|to|40|m|ft}} in the Ängelholm, Helsingborg and Landskrona areas. In the Kävlinge area, the thickness is about {{convert|75|m|ft}}. 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.Ahlberg et al., 2003, p.534

;Rydebäck Member

The late Pliensbachian to late Aalenian Rydebäck Member (Swedish Rydebäcksledet) is up to {{convert|70|m|ft}} 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.

File:Laurasia 200Ma.jpg

Tethys Sea transgression entailed formation of fossil-bearing marine deposits in Skane, also associated with an increased tectonic activity.Greiff, 2019-8 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.

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 central Skane and the Sorthat Formation of Denmark, with which it shares the Spheripollenites–Leptolepidites and Callialasporites–Perinopollenites Zones.Nielsen et al., 2003, p.588Nielsen et al., 2003, p.590 The formation also correlates with the Fjerritslev Formation of the Danish Basin,Frandsen & Surlyk, 2003, p.543 and the Gassum Formation of the Øresund Basin.Erlström et al., 2018, p.138 The storm-dominated, hummocky cross-stratified Hasle Formation on Bornholm is contemporaneous with the muddy Katslösa Member of the Rya Formation.

File:Avalonia_Baltica_Sarmatia_geologi.png

;Basement

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.

File:CAMP Magmatism in the context of Pangea.jpg

;Break-up of Pangea

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 {{convert|11000000|km2|sqmi}} 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.Bryan & Ferrari, 2013, p.1058 The first and the main volcanic phase of this volcanic province occurred in the Early Jurassic (late Sinemurian to Toarcian) at 191–178 Ma.Bergelin, 2009 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.Augustsson, 2009 No correlative pyroclastic beds have yet been identified in sedimentary basins surrounding central Skåne.Ahlberg et al., 2003, p.539

;Toarcian

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.Harries & Little, 1999

File:Early Jurassic paleogeographic map of northwest Europe with the occurrences of Agaleus.jpg

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:Erlström et al., 2018, p.139

• Net sand thickness - {{convert|60|to|100|m|ft}}
• Porosity - 18 to 34%
• Permeability - 50 to 1500 mD
• Cl⁻ concentration - 120 to 190 gram/liter
• Productivity index - 7.0 m3/hr/bar

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.Sjöberg, 2018, p.90

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.

File:Grimmen_Formation_distribution.png and adjacent units, with the Rya Fm marked by the 107 (=Vilhelmsfält Borehole)]]

The sedimentological evolution of the Jurassic in southwestern Skåne, specially the Rya Formation, has provided depth diverse data about its different environments, specially on those samples recovered on the Höllviken-2 core and sidewall cores from the FFC-1 well.Bou Daher (2012)-p10 The unit was linked on all its 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.Bou Daher (2012)-p7 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.Bou Daher (2012)-p37 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 environments, 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.Bou Daher (2012)-p14 Some sections are suggested to be tidal flat zones and/or distal bar deltaic deposits.Bou Daher (2012)-p15 Coeval with the Rydebäck member, at Anholt (Fjerritslev Formation) where studied several levels that point to a connected fluvial system.Seidenkrantz & Koppelhus (1993)-p201 Concretely the Upper Pliensbachian-Toarcian boundary marks the beginning of a major regression, which continued through the Toarcian and Aalenian. The discovery of the foraminifera Eoguttuliiia liassica, Bony Fishes and Scolecodonts, points that the Pliens-Toar boundary has a shallow water environment, possibly of reduced salinity.Seidenkrantz & Koppelhus (1993)-p210 The Pollen and spores, identical of those found on the Rydebäck member (Vilhelmsfält Bore No. 1 and

Karindal bore no. 1), increase, and the dinoflagellate cysts decrease, suggesting more proximal shoreline. This layers, on both Anholt and the Rydebäck member, are considered to represent a regression from marine inner shelf environments to near lagoonal or deltaic conditions during the late Pliensbachian and early Toarcian, but with light marine influence, as show the presence of Dactylioceras on the Rydebäck member. The sequence points concretely than in both units The Late Pliensbachian sediments at were deposited in a storm-influenced Inner Shelf setting, that changed on the Lower Toarcian into a more restricted, marginal-marine conditions with delta progradation.Nagy, J. (2003)-p28 Then in the late Toarcian increased brackish conditions, to end on a short marine encroachment during the Early Aalenian.

The study of the Jurassic sediments has allowed to know that the basement rocks of southern Sweden were deeply weathered in Late Triassic-Cretaceous times, with formed saprolites on the sub-mesozoic basement and high amount of Kaolinite on the stronger weathered profiles, opposed to smectite on the less weathered ones.Ahlberg, Olsson & Šimkevičius, 2003-p15 Thus, fluvial currents released smectite-rich weathering material to the Late Triassic–Jurassic receiving basins. The members of the Rya Formation recover a transition from deltaic to paralic coast and shallow marine, dominated by kaolinite, along with peaks of illite and smectite.Ahlberg, Olsson & Šimkevičius, 2003-p17 The record of this minerals showed that at the time of deposition of the Rya Formation, mid-latitude warmth and pronounced humidity to drier pseudomediterranean climates allowed on the denuded bedrock in the Fennoscandian Shield, composed of Gneisses or Granites, at places intersected by Dolerite dykes, fracturation and active erosion/weathering.Ahlberg, Olsson & Šimkevičius, 2003-p19 The coeval Djupadal Formation volcanic ash falls at the east Skarup Platform-Cenntral Skane Volcanic Province, may have diluted the marine sediments, with raised smectite content. The pronounced mineralogical maturity of most Swedish post-Norian Mesozoic arenites confirms widespread feldspar destruction in the weathering profiles of the Paleozoic crystalline basement at the north, as a consequence of the increased humidity.Ahlberg, Olsson & Šimkevičius, 2003-p21 A fish tooth recovered from the lower Toarcian of the North West German Basin presents a radiogenic seawater value of −6 ε-units, which is quite counter-intuitive to the idea of massive unradiogenic crustal-derived inputs from Laurasia. Clastic fractions found on the same layer suggest brief radiogenic Nd influxes from the Skåne flood basalts erupted at this time.Dera, Prunier, Smith, Haggart, Popov, Guzhov, Rogovf, Delsate, Detlev, Pucéatj, Charbonnierk & Germain (2015)-p1610

;Pliensbachian

Lower-late Pliensbachian Layers at Katslösa are similar in faunal composition. The Katslösa Member composition suggest deposition on a Low Energy Marginal marine environment with absence of changes in the salinity (As proven by the presence of Echinoderms and other low salt intolerant fauna), with active bottoms filled by traces of diverse invertebrates and abundance of Bivalves. The Upper Pliensbachian section that mark the appearance of the Rydebäck Member continues the stable salinity environment with increased presence of Echinoderms, but lack of a diverse Bivalve fauna as in the older section. This unit was deposited likely on a marine setting more proximal to the shore and low-energy, more strongly burrowed than older layers. The presence of Selachian fauna can be more likely derived from a more suitable depositional setting for this remains than a biota turnover. Palynology in this section is dominated by spores in the Karindal bore no. 1, suggesting a humid climate on nearby emerged lands.

;Toarcian

Toarcian layers of the formation where influenced by the ongoing vulcanism located in the Central Skåne Volcanic Province (Djupadal Formation), as, marine water influence is observed in the main outcrop of the last unit, where enriched Zeolite by Barium is suggested to derive from oceanic water, that may have circulated as hydrothermal flows in the lapilli tuff and facilitating diagenetic changes.Augustsson (2001)-p28 Is also known by palynological analysis on the Bonnarp Cone, where saltwater/brackish acritarchs like Leiosphaera and Leiofusa or Dinoflajellates like Nannoceratopsis where recovered.Bölau & Kockel-Brosius (1965)-p55 This section also recovers the increased influence of Terrestrial weathering measured in the layers after the Toarcian AOE, as seen in the Vilhelmsfalt borehole, where plant remains increase their presence, suggesting a regression of the coast influenced by the increased volcanic-derived materials.Dera, Prunier, Smith, Haggart, Popov, Guzhov, Rogovf, Delsate, Detlev, Pucéatj, Charbonnierk & Germain (2015)-p1611 The Palynology in this section is dominated by the Pollen of Chasmatosporites (Cycads), with at least six species recovered, playing more than 50% of the total palynological samples, implicating a clear dominant role of the producer of this Pollen and suggesting along the increased amount of Cheirolepidiaceae pollen and general decrease of spores a shif towards a more arid climate on nearby settings.Guy-Ohlson, 1988-p11

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.[https://paleobiodb.org/classic/displayCollResults?collection_no=90692 Rya Formation] at Fossilworks.org

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• Eklexibella johanniWeitschat & Gründel (2002)-p39
• Serpula quinquesulcata
• Serpula terquemiTroedsson (1951)-p146-147
• Serpula cf. raricostati

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• ?Acrosaleniidae Indeterminate
• Balanocrinus subteroidesTroedsson (1951)-p15
• Hispidocrinus scalaris
• Isocrinus ranaeHunter, A.W. & Rees, J.(2010)-p10-24
• Pentacrinus basaltiformis

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• Agassiceras nodulatumReyment (1959)-p118
• Amaltheus margaritatus
• Amauroceras ferrugineumDoguzhaeva, Mutvei & Weitschat (2003)-p83
• Arnioceras cf. falcariesReyment (1959)-p129
• Arnioceras sp. indet.Reyment (1959)-p130
• Asteroceras obtusumFrandsen & Surlyk, 2003, p.545
• Coroniceras rejnesiReyment (1959)-p110
• Cymbites striariesReyment (1959)-p134
• Dactylioceras tenuicostatumReyment (1959)-p142
• Dactylioceras cf. semicelatum
• Echioceras raricostatumSivhed, U. (1984)- p.251
• Eleganticeras elegantulumLehmann (1961)-p42-43
• Eparietites sp. indet.Reyment (1959)-p132
• Euagassiceras resupinatum
• Euagassiceras spinaries
• Euagassiceras lundgreni
• Euagassiceras cf. lundgreni
• Megarietites meridionalisReyment (1959)-p112
• Oxynoticeras oxynotum
• Oxynoticeras? sp. indet.Reyment (1959)-p136
• Paracoroniceras crossiReyment (1959)-p114
• Pleuroceras spinatum
• Pleuroceras hawskerenseDoguzhaeva, Mutvei & Weitschat (2003)-p86
• Polymorphites angustusReyment (1959)-p139
• Prodactylioceras davoei
• Promicroceras planicostatum
• Promicroceras sp. juv.Reyment (1959)-p137
• Tragophylloceras ibex
• Uptonia jamesoniSivhed, U. 1984-p19

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• "Belemnites" elongatusDoguzhaeva, Mutvei & Weitschat (2003)-p80
• "Belemnites" milleriDoguzhaeva, Mutvei & Weitschat (2003)-p81
• Passaloteuthis alveolataTroedsson (1951)-p243-245
• Passaloteuthis apicicurvata
• Passaloteuthis cf. virgata
• ?Passaloteuthis sp.Doguzhaeva, Mutvei & Weitschat (2003)-p79
• Pseudohastites charmouthensis
• Pseudohastites cf. arundineus

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• Rhynchonella deffneri
• Spiriferina walcotti
• Zeilleria numismalis
• Zeilleria perforataTroedsson (1951)-p148-150

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• Anomia pellucidaTroedsson (1951)-p224
• Anisocardia luggudensis
• Arcomya decora
• Arcomya cf. elongataTroedsson (1951)-p193
• Astarte angeliniTroedsson (1951)-p167
• Astarte fructuumTroedsson (1951)-p168
• Astarte scanensis
• Astarte fortunaTroedsson (1951)-p169
• Astarte deltoideaTroedsson (1951)-p170
• Astarte oerbyensisTroedsson (1951)-p171
• Astarte ryensis
• Astarte sp.
• Barbatia pullaTroedsson (1951)-p159
• Cardinia tolliniTroedsson (1951)-p160
• Cardinia expansaTroedsson (1951)-p161
• Cardinia ingelensisTroedsson (1951)-p162
• Cardinia kullensisTroedsson (1951)-p163
• Cardinia spp.
• Chlamys interpunctata
• Chlamys textoria
• Chlamys janiformisTroedsson (1951)-p211
• Chlamys subulataTroedsson (1951)-p212
• Chlamys tullbergiTroedsson (1951)-p213
• Chlamys textaria
• Chlamys interpunctataTroedsson (1951)-p214
• Dimyodon sp.Troedsson (1951)-p220
• Entolium sp.
• Entolium hehliTroedsson (1951)-p216
• Entolium calvum
• Entolium cingulatumTroedsson (1951)-p217
• Entolium lundgreniTroedsson (1951)-p218
• Eotrapezium gerrnariTroedsson (1951)-p181
• Eotrapezium pullastra
• Eotrapezium hebertiTroedsson (1951)-p184
• Eotrapezium menkeiTroedsson (1951)-p185
• Gervillia angeliniTroedsson (1951)-p203
• Gervillia scanicaTroedsson (1951)-p204
• Gervillia hagenowiTroedsson (1951)-p205
• Gervillia sjögreniTroedsson (1951)-p206
• Goniomya heteropleuraTroedsson (1951)-p195
• Grammatodon cypriniformis
• Grammatodon sinuatusTroedsson (1951)-p157
• Grammatodon subrhomboidalisTroedsson (1951)-p158
• Homomya sp.
• Homomya ovalisTroedsson (1951)-p188
• Homomya venulithusTroedsson (1951)-p189
• Homomya centralisTroedsson (1951)-p191
• Homomya librataTroedsson (1951)-p192
• Isognomon sp. Troedsson (1951)-p207
• Leda sp.
• Liastrea hisingeriTroedsson (1951)-p225
• Lima duplicata
• Lima pectinoidesTroedsson (1951)-p208
• Limea acuticostataTroedsson (1951)-p210
• Limea katsloesensis
• Liogryphaea sp.
• Liogryphaea arcuataTroedsson (1951)-p226
• Liogryphaea lataTroedsson (1951)-p227
• Lioqryphaea regularisTroedsson (1951)-p228
• Modiola hillana
• Modiola ruuthiTroedsson (1951)-p231
• Modiola cf. tenuissimaTroedsson (1951)-p232
• Modiola scalprum
• Myoconcha decorataTroedsson (1951)-p234
• Mytilus cf. lamellosusTroedsson (1951)-p233
• Nucula sp.
• Nucula distinguendaTroedsson (1951)-p154
• Nuculana sp.
• Nuculana zieteni
• Nuculana dorisTroedsson (1951)-p152
• Oxytoma sinemurensis
• Oxytoma inaequivalvisTroedsson (1951)-p200
• Oxytoma scanica
• Palaeoneilo sp.
• Palaeoneilo galateaTroedsson (1951)-p149
• Palaeoneilo bornholmiensisTroedsson (1951)-p150
• Palaeoneilo oviformisTroedsson (1951)-p151
• Plagiostoma succincta
• Platymya aquarumTroedsson (1951)-p187
• Pleuromya sp.
• Pleuromya forchhammeri
• Pleuromya corrugataTroedsson (1951)-p194
• Plicatula spinosa
• Plicatula orbiculoidesTroedsson (1951)-p221
• Protocardia philippiana
• Protocardia oxynoti
• Protocardia truncataTroedsson (1951)-p179
• Pseudopecten aequivalvisTroedsson (1951)-p219
• Pseudopis sp.
• Rollieria sp.
• Rollieria bronniTroedsson (1951)-p153
• Sphaeriola kurremolinaeTroedsson (1951)-p178
• Taeniodon nathorsti
• Tancredia arenacea
• Tancredia securiformisTroedsson (1951)-p175
• Tancredia erdmanniTroedsson (1951)-p176
• Tancredia johnstrupi
• Tancredia lineataTroedsson (1951)-p177
• Terquemia arietisTroedsson (1951)-p223
• Trigonia primaevaTroedsson (1951)-p165
• Trigonia modestaTroedsson (1951)-p166
• Tutcheria cingulataTroedsson (1951)-p172
• Tutcheria cf. rickardsoniTroedsson (1951)-p173

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• Actaeonina nathorstiTroedsson (1951)-p238-240
• Actaeonina cf. striata
• Chemnitzia sp.
• Chrysostoma cf. solarium
• Kalchreuthia frankeiWeitschat & Gründel (2002)-p40
• Ptychomphalus cf. expansus
• Trochus cf. imbricatus
• Trochus laevis

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• Baltodentalium weitschatiEngeser & Riedel (1992)-p49-50
• "Dentalium" hexagonale
• Laevidentalium elongatumTroedsson (1951)-p230-245
• Laevidentalium sp.Engeser & Riedel (1992)-p46
• Prodentalium bandeliEngeser & Riedel (1992)-p43
• Progadilina spaethiEngeser & Riedel (1992)-p47
• Progadilina subtrigonalisEngeser & Riedel (1992)-p48

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• Kuqaia scanicusPeng, Slater, McLoughlin & Vajda, (2023)-p4-20

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• Astacolus denticulina carinata
• Brizalina liassica amalthea
• Citharina inaequistriata
• Cristacythere crassireticulata
• Marginulina spinata spinata
• Nanacythere simplex
• Ogmoconchella danica
• Ogmoconchella mouhersensis
• Ogmoconchella adenticulata
• Ogmoconcha amalthei amalthei
• Pleurifera harpa

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• Hydrozetes nsp.Sivhed & Wallwork (1978)-p65-66

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• Chondrites sp.Frandsen & Surlyk, 2003, p.546
• Diplocraterion sp.
• Planolites sp.
• Rhizocorallium sp.
• Skolithos sp.
• Teichichnus sp.

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Apart from a few teeth of the hybodont Hybodus reticulatus, the shark fauna from the Rya Formation is exclusively neoselachian.Rees, 2000, p.411

{{Paleobiota-key-compact}}

Coalified wood occurs as scattered pieces up to {{convert|6|cm|in}} long and indeterminate belemnites, echinoids, serpulids, ostracods and nodosariid foraminifera were also recorded in the formation.Frandsen & Surlyk, 2003, p.547

Ammonites where found on layers with plant fossils. Fragments of Dactylioceras were found at a depth of 170 m in the Vilhelmsfalt borehole, together with plant remains and

beautifully preserved Pelecypods.Reyment (1959)-p152 The plant material, probably derived from watercourses emptying in the neighborhood, consists mostly of small fragments that seem to have been intimately sedimented with the muddy material that flocculated on meeting the seawater. Other specimen, Arnioceras sp. indet. occurs on what appears to be a transitional environment, probably a back-beach with coalified fragments of plants, some of a large size. Probably due to the shell being washed to land due to a storm.

• List of fossiliferous stratigraphic units in Sweden
• Kristianstad Basin
• Toarcian formations

{{div col|colwidth=25em}}

• Djupadal Formation, Central Skane
• Marne di Monte Serrone, Italy
• Calcare di Sogno, Italy
• Mizur Formation, North Caucasus
• Sachrang Formation, Austria
• Saubach Formation, Austria
• Posidonia Shale, Lagerstätte in Germany
• Ciechocinek Formation, Germany and Poland
• Krempachy Marl Formation, Poland and Slovakia
• Lava Formation, Lithuania

{{div col end}}

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{{commons category-inline|Rya Formation}}

{{Mesozoic Sweden|state=expanded}}

Category:Geologic formations of Denmark

Category:Geologic formations of Sweden

Category:Jurassic System of Europe

Category:Early Jurassic Europe

Category:Middle Jurassic Europe

Category:Jurassic Denmark

Category:Jurassic Sweden

Category:Sinemurian Stage

Category:Pliensbachian Stage

Category:Toarcian Stage

Category:Aalenian Stage

Category:Siltstone formations

Category:Shale formations

Category:Sandstone formations

Category:Mudstone formations

Category:Coal formations

Category:Coal in Sweden

Category:Open marine deposits

Category:Shallow marine deposits

Category:Paleontology in Sweden

Formations

Category:Denmark–Sweden border