[18] The first fossils, mostly ammonites (that allowed a more precise datation) and insects where recovered in 1894, where Geinitz related the local finds with the southern liassic shales that he studied at the same time, yet he was surprised about the abundance of phyllopods and coeloptera elytrons in the sediments, suggesting a more freshwater/terrestrial influence.

It also does the first comparation with the slightly younger Seria borucicka (Borurice Beds), and estimate that the rocks were approximately of Late Liassic in age, with the possibility of finding Dogger Sediments on the uppermost parts.

[22] Later works use the name Ciechocinek Series for the Polish Basin sediments, doing studies about sedimentology on the layers already Drilled, or founding new Boreholes with similar composition of Kaolinite and related materials.

[17] The Dobbertin pit however, has been under protection as a geological natural monument since 1991, as the exposed layers are considered an exceptional land–sea facies distribution during the Toarcian and also its international fame, due to its wealth of fossils from the northern margin of Fennoscandia.

[33] The most clear hint link this deposits with the Ciechocinek Fm, as they're identical in fauna and facies composition of Grimmen and Dobbertin, also affected by subglacial erosion and thrusting, suggesting a close stratigraphic and palaeogeographical origin.

[36] There is also a high content and proportion of unstable heavy minerals (pyrolusite, manganite, birnessite, todorokite and rhodochrosite) in the Toarcian clays, that indicate basaltic volcanism sediments, translated probably from nearest inland strata, such as the coeval Djupadal Formation.

This is seen as, after the increased amount of clays with abundant volcanic materials, sands were repeatedly poured into the North German Basin from Skåne, as result of the erosion of the Höör sandstone.

[39] The presence of kaolinite, related to continental formation in tropical climate environments for the chemical weathering of different igneous, metamorphic and sedimentary rocks, along with chlorite and biotite, suggest a deposition linked to fluvial and deltaic forces.

[39] The basal layers of the unit are overlaying the latest Pliensbachian local exposures, that is composed mostly by coarse to fine grey and green sands and sandstones, derived from a marginal marine setting, with echinoderms and abundance of stenohaline fauna.

[44] On the Warszawa IG-1 Borehole and Stara Iwiczna drill cores the subunit appears at 1,639.3 - 1,738.9 m, and is composed by green-gray mudstone, sandstones, mules[clarification needed] and clayey interlining, sometimes laminated, gray and mottled, where the limit between the Lower Toarcian and the Middle Jurassic isn't clear.

[50] Distal settings show the influence of the storms with due to the presence of several laminated deposition of sand-silt streaks, cross-laminated silt, small sand lenses and interlaid mud-silt-sand heteroliths.

[50] The main component of the deposits are muds, intercalated sandstones and silts disposed on a high variety of structures, with at least twelve lithofacies that run from fine-grained sedimentation to wave-dominated sandy shoals.

[51] It contains several marine dinoflagellate cysts, Foraminiferal linings and a relatively di verse trace fossil, such as Planolites, Palaeophycus, Helminthopsis, Gyrochorte, Protovirgularia, Spongeliomorpha and Diplocraterion associated with pyrite mineralization.

Gray-yellow Sandstone, horizontal layering, tabular and wrinkle diagonals, bottom 50 cm carbonate binder (dolomitic), followed by 2.0 m of gray-green mudstone, lenticular lamination, siderite concretions.

[53] Kaolinite varieties that can be made into ceramic raw materials can only be expected locally in regions where its content was additionally increased as a result of erosion and re-sedimentation of older (Pliensbachian specially) weathered covers.

[53] Due to the lower Toarcian global warming and dampening the climate enrichment with kaolinite was commonly seen in the upper part of the formation, but the periodic increase in progression had caused these deposits to left only silt and sandy heteroliths.

[56] This zone has more developed aquatic conditions with a marked marine influence, where the presence of a river coming from Czech Republic, as the organic matter that was translated to the shore was more probably derived from thermally mature sediments, Carboniferous strata present on the eastern margin of the massif.

[56] In the Polish basin, it has recently been found (based on studies of phytoclasts in terrigenous material) sharp negative anomalies (CIE) on the 13C curves, attesting to further episodes of gradually increasing warming.

[61] In the middle part of the Ciechocinek Formation, as exposure of the abundant amount of saolinite shows that was developed as a result of intense humidity of the environments, with the increasing presence of several fossils and minerals on the strata outside the measurements of the iron precipitation.

[63][64] The organic matter found includes the oldest known biomolecules (labdanoic acid, ferruginol, sugiol and 7-oxototarol) from the "Blanowice brown coals", which probe the presence of abundant wildfires and/or peat fires on the formation, with the Cupressaceae and/or Podocarpaceae families the main peat-forming plant species.

[67] The presence of abundant spores is related to palaeoclimatic factors, as sediments show that the climate at that time was much warmer and much more humid (with a small exception on the Tenuicostatum biochronozone) than in the Hettangian-Pliensbachian interval.

[67] These finds are related with the pollen and plant remains found on the Chinese Hsiangchi Formation (Also Toarcian), pointing to a warm and humid climate, that changed after to a drier conditions, as observed on the Quaidam Basin.

[4] The uppermost section, referred to me Bifrons-Thoaurense zone is composed by fine-grained sand with clay streaks, deposited very likely on a growing deltaic system, as plant remains increase dramatically, which probes a decrease of the nearby marine water depths with a progadation of the delta front coming from the north, from the Fennoscandian mainland.

[6] In a wider palaeogeographical scope, sediment and terrestrial biota clearly originate from the southern margin of Fennoscandia, where the eroding rim of the crystalline Proterozoic craton delivered large amounts of material.

The clay dominated settings of the Ciechocinek Formation were deposited on a restricted basin, with absence of major ripples and wavy undulation that discards the influence of wave action.

[29] This palynological record matches with the data of the sister Sorthat Formation Toarcian levels, where Spheripollenites comprises the 95% of the palynoflora, along the cheirolepidaceous cuticle Dactyletrophyllum ramonensis and the peak of the Pagiophyllum leaves, indicators of semidesertic to Mediterranean climates, implying an abrupt warming event.

[11] The North German Basin shows that on approximately 14.4 m.a, four third-order relative sea-level fluctuations led the subsequent formation of four individual delta generations in the Bifrons-Thouarsense (Toarcian), Murchisonae-Bradfordensis (Aalenian) and Humpresianum-Garatiana (Bajocian).

[11] On the lower delta plain lithofacies plant detritus and wood debris are very common, deposited probably on interdistributary bays formed embayments, thanks to overbank flooding from near distributaries, that covered approx.

[72][8] On the Polish realm the fauna is represented by Conchostracans, rare Foraminifera and scarce Ostracoda as the main components, with occasional undetermined bivalves, gastropods and fish teeth and scales.

[78] These layers are abundant in ichnospecies of invertebrate fauna, including mostly marine organisms, such as Planolites (Worm-like animals), Palaeophycus (Polychaeta), Protovirgularia (Nuculoidea) and Spongeliomorpha (Decapoda).