The La Forestal section includes part of the fossiliferous marly-limestone of the Member 2 of Alonso-Chaves et al. (2004). There are three parts differentiated according to the sedimentary structures and the presence of trace fossils and macroinvertebrates (Figs. 4 and 5). Limestones dominate over marly layers (Figs. 3 and 4) and a general trend toward increasing carbonate content is recognisable throughout the section (Fig. 3).

The lower five meters of the studied interval consists of an alternance of laminated marls and limestones (Figs. 3, 4A, B). The limestone intervals are thin bedded (5 to 15 cm thick) and made up of a mudstone with usually well-preserved lamination, mainly at the base of the beds (Fig. 4F, 6A, B) and trace fossils toward the top (Fig. 6C). Some layers are wackestones (locally packstones) including fragments of thin-shelled bivalves, gastropods and recrystallised benthic foraminifera such as in the bed LF-1 (Fig. 6D). The beds composing LF-2 display well-developed lamination is in (Fig. 3). Marly beds have a characteristic yellowish to pink colour (Fig. 4A, B). The top of some beds is rich in lumps and moulds of small bivalves (Fig. 5), and secondarily coal remains (< 2 cm). Trace fossils at the lower part of the studied section are scarce, only Rhizocorallium is locally present in limestone beds of LF-5. The upper part of this stratigraphic interval ends in a thick carbonate bed (LF-6) with some layers characterised by ferruginous tops with common bivalves and unbranched horizontal trace fossils with irregular meandering corresponding to Helminthopsis.

The second part of the section (5.7 m thick) has an increased carbonate content, abundant trace fossils, and benthic macroinvertebrates (Fig. 3, 4C). This interval consists of two thickening-upwards sequences of around 250 cm each, composed of thin-bedded limestones (5-10 cm thick) changing upward into thick limestone beds (70 cm and 80 cm thick in each sequence, LF-8 and LF-10 in Figure 2). The thin-bedded limestones at the base are laminated mudstone in contrast with the thick beds at top, which are densely bioturbated (Helminthopsis and secondarily Thalassinoides) wackestone rich in fossil bivalves (Fig. 5A, B). Among the thin-bedded limestones, thin marly layers occur. The thick limestone beds are highly bioturbated (Helminthopsis) and the top is rich in bivalves and iron oxides (Fig. 5C, D).

The third stratigraphic interval (6.6 m thick) contains non-laminated limestones with abundant trace fossils, bivalves, and common iron oxides at bed tops (Fig. 5E, F). Marly layers are very scarce. Most of the interval is a thin-bedded mudstone with intercalated bioclastic packstone layers with erosive bases (Fig. 6E and F). Bivalves are the main component of the bioclastic packstone. The top of the section consists of several fine-breccia layers with abundant intraclasts corresponding to fragmented (re-elaborated) trace fossils.

Fossils in the study section are mainly bivalves belonging to Pseudocorbula gregaria, Costatoria sp., Limea sp., Homomya sp., Pseudoplacunopsis flabellum, Unionites sp. and Umbostrea sp., and small moulds of gastropods (Fig. 5). The species Pseudocorbula gregaria is dominant. A fragment of an indeterminate small ammonite was also recorded (bed LF-10). Small gastropods and echinoderms are recognisable in thin section. Costatoria and Unionites are preserved as recrystallized shells. Pseudocorbula gregaria appears at the top of some levels as dense accumulations mainly preserved as inner moulds (Fig. 5B).

A long curved fossil bone, corresponding to a dorsal rib of a sauropterygian, occur in the bed LF-13 at the lower part of the third stratigraphic interval. The bone occurred at the top of a horizon with Helminthopsis. It is well preserved without evidence of original fragmentation, borings, or encrustations. This rib is 14.98 cm long and the width varies from 9.7 to 24.1 mm (Fig. 7), with the thickest section in the distal region. The rib presents relative pachyostosis related to the compactness of the bone and the strong distal expansion. A thin neck (9.7 mm in diameter) with a low ridge in the dorsal side connects the rib head (proximal region). The head of the rib is swollen and shows a concave facet of articulation with vertebrae. The posterior third of the rib is slightly curved close to the position of the vertebrae. The internal surface is flat (ventrally flat, Fig. 7A) and the external surface of the rib is convex (dorsally convex, Fig. 7B), both striate to the distal region. The convexity increases to the proximal region in relation to the presence of a low ridge with a progressive development of triangular and finally pseudo-pentagonal cross-section (Fig. 7C).

The laminated mudstones at the lower part of the section were deposited in a shallow environment, sometimes densely colonised by tracemakers doing subhorizontal burrows corresponding to Helminthopsis (less commonly to Thalassinoides). Helminthopsis was interpreted as grazing trails produced by deposit feeders, probably polychaetes (Bromley, 1996) that proliferated when sedimentation rate was reduced. The dense concentration and the small size of these trace fossils indicate large populations of tracemakers, and most likely an opportunistic behaviour. In addition, the dense concentration could depend on the time available for colonization the bottom. The recorded trace fossils commonly occur in yellowish horizons resembling omission surfaces. The local record of Rhizocorallium indicates reduced sediment input and omission-surface and firmground development (e.g., Cotillon et al., 2000; Worsley & Mørk, 2001; Rodríguez-Tovar et al., 2007; Reolid et al., 2014b). The presence of pebbly mudstones at bed tops is related to reworking that are associated to high-energy processes.

The base of the second interval (Fig. 3) is characterised by the record of laminated limestones with tops densely colonised by small subhorizontal trace fossils of Helminthopsis (and scarce Thalassinoides), indicating the opportunist colonization of the bottom when sedimentation rate decreased. The elementary sequences clearly display an upward increase in carbonate content and with densely burrowed tops that may represent gradual changes in the consistence of the substrate. The preservation of the burrows is an indicator of substrate consistence (Taylor et al., 2003), and consequently facilitates reconstruction of the sedimentation rate or depositional breaks. The record of horizons rich in trace fossils and iron oxides represents the transition from softground to firmground conditions. The tops of the elementary sequences with high concentrations of Pseudocorbula indicate a colonization of very shallow softground by infauna and the subsequent colonization of firmground (or hardground) by sessil epifauna.

The sedimentary features such as lamination are indicative of a shallow intertidal to subtidal environment whereas the densely bioturbated levels distinctive of subtidal to offshore facies. The sequences, of decimetric scale within beds and also of metric scale in thickening upward sequences, beginning with laminated limestones, followed by bioturbated limestones and occasionally finishing with fossiliferous horizons with iron oxides can be interpreted as deepening upward sequences (Fig. 3). The tops of these sequences are indicative omission surfaces or a hardgrounds, which include fragmentation and reworking of burrows resulting as lumps. These features resemble the flat-pebble breccias, typical product of storms in tidal carbonate areas. Assuming that subaerial early diagenetic processes were not responsible for lithification of the carbonate layers, the submarine early cementation driving to hardground formations was a necessary step in the origin of flat-pebbles included fragments of Helminthopsis. The reworking of these early cemented horizons was the source of flat-pebbles (Myrow et al., 2004). The flat-pebbles have been typically described from Palaeozoic, but also from Triassic (Wignall & Twitchett, 1999). The studied succession is constituted by typical sequences of Lofer cyclothems in the sense of Fischer (1964) that indicate deepening sequences from intertidal to subtidal in each sequence (Goldhammer et al., 1990; Satterley & Brandner, 1995). However, some type cycles of Lofer cyclothems have been reinterpreted as shoaling upward (Enos & Samankassou, 1998; Cozzi et al., 2005).

The bivalve association is similar to that of the Muschelkalk of the Iberian Ranges in the Landete Formation, Mediterranean Triassic domain, and at the base of the Cañete Formation, Levantine-Balearic Triassic domain (Escudero-Mozo et al., 2015). This association corresponds to the Sephardic Bioprovince that colonised the westernmost palaeogeographic regions of the Tethys (Márquez-Aliaga et al., 1986; Pérez-López et al., 1991), which currently constitute the Subbetic and Prebetic domains. This assemblage also colonised many areas of the Alpujarride Domain (López-Garrido et al., 1997). The association (Pseudocorbula, Costatoria, Limea, Homomya, Pseudoplacunopsis and Unionites) is characterised by low diversity and is often composed of dominant cosmopolitan specimens in the Alpine/Germanic facies (Palaeotethys) related to shallow and/or restricted environments. Senkowiczowa (1985) interpreted these cosmopolitan species as related to muddy bottoms, which is congruent with their occurrence in mudstones in La Forestal section. These genera of bivalves were pioneer taxa and probably lived under stressful environmental conditions (Escudero-Mozo et al., 2015). Unionites is indicative to marine and brackish waters (Márquez-Aliaga et al., 1986; Reolid & Reolid, 2017). The bivalve assemblage is consistent with the stressful conditions related to the tidal environment.

The proposed sedimentary environment is congruent with the habitat of marine reptiles such as basal sauropterygians, however during the Late Triassic some sauropterygians were adapted to pelagic environments. From the taphonomic point of view, the record of an isolated but well-preserved rib of a nothosaur is probably due to decoupling and transport of bones. The good preservation indicates short transport distances, para-autochthonous remain. In addition, there are not taphonomic features that evidence the activity of scavengers or long exposition on the sea-bottom before burial (such as potential record of borings or encrustations by sessile benthic organisms on the bone).

The features of the rib (the compactness of the bone, the distal expansion of the rib and the rib head connected by a thin neck with a low ridge in the dorsal side, slightly curved in its posterior third, among other features) indicate this corresponds to Eosauropterygia. Placodontia are excluded because they are not pachyostotic in the dorsal ribs (see more details of ribs of Placodontia in Diedrich, 2010; Klein & Scheyer, 2014; Klein et al., 2019). In the case of Paraplacodus, this is also excluded due to dorsal ribs of this genus present posteriorly directed uncinated processes (Klein & Sichelschmidt, 2014). In addition, placodontids do not have the characteristic distal expansion of the rib here described and a thin neck does not connect the rib head. However, the striated distal end resemble the dorsal rib of Pararcus diependroeki of the Muschelkalk of Netherland (Klein & Scheyer, 2014). Pachypleurosauria are also excluded because they do not present a rib morphology similar to the studied fossil remain and they are small-size sauropterygians (e.g. Rieppel, 2019).

Comparison of distal region of the rib with the same costal interval in typical Nothosauroidea such as Nothosaurus and Lariosaurus evidences that these genera maintain a more constant narrow diameter than the studied specimen does. The shape of the rib, with distal expansion, also resemble those of Paludidraco multidentatus a simosaurid recorded in the Upper Triassic of Central Spain (Miguel Chaves et al., 2018). The holotype exposed in the Museo de Paleontología de Castilla-La Mancha (Spain) shows a relatively constricted proximal region versus a strongly robust and expanded distal with relative degree of pachyostosis. In addition, the size proportions of the dorsal ribs of the Paludidraco holotype are within the size of the studied fossil rib.

The comparison with different genera of eosauropterygians (mainly Nothosauroidea such as Lariosaurus, Nothosaurus, “Paranothosaurus”, Simosaurus and Paludidraco, see Rieppel, 2000; Diedrich, 2012; Miguel Chaves et al., 2018) allow us for interpreting a total length of the specimen between 2.5 and 3.2 m, according to the length of the studied rib. The genus Lariosaurus is relatively common in some areas of the western shoreline of the Tethys with Alpine facies, for example in the Besano Formation (Southern Alps of Switzerland and Italy; see Rieppel, 2019). However, the recorded rib does not belong to Lariosaurus, a small-size Eosauropterygian with absence of the distal expansion. The estimated length are indicative of Nothosaurus, “Paranothosaurus”, and Simosaurus, but according to the morphology of the studied rib, the simosaurid Paludidraco seems to be a plausible candidate. However, only with an isolated rib, the reptile can exclusively be assigned to an indeterminate member large-size Eosauropterygian.

The occurrence of sauropterygians in the Member 2 of the Lújar Unit of the Alpujarride Complex (Fossiliferous marly-limestone Member) can be considered as the equivalent in the Alpine facies of the record of sauropterygians in Ladinian Muschelkalk facies of the External Zones of the Betic Cordillera, (e.g. Niemeyer, 2002). The record of marine reptiles in Triassic marine sediments of Europe is diverse and abundant in the Germanic Basin as well as in the Alpine Triassic (Rieppel, 2000; Motani, 2009; Diedrich, 2012). Along the Iberian palaeomargin, with Germanic facies, the record of marine reptiles is relatively rich but most of the reported remains consist of isolated elements, commonly reworked (see Sanz, 1976, 1983a, b; Alafont, 1992; Fortuny et al., 2011; Miguel Chaves et al., 2015, 2016, 2017; Márquez-Aliaga et al., 2019). The marine reptile fauna of northeastern Iberia includes diverse Sauropterygia with the nothosaur Lariosaurus balsami being the most common (Sanz et al., 1993; Rieppel & Hagdorn, 1998). In the south-eastern Iberian Palaeomargin, including the Tabular Cover and the External Zones of the Betic Cordillera, marine reptiles are represented by the nothosaurians Nothosaurus, Simosaurus, and Lariosaurus, by the placodonts Psephosaurus and Henodus, and by the Protorosauria Tanystropheus (Niemeyer, 2002, Reolid et al., 2014a). Those sauropterygian are the geographically nearer to the specimen studied in this work, but the south Iberian Palaeomargin and the Mesomediterranean Massif palaeomargin were separated by a marine corridor (Fig. 1). This fact gives relevance to this first record from a different palaeogeographic area, being the first record of a saurpterygian in the Alpine Domain of SE Spain.