Tremp Formation

Tremp Formation
Ma PreꞒ Ꞓ O S D C P T J K Pg N
Approximate paleocoordinates		34°06′N 0°54′E / 34.1°N 0.9°E / 34.1; 0.9
Outline of the Tremp Formation in the Tremp Basin

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Type locality of the Tremp Formation in Spain

The Tremp Formation (

Shortly after deposition of the Tremp Formation, the Boixols Thrust, active to the north of the Tremp Basin and represented by the Sant Corneli anticline, started a phase of tectonic inversion, placing upper Santonian rocks on top of the northern Tremp Formation. The main phase of movement of another major thrust fault, the Montsec to the south of the Tremp Basin, happened not before the Early Eocene. Subsequently, the western Tremp Basin was covered by thick layers of conglomerates, creating a purely continental foreland basin, a trend observed going westward in the neighboring foreland basins of Ainsa and Jaca.

A rich and diverse assemblage of fossils has been reported from the formation, among which more than 1000

The Tremp Formation was defined and named in 1968 by Mey et al., just as the Tremp Basin after the Pre-Pyrenean town of Tremp.^[7] The various subdivisions of the formation or alternatively called group, are named after the villages, rivers, canyons and hills in the basin.^[8][9]

Description

The Tremp Formation is a marginally marine to

The formation comprises several different lithologies, as sandstones, shales, limestones, marls, lignites, gypsum beds, conglomerates and siltstones have been registered.^[12][18]

The start age of the Tremp Formation has been established on the basis of the presence of Abathomphalus mayaroensis, a planktonic foraminiferan indicative of the latest Maastrichtian age of the formation.^[19] The lower section of the formation at the Elías site has been dated at 67.6 Ma,^[20] while the top of the Tremp Formation, in the western portion of the basin overlain by the Alveolina Limestone,^[21] named due to the abundance of Alveolina, is set at 56 Ma.^[22]

On the northern side of the Axial Zone of the Pyrenees, in the French sub-Pyrenean zone and Aquitaine Platform of the foreland basin bordering the mountain range, the time-equivalent stratigraphic units of the Tremp Formation are the Mas d'Azil Formation and Marnes d'Auzas Formation for the latest Maastrichtian, the Entonnoir Formation for the Danian and the Rieubach Group correlating with the Thanetian portion of the Tremp Formation.^[23]

Subdivisions

Studies performed in the 1990s described the Tremp Formation, also called Garumnian (Spanish: Garumniense de Tremp),^[24][25] as a group with a subdivision into:^[12]

Claret Formation

• Etymology - Claret
• Type section - along the road 1311^[26]
• Thickness - up to 350 metres (1,150 ft)
• Lithologies - ochre to red shales, gypsum beds and intercalated sandstones and conglomerates
• Depositional environment - transitional marine to continental

La Guixera Member

• Etymology - La Guixera
• Type section - Mongai^[26]
• Thickness - 60 to 350 metres (200 to 1,150 ft)
• Lithologies - gypsum beds alternating with shales, sandstones and conglomerates
• Depositional environment - evaporitic lacustrine deposits at times of retrogradation of alluvial fans^[27]

Esplugafreda Formation

• Etymology - Esplugafreda canyon
• Type section - Barranco de Esplugafreda, in the valley of the Ribagorçana River east of Areny de Noguera^[9]
• Thickness - 70 to 350 metres (230 to 1,150 ft)
• Lithologies - continental red beds; shales, sandstones and conglomerates
• Depositional environment - alluvial fans

Sant Salvador de Toló Formation

• Etymology - Sant Salvador de Toló
• Type section - Conquès River^[9]
• Thickness - 70 to 350 metres (230 to 1,150 ft)
• Lithologies - micritic limestones and greenish shales
• Depositional environment - lacustrine to coastal

Talarn Formation

• Etymology - Talarn
• Type section - Barranco de La Mata^[28]
• Thickness - 140 metres (460 ft)
• Lithologies - fining-upward sequence of sandstones and conglomerates at the base, grading into siltstones and shales near the top
• Depositional environment - alluvial channel and overbank deposits

Conquès Formation

• Etymology - Conquès River
• Type section - Barranco de Basturs^[8]
• Thickness - 60 to 500 metres (200 to 1,640 ft)
• Lithologies - greenish shales, sandstone lenses and conglomerates at the base
• Depositional environment - perilagoonal^{[note 1]}

Tossal d'Obà Member

• Etymology - Tossal d'Obà
• Type section - Tossal d'Obà Hill^[8]
• Thickness - 7 metres (23 ft)
• Lithologies - micritic limestones and marls
• Depositional environment - distal fluvial to lagoonal-barrier island

Basturs Member

• Etymology - Basturs
• Type section - Barranco de Basturs^[8]
• Thickness - 2.5 to 80 metres (8.2 to 262.5 ft)
• Lithologies - micritic limestones, greenish shales and bioturbated fine sandstones
• Depositional environment - perilagoonal

Posa Formation

• Etymology - Ermita La Posa^[30]
• Type section - Isona anticlinal^[31]
• Thickness - 180 metres (590 ft)
• Lithologies - grey shales, limestones, marls, lignite and sandstones
• Depositional environment - lagoonal to barrier island

Alternative subdivisions

An alternative subdivision uses Grey Garumnian at the base, overlain by Lower Red Garumnian and Vallcebre Limestone at the top.^[32] The Vallcebre limestone is laterally equivalent with another described unit, the Suterranya Limestone.^[33] Pujalte and Schmitz in 2005 defined another member, the Claret Conglomerate, as representative of a conglomeratic bed inside the Claret Formation.^[2]

In 2015, a new unit was allocated to the uppermost Cretaceous section of the Tremp Group, near the top of the Lower Red Garumnian. The 7 metres (23 ft) thick series of lithologically mature coarse-grained sandstones and microconglomerates rich in feldspars is positioned 7 to 10 metres (23 to 33 ft) below the Danian Vallcebre Limestone and was called the Reptile Sandstone.^[34]

Tectonic evolution

The Tremp Basin was formed in the northeastern corner of the

Approximately from the late Berriasian to late Albian (120 to 100 Ma), the Iberian Plate was an isolated island, separated from current southern France by a mostly shallow sea with a deeper pelagic channel in between the southwestern Eurasian and northeastern Iberian coasts. The present-day area of the Pyrenees with an area of 1,964 square kilometres (758 sq mi) in those times was much larger due to the various episodes of compressional tectonic forces and resulting shortening afterwards. The Tremp Basin, alternatively called Organyà Basin, was the depocenter of sedimentation during the late Early Cretaceous, showing an estimated vertical sedimentary thickness of 4,650 metres (15,260 ft) comprising mostly hemipelagic marls and limestones,^[40] deposited in a back-arc basin setting with normal faults parallel to the Pyrenean axis,^[41] and cross-cut by transverse faults, separating the various west-to-east minibasins. These minibasins showed a deepening trend from the Gulf of Biscay to the Mediterranean.^[36][42][43]

At the end of formation of the back-arc basin, around 95 Ma, high temperature

From the late Santonian to the late Maastrichtian,[53] on the different thrust sheets of the southward compressional Pre-Pyrenees, a series of piggyback basins were formed,^[54] one of which was the Tremp Basin.^[55] The bathymetry of these basins show a general deepening towards the west, with major turbidite deposition in the Ainsa Basin and farther west.^[53] Subsequent ongoing inversion of the basins show a similar trend, with compressional phases becoming younger from east to west. While the onlap and erosion in the Clamosa area started in the early Eocene, around 49 Ma, the western portion experienced this phase terminating around the end of the Eocene, approximately at 35 Ma.^[56] In the Jaca Basin, to the west of the Ainsa and Tremp Basins, during the Middle Eocene, flysch was deposited in an underfilled basin setting,^[57] while in the western Tremp Basin thick conglomerates, known as the Collegats Formation, were deposited, sourced by the various thrust sheets in the hinterland.^[58]

Boixols and Montsec thrusting

The Boixols–Cotiella thrust sheet was emplaced since the Late Cretaceous, placing late Santonian rocks on top of the northernmost Tremp Formation, found in the subsurface underneath the Sant Corneli anticline. This was followed by the tectonic movement of the Montsec–Peña Montañesa thrust sheet during the Early Eocene and the western Sierras Exteriores thrust sheet from the Mid-Eocene to Early Miocene.^[59] The dating of the Montsec Thrust has been established on the basis of the stratigraphies of the overlying hanging wall (Triassic to Cretaceous) onto the Lutetian (locally called Cuisian) fluvial sediments of the Àger Basin to the south of the Montsec.^[60][61] These tectonic movements are indicative of the main uplift phase of the Pyrenees.^[36]

Salt tectonics

The involvement of evaporites as décollement surfaces in compressional tectonic regimes is a widespread phenomenon on Earth. The evaporites, mainly

In the western Cotiella Basin, salt inflation and withdrawal played a major role in the differential sedimentary thicknesses, facies changes and tectonic movements.[76]

Eocene to recent

After the Middle Eocene, thick conglomerates were deposited in the western Tremp Basin and the thrust sheets reached their maximum displacement, this led to a shift of the depocenter from the Pre-Pyrenees towards the Ebro Basin.^[77] Paleomagnetic data show that the Iberian Plate went through another phase of counterclockwise rotation, though not as fast as in the Santonian. Between 25 and 20 Ma, in the late Oligocene and early Miocene, a rotation of 7 degrees has been noted.^[78] This phase of rotation correlated with the thrusting in the westernmost areas of the southern Pre-Pyrenees, the Sierras Marginales, leading to continental conditions in that area from the early Miocene (Burdigalian) onwards.^[79]

Depositional history

The

Four phases in the depositional history of the Tremp Formation are noted:[82]

1. Formation of an estuarine regime near the end of a Cretaceous
   regression
   in the Pyrenean basins, characterized by coastal plains where thick clays were deposited, cut by sporadic fluvial channels. At the margins of the basin, swampy conditions existed with sedimentation of carbonates. In these zones, the last dinosaurs inhabiting the area before the Cretaceous-Paleogene boundary left their marks in tracks, eggs and bones. These areas were accompanied by marshes, as evidenced by the many plant remains that produced the lignite deposits found in the lower part of the Tremp Formation. During this first phase in the sedimentary sequence of the formation, the Montsec was already a slightly elevated area in the south and along the submerged slopes of that hill, lacustrine limestones were deposited.
2. At the end of the Cretaceous, a geologically sudden drop of sea level happened, giving rise to a wide fluvial-dominated basin. In this environment, river channels deposited sandstones and abundant overbank clays with numerous paleosols in the basin. On the southern side of the rising Montsec, the Àger Basin, a similar fluvial system developed with a far more coarse-grained sandy character than in its northern counterpart around Tremp. The paleocurrents in the Àger Basin were towards the north and northwest.^[83] The enclosed continental basin turned into a more coastal environment at a transgressional phase with smaller channels where oncolites were laid down. The river systems on both sides of the Montsec were sourced by the easternmost parts of the present Pyrenees, with the Empordà High as provenance area. This east-to-west fluvial system, contrary to the present-day west–east flowing direction of the Ebro Basin, persisted until the Late Eocene. The uppermost unit of the Maastrichtian sequence, the coarse-grained Reptile Sandstone, has been interpreted as a fast-flowing braided river channel.^[34]
3. The start of the Paleocene was marked by a more tranquil deposition of lacustrine character. It has been hypothesized that the Alpine orogeny during this phase was less active and/or a regional rise in sea level allowed the basin to be flooded. During this phase, the limestones of Vallcebre and its lateral equivalents were deposited in the lake.
4. A renewed phase of tectonic activity reactivated the fluvial to alluvial sedimentation, with abundant conglomerates and conglomeratic sandstones as a result. The provenance area for these uppermost sections of the Tremp Formation were first interpreted as the presently high mountains of the Axial Zone of the Pyrenees, at that time a forming orogen. Detailed provenance analysis published in 2015 by Gómez et al. however shows that the Àger basin was fed from the south (Prades area) and the Cadí-Vallcebre area was fed from the southeast (Montseny area), both areas belonging to the Ebro Massif. The Pyrenean basement (Axial Zone) was not a source area during the sedimentation of the Tremp Formation.^[84] The latest phase of depositional evolution is noted in a wider area in the Pre-Pyrenees and to the south in the Ebro Basin, that began its formation during the Eocene, building up to its present shape in Oligocene and Miocene times.

Cretaceous-Paleogene boundary

The Tremp Formation spans the latest stage of the

The Tremp Formation provided many fossilized dinosaur eggs.^[88] The dinosaur eggs of Basturs are contained in the formation bordering the Arén Formation and the area where eggs are found stretches out for 6,000 square metres (65,000 sq ft). A great number of nests are visible as well as numerous fragments of egg shells. The presence of wave ripples indicates a beach-like environment where dinosaurs laid their eggs for a long time. The eggs are subcircular with diameters of approximately 20 centimetres (7.9 in) and egg shell thicknesses between 1.5 and 2 millimetres (0.059 and 0.079 in). Many eggs are found in groups of between four and seven gatherings, indicating the in situ preservation of the nests.^[89]

Also, remains of several genera of dinosaurs are described from the Tremp Formation.

A detailed analysis of the nesting sites of Coll de Nargó, at the Pinyes locality, has been performed in 2010 by Vilat et al. The eggs were found in the lower portion of the Lower Red Garumnian, with local facies comprising calcareous silty mudstones, very fine to fine-grained sand bodies, and medium to coarse-grained sandstones. The rocks, in a 36 metres (118 ft) thick interval,^[100] are interpreted as sedimentary deposits of a fluvial environment located some distance away from an active stream channel.^[101]

Most eggs exposed at the Pinyes locality were incompletely preserved because of recent erosion; however, excavation occasionally revealed relatively intact specimens in the subsurface. Some eggs exposed in cross-section revealed numerous eggshell fragments, predominantly oriented concave up within the mudstone matrix that filled the egg interior. Analysis of the eggshells at Pinyes provided a range of 2.23 to 2.91 millimetres (0.088 to 0.115 in) in shell thickness, with a mean range of 2.40 to 2.67 millimetres (0.094 to 0.105 in). Radial thin sections and

The mudstones surrounding the eggs displayed extensive bioturbation, minor faults, and penetrative foliation with a northeast–southwest orientation. Eggshell fragments were often displaced and overlap one another, and the eggs exhibited significant deformation due to compression. Most eggs mapped in the field showed a long axis direction 044, thus having a general northeast–southwest orientation, which coincides with regional stress fields resulting from tectonic compression.^[102]

The eggs, in clusters or "clutches" of up to 28 individual eggs, were described as

An interpretation of the nest excavation at Pinyes was made and compared to other nesting sites of sauropods found all over the world, in particular in the

Sanpetru Formation of Hațeg paleo-island in Romania, the Los Llanos Formation at Sanagasta geological park [es] in Argentina, and the Boseong Formation of the Gyeongsang Basin in South Korea.^[105]

A common nest size of 25 eggs has been suggested for the Pinyes locality. Small egg clusters that display linear or grouped egg arrangements reported at Pinyes and other localities likely reflect recent erosion. The distinct clutch geometry reported at Pinyes and other megaloolithid localities worldwide, strongly suggests a common reproductive behavior that resulted from the use of the hind foot for scratch-digging during nest excavation.[106] Due to their size and weight, the titanosaurs could not heat the eggs by direct body contact, so must have relied on external environmental heat for incubating their eggs.^[107] However, modern megapode birds as the maleo (Macrocephalon maleo), the Moluccan megapode (Eulipoa wallacei) and scrubfowls (Megapodius spp.) in Southeast Asia and Australia, burrow their eggs using the heat in the top soil to incubate them and provide protection from predators.^[108] The egg spatial distribution, in small clusters linearly to compactly grouped, but contained in round shaped areas of up to 2.3 metres (7.5 ft) would either support burrow- or mound-nesting at Pinyes.^[109]

Hadrosaur ichnofossils

Over 45 fossil localities yielded hadrosaurid fossils in the Lower Red Garumnian of the eastern Tremp Syncline.^[16] Various new specimens of indeterminate Lambeosaurinae were described in 2013 by Prieto Márquez et al.^[110] Furthermore, many hadrosaur ichnofossils have been found in the Tremp Formation and were analyzed in great detail by Vila et al. in 2013. The most abundant track types in fluvial settings are the pedal prints of hadrosaurs, while titanosaur ichnofossils and a single theropod track were found in lagoonal environments.^[111] The authors concluded:^[112]

1. The fluvial lower red unit of the Tremp Formation exhibits meandering and braided fluvial systems with favorable conditions for track production and preservation, like those of North America and Asia.
2. The dinosaurs mainly produced the tracks on the floodplain, within the channels, and on and within crevasse splay deposits in low water stage conditions, and the footprints were infilled by sands during high water stage (stream reactivation).
3. The track record is composed of abundant hadrosaur and scarce sauropod and theropod tracks. The hadrosaur tracks are significantly smaller in size but morphologically similar to comparable records in North America and Asia. They are attributable to the
   ichnogenus Hadrosauropodus
   .
4. A rich track succession composed of more than 40 distinct track levels indicates that hadrosaur footprints are found above the early Maastrichtian–late Maastrichtian boundary and most noticeably in the late Maastrichtian, with tracks occurring abundantly in the Mesozoic part of the C29r magnetochron, during the last 300,000 years of the Cretaceous.
5. The occurrence of hadrosaur tracks in the Ibero-Armorican island seems to be characteristic of the late Maastrichtian time interval and thus they are important biochronostratigraphic markers in the faunal successions of the Late Cretaceous in southwestern Europe.

Fossil content

Group	Name	Member	Image	Notes
Mammals	Afrodon ivani	MP 6 mammal zone		[95][113]
	Nosella europaea	MP 6		[95][113]
	Teilhardimys musculus	MP 6		[95][113]
	Paschatherium cf. dolloi	MP 6		[95][113][114]
	Adapisorex sp.	MP 6		[95][113]
	Hainina pyrenaica	MP 6		[95][96][113]
	Pleuraspidotherium sp.	upper		[95]
	Condylarthra indet.	MP 6		[95][113][114]
Crocodiles	Allodaposuchus hulki	Conquès		[115][116]
	Allodaposuchus palustris	Grey Garumnian		[117][118]
	Allodaposuchus precedens	La Posa		[119]
	Agaresuchus subjuniperus	Conquès		[120][121]
	Arenysuchus gascabadiolorum	Conquès		[122]
	Acynodon sp.	Conquès		[123]
	Crocodylia indet.	La Posa Reptile Sst.		[98][124]
Lizards	Lacertilia indet.	La Posa		[125]
Turtles	Polysternon isonae	Conquès		[126]
	Solemys sp.	Grey Garumnian		[127]
	Testudinata indet.	La Posa		[124]
	Chelonii indet.	Reptile Sst.		[97]
	Bothremydidae indet.	Conquès Reptile Sst.		[98][123]
	Helochelydrinae indet.	Conquès		[123]
Ankylosaurs	Nodosauridae indet.	La Posa		[119]
Styracosternans	Calvarius rapidus	Talarn		[128]
Hadrosaurs	Adynomosaurus arcanus	Conquès		[129]
	Arenysaurus ardevoli	Conquès		[130][131][132]
	Koutalisaurus kohlerorum			[131][note 2]
	Pararhabdodon isonensis	Conquès		[131][134]
	cf. Orthomerus sp.	La Posa		[119]
	Hadrosauria indet.	La Posa Reptile Sst.		[99][119]
	Lambeosaurinae indet.	La Posa		[124]
Iguanodonts	Iguanodontidae indet.	La Posa		[119]
Rhabdodontids	Pareisactus evrostos	Conquès		[135]
	Rhabdodon priscus	La Posa		[125]
Sauropods	Abditosaurus kuehnei	Conquès		[136]
	Titanosaurus cf. indicus	La Posa		[137]
	?Hypselosaurus priscus	La Posa		[119][138]
	Sauropoda indet.	Grey Garumnian		[139]
	Somphospondyli indet.	Conquès		[140]
	Titanosauria indet.	La Posa		[119][127]
Theropods	Richardoestesia sp.	La Posa Conquès		[119][123]
	?Paronychodon sp.	Conquès		[123]
	?Pyroraptor olympius	La Posa		[119]
	Tamarro insperatus	Talarn		[141]
	Coelurosauria indet.	La Posa		[119]
	Maniraptoriformes indet.	Conquès		[123]
	?Megalosauridae indet. (Abelisauridae)	La Posa		[119][142]
	?Neoceratosauria indet.	La Posa		[119]
Theropoda indet.	Reptile Sst.		[98]
Lizards	Anguidae indet.	Conquès		[123]
	Scleroglossa indet.	Conquès		[123]
Snakes	Alethinophidia indet.	Conquès		[123]
Squamata	Squamata indet.	Conquès		[123]
Eggs	Cairanoolithus roussetensis	upper		[143]
	Megaloolithus aureliensis	upper		[143]
	Megaloolithus baghensis	La Posa Conquès Lower Red Garumnian		[143][144] [145][146]
	Megaloolithus mamillare	La Posa Conquès Lower Red Garumnian		[119][143][145] [147][148]
	Megaloolithus siruguei	Conquès Grey Garumnian Lower Red Garumnian		[117][143] [149][150][151]
	Prismatoolithidae indet.	Conquès		[123]
Ichnofossils	Ornithopodichnites magna	La Posa		[152]
	Orcauichnites garumniensis	La Posa		[152]
	Hadrosauropodus sp.	Conquès Lower Red Garumnian		[153][154]
	Ophiomorpha sp.	upper		[143]
	Spirographites ellipticus	Conquès		[126]
	Taenidium barretti, T. bowni, Arenicolites isp., Loloichnus isp., Palaeophycus isp., Planolites isp.	Lower Red Garumnian		[155]
Amphibians	Albanerpeton nexuosus	Conquès		[123]
	aff. Paradiscoglossus sp.	Conquès		[123]
	Amphibia indet.	Conquès		[123]
	Palaeobatrachidae indet.	Conquès		[123]
Fish	Coupatezia trempina, Paratrygonorrhina amblysoda, Hemiscyllium sp., Lamniformes indet.	La Posa		[156]
	Igdabatis indicus, Rhombodus ibericus	La Posa		[157]
	Batoidea indet.	La Posa		[119]
	Lepisosteidae indet.	Conquès		[123]
	Osteichthyes indet.	La Posa		[119]
	Pycnodontiformes indet.	Conquès		[123]
	Teleostei indet.	Conquès		[123]
Bivalves	Apricardia sicoris, Hippuritella castroi, H. lapeirousei, Radiolitella pulchellus	lower		[158]
	Corbicula laletana			[159]
	Ostrea garumnica	La Posa		[119]
Rudists	Hippurites castroi			[159]
	Praeradiolites boucheroni	lower		[158]
Gastropods	Pyrgulifera cf. stillens	La Posa		[119]
	Cerithium sp.	Grey Garumnian		[139]
	Cyclophorus sp.	La Posa		[124]
	Lychnus sp.	La Posa		[124]
	Melanoides sp.	La Posa		[125]
	Neritina sp.	La Posa		[119]
	Pyrgulifera sp.	Grey Garumnian		[127]
Ostracods	Ilyocypris colloti	Grey Garumnian		[160]
Flora	Celastrophyllum bilobatum	Grey Garumnian		[161]
	Cinnamomophyllum vicente-castellum	Grey Garumnian		[162]
	Cornophyllum herendeenensis	Grey Garumnian		[163]
	Menispermophyllum isonensis	Grey Garumnian		[164]
	Saliciphyllum serratum	Grey Garumnian		[165]
	Dicotylophyllum cf. proteoides	Grey Garumnian		[166]
	Sabalites cf. longirhachis	Grey Garumnian		[127]
	Alnophyllum sp.	Grey Garumnian		[167]
	Betuliphyllum sp.	Grey Garumnian		[168]
	Daphnogene sp.	Grey Garumnian		[169]
	Ettingshausenia sp.	Grey Garumnian		[170]
	Myrtophyllum sp.	Grey Garumnian		[171]
	Tracheophyta indet.	Grey Garumnian		[139]
Algae	Amblyochara concava	Conquès		[123]
	Peckichara sertulata	Conquès		[123]
	Microchara cristata, M. nana, M. punctata, M. aff. laevigata			[172]
	Nitellopsis (Campaniella) paracolensis, Microchara sp., Vidaliella gerundensis	upper		[138]
	Feistiella sp.	Conquès		[123]
Fungi	Microcodium			[173]
Cyanobacteria	Girvanella			[173]

Pollen

Additionally, many pollen have been described from the Tremp Formation, east of Isona and 22 kilometres (14 mi) east of Tremp:^[174]

• Polypodiaceoisporites gracicingulis, P. maximus, P. tatabanyensis, P. vitiosus
• Leiotriletes adriennis, L. dorogensis, L. microadriennis
• Cycadopites kyushuensis, C. minar
• Monocolpopollenites dorogensis, M. tranquillus
• Semioculopollis croxtonae, S. praedicatus
• Cicatricosisporites cf. triangulus
• Cupressacites insulipapillatus
• Cupuliferoipollenites pusillus
• Cyrillaceaepollenites barghoorniacus
• Granulatisporites palaeogenicus
• Inaperturopollenites giganteus
• Labraferoidaepollenites menatensis
• Laevigatosporites haardti
• Minorpollis hojstrupensis
• Nudopollis minutus
• Oculopollis cf. minoris
• Pityosporites insignis
• Plicapollis serta
• Punctatisporites luteticus
• Retitricolporites andreanszkyi
• Rugulitriporites pflugi
• Subtriporopollenites constans
• Suemigipollis cf. triangulus
• Tetracolporopollenites halimbaense
• Trilobosporites (Tuberosisporites)
• Vacuopollis cf. concavux
• Granomonocolpites
• Patellasporites
• Platycaryapollenites
• Polyporites
• Retimonocolpites

Research and exhibitions

Every year, over 800 geologists visit El Pallars Jussà and more than 1500 university students from all over Europe come to the Tremp-Graus Basin to carry out their geological fieldwork. The basin is also regarded by petroleum companies as a perfect place to study the interplay of tectonic movements with the different types of lithologies. The Museu Comarcal de Ciències Naturals ("Local District Natural Science Museum") in Tremp, built attached to the Torre de Soldevila in the center of town, is a popular destination for school visits. It houses a permanent fossil exhibition with a wide variety of remains, ranging from dinosaurs to fossilized invertebrates such as corals, bivalves, gastropods, and more.^[175]

The Museu de la Conca Dellà of Isona houses replicas of bone remains, restorations of dinosaurs and an authentic nest of eggs,^[176] left behind by the last dinosaurs to have lived in the valley during the Cretaceous period. The museum also contains numerous other archaeological remains from the Roman settlement of Isona. In recent years, the Consell Comarcal (Regional Council) has promoted several new initiatives, including the creation of a geological program especially adapted to local schools and a series of guided visits to the main archaeological sites of the region.^[177]

The unique paleoenvironment, well-exposed geology, and importance as national heritage have sparked proposals to designate the Tremp Formation and its region as a protected geological site of interest, much like the

Global Geoparks Network.^[178] On April 17, 2018, UNESCO accepted the proposal and designated the site as Conca de Tremp-Montsec Global Geopark, stating:^[5]

"This area is internationally recognized as a natural laboratory for sedimentology, tectonics, external geodynamics, palaeontology, ore deposits and pedology. In addition, other natural and cultural heritage is also remarkable including astronomy and archaeological sites."

Panoramas

View of the eastern part of the Tremp Basin with the Tremp Formation in the foreground

Panorama of the red beds in the Tremp Formation, from Abella de la Conca

See also

Wikimedia Commons has media related to Tremp Formation.

• List of dinosaur-bearing rock formations
• List of Vertebrate fauna of the Maastrichtian stage
• Timeline of Cretaceous–Paleogene extinction event research
• Climate across Cretaceous–Paleogene boundary
• Geology of the Pyrenees
• Hell Creek Formation - Cretaceous-Paleogene contemporaneous fossiliferous formation of the United States
• Cerrejón Formation - Paleocene contemporaneous fossiliferous formation of Colombia

Notes and references

Notes

1. ^ Other authors consider the Conquès Formation a lateral equivalent of the lower red unit of the Tremp Formation^[29]
2. ^ Considered synonymous with Pararhabdodon according to Fossilworks^[133]

References

1. ^ Area Calculator Google Maps
2. ^ ^{a b} Pujalte & Schmitz, 2005, p.82
3. ^ ^{a b} Bosch Lacalle, 2004, p.40
4. ^ ^{a b} Geoparc Mundial de la UNESCO Conca de Tremp-Montsec
5. ^ ^{a b} Conca de Tremp-Montsec Global Geopark - UNESCO.org
6. ^ Global Geoparks Network - Members list
7. ^ Rosell et al., 2013, p.19
8. ^ ^{a b c d} Cuevas, 1992, p.100
9. ^ ^{a b c} Cuevas, 1992, p.102
10. ^ Arribas et al., 1996, p.11
11. ^ Bosch Lacalle, 2004, p.18
12. ^ ^{a b c} Cuevas, 1992, p.96
13. ^ Bosch Lacalle, 2004, p.23
14. ^ Blanco et al., 2014, p.3
15. ^ López Martínez et al., 1996, p.63
16. ^ ^{a b} Prieto Márquez et al., 2013, p.2
17. ^ De Renzi, 1996, p.205
18. ^ ^{a b} Arribas et al., 1996, p.17
19. ^ ^{a b} Canudo et al., 2000, p.340
20. ^ Puértolas et al., 2011, p.2
21. ^ Serra Kiel et al., 1994, p.276
22. ^ Barnolas & Gil Peña, 2001, p.24
23. ^ Ford et al., 1967, p.434
24. ^ Cuevas, 1992, p.97
25. ^ Arribas et al., 1996, p.10
26. ^ ^{a b} Cuevas, 1992, p.103
27. ^ Cuevas, 1992, p.106
28. ^ Cuevas, 1992, p.101
29. ^ Puértolas et al., 2010, p.73
30. ^ Museu de la Conca Dellà - La Posa
31. ^ Cuevas, 1992, p.99
32. ^ Bravo et al., 2005, p.51
33. ^ Díez Canseco, 2016, p.53
34. ^ ^{a b} Blanco et al., 2015b, p.148
35. ^ Andeweg, 2002, Ch.1 p.1
36. ^ ^{a b c d e} Sibuet et al., 2004, p.3
37. ^ García Senz, 2002, p.264
38. ^ López Mir et al., 2014, p.15
39. ^ Rushlow et al., 2013, p.844
40. ^ García Senz, 2002, p.7
41. ^ García Senz, 2002, p.257
42. ^ ^{a b c} Sibuet et al., 2004, p.14
43. ^ García Senz, 2002, p.31
44. ^ Muñoz, 1992, p.238
45. ^ García Senz, 2002, p.105
46. ^ García Senz, 2002, p.201
47. ^ López Mir et al., 2014, p.14
48. ^ Rosenbaum et al., 2002, p.124
49. ^ Rosenbaum et al., 2002, p.122
50. ^ Dinarès Turell et al, 1992, p.265
51. ^ Sibuet et al., 2004, p.12
52. ^ Muñoz, 1992, p.244
53. ^ ^{a b} García Senz, 2002, p.285
54. ^ Muñoz, 1992, p.241
55. ^ Dinarès Turell et al, 1992, p.267
56. ^ Barnolas & Gil Peña, 2001, p.31
57. ^ Teixell et al., 2016, p.262
58. ^ Nijman, 1998, p.140
59. ^ Fernández et al., 2012, p.545
60. ^ Teixell & Muñoz, 2000, p.257
61. ^ Fernández et al., 2012, p.548
62. ^ Ten Veen et al., 2012, p.460
63. ^ Jaillard et al., 2017, p.232
64. ^ Khadivi, 2010, p.56
65. ^ Muñoz et al., 2017, p.16
66. ^ Krzywiec & Sergés, 2006, p.81
67. ^ FGarcía & Jiménez, 2016, p.31
68. ^ Parravano et al., 2015, p.25
69. ^ Claringbould et al., 2011, p.1
70. ^ Brown et al., 2010, p.80
71. ^ Legeay et al., 2017, p.20
72. ^ Ghani et al., 2017, p.38
73. ^ Backé et al., 2010, p.59
74. ^ López Mir et al., 2017, p.110
75. Universidade Fernando Pessoa
76. ^ López Mir et al., 2014, p.12
77. ^ Nijman, 1998, p.138
78. ^ Rosenbaum et al., 2002, p.121
79. ^ Millán Garrido et al., 2000, p.294
80. ^ López Martínez et al., 1996, p.65
81. ^ ^{a b} López Martínez & Peláez Campomanes, 1999, p.694
82. ^ Rosell et al., 2001, pp.54-55
83. ^ Gómez, 2015, p.9
84. ^ Gómez et al., 2015, p.12
85. ^ López Martínez et al., 1996, p.64
86. ^ Meléndez & Molina, 2008, p.108
87. ^ Meléndez & Molina, 2008, pp.112-113
88. ^ Hundreds of dinosaur eggs found in Spain - Inquisitr.com
89. ^ Bosch Lacalle, 2004, p.44
90. ^ Weishampel et al., 2004, pp.588-593
91. ^ ^{a b} Paleontology - Parc Cretaci - Museu de la Conca Dellà
92. ^ Canudo et al., 2000, p.341
93. ^ Marmi et al., 2012, p.133
94. ^ López Martínez et al., 2001, p.53
95. ^ ^{a b c d e f g h i} López Martínez & Peláez Campomanes, 1999, p.686
96. ^ ^{a b} Peláez Campomanes et al., 2000, p.702
97. ^ ^{a b} Blanco et al., 2015, p.149
98. ^ ^{a b c d} Blanco et al., 2015, p.152
99. ^ ^{a b} Blanco et al., 2015, p.154
100. ^ ^{a b} Vilat et al., 2010, p.3
101. ^ Vilat et al., 2010, p.2
102. ^ Vilat et al., 2010, p.4
103. ^ Vilat et al., 2010, p.7
104. ^ Vilat et al., 2010, p.11
105. ^ Hechenleitner et al., 2015, p.6
106. ^ Vilat et al., 2010, p.12
107. ^ Hechenleitner et al., 2015, p.16
108. ^ Hechenleitner et al., 2015, p.17
109. ^ Hechenleitner et al., 2015, p.19
110. ^ Prieto Márquez et al., 2013, pp.22-34
111. ^ Vila et al., 2013, p.5
112. ^ Vila et al., 2013, pp.12-14
113. ^ ^{a b c d e f g} Claret 4 at Fossilworks.org
114. ^ ^{a b} Claret 0 at Fossilworks.org
115. ^ Casa Fabà at Fossilworks.org
116. ^ Blanco et al., 2015a, p.10
117. ^ ^{a b} Fumanya Sud at Fossilworks.org
118. ^ Blanco et al., 2014, p.7
119. ^ ^{a b c d e f g h i j k l m n o p q r} Els Nerets at Fossilworks.org
120. ^ Amor-3 at Fossilworks.org
121. ^ Puértolas et al., 2014, p.4
122. ^ Elías site at Fossilworks.org
123. ^ ^{a b c d e f g h i j k l m n o p q r s t u} Blasi 2 at Fossilworks.org
124. ^ ^{a b c d e} Sant Esteve de la Sarga, Moró at Fossilworks.org
125. ^ ^{a b c} Suterranya mine at Fossilworks.org
126. ^ ^{a b} Barranc de Torrebilles-1 at Fossilworks.org
127. ^ ^{a b c d} Mina Esquirol-1 at Fossilworks.org
128. S2CID 259335419
     .
129. ^ Prieto Márquez et al., 2019
130. ^ Puértolas et al., 2011, p.3
131. ^ ^{a b c} Le Loeuff, 2012, p.551
132. ^ Puértolas et al., 2010, p.71
133. ^ Pararhabdodon at Fossilworks.org
134. ^ Les Llaus at Fossilworks.org
135. ^ Párraga & Prieto Márquez, 2019
136. S2CID 246650381
     .
137. ^ Norets at Fossilworks.org
138. ^ ^{a b} Ullastre & Masriera, 1998, p.115
139. ^ ^{a b c} Mina Esquirol-2 at Fossilworks.org
140. ^ Costa de Castelltallat at Fossilworks.org
141. PMID 33649418
     .
142. PMID 25610343
     .
143. ^ ^{a b c d e f} Coll de Nargó at Fossilworks.org
144. ^ Orcau-1 at Fossilworks.org
145. ^ ^{a b} Els Terrers at Fossilworks.org
146. ^ Serrat de Pelleu at Fossilworks.org
147. ^ Bravo et al., 2005, p.55
148. ^ Costa de la Coma at Fossilworks.org
149. ^ Biscarri, Isona at Fossilworks.org
150. ^ Bravo et al., 2005, p.54
151. ^ Els Terrers 2 at Fossilworks.org
152. ^ ^{a b} Orcau-2 tracksite at Fossilworks.org
153. ^ Torrent de Guixers tracksite at Fossilworks.org
154. ^ Cingles del Boixader at Fossilworks.org
155. ^ Díez Canseco, 2016, p.75
156. ^ Orcau 2 at Fossilworks.org
157. ^ Suterranya-1 at Fossilworks.org
158. ^ ^{a b} St. Corneli at Fossilworks.org
159. ^ ^{a b} Kedves et al., 1985, p.249
160. ^ Ullastre & Masriera, 1998, p.101
161. ^ Marmi, 2016, p.88
162. ^ Marmi, 2016, p.63
163. ^ Marmi, 2016, p.71
164. ^ Marmi, 2016, p.74
165. ^ Marmi, 2016, p.69
166. ^ Marmi, 2016, p.96
167. ^ Marmi, 2016, p.78
168. ^ Marmi, 2016, p.90
169. ^ Marmi, 2016, p.59
170. ^ Marmi, 2016, p.85
171. ^ Marmi, 2016, p.66
172. ^ Blanco et al., 2015a, p.30
173. ^ ^{a b} Arribas et al., 1996, p.12
174. ^ Kedves et al., 1985, pp.249-250
175. ^ Museu Comarcal de Ciències Naturals de Tremp
176. ^ Parc Cretaci - Museu de la Conca Dellà
177. ^ El Pallars Jussà, a geological paradise
178. ^ Global Geoparks UNESCO conference

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Local geology

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Salt tectonics

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• Khadivi, Shokofeh. 2010. Tectonic evolution and growth of the Zagros Mountain Belt (Fars, Iran): constraints from magnetostratigraphy, sedimentology and low-temperature thermochronometry (PhD thesis), 1–225. Université Pierre & Marie Curie. Accessed 2018-05-24.
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Paleontology publications

Dinosaurs

• Bravo, Ana María; Bernat Vila; Àngel Galobart, and Oriol Oms. 2005. Restos de huevos de dinosaurio en el Cretácico Superior del sinclinal de Vallcebre (Berguedà, provincia de Barcelona) - Remains of dinosaur eggs in the Upper Cretaceous of the Vellcebre syncline (Berguedà, Barcelona province). Revista Española de Paleontología 10. 49–57. Accessed 2018-05-24. (in Spanish)
• Canudo, J.I.; X. Pereda Suberbiola, and N. López Martínez. 2000. Los dinosaurios del maastrichtiense superior de Huesca y su importancia en el estudio de la extinción del límite Cretácico/Terciario. Geo-Temas 1. 339–342. Accessed 2018-05-24. (in Spanish)
• Hechenleitner, E. Martín; Gerald Grellet Tinner, and Lucas E. Fiorelli. 2015. What do giant titanosaur dinosaurs and modern Australasian megapodes have in common?. PeerJ 3:e1341. 1–32. Accessed 2018-05-24.
• López Martínez, Nieves; José Ignacio Canudo; Lluís Ardèvol; Xabier Pereda Suberbiola; Xabier Orue Etxebarria; Gloria Cuenca Bescós; José Ignacio Ruiz Omeñaca; Xabier Murelaga, and Monique Feist. 2001. New dinosaur sites correlated with Upper Maastrichtian pelagic deposits in the Spanish Pyrenees: implications for the dinosaur extinction pattern in Europe. Cretaceous Research 22. 41–61. Accessed 2018-05-24.
• Prieto Márquez, Albert; Víctor Fondevilla; Albert G. Sellés; Jonathan R. Wagner, and Àngel Galobart. 2019. Adynomosaurus arcanus, a new lambeosaurine dinosaur from the Late Cretaceous Ibero-Armorican Island of the European Archipelago. Cretaceous Research 96. 19–37. Accessed 2019-02-04.
• Prieto Márquez, Albert; Fabio M. Dalla Vecchia; Rodrigo Gaete, and Àngel Galobart. 2013. Diversity, Relationships, and Biogeography of the Lambeosaurine Dinosaurs from the European Archipelago, with Description of the New Aralosaurin Canardia garonnensis.
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• Prieto Márquez, A., and J.R. Wagner. 2009. Pararhabdodon isonensis and Tsintaosaurus spinorhinus: a new clade of lambeosaurine hadrosaurids from Eurasia. Cretaceous Research 5. 1238. Accessed 2018-05-24.
• Prieto Márquez, A.; R. Gaete; G. Rivas; Á. Galobart, and M. Boada. 2006. Hadrosauroid dinosaurs from the Late Cretaceous of Spain: Pararhabdodon isonensis revisited and Koutalisaurus kohlerorum, gen. et sp. nov.. Journal of Vertebrate Paleontology 26. 929–943. .
• Vila, Bernat; Oriol Oms; Víctor Fondevilla; Rodrigo Gaete; Àngel Galobart; Violeta Riera, and José Ignacio Canudo. 2013. The Latest Succession of Dinosaur Tracksites in Europe: Hadrosaur Ichnology, Track Production and Palaeoenvironments.
  PLoS One
  8. 1–15. Accessed 2018-05-24.
• Vila, Bernat; Frankie D. Jackson; Josep Fortuny; Albert G. Sellés, and Àngel Galobart. 2010. 3-D Modelling of Megaloolithid Clutches: Insights about Nest Construction and Dinosaur Behaviour.
  PLoS One
  5. 1–13. Accessed 2018-05-24.
• Weishampel, David B. et al. 2004. Dinosaur distribution (Late Cretaceous, Europe), 588–593. The Dinosauria, 2nd, Berkeley: University of California Press.

Other groups

• Arribas, M.E.; R. Estrada; A. Obrador, and G. Rampone. 1996. Distribución y ordenación de Microcodium en la Formación Tremp: anticlinal de Campllong (Pirineos Orientales, provincia de Barcelona). Revista de la Sociedad Geológica de España 9. 9–18. Accessed 2018-05-24. (in Spanish)
• Blanco, Alejandro; Josep Fortuny; Alba Vicente; Angel H. Luján; Jordi Alexis García Marçà, and Albert G. Sellés. 2015a. A new species of Allodaposuchus (Eusuchia, Crocodylia) from the Maastrichtian (Late Cretaceous) of Spain: phylogenetic and paleobiological implications. PeerJ 3:e1171. 1–35. Accessed 2018-05-24.
• Blanco, Alejandro; Josep M. Méndez, and Josep Marmi. 2015b. The fossil record of the uppermost Maastrichtian Reptile Sandstone (Tremp Formation, northeastern Iberian Peninsula). Spanish Journal of Palaeontology 30. 147–160. Accessed 2018-05-24.
• Blanco, Alejandro; Eduardo Puértolas Pascual; Josep Marmi; Bernat Vila, and Albert G. Sellés. 2014. Allodaposuchus palustris sp. nov. from the Upper Cretaceous of Fumanya (South Eastern Pyrenees, Iberian Peninsula): Systematics, Palaeoecology and Palaeobiogeography of the Enigmatic Allodaposuchian Crocodylians.
  PLoS One
  9. 1–34. Accessed 2018-05-24.
• Kedves, M.; N. Sole de Porta; J. De Porta, and J. Civis. 1985. Estudio palinológico de los sedimentos maastrichtienses del Barranco de la Posa (Prepirineo, Lérida, España). An. Asoc. Palinol. Lcng. Esp. 2. 247–253. Accessed 2018-05-24. (in Spanish)
• López Martínez, Nieves, and Pablo Peláez Campomanes. 1999. New mammals from south-central Pyrenees (Tremp Formation, Spain) and their bearing on late Paleocene marine-continental correlations. Bulletin de la Société Géologique de France 170. 681–696. Accessed 2018-05-24.
• Marmi, Josep. 2016. Taxonomic revision of the J. Vicente collection dicotyledon leaves from the lower Maastrichtian of Isona (northeastern Iberia). Treballs del Museu de Geología de Barcelona 22. 57–100. Accessed 2018-05-24.
• Marmi, J.; Á.H. Luján; V. Riera; R. Gaete; O. Oms, and À Galobart. 2012. The youngest species of Polysternon: A new bothremydid turtle from the uppermost Maastrichtian of the southern Pyrenees. Cretaceous Research 35. 133–142. Accessed 2018-05-24.
• Párraga, Javier, and Albert Prieto Márquez. 2019. Pareisactus evrostos, a new basal iguanodontian (Dinosauria: Ornithopoda) from the Upper Cretaceous of southwestern Europe. Zootaxa 4555(2). 247–258. Accessed 2019-02-28.
• Peláez Campomanes, P.; N. López Martínez; M.A. Álvarez Sierra, and R. Daams. 2000. The earliest mammal of the European Paleocene: the multituberculate Hainina. Journal of Paleontology 74. 701–711. Accessed 2018-05-24.
• Puértolas Pascual, E.; J.I. Canudo, and M. Moreno Azanza. 2014. The eusuchian crocodylomorph Allodaposuchus subjuniperus sp. nov., a new species from the latest Cretaceous (upper Maastrichtian) of Spain. Historical Biology 26. 91–109. Accessed 2018-05-24.
• Puértolas Pascual, E.; P. Cruzado Caballero; J.I. Canudo; J.M. Gasca; M. Moreno Azanza; D. Castanera; J. Parrilla, and L. Ezquerro. 2012. Nuevos yacimientos de vertebrados del Maastrichtiense superior (Cretácico Superio) de Huesca (España) - New vertebrate sites of the late Maastrichtian (Upper Cretaceous) from Huesca (Spain). Geo-Temas 14. 1–4. Accessed 2018-05-24. (in Spanish)
• Puértolas, Eduardo; José I. Canudo, and Penélope Cruzado Caballero. 2011. A New Crocodylian from the Late Maastrichtian of Spain: Implications for the Initial Radiation of Crocodyloids.
  PLoS One
  6. 1–12. Accessed 2018-05-24.
• Puértolas, E.; P. Cruzado Cabellero; A. Badiola; J.M. Gasca; M. Moreno Azanza, and J.I. Canudo. 2010. Nuevo crocodilomorfo eusuquio de la cuenca de Tremp (Maastrichtiense superior, Arén, Huesca, España) - New eusuchian crocodilomorph from the Tremp basin (late Maastrichtian, Arén, Huesca, Spain), 71–74. V Jornadas Internacionales sobre Paleontología de Dinosaurios y su Entorno. Accessed 2018-05-24. (in Spanish)

Further reading

• Ako, Ojong Gilbert. 2008. Structural development of the Ypresian – Lutetian Sequence of the northeastern Ainsa Basin, Pyrenees, Spain (MSc. thesis), 1–103. University of Oslo. Accessed 2018-05-24.
• Barnolas Cortinas, A. et al.. 1991. Evolución sedimentaria entre la cuenca de Graus-Tremp y la cuenca de Jaca-Pamplona, 1–62. I Congreso del Grupo Español del Terciario. Accessed 2018-05-24. (in Spanish)
• Bentham, Peter A.; Douglas W. Burbank, and Cai Puigdefábregas. 1992. Temporal and spatial controls on the alluvial architecture of an axial drainage system: late Eocene Escanilla Formation, southern Pyrenean foreland basin, Spain. Basin Research 4. 335–352. Accessed 2018-05-24.
• López Martínez, N. 2001. La extinción de los dinosaurios y su registro en los Pirineos meridonales - The dinosaur extinction and its South-Pyrenean record, 70–98. II Jornadas de Paleontología de Dinosaurios y su Entorno. Salas de los Infantes (Burgos, España). Accessed 2018-05-24. (in Spanish)
• Muñoz, Josep Anton; Elisabet Beamud; Oscar Fernández; Pau Arbués; Jaume Dinarès Turell, and Josep Poblet. 2013. The Ainsa Fold and thrust oblique zone of the central Pyrenees: Kinematics of a curved contractional system from paleomagnetic and structural data. Tectonics 32. 1142–1175. Accessed 2018-05-24.
• Puigdefàbregas, C.; J.A. Muñoz, and J. Vergés. 1992. Thrusting and foreland basin evolution in the Southern Pyrenees, 247–254. Thrust Tectonics, Springer, Dordrecht. Accessed 2018-05-24.
• Rahl, Jeffrey M.; Samuel H. Haines, and Ben A. van der Pluijm. 2011. Links between orogenic wedge deformation and erosional exhumation: Evidence from illite age analysis of fault rock and detrital thermochronology of syn-tectonic conglomerates in the Spanish Pyrenees. Earth and Planetary Science Letters 307. 180–190. Accessed 2018-05-24.
• Riera Rubio, Violeta. 2010. Estudio integrado (geología y paleontología) de la sucesión de dinosaurios (Maastrichtiense) de la vertiente subpirenaica (PhD thesis), 1–274.
  Universitat Autònoma de Barcelona
  . Accessed 2018-05-24. (in Spanish)
• Ullastre, Juan, and Alicia Masriera. 2006. El anticlinal de Bóixols - Muntanya de Nargó: consideraciones estratigráficas y estructurales basadas en una nueva cartografía geológica (Pirineo catalán, España). Treballs del Museu Geológico de Barcelona 14. 5–35. Accessed 2018-05-24. (in Spanish)
• Vila, Bernat; Oriol Oms; Josep Marmi; Àngel Galobart, and Rodrigo Gaete. 2006. Los últimos dinosaurios de los Pirineos y sus huellas. Enseñanza de las Ciencias de la Tierra 14. 240–246. Accessed 2018-05-24. (in Spanish)

External links

• (in Spanish) Formation of the Pyrenees