Cuche Formation

The Cuche Formation (Spanish: Formación Cuche, Cc) is a geological formation of the Floresta Massif, Altiplano Cundiboyacense in the Eastern Ranges of the Colombian Andes. The sequence of siltstones, shales, and sandstone beds dates to the Late Devonian and Early Carboniferous periods, and has a maximum thickness of 900 metres (3,000 ft).

Cuche Formation
Stratigraphic range: Frasnian-Early Carboniferous
~385–355 Ma
TypeGeological formation
Unit ofFloresta Massif
UnderliesGirón Fm., Tibasosa Fm.
OverliesFloresta Formation
Area~36 km2 (14 sq mi)
Thickness300–900 m (980–2,950 ft)
Lithology
PrimarySandstone, siltstone
OtherShale
Location
Coordinates5°51′37.2″N 72°56′57.6″W
RegionAltiplano Cundiboyacense
Eastern Ranges, Andes
Country Colombia
Type section
Named forVereda Cuche
Named byBotero
LocationFloresta
Year defined1950
Coordinates5°51′37.2″N 72°56′57.6″W
Approximate paleocoordinates51.7°S 48.1°W / -51.7; -48.1
RegionBoyacá
Country Colombia

Paleogeography of the Middle Devonian
380 Ma, by Stampfli & Borel
Contrasting with the original coastal depositional environment, the Cuche Formation is found at altitudes of more than 2,500 metres (8,200 ft) in the Eastern Colombian Andes around Floresta, Boyacá

The formation was deposited in a tidal-dominated deltaic environment at high southern paleolatitudes at the edge of the Paleozoic Paleo-Tethys Ocean. The Cuche Formation is highly fossiliferous; many Placoderm fish fossils, flora, bivalves, arthropods, crustaceans and ostracods have been discovered in the youngest Paleozoic strate of the Floresta Massif, while the underlying Floresta Formation is richer in trilobite biodiversity.[1]

Etymology

The formation was first described as part of the Floresta Series by Olsson and Carter in 1939. The current definition was given by Botero in 1950.[2] The formation is named after the vereda Cuche of Floresta, Boyacá, where the formation outcrops.[3] The word Cuche is taken from Muysccubun, the language of the indigenous Muisca, who inhabited the Altiplano Cundiboyacense before the Spanish conquest.[4]

Regional setting

The Floresta Massif is a block in the northern part of the Altiplano Cundiboyacense, marked by a metamorphic crystalline core overlain by Devonian to Carboniferous sedimentary sequences; from old to young, the El Tíbet, Floresta and Cuche Formations. The Paleozoic succession is overlain by sediments of much younger date; the Late Jurassic Girón and Early Cretaceous Tibasosa Formations. The massif is bound to the east by the Soapaga Fault and to the west by the Boyacá Fault.[5]

At time of deposition of the Devonian formations, present-day northern South America was located at the edge of the Paleo-Tethys Ocean on the southern hemisphere. The Paleozoic occurrence on the Altiplano is localized in outcrop; the majority of surface sediments are Cretaceous to Paleogene in age. Neogene uplift of the Eastern Ranges, with its main phase in the Plio-Pleistocene, caused the exhumation of older units at surface along major thrust faults in the Eastern Andes. In two phases during the Paleozoic, intrusions occurred into the sedimentary sequence, causing local metamorphism. The first phase is considered pre-Devonian and the latter phase post-Devonian. The remaining stratigraphy of the Cuche Formation appears little affected by this intrusive phase,[6] although slight metamorphism has been identified in later research.[7]

Description

Lithologies

The Cuche Formation is characterised by mostly cream and purple coloured shales, with a basal unit of micaceous siltstones with intercalated yellowish-grey shales and 30 metres (98 ft) thick quartzitic and feldspar-rich sandstone beds that colour red caused by meteoric waters. The sandstones have an iron-rich cementation.[3] A middle unit of fine-grained sandstones with thin banks of siltstones follows the lower part and an upper sequence of shales with interbedded ferruginous red beds.[2] The lower sequence contains runzelmark syn-sedimentary structures.[3]

Stratigraphy and depositional environment
The depositional environment of the Cuche Formation has been analysed to be a low-energy tidal-dominated deltaic setting, with frequent marine incursions into continental and lagoonal areas marked by the presence of both the flora and the many fish species found in the formation

The Cuche Formation in some places discordantly and in other areas transitionally defined by colour changes,[8][9] overlies the Floresta Formation in Boyacá and the Mogotes Formation in Santander,[10] and is, by an angular unconformity up to 60 degrees,[11] overlain by the Upper Jurassic Girón,[12] and Early Cretaceous Tibasosa Formations.[3] The angular unconformity between the Paleozoic and Mesozoic is exposed along the road between Duitama and Sogamoso, and is the location where the first flora fossils were found in 1978.[11]

The age of the Cuche Formation has been estimated to be Late Devonian to Early Carboniferous,[2][13] after an original designation as Permian-Carboniferous by Botero in 1950, further restricted to the Carboniferous by Julivert in 1968.[14] The formation covers an area of approximately 36 square kilometres (14 sq mi) and ranges in thickness between 300 and 900 metres (980 and 2,950 ft).[2] Stratigraphically, the Cuche Formation is time equivalent with the Diamante Formation of the Santander Massif to the north of the Altiplano Cundiboyacense.[15] To the west of Paz de Río, the Cuche Formation is thrusted upon the Neogene Concentración Formation by the Soapaga Fault.[16] In the northern part of the Floresta Massif, the contact between the metamorphic Otengá Stock and the Cuche Formation is formed by the Duga Fault.[17]

Based on the preservation of fossils, the lithologies, syn-sedimentary structures and stratigraphic position, a depositional environment of shallow low energy waters has been proposed, possibly in a lagoonal setting at the edge of a regressional Paleo-Tethys Ocean.[1][18] Other parts of the Cuche Formation were deposited in a continental environment, evidenced by the red beds and absence of marine fossils and abundant root imprints.[19] Overall, the sequence represents a coastal deltaic environment with frequent marine incursions, a tidal deltaic setting.[20][21]

Fossil content
Fossil flora from the Cuche Formation were identified as "Ginkgo-like" species, as this Baiera reconstruction. Proper Ginkgo do not appear in the geological record until the Middle Permian

The first identification of fossil content of the Cuche Formation was done by Botero, who studied the formation in 1950. Research in the early 1980s revealed the presence of many more fossils in the formation and among the first fossil flora found were species then identified as the genera Ginkgo and Baiera.[14] The lower units show poorly preserved plant remains and the overlying shales provided arthropods and crustaceans. In the middle units of the formation, more and better preserved plant fossils were found alongside bivalves, ostracods (of the genus Welleria) and arthropods.[22]

The Cuche Formation contains unique Placoderm fish fossils, first noted by Mojica and Villarroel in 1984.[23] Across the section, also plant fossils and bivalves are found. In this part of the sequence the first fish fossils were discovered. The top section provided brachiopods (genus Lingula) and other at that moment undetermined fossil fragments.[24]

Later research has provided more insight into the flora of the formation, with the "Ginkgo" species possibly a Ginkgophyton sp..[25] Additionally, fossil flora of Colpodexylon cf. deatsii and cf. Archaeopteris sp. have been described from the formation.[26] In the continental sandstone facies of the Cuche Formation, ichnofossils of Diplichnites have been described.[27]

Fishes
Antarctilamna (Gondwanan)
Bothriolepis (Euramerican)
Holoptychius (Euramerican)
The fossil assemblage of the Cuche Formation is unique in the mixture of typical Euramerican (Laurussian) and Gondwanan fish and flora species.

A closer paleogeographical relation between the paleocontinents has been suggested to explain this curious combination.

Remains of the cartilaginous fish Antarctilamna sp., the Placoderms Asterolepis sp. and two species of Bothriolepis,[28] the spiny shark ?Cheiracanthoides sp., the Porolepiform Holoptychius sp., and the Rhizodontid ?Strepsodus sp. have been uncovered from the Cuche Formation.[23] Several other fossils are less well recognizable at the genus level, among others Actinopterygii, Sarcopterygii,[29] and Osteolepiformes.[30] The fish specimens were found in sediments possibly representing localized transgressive marine incursions into brackish lagoonal settings,[20][31] in all cases associated with the presence of bivalves, ostracods and brachiopods.[32]

The fossil fish assemblage of the Cuche Formation presents a curious mixture of Euramerican "Old Red Sandstone" (Catskills, Greenland, Scotland and the Baltic states)[20] species (Asterolepis and Holoptychius), and Gondwanan taxa (Antarctilamna), suggesting the interchange of species between the paleogeographical regions, possibly at closer distance than is presented in most paleogeographical models.[33][34] This hypothesis is further strengthened by the discovery of typical Euramerican flora, as Archaeopteris.[26]

Asterolepis has been known only from Euramerican fossils, except for a specimen found in Iran.[20] The fish of the Cuche Formation are quite different from Bolivian Devonian fossils, with the exception of Antarctilamna. The similar sediments of the Colpacucho Formation in Bolivia have not provided the species discovered in the Cuche Formation, probably because of the cooler climate of the Devonian Bolivian seas more to the south than the paleogeographical position of northern Colombia (already around 51°S) at that time.[34]

Fossils assigned to Florestacanthus cf. morenoi, Colombiaspis rinconensis and Colombialepis villarroeli were later described from the Cuche Formation.[35][36][37]

Eurypterids

In 2019, fragments of the eurypterid Pterygotus were retrieved from the formation. The find represents the first sea scorpion from Colombia and the fourth from South America.[38] The specimen (SGC-MGJRG.2018.I.5), assigned with uncertainty to P. bolivianus due to similarities with its holotype, represents the first eurypterid of Colombia and the fourth of South America. The fossil was dated as Frasnian (Late Devonian), showing that Pterygotus did not become extinct during the Middle Devonian as previously thought.[39]

Outcrops
Type locality of the Cuche Formation in the north of the Altiplano Cundiboyacense

The Cuche Formation is found at the Floresta Massif around its type locality in Floresta, Boyacá, stretching across Floresta to the west close to Belén and Paz de Río,[2][40] up to north of Tibasosa in the valley of the Chicamocha River.[41]

Regional correlations
Stratigraphy of the Llanos Basin and surrounding provinces
MaAgePaleomapRegional eventsCatatumboCordilleraproximal Llanosdistal LlanosPutumayoVSMEnvironmentsMaximum thicknessPetroleum geologyNotes
0.01Holocene
Holocene volcanism
Seismic activity		alluviumOverburden
1Pleistocene
Pleistocene volcanism
Andean orogeny 3
Glaciations		GuayaboSoatá
Sabana		NecesidadGuayaboGigante
Neiva		Alluvial to fluvial (Guayabo)550 m (1,800 ft)
(Guayabo)		[42][43][44][45]
2.6Pliocene
Pliocene volcanism
Andean orogeny 3
GABI		Subachoque
5.3MessinianAndean orogeny 3
Foreland		MarichuelaCaimánHonda[44][46]
13.5LanghianRegional floodingLeónhiatusCajaLeónLacustrine (León)400 m (1,300 ft)
(León)		Seal[45][47]
16.2BurdigalianMiocene inundations
Andean orogeny 2		C1Carbonera C1OspinaProximal fluvio-deltaic (C1)850 m (2,790 ft)
(Carbonera)		Reservoir[46][45]
17.3C2Carbonera C2Distal lacustrine-deltaic (C2)Seal
19C3Carbonera C3Proximal fluvio-deltaic (C3)Reservoir
21Early MiocenePebas wetlandsC4Carbonera C4BarzalosaDistal fluvio-deltaic (C4)Seal
23Late Oligocene
Andean orogeny 1
Foredeep		C5Carbonera C5OritoProximal fluvio-deltaic (C5)Reservoir[43][46]
25C6Carbonera C6Distal fluvio-lacustrine (C6)Seal
28Early OligoceneC7C7PepinoGualandayProximal deltaic-marine (C7)Reservoir[43][46][48]
32Oligo-EoceneC8UsmeC8onlapMarine-deltaic (C8)Seal
Source		[48]
35Late Eocene
MiradorMiradorCoastal (Mirador)240 m (790 ft)
(Mirador)		Reservoir[45][49]
40Middle EoceneRegaderahiatus
45
50Early Eocene
SochaLos CuervosDeltaic (Los Cuervos)260 m (850 ft)
(Los Cuervos)		Seal
Source		[45][49]
55Late PaleocenePETM
2000 ppm CO2		Los CuervosBogotáGualanday
60Early PaleoceneSALMABarcoGuaduasBarcoRumiyacoFluvial (Barco)225 m (738 ft)
(Barco)		Reservoir[42][43][46][45][50]
65Maastrichtian
KT extinctionCatatumboGuadalupeMonserrateDeltaic-fluvial (Guadalupe)750 m (2,460 ft)
(Guadalupe)		Reservoir[42][45]
72CampanianEnd of riftingColón-Mito Juan[45][51]
83SantonianVilleta/Güagüaquí
86Coniacian
89TuronianCenomanian-Turonian anoxic eventLa LunaChipaqueGachetáhiatusRestricted marine (all)500 m (1,600 ft)
(Gachetá)		Source[42][45][52]
93Cenomanian
Rift 2
100AlbianUneUneCaballosDeltaic (Une)500 m (1,600 ft)
(Une)		Reservoir[46][52]
113Aptian
CapachoFómequeMotemaYavíOpen marine (Fómeque)800 m (2,600 ft)
(Fómeque)		Source (Fóm)[43][45][53]
125BarremianHigh biodiversityAguardientePajaShallow to open marine (Paja)940 m (3,080 ft)
(Paja)		Reservoir[42]
129Hauterivian
Rift 1Tibú-
Mercedes		Las JuntashiatusDeltaic (Las Juntas)910 m (2,990 ft)
(Las Juntas)		Reservoir (LJun)[42]
133ValanginianRío NegroCáqueza
Macanal
Rosablanca		Restricted marine (Macanal)2,935 m (9,629 ft)
(Macanal)		Source (Mac)[43][54]
140BerriasianGirón
145TithonianBreak-up of PangeaJordánArcabucoBuenavista
Batá
SaldañaAlluvial, fluvial (Buenavista)110 m (360 ft)
(Buenavista)		"Jurassic"[46][55]
150Early-Mid Jurassic
Passive margin 2La Quinta
Montebel

Noreán		hiatusCoastal tuff (La Quinta)100 m (330 ft)
(La Quinta)		[56]
201Late Triassic
MucuchachiPayandé[46]
235Early Triassic
Pangeahiatus"Paleozoic"
250Permian
300Late Carboniferous
Famatinian orogenyCerro Neiva
()		[57]
340Early CarboniferousFossil fish
Romer's gap		Cuche
(355-385)		Farallones
()		Deltaic, estuarine (Cuche)900 m (3,000 ft)
(Cuche)
360Late Devonian
Passive margin 1Río Cachirí
(360-419)		Ambicá
()		Alluvial-fluvial-reef (Farallones)2,400 m (7,900 ft)
(Farallones)		[54][58][59][60][61]
390Early Devonian
High biodiversityFloresta
(387-400)
El Tíbet		Shallow marine (Floresta)600 m (2,000 ft)
(Floresta)
410Late SilurianSilurian mystery
425Early Silurianhiatus
440Late Ordovician
Rich fauna in BoliviaSan Pedro
(450-490)		Duda
()
470Early OrdovicianFirst fossilsBusbanzá
(>470±22)
Chuscales
Otengá		Guape
()		Río Nevado
()		Hígado
()
Agua Blanca
Venado
(470-475)
[62][63][64]
488Late Cambrian
Regional intrusionsChicamocha
(490-515)		Quetame
()		Ariarí
()		SJ del Guaviare
(490-590)		San Isidro
()		[65][66]
515Early CambrianCambrian explosion[64][67]
542Ediacaran
Break-up of Rodiniapre-Quetamepost-ParguazaEl Barro
()		Yellow: allochthonous basement
(Chibcha Terrane)
Green: autochthonous basement
(Río Negro-Juruena Province)		Basement[68][69]
600Neoproterozoic
Cariri Velhos orogenyBucaramanga
(600-1400)		pre-Guaviare[65]
800
Snowball Earth[70]
1000Mesoproterozoic
Sunsás orogenyAriarí
(1000)		La Urraca
(1030-1100)		[71][72][73][74]
1300Rondônia-Juruá orogenypre-AriaríParguaza
(1300-1400)		Garzón
(1180-1550)		[75]
1400
pre-Bucaramanga[76]
1600PaleoproterozoicMaimachi
(1500-1700)		pre-Garzón[77]
1800
Tapajós orogenyMitú
(1800)		[75][77]
1950Transamazonic orogenypre-Mitú[75]
2200Columbia
2530Archean
Carajas-Imataca orogeny[75]
3100Kenorland
Sources
Legend
  • group
  • important formation
  • fossiliferous formation
  • minor formation
  • (age in Ma)
  • proximal Llanos (Medina)[note 1]
  • distal Llanos (Saltarin 1A well)[note 2]

See also
Geology of the Eastern Hills
Geology of the Ocetá Páramo
Geology of the Altiplano Cundiboyacense
Bogotá, Cerrejón, Paja Formations, Honda Group

Notes
  1. based on Duarte et al. (2019)[78], García González et al. (2009),[79] and geological report of Villavicencio[80]
  2. based on Duarte et al. (2019)[78] and the hydrocarbon potential evaluation performed by the UIS and ANH in 2009[81]

References
  1. Morzadec et al., 2015, p.331
  2. Rodríguez & Solano, 2000, p.57
  3. Mojica & Villarroel, 1984, p.65
  4. Giraldo Gallego, 2014
  5. Mojica & Villarroel, 1984, p.60
  6. Mojica & Villarroel, 1984, p.63
  7. Geoestudios, 2006, p.68
  8. Rodríguez & Solano, 2000, p.58
  9. Mojica & Villarroel, 1984, p.67
  10. Rodríguez Gutiérrez, 2017, p.75
  11. Mojica & Villarroel, 1984, p.68
  12. Rodríguez & Solano, 2000, p.41
  13. Villarroel & Mojica, 1985, p.85
  14. Mojica & Villarroel, 1984, p.71
  15. Villafañez Cardona, 2012, p.39
  16. Geoestudios, 2006, p.14
  17. Geoestudios, 2006, p.202
  18. Mojica & Villarroel, 1984, p.75
  19. Giroud López, 2014, p.146
  20. Janvier & Villarroel, 2000, p.756
  21. Giroud López, 2014, p.147
  22. Mojica & Villarroel, 1984, p.72
  23. Janvier & Villarroel, 2000, p.729
  24. Mojica & Villarroel, 1984, p.66
  25. Mojica & Villarroel, 1984, p.74
  26. Berry et al., 2000
  27. Gómez Cruz et al., 2015
  28. Janvier & Villarroel, 1998, p.7
  29. Janvier & Villarroel, 1998, p.11
  30. Janvier & Villarroel, 1998, p.12
  31. Janvier & Villarroel, 1998, p.9
  32. Janvier & Villarroel, 1998, p.14
  33. Janvier & Villarroel, 1998, p.15
  34. Janvier & Villarroel, 2000, p.757
  35. Olive et al., 2019, p.4
  36. Olive et al., 2019, p.6
  37. Olive et al., 2019, p.8
  38. Olive et al., 2019, p.17
  39. Olive et al., 2019, p.13
  40. Plancha 172, 1998
  41. Pardo Díaz et al., 2014, p.55
  42. García González et al., 2009, p.27
  43. García González et al., 2009, p.50
  44. García González et al., 2009, p.85
  45. Barrero et al., 2007, p.60
  46. Barrero et al., 2007, p.58
  47. Plancha 111, 2001, p.29
  48. Plancha 177, 2015, p.39
  49. Plancha 111, 2001, p.26
  50. Plancha 111, 2001, p.24
  51. Plancha 111, 2001, p.23
  52. Pulido & Gómez, 2001, p.32
  53. Pulido & Gómez, 2001, p.30
  54. Pulido & Gómez, 2001, pp.21-26
  55. Pulido & Gómez, 2001, p.28
  56. Correa Martínez et al., 2019, p.49
  57. Plancha 303, 2002, p.27
  58. Terraza et al., 2008, p.22
  59. Plancha 229, 2015, pp.46-55
  60. Plancha 303, 2002, p.26
  61. Moreno Sánchez et al., 2009, p.53
  62. Mantilla Figueroa et al., 2015, p.43
  63. Manosalva Sánchez et al., 2017, p.84
  64. Plancha 303, 2002, p.24
  65. Mantilla Figueroa et al., 2015, p.42
  66. Arango Mejía et al., 2012, p.25
  67. Plancha 350, 2011, p.49
  68. Pulido & Gómez, 2001, pp.17-21
  69. Plancha 111, 2001, p.13
  70. Plancha 303, 2002, p.23
  71. Plancha 348, 2015, p.38
  72. Planchas 367-414, 2003, p.35
  73. Toro Toro et al., 2014, p.22
  74. Plancha 303, 2002, p.21
  75. Bonilla et al., 2016, p.19
  76. Gómez Tapias et al., 2015, p.209
  77. Bonilla et al., 2016, p.22
  78. Duarte et al., 2019
  79. García González et al., 2009
  80. Pulido & Gómez, 2001
  81. García González et al., 2009, p.60

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