Regadera Formation
Stratigraphic range: Middle to Late Eocene
~
TypeGeological formation
UnderliesUsme Fm., Tilatá Fm.
OverliesBogotá Formation
Thicknessup to 756 metres (2,480 ft)
Lithology
PrimarySandstone, conglomerate
OtherShale
Location
Coordinates4°23′30.8″N 74°08′26.3″W / 4.391889°N 74.140639°W / 4.391889; -74.140639
RegionBogotá savanna, Altiplano Cundiboyacense
Eastern Ranges, Andes
Country Colombia
Type section
Named forLa Regadera Reservoir
Named byJulivert
LocationUsme, Bogotá
Year defined1963
Coordinates4°23′30.8″N 74°08′26.3″W / 4.391889°N 74.140639°W / 4.391889; -74.140639
RegionCundinamarca
Country Colombia

Paleogeography of Northern South America
50 Ma, by Ron Blakey

The Regadera Formation (Spanish: Formación Regadera, E2r, Tpr) is a geological formation of the Bogotá savanna, Altiplano Cundiboyacense, Eastern Ranges of the Colombian Andes. The predominantly sandstone and conglomeratic formation, with pink shale beds intercalated, dates to the Paleogene period; Middle to Late Eocene epoch, and has a maximum thickness of 765 metres (2,510 ft).

Etymology

The formation was first described by Hubach in 1931 as part of the Usme Formation and redefined and named in 1963 by Julivert after the La Regadera Reservoir.[1]

Description

Lithologies

The Regadera Formation consists mainly of quartz arenitic sandstone and conglomerates with some shale beds.[1][2]

Stratigraphy and depositional environment

The Regadera Formation overlies the Bogotá Formation and is overlain by the Usme and Tilatá Formations. The age has been estimated, based on palynological data of Echitriporites trianguliformis var. orbicularis, Nothofagidites sp. and Multiporopollenites pauciporatus, to be Middle to Late Eocene.[3] The depositional environment has been interpreted as a braided river setting.[4]

Outcrops

Regadera Formation is located in the Bogotá savanna
Regadera Formation
Type locality of the Regadera Formation to the south of the Bogotá savanna

The Regadera Formation is apart from its type locality in the synclinal of Usme, the valley of the Tunjuelo River, found in the synclinal of Sisga.[1] In the Tunjuelo River valley, the Regadera Formations is present in the escarpments on the river banks.[5]

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)		[6][7][8][9]
2.6Pliocene
Pliocene volcanism
Andean orogeny 3
GABI		Subachoque
5.3MessinianAndean orogeny 3
Foreland		MarichuelaCaimánHonda[8][10]
13.5LanghianRegional floodingLeónhiatusCajaLeónLacustrine (León)400 m (1,300 ft)
(León)		Seal[9][11]
16.2BurdigalianMiocene inundations
Andean orogeny 2		C1Carbonera C1OspinaProximal fluvio-deltaic (C1)850 m (2,790 ft)
(Carbonera)		Reservoir[10][9]
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[7][10]
25C6Carbonera C6Distal fluvio-lacustrine (C6)Seal
28Early OligoceneC7C7PepinoGualandayProximal deltaic-marine (C7)Reservoir[7][10][12]
32Oligo-EoceneC8UsmeC8onlapMarine-deltaic (C8)Seal
Source		[12]
35Late Eocene
MiradorMiradorCoastal (Mirador)240 m (790 ft)
(Mirador)		Reservoir[9][13]
40Middle EoceneRegaderahiatus
45
50Early Eocene
SochaLos CuervosDeltaic (Los Cuervos)260 m (850 ft)
(Los Cuervos)		Seal
Source		[9][13]
55Late PaleocenePETM
2000 ppm CO2		Los CuervosBogotáGualanday
60Early PaleoceneSALMABarcoGuaduasBarcoRumiyacoFluvial (Barco)225 m (738 ft)
(Barco)		Reservoir[6][7][10][9][14]
65Maastrichtian
KT extinctionCatatumboGuadalupeMonserrateDeltaic-fluvial (Guadalupe)750 m (2,460 ft)
(Guadalupe)		Reservoir[6][9]
72CampanianEnd of riftingColón-Mito Juan[9][15]
83SantonianVilleta/Güagüaquí
86Coniacian
89TuronianCenomanian-Turonian anoxic eventLa LunaChipaqueGachetáhiatusRestricted marine (all)500 m (1,600 ft)
(Gachetá)		Source[6][9][16]
93Cenomanian
Rift 2
100AlbianUneUneCaballosDeltaic (Une)500 m (1,600 ft)
(Une)		Reservoir[10][16]
113Aptian
CapachoFómequeMotemaYavíOpen marine (Fómeque)800 m (2,600 ft)
(Fómeque)		Source (Fóm)[7][9][17]
125BarremianHigh biodiversityAguardientePajaShallow to open marine (Paja)940 m (3,080 ft)
(Paja)		Reservoir[6]
129Hauterivian
Rift 1Tibú-
Mercedes		Las JuntashiatusDeltaic (Las Juntas)910 m (2,990 ft)
(Las Juntas)		Reservoir (LJun)[6]
133ValanginianRío NegroCáqueza
Macanal
Rosablanca		Restricted marine (Macanal)2,935 m (9,629 ft)
(Macanal)		Source (Mac)[7][18]
140BerriasianGirón
145TithonianBreak-up of PangeaJordánArcabucoBuenavista
Batá
SaldañaAlluvial, fluvial (Buenavista)110 m (360 ft)
(Buenavista)		"Jurassic"[10][19]
150Early-Mid Jurassic
Passive margin 2La Quinta
Montebel

Noreán		hiatusCoastal tuff (La Quinta)100 m (330 ft)
(La Quinta)		[20]
201Late Triassic
MucuchachiPayandé[10]
235Early Triassic
Pangeahiatus"Paleozoic"
250Permian
300Late Carboniferous
Famatinian orogenyCerro Neiva
()		[21]
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)		[18][22][23][24][25]
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)
[26][27][28]
488Late Cambrian
Regional intrusionsChicamocha
(490-515)		Quetame
()		Ariarí
()		SJ del Guaviare
(490-590)		San Isidro
()		[29][30]
515Early CambrianCambrian explosion[28][31]
542Ediacaran
Break-up of Rodiniapre-Quetamepost-ParguazaEl Barro
()		Yellow: allochthonous basement
(Chibcha Terrane)
Green: autochthonous basement
(Río Negro-Juruena Province)		Basement[32][33]
600NeoproterozoicCariri Velhos orogenyBucaramanga
(600-1400)		pre-Guaviare[29]
800
Snowball Earth[34]
1000Mesoproterozoic
Sunsás orogenyAriarí
(1000)		La Urraca
(1030-1100)		[35][36][37][38]
1300Rondônia-Juruá orogenypre-AriaríParguaza
(1300-1400)		Garzón
(1180-1550)		[39]
1400
pre-Bucaramanga[40]
1600PaleoproterozoicMaimachi
(1500-1700)		pre-Garzón[41]
1800
Tapajós orogenyMitú
(1800)		[39][41]
1950Transamazonic orogenypre-Mitú[39]
2200Columbia
2530Archean
Carajas-Imataca orogeny[39]
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

Notes and references

Notes

  1. ↑ based on Duarte et al. (2019)[42], García González et al. (2009),[43] and geological report of Villavicencio[44]
  2. ↑ based on Duarte et al. (2019)[42] and the hydrocarbon potential evaluation performed by the UIS and ANH in 2009[45]

References

  1. 1 2 3 Montoya & Reyes, 2005, p.60
  2. ↑ Bayona et al., 2010, p.5
  3. ↑ Montoya & Reyes, 2005, p.64
  4. ↑ Bayona et al., 2010, p.7
  5. ↑ Bayona et al., 2010, p.11
  6. 1 2 3 4 5 6 García González et al., 2009, p.27
  7. 1 2 3 4 5 6 García González et al., 2009, p.50
  8. 1 2 García González et al., 2009, p.85
  9. 1 2 3 4 5 6 7 8 9 10 Barrero et al., 2007, p.60
  10. 1 2 3 4 5 6 7 8 Barrero et al., 2007, p.58
  11. ↑ Plancha 111, 2001, p.29
  12. 1 2 Plancha 177, 2015, p.39
  13. 1 2 Plancha 111, 2001, p.26
  14. ↑ Plancha 111, 2001, p.24
  15. ↑ Plancha 111, 2001, p.23
  16. 1 2 Pulido & Gómez, 2001, p.32
  17. ↑ Pulido & Gómez, 2001, p.30
  18. 1 2 Pulido & Gómez, 2001, pp.21-26
  19. ↑ Pulido & Gómez, 2001, p.28
  20. ↑ Correa Martínez et al., 2019, p.49
  21. ↑ Plancha 303, 2002, p.27
  22. ↑ Terraza et al., 2008, p.22
  23. ↑ Plancha 229, 2015, pp.46-55
  24. ↑ Plancha 303, 2002, p.26
  25. ↑ Moreno Sánchez et al., 2009, p.53
  26. ↑ Mantilla Figueroa et al., 2015, p.43
  27. ↑ Manosalva Sánchez et al., 2017, p.84
  28. 1 2 Plancha 303, 2002, p.24
  29. 1 2 Mantilla Figueroa et al., 2015, p.42
  30. ↑ Arango Mejía et al., 2012, p.25
  31. ↑ Plancha 350, 2011, p.49
  32. ↑ Pulido & Gómez, 2001, pp.17-21
  33. ↑ Plancha 111, 2001, p.13
  34. ↑ Plancha 303, 2002, p.23
  35. ↑ Plancha 348, 2015, p.38
  36. ↑ Planchas 367-414, 2003, p.35
  37. ↑ Toro Toro et al., 2014, p.22
  38. ↑ Plancha 303, 2002, p.21
  39. 1 2 3 4 Bonilla et al., 2016, p.19
  40. ↑ Gómez Tapias et al., 2015, p.209
  41. 1 2 Bonilla et al., 2016, p.22
  42. 1 2 Duarte et al., 2019
  43. ↑ García González et al., 2009
  44. ↑ Pulido & Gómez, 2001
  45. ↑ García González et al., 2009, p.60

Bibliography

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