Santa Teresa Formation, Colombia

Santa Teresa Formation
Santa Teresa Formation
Stratigraphic range: Late Oligocene (Deseadan); ~
Type	Geological formation
Underlies	alluvium
Overlies	San Juan de Río Seco Formation
Thickness	Type section: 118 m (387 ft); Maximum: 150 m (490 ft)
Lithology
Primary	Claystone
Other	Siltstone, calcareous sandstone
Location
Coordinates	4°50′55″N 74°37′14″W
Country	Colombia
Extent	Western Eastern Ranges, Andes; Southern Middle Magdalena Valley
Type section
Named for	Vereda Santa Teresa
Named by	De Porta
Location	San Juan de Rioseco
Year defined	1966
Coordinates	4°50′55″N 74°37′14″W
Region	Cundinamarca
Country	Colombia
Thickness at type section	118 m (387 ft)
	; Paleogeography of Northern South America; 35 Ma, by Ron Blakey

The Santa Teresa Formation (Spanish: Formación Santa Teresa, Tist, Pgst) is a geological formation of the western Eastern Ranges of the Colombian Andes, west of the Bituima Fault, and the southern Middle Magdalena Valley. The formation spreads across the western part of Cundinamarca and the northern portion of Tolima. The formation consists of grey claystones intercalated by orange quartz siltstones and sandstones of small to conglomeratic grain size. The thickness at its type section has been measured to be 118 metres (387 ft) and a maximum thickness of 150 metres (490 ft) suggested.

In the formation, dated on the basis of its fossil content to the Late Oligocene, many leaf imprints and mollusks were found, suggesting a lacustrine to deltaic depositional environment with periodical marine incursions.

Etymology

The formation was defined by De Porta in 1966 and named after the vereda Santa Teresa, San Juan de Rioseco.[1]

Description

Santa Teresa Formation, Colombia is located in Cundinamarca Department

Type locality of the Santa Teresa Formation in Cundinamarca

The Santa Teresa Formation is the youngest unit outcropping in the Jerusalén-Guaduas synclinal, western Eastern Ranges, covering the San Juan de Río Seco Formation. The formation was formerly called La Cira Formation. In the Balú quebrada, the formation shows a thickness of 118 metres (387 ft), while the maximum thickness could reach 150 metres (490 ft).[1]

The lower boundary of the formation is marked by the first occurrence of grey claystones, covering the light brown claystones of the San Juan de Río Seco Formation. The formation comprises grey claystones intercalated by orange quartz siltstones and sandstones of small to conglomeratic grain size. The roundness of the sandstone grains has been characterized as angular to subangular by Lamus Ochoa et al. in 2013.[2] The claystones occur in thick layers with wavy lamination.[1]

In these thick packages of claystones, the formation has provided fossil leaves in various forms and sizes, and to a lesser extent the remains of mollusks; gastropods and bivalves. The basal contacts of these beds are straight to transitional and most of the time are coarsening upward towards quartz arenites where the gastropods dominate. These facies sequences have a thickness of about 2 metres (6.6 ft). Locally, bioturbation, siderite nodules and coal beds occur in the formation. The sandstones occur in very thin to very thick beds, characterized by plain parallel lamination, in lenses and very locally in flasers. The cement of the arenites is calcareous.[1] The grain composition of the lithic fraction comprises zircon,[3] epidote, zoisite, clinozoisite and pyroxenes, which at the top of the formation amounts to 86 percent.[4]

Stratigraphy and depositional environment

The Santa Teresa Formation conformably overlies the San Juan de Río Seco Formation and is covered by subrecent alluvium.[1] The formation is part of the sequence after the Eocene unconformity.[5]

The age has been inferred to be Late Oligocene. The depositional environment has been interpreted as lacustrine with marine influence in the form of channels. The abundance of brackish and fresh water gastropods suggests these environmental conditions prevailed in the Oligocene of central Colombia.[1]

In the type section at the Balú quebrada, facies traits that confirm this interpretation can be observed. The lacustrine areas were probably shallow water environments with reducing conditions and a continuous supply of siliciclastics by small deltas. The many leaf imprints and coal layers support the presence of a lush vegetation at the time of deposition.[1] The abundance of lithic clasts near the top of the formation supports a renewed provenance area to the east; the uplift of the Eastern Ranges of the Colombian Andes,[6] due to activity of the La Salina Fault.[7]

Paleontology

The Santa Teresa Formation has provided fossil mollusks, described by De Porta and Solé De Porta in 1962 and De Porta Anodontites laciranus, Diplodon oponcintonis, Diplodon waringi,[8] and Corbula sp., among other mollusks described by De Porta in 1966.[1]

Regional correlations

Stratigraphy of the Llanos Basin and surrounding provinces
Ma	Age	Regional events	Catatumbo	Cordillera	proximal Llanos	distal Llanos	Putumayo	VSM	Environments	Maximum thickness	Petroleum geology	Notes
0.01	Holocene	Holocene volcanism Seismic activity	alluvium								Overburden
1	Pleistocene	Pleistocene volcanism Andean orogeny 3 Glaciations	Guayabo	Soatá Sabana	Necesidad	Guayabo	Gigante Neiva		Alluvial to fluvial (Guayabo)	550 m (1,800 ft) (Guayabo)		[9][10][11][12]
2.6	Pliocene	Pliocene volcanism Andean orogeny 3 GABI		Subachoque			Gigante Neiva
5.3	Messinian	Andean orogeny 3 Foreland		Marichuela			Caimán	Honda				[11][13]
13.5	Langhian	Regional flooding	León	hiatus	Caja	León	Caimán		Lacustrine (León)	400 m (1,300 ft) (León)	Seal	[12][14]
16.2	Burdigalian	Miocene inundations Andean orogeny 2	C1		Carbonera C1		Ospina		Proximal fluvio-deltaic (C1)	850 m (2,790 ft) (Carbonera)	Reservoir	[13][12]
17.3			C2		Carbonera C2				Distal lacustrine-deltaic (C2)		Seal
19			C3		Carbonera C3				Proximal fluvio-deltaic (C3)		Reservoir
21	Early Miocene	Pebas wetlands	C4		Carbonera C4			Barzalosa	Distal fluvio-deltaic (C4)		Seal
23	Late Oligocene	Andean orogeny 1 Foredeep	C5		Carbonera C5		Orito		Proximal fluvio-deltaic (C5)		Reservoir	[10][13]
25	Late Oligocene		C6		Carbonera C6		Orito		Distal fluvio-lacustrine (C6)		Seal
28	Early Oligocene		C7		C7		Pepino	Gualanday	Proximal deltaic-marine (C7)		Reservoir	[10][13][15]
32	Oligo-Eocene		C8	Usme	C8	onlap			Marine-deltaic (C8)		Seal Source	[15]
35	Late Eocene		Mirador	Usme	Mirador				Coastal (Mirador)	240 m (790 ft) (Mirador)	Reservoir	[12][16]
40	Middle Eocene			Regadera				hiatus
45	Middle Eocene
50	Early Eocene		Socha		Los Cuervos				Deltaic (Los Cuervos)	260 m (850 ft) (Los Cuervos)	Seal Source	[12][16]
55	Late Paleocene	PETM 2000 ppm CO₂	Los Cuervos	Bogotá	Los Cuervos			Gualanday	Deltaic (Los Cuervos)	260 m (850 ft) (Los Cuervos)	Seal Source
60	Early Paleocene	SALMA	Barco	Guaduas	Barco		Rumiyaco	Gualanday	Fluvial (Barco)	225 m (738 ft) (Barco)	Reservoir	[9][10][13][12][17]
65	Maastrichtian	KT extinction	Catatumbo	Guadalupe				Monserrate	Deltaic-fluvial (Guadalupe)	750 m (2,460 ft) (Guadalupe)	Reservoir	[9][12]
72	Campanian	End of rifting	Colón-Mito Juan					Monserrate				[12][18]
83	Santonian						Villeta/Güagüaquí
86	Coniacian
89	Turonian	Cenomanian-Turonian anoxic event	La Luna	Chipaque	Gachetá	hiatus			Restricted marine (all)	500 m (1,600 ft) (Gachetá)	Source	[9][12][19]
93	Cenomanian	Rift 2		Chipaque	Gachetá				Restricted marine (all)	500 m (1,600 ft) (Gachetá)	Source
100	Albian			Une	Une		Caballos		Deltaic (Une)	500 m (1,600 ft) (Une)	Reservoir	[13][19]
113	Aptian		Capacho	Fómeque			Motema	Yaví	Open marine (Fómeque)	800 m (2,600 ft) (Fómeque)	Source (Fóm)	[10][12][20]
125	Barremian	High biodiversity	Aguardiente	Paja					Shallow to open marine (Paja)	940 m (3,080 ft) (Paja)	Reservoir	[9]
129	Hauterivian	Rift 1	Tibú- Mercedes	Las Juntas	hiatus				Deltaic (Las Juntas)	910 m (2,990 ft) (Las Juntas)	Reservoir (LJun)	[9]
133	Valanginian		Río Negro	Cáqueza Macanal Rosablanca					Restricted marine (Macanal)	2,935 m (9,629 ft) (Macanal)	Source (Mac)	[10][21]
140	Berriasian		Girón	Cáqueza Macanal Rosablanca					Restricted marine (Macanal)	2,935 m (9,629 ft) (Macanal)	Source (Mac)
145	Tithonian	Break-up of Pangea	Jordán	Arcabuco	Buenavista Batá		Saldaña		Alluvial, fluvial (Buenavista)	110 m (360 ft) (Buenavista)	"Jurassic"	[13][22]
150	Early-Mid Jurassic	Passive margin 2	La Quinta	Montebel Noreán	hiatus		Saldaña		Coastal tuff (La Quinta)	100 m (330 ft) (La Quinta)		[23]
201	Late Triassic	Passive margin 2	Mucuchachi	Montebel Noreán			Payandé					[13]
235	Early Triassic	Pangea		hiatus							"Paleozoic"
250	Permian	Pangea
300	Late Carboniferous	Famatinian orogeny						Cerro Neiva ()				[24]
340	Early Carboniferous	Fossil fish Romer's gap		Cuche (355-385)	Farallones ()			Cerro Neiva ()	Deltaic, estuarine (Cuche)	900 m (3,000 ft) (Cuche)
360	Late Devonian	Passive margin 1	Río Cachirí (360-419)	Cuche (355-385)	Farallones ()			Ambicá ()	Alluvial-fluvial-reef (Farallones)	2,400 m (7,900 ft) (Farallones)		[21][25][26][27][28]
390	Early Devonian	High biodiversity	Floresta (387-400) El Tíbet					Ambicá ()	Shallow marine (Floresta)	600 m (2,000 ft) (Floresta)
410	Late Silurian	Silurian mystery	Floresta (387-400) El Tíbet
425	Early Silurian	Silurian mystery	hiatus
440	Late Ordovician	Rich fauna in Bolivia	San Pedro (450-490)		Duda ()
470	Early Ordovician	First fossils	San Pedro (450-490)	Busbanzá (>470±22) Chuscales Otengá	Guape ()		Río Nevado ()	Hígado () Agua Blanca Venado (470-475)				[29][30][31]
488	Late Cambrian	Regional intrusions	Chicamocha (490-515)	Quetame ()	Ariarí ()		SJ del Guaviare (490-590)	San Isidro ()				[32][33]
515	Early Cambrian	Cambrian explosion		Quetame ()				San Isidro ()				[31][34]
542	Ediacaran	Break-up of Rodinia		pre-Quetame		post-Parguaza		El Barro ()	Yellow: allochthonous basement (Chibcha Terrane) Green: autochthonous basement (Río Negro-Juruena Province)		Basement	[35][36]
600	Neoproterozoic	Cariri Velhos orogeny	Bucaramanga (600-1400)				pre-Guaviare					[32]
800	Neoproterozoic	Snowball Earth										[37]
1000	Mesoproterozoic	Sunsás orogeny			Ariarí (1000)			La Urraca (1030-1100)				[38][39][40][41]
1300		Rondônia-Juruá orogeny			pre-Ariarí	Parguaza (1300-1400)		Garzón (1180-1550)				[42]
1400			pre-Bucaramanga					Garzón (1180-1550)				[43]
1600	Paleoproterozoic					Maimachi (1500-1700)		pre-Garzón				[44]
1800		Tapajós orogeny				Mitú (1800)						[42][44]
1950		Transamazonic orogeny				pre-Mitú						[42]
2200		Columbia
2530	Archean	Carajas-Imataca orogeny										[42]
3100	Archean	Kenorland
Sources

Legend

group
important formation
fossiliferous formation
minor formation
(age in Ma)
proximal Llanos (Medina)[note 1]
distal Llanos (Saltarin 1A well)[note 2]

Notes and references

Notes

based on Duarte et al. (2019)[45], García González et al. (2009),[46] and geological report of Villavicencio[47]
based on Duarte et al. (2019)[45] and the hydrocarbon potential evaluation performed by the UIS and ANH in 2009[48]

References

Acosta & Ulloa, 2001, p.64
Lamus Ochoa et al., 2013, p.29
Lamus Ochoa et al., 2013, p.34
Lamus Ochoa et al., 2013, p.32
Lamus Ochoa et al., 2013, p.22
Lamus Ochoa et al., 2013, p.35
Caballero et al., 2010, p.74
Acosta Garay et al., 2002, p.49
García González et al., 2009, p.27
García González et al., 2009, p.50
García González et al., 2009, p.85
Barrero et al., 2007, p.60
Barrero et al., 2007, p.58
Plancha 111, 2001, p.29
Plancha 177, 2015, p.39
Plancha 111, 2001, p.26
Plancha 111, 2001, p.24
Plancha 111, 2001, p.23
Pulido & Gómez, 2001, p.32
Pulido & Gómez, 2001, p.30
Pulido & Gómez, 2001, pp.21-26
Pulido & Gómez, 2001, p.28
Correa Martínez et al., 2019, p.49
Plancha 303, 2002, p.27
Terraza et al., 2008, p.22
Plancha 229, 2015, pp.46-55
Plancha 303, 2002, p.26
Moreno Sánchez et al., 2009, p.53
Mantilla Figueroa et al., 2015, p.43
Manosalva Sánchez et al., 2017, p.84
Plancha 303, 2002, p.24
Mantilla Figueroa et al., 2015, p.42
Arango Mejía et al., 2012, p.25
Plancha 350, 2011, p.49
Pulido & Gómez, 2001, pp.17-21
Plancha 111, 2001, p.13
Plancha 303, 2002, p.23
Plancha 348, 2015, p.38
Planchas 367-414, 2003, p.35
Toro Toro et al., 2014, p.22
Plancha 303, 2002, p.21
Bonilla et al., 2016, p.19
Gómez Tapias et al., 2015, p.209
Bonilla et al., 2016, p.22
Duarte et al., 2019
García González et al., 2009
Pulido & Gómez, 2001
García González et al., 2009, p.60

Bibliography

See also sources for the correlation table

Acosta Garay, Jorge, and Carlos E. Ulloa Melo. 2001. Geología de la Plancha 227 La Mesa - 1:100,000, 1–80. INGEOMINAS.
Acosta Garay, Jorge Enrique; Rafael Guatame; Juan Carlos Caicedo A., and Jorge Ignacio Cárdenas. 2002. Geología de la Plancha 245 Girardot - 1:100,000, 1–101. INGEOMINAS.
Caballero, Víctor; Mauricio Parra, and Andrés Roberto Mora Bohórquez. 2010. Levantamiento de la Cordillera Oriental de Colombia durante el Eoceno tardío – Oligoceno temprano: Proveniencia sedimentaria en el Sinclinal de Nuevo Mundo, Cuenca Valle Medio del Magdalena, 45–77. 32; Boletín de Geología.
Lamus Ochoa, Felipe; Germán Bayona; Agustín Cardona, and Andrés Mora. 2013. Procedencia de las unidades cenozoicas del Sinclinal de Guaduas: implicación en la evolución tectónica del sur del Valle Medio del Magdalena y orógenos adyacentes, 1–42. 35; Boletín de Geología.

Maps

Barrero, Darío, and Carlos J. Vesga. 2010. Plancha 207 - Honda - 1:100,000, 1. INGEOMINAS. Accessed 2017-06-06.
Barrero, Darío, and Carlos J. Vesga. 2010. Plancha 226 - Líbano - 1:100,000, 1. INGEOMINAS. Accessed 2017-06-06.
Ulloa, Carlos E.; Erasmo Rodríguez, and Jorge E. Acosta. 1998. Plancha 227 - La Mesa - 1:100,000, 1. INGEOMINAS. Accessed 2017-06-06.
Acosta, Jorge E.; Rafael Guatame; Oscar Torres, and Frank Solano. 1999. Plancha 245 - Girardot - 1:100,000, 1. INGEOMINAS. Accessed 2017-06-06.

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[48] sed on Duarte et al. (2019)[45], García González et al. (2009),[46] and geological report of Villavicencio[47]

[50] sed on Duarte et al. (2019)[45] and the hydrocarbon potential evaluation performed by the UIS and ANH in 2009[48]

[Memoria227_p64-1] Acosta & Ulloa, 2001, p.64

[2] Lamus Ochoa et al., 2013, p.29

[3] Lamus Ochoa et al., 2013, p.34

[4] Lamus Ochoa et al., 2013, p.32

[5] Lamus Ochoa et al., 2013, p.22

[6] Lamus Ochoa et al., 2013, p.35

[7] Caballero et al., 2010, p.74

[Memoria245_p49-8] Acosta Garay et al., 2002, p.49

[UISANH2009_p27-9] García González et al., 2009, p.27

[UISANH2009_p50-10] García González et al., 2009, p.50

[UISANH2009_p85-11] García González et al., 2009, p.85

[ANH2007_p60-12] Barrero et al., 2007, p.60

[ANH2007_p58-13] Barrero et al., 2007, p.58

[Plancha111_p29-14] Plancha 111, 2001, p.29

[Plancha177_p39-15] Plancha 177, 2015, p.39

[Plancha111_p26-16] Plancha 111, 2001, p.26

[Plancha111_p24-17] Plancha 111, 2001, p.24

[Plancha111_p23-18] Plancha 111, 2001, p.23

[Pulido2001_p32-19] Pulido & Gómez, 2001, p.32

[Pulido2001_p30-20] Pulido & Gómez, 2001, p.30

[Pulido2001_pp21_26-21] Pulido & Gómez, 2001, pp.21-26

[Pulido2001_p28-22] Pulido & Gómez, 2001, p.28

[Correa2019_p49-23] Correa Martínez et al., 2019, p.49

[Plancha303_p27-24] Plancha 303, 2002, p.27

[Terraza2008_p22-25] Terraza et al., 2008, p.22

[Plancha229_pp46_55-26] Plancha 229, 2015, pp.46-55

[Plancha303_p26-27] Plancha 303, 2002, p.26

[Moreno2009_p53-28] Moreno Sánchez et al., 2009, p.53

[Figueroa2015_p43-29] Mantilla Figueroa et al., 2015, p.43

[Manosalva2017_p84-30] Manosalva Sánchez et al., 2017, p.84

[Plancha303_p24-31] Plancha 303, 2002, p.24

[Figueroa2015_p42-32] Mantilla Figueroa et al., 2015, p.42

[Arango2012_p25-33] Arango Mejía et al., 2012, p.25

[Plancha350_p49-34] Plancha 350, 2011, p.49

[Pulido2001_pp17_21-35] Pulido & Gómez, 2001, pp.17-21

[Plancha111_p13-36] Plancha 111, 2001, p.13

[Plancha303_p23-37] Plancha 303, 2002, p.23

[Plancha348_p38-38] Plancha 348, 2015, p.38

[Plancha367_414_p35-39] Planchas 367-414, 2003, p.35

[Toro2014_p22-40] Toro Toro et al., 2014, p.22

[Plancha303_p21-41] Plancha 303, 2002, p.21

[Bonilla2016_p19-42] Bonilla et al., 2016, p.19

[GeoMap2015_p209-43] Gómez Tapias et al., 2015, p.209

[Bonilla2016_p22-44] Bonilla et al., 2016, p.22

[Duarte2019-45] Duarte et al., 2019

[UISANH2009-46] García González et al., 2009

[Pulido2001-47] Pulido & Gómez, 2001

[UISANH2009_p60-49] García González et al., 2009, p.60