Basin Development and Tectonic History of the Middle Magdalena Valley

Basin development and tectonic history of the Middle Magdalena Valley

Nomenclatura estándar del Standard Nomenclature for Middle ISC 2018 Valle Medio del Magdalena - Magdalena Valley - Colombia ICS - IUGS Colombia, Servicio Geológico L.G. Morales et al., 1958 Colombiano, 2019

Maastrichtiano Formación Umir 72

Umir Shale

Campaniano Formación La Renta

Santoniano 86 Galembo Member Formación Galembo Coniaciano La Luna 90 Fm. Pujamana Member Formación Pujamana Turoniano Formación Salada Salada Member 94

Cenomaniano Formación El Salto Salto Limestone 100

Formación Simití Albiano Simití Shale Fm. Tablazo

113 Tablazo Limestone Basal Formación La Paja L i Aptiano m e Paja Formation s t 125 o n Barremiano e Rosa Blanca Fm. 129

Gr. Hauteriviano 133

Valanginiano Formación Rosa Blanca Tambor Formation 140

Berriasiano Formación Cumbre

145 Formación Los Santos

“Howewer, as our studies continue, more and more concealed breaks become apparent”

Dereck Victor Ager Portadilla: Standard nomenclature for the Middle Magdalena Valley adopted by the Servicio Geológico Colombiano.

Citación Etayo-Serna, Fernando. 2019. “Basin development and tectonic history of the Middle Magdalena Valley”. En Estudios geológicos y paleontológicos sobre el Cretácico en la región del embalse del río Sogamoso, Valle Medio del Magdalena, dirección científica y edición de Fernando Etayo-Serna. Compilación de los Estudios Geológicos Oficiales en Colombia vol. XXIII. Bogotá: Servicio Geológico Colombiano. Basin development and tectonic history of the Middle Magdalena Valley Fernando Etayo-Serna 8 Hans Stille's work initiated tectonic studies in the basin” (Barrero et al. 2007) of late Cenozoic age Middle Magdalena Valley and introduced the word (Cáceres, Cediel and Etayo-Serna 2003) (fig. 1). graben (Hubach 1929). Years later, Harrison wro- te: “The Upper Magdalena Valley is a trough like The tectonic framework of the MMV basement in- depression or Graben (1930, 399. Notice the equi- termittently affected its stratigraphic architectu- vocal Upper) … … would recall the northern end of the Red Sea”. According modern speculations not based on any direct ob- to Harrison, this[ ] that“trench if could … brokebe flooded down [ in] early re.servation More field and informationat the same istime, necessary as advised to validate by J. T. Tertiary times” (op. cit., 408). Likewise, pre-Paleo- Wilson (1990), we should not permit “Neglect of zoic and Paleozoic rocks of[ Colombia] were named what is already known”. basement, while cover was used for rocks of Meso- zoic to Pleistocene age (Hubach 1929, after Stille INTERPLAY OF TECTONISM AND SEA 1907). The acceptance of a Tertiary age for the LEVEL CHANGES IN THE MMV DURING MMV led to the adoption of Dana's geosynclinal terminology to name the space of deposition of THE CRETACEOUS Cretaceous sediments in the MMV (Hubach 1929; Cizancourt 1933; Morales and The Colombian Pe- In a plate tectonic setting, the Middle Magdalena Va- troleum Industry 1958; Bürgl 1961; Julivert 1961). lley was generated during the “extensional stage” of a Late Triassic to Jurassic rifting episode that affec- A thorough analysis of the distribution of Creta- ted northwestern South América (Cáceres, Cediel ceous sedimentary rocks in Colombia (Etayo, Ren- and Etayo-Serna 2003) (fig. 1). The original structu- zoni and Barrero 1969, 1976) showed that these re of the MMV is that of an asymmetric rift that pro- gressively slants to the west. Proximity to the faulted (1983) reintroduced the idea of a graben, adding and raised block of the Santander Massif has caused rocksthat it didwas notactive fit since a geosynclinal the Early Cretaceous, outline. Fabre and up and down movements of basement blocks like pia- renamed it the Magdalena-Tablazo Basin. no keys, which caused the following features. 1) An angular unconformity between Cretaceous Los San- Inasmuch as Harrison's paper was included in Sec- tion VI-Rift Valleys of the 15th International Geo- Schuchert 1935; Julivert and Téllez 1963; Cediel logical Congress in Pretoria, terms such as Edward tos1968; and Laverde Jurassic 1995; Jordán Rolón Formations and Carrero (Notestein 1995) (fig. in Suess's graben and J. W. Gregory's rift (Willis 1928) 2A). 2) A disconformity between the lower upper Va- become almost synonymous and commutative in langinian Carrizal Member and the lower Hauteri- the geological literature on Colombia (Sarmiento fig. Rojas 2001; Toro et al. 2002; Rolón 2004; Barrero 2B). 3) Condensation of middle Barremian beds and et al. 2007). viana paraconformity Zo Member ofbetween the Rosa these Blanca and theFormation upper lower ( - OVERVIEW OF THE CRETACEOUS IN rrasse and Etayo-Serna 2013) (fig. 2D). 4) A para- THE MIDDLE MAGDALENA VALLEY Aptianconformity beds between of the La the Paja cuspidal Formation beds (Gaona, of the MauRosa

The Río Magdalena basin consists of three geomor- fig. 2C). 5) Progra- phically distinct sectors, each with a different geo- Blancading and Formation retrograding and basalsequences upper in lower the upperBarremian beds logical history: (1) the south sector or Upper Mag- beds of the La Paja Formationfig. ( 3). 6) A composite dalena Valley, extending from the riverhead to - Honda, occupies the axial domain of a Mesozoic oftion, the upper Tablazo lower Formation Albian (fig. ( 2E). 7) Beveled contact back-arc; (2) the middle sector or Middle Magdale- hardground surface at the top of the Tablazo Forma na Valley, extends from Honda to El Banco and occupies the Mesozoic rifted central part of Colombia; Itbetween has been the demonstrated Simití and El Salto that Formations.“Compressional tec- and (3) the northeast lower sector, the Lower Mag- tonics … controlled the stratigraphic and structu- dalena Valley, goes from El Banco to Barranquilla ral attributes of the southern Middle Magdalena Va- and developed over a “triangular transtensional lley Basin[ ] since 70 Ma” (Gómez et al. 2003, 146).

415 Servicio Geológico Colombiano | Fernando Etayo-Serna

Figure 1. Taken from: Facies distribution and tectonic setting through the Phanerozoic of Colombia (Cáceres, Cediel and Etayo-Serna 2003).

416 Capítulo 8 | MMV - Basin Development

Figure 2C. Paraconformity between medial beds of the La Paja Formation (organic-rich marlstone, calcareous clay shales and clay shales) of upper lower Aptian age overlying condensed middle Barremian wackestone, Curití Quarry. Photo by F. Etayo-Serna (Gaona, Maurrasse and Etayo-Serna 2013).

Figure 2D. Paraconformity between cuspidal beds of the Rosa Blanca Forma- tion and basal beds of the La Paja Formation. Private road from Los Santos to El Carrancho gypsum mine. Photo by D. Montoya (see D. Montoya 2019a).

Figure 2E. Composite hardground surface at top of the Tablazo Formation. Figure 2A. Angular unconformity between moderately dipping Jordán Formation Eastern side of Lebrija-San Vicente de Chucurí road, near the bridge over the beds and horizontal Los Santos Formation. Photo taken from N scarp of the Chicamo- Sogamoso River (N: 1.269.645°, E: 1.081.053°, Z: 352 m). Photo by D. Montoya cha River, Camino del Roto, looking SE. (see fig. 4). Photo by F. Etayo-Serna. (see Montoya 2019b; Immenhauser et al. 2000, fig. 11).

Figure 2B. Disconformity between the upper beds of the Carrizal Member, slightly bent, and bed P at the base of the Zo Member, both of the Rosa Blanca Formation. W side of El Platanalito Creek near its confluence with the Sogamoso River. Photo by D. Montoya (Etayo- Serna and Guzmán Ospitia 2019).

417 Servicio Geológico Colombiano | Fernando Etayo-Serna

Segmento VII

Segmento V

Figure 3A. View of segments VII to V of the Tablazo Formation. A cliff section at the junction of the highway to San Vicente de Chucurrí and the road to Betulia (Estadero El Nuevo Ramo, km 22+200). Photography by D. Montoya, taken from the southern end of the bridge over Quebrada El Ramo. Notice the increase in bed thickness downdip in a fan-like arrangement from the top of the hill toward the river level.

Figure 3B. Oblique close-up picture to show the internal stratification of segment V of the Tablazo Formation. Observe the primary inclination of the bedding: sediments accumulated on a tilted bottom reflecting some significant tectonic episo- Figure 3C. Outcrop of stratigraphic segment V (conjunto N2 -dark- and conjun- de, as demonstrated by the truncation at the top of both sets of beds (Ravnås and to O -light-) of the Tablazo Formation to show the fan-shaped arrangement of Steel 1998, fig. 2). Roadside outcrop in front of Estadero El Nuevo Ramo. beds. Cerro El Tablazo (D. Montoya, this book 2019b, fig. 90A).

418 Capítulo 8 | MMV - Basin Development

- - quence by the occurrence of Mediterranean short-lived ammoni- racterized by the alternation of dark calcareous and argilla- Globaltes of the sea early level late rises Valanginian seem reflected Saynoceras in the MMV verrucosum stratigraphic ( se , Atceous the typemudstones section,. In the segment La Paja I,Formation calcareous (4), mudstones 290 m, is chaare 1841), the late early Barremian Nicklesia pulchella ( , predominant, with organic matter and abundant Dasyclada- 1841) and Parasaynoceras horridum ( , 1850) (Etayo-SerOrbigny- cean algae remains. Segment II has similar lithology but na 1993; 2019), and the early middle Albian OxytropidocerasOrbigny (Mi- rapelia) mirapelianum ( , 1850)Orbigny (Orbigny, 1842; Rawson and veins. Segment III consists of predominantly argilla- 1993; Etayo-Serna 1993). It must be said here that oceanic surface showsceous mudstones lenses of fibrous with organic calcite matter. and abundant Segment gypsum IV comprises lenses waters (Tethyan) were circulatingOrbigny from E to W in the Early Creta- tabular thick-bedded calcareous mudstone (bindstones) in- terbedded with metric argillaceous mudstones. Segment V is composed of argillaceous mudstones with organic matter THEceous (Luyendyk,MAPPABLE Forsyth LITHOLOGIC and Phillips 1972; UNITS Etayo-Serna 1983). and conspicuous recrystallized bindstones toward its upper AND THE GEOLOGICAL HISTORY OF THE MMV - part.mation The is accumulationdated lower Barremian of the La Paja to middle Formation Barremian, took place ex- The earliest Cretaceous lithostratigraphic unit recorded in the including the supratidal the lowermost to lower Barremian intertidal for domain. segment The I. La The Paja upper For Hidrosogamoso region ( and ) is represented by the figs. 2A 4 Barremian and lower Aptian ammonite zones are not represented. Segment II represents the upper part of the lower Etayo-Serna and Rodríguez 1985). Immediately above follows Aptian, while Segment III corresponds to the upper Aptian. continental siliciclastic Los Santos Formation (1) (Cediel 1968; Segment IV and the lower part of Segment V correspond to palynomorphs have been recovered at quebrada Aguablanca the cuspidal upper Aptian, while the rest of segment V co- the(zanjón transitional Aguas Gordas): Cumbre Inaperturopollenites Formation (2), from sp., whichAraucariacites diverse rresponds to the lower lower Albian (Montoya 2019a). sp., Classopollis sp. (probably Corollina ecopetrolis Olivella), Ephedripites sp. and the spore Cyathidites sp. (D. Pons in Etayo- - morphologic unit, generates four cuestas and three valleys; Platanalito gypsum mine yields shark teeth and bivalves simi- The270 m.Tablazo The elements Formation that (5), form a noticeable cuestas are stratigraphic calcareous andmudsto geo- Serna 1989). Outcrops of the Cumbre Formation on the road to ne, wackestone and packstone lar to those of the Batá Formation (Etayo-Serna et al. 2003). - forming units are predominantlywith made minor of proportionsargillaceous ofmuds fine- tion (3) initiates with the Lagunetas Member (new), which shows toneto very. The fine occurrence quartzitic of sandstone; microcodium on microfossilsthe contrary, and the nodular valley- an E to W change from sabkha deposits (supratidal) to stromato- In ascending order above the Cumbre, the Rosa Blanca Forma rubble are reminders of subaerial exposure. Occasional orga- litic limestone (subtidal); 80 m. The age of the Los Santos and nic matter is common at levels I to III, from which it decreases. - Walter's principle of contiguity of facies, is considered Berriasian. mation. Tablazo sediments accumulated between the suprati- Cumbre Formations and the Lagunetas Member, based on Thedal and lower middle part partsof the ofunit an looks oscillating transitional shallow to carbonate the La Paja ramp. For Sealing an erosional scar, the oolitic calcareous basal bed of the Carrizal Member (new) follows, composed of conspicuous Thalas- sinoides beds and decimetric wackestone beds in alternation with The(Hubbard Tablazo 1988; Formation Montoya represents 2019b) (fig. the 3 ).lower Albian and is an calcareous mudstone; 110 m. The age of this member ranges from example of vertical tectonics influencing accumulation lower Valanginia to upper Valanginian, pars. Above the Carrizal Member in disconformable contact follows the Zo Member (new), mudstone (shales), interspersed throug- composed of pluridecimetric cross-bedded packstone and wac- The Simití Formation (6), 125 m, consists of dark, terrigenous, kestone that alternate with terrigenous mudstone; the occurrence muscovitic and fissile of benthonic foraminifera is noticeable; 40 m. houtthan not the glauconitic. unit with fine-grained, The accumulation quartzitic of this sandstones unit started with af- calcareouster an interlude cement of nondeposition (Etayo-Serna 2019,and subaerial fig. 5A), exposure more often of In a rapid transition follows the El Sapo Member (new), composed fig. 2E): sea level rose of conspicuous Thalassinoides beds and decimetric wackestone in possibly as an indirect consequence of the separation of Afri- alternation with terrigenous calcareous mudstone; 80 m. theca from top bed South of theAmerica; Tablazo this Formation way, the ( Tablazo ramp was ra- pidly inundated and at the same time received a great input of by the Zapatoca Member (new), composed of ferruginous Themetric upper sandstones part of the in Rosathe lower Blanca part; Formation 35 m, and is represented wackestone fine detrital particles from the mud discharges of a large and packstone of bivalves at the top; 25 m. southernrepresents river the lowerflowing middle E to Albian,W (Numpaque pars. Exposures and Rolón are 1998, poor. fig. 5). Based on its ammonite content, the Simití Formation Members Zo, El Sapo and Zapatoca are dated Lower Hauteri- The El Salto limestone (7) lies immediately above the Simití vian (Etayo Serna and Guzmán Ospitia 2019). shales with a thickness of 7 m. It is a unit not formally establis-

419 Servicio Geológico Colombiano | Fernando Etayo-Serna

SERVICIO GEOLÓGICO COLOMBIANO

Figure 4. Map of localities mentioned in the text. hed by Morales and The Colombian Petroleum Industry often mixed with limestone, and a strong bituminous odor yielded by the rock when freshly broken open” (Wheeler - 1929). Large discoidal calcareous concretions in the lower (1958)mestone— but haswackestone great significance and packstone to the with geologic Rhynchostreon history of there- segment. Benueites species of ammonites indicate a lower MMV.mains—thickens From E to NW, from Sogamoso 7 m to 50 River m and to at Simití, the same the timeEl Salto over li- Turonian age (Terraza 2019). lies younger beds; that is to say, its base makes a bevel in the - - tion with coeval slanting to the west of the whole MMV base- tated formation. “It consists of black thin bedded calcareous Simitíment (Terraza Formation 2019). illustrating a probable direct causal connec shale.Pujamana Hills Formation composed (9); of this57 m shale - 111 slumpm. This badly unit is”. anotherWheeler res re- ports 325 m of thickness, but he himself advised “that amount - might be excessive”. This same section was remeasured by Te- ted for this unit. It is “composed of hard, black thin bedded, rraza (2019). At this point, it is worth remembering Ernst Cloos' Salada Formation (8); 118 m. The formation status is resta caveat (1942, 402): “ … the question arises whether or not thic- on outcrop [...] presence of concretions and streaks of pyrite, knesses as measured in folded regions are thicknesses of depo- finely laminated-limy shales that appear very much as slates [ ] 420 Capítulo 8 | MMV - Basin Development sition”. Specimens of the ammonites Subprionocyclus support a “South Tethyan phosphorite province” that included Colom- referring this unit to the upper Turonian. bia (Terraza 2019; Pufahl et al. 2003).

The last Cretaceous unit (12) that crops out in the Hidroso- Galembo is restated to the formation category. According Galemboto the precise Formation original (10); description 96 m - 177 “The m. Galembo In this book,is predo the- Colombian Petroleum Industry 1958, 655), which lies un- minantly a limestone formation … the limestones are gamoso region is the Umir Formation (Morales and The in angular unconformity or in paraconformity (Maughan bituminous, occasionally shaly, and[ ] commonly occur in conformably on the La Renta or Galembo Formations 2019, hard,beds 4black, to 6 inches(thin bedded), thick separated thinly laminated, by thin or fine minute textured, shale Bucaramanga-Barrancabermeja road, is 300 m thick and partings. This rhythmic type of bedding is distinctly cha- et al. 1979, fig. 6). The Umir, as measured along the new- racteristic of the formation in the Sogamoso area … these - limestones yield a distinct odor of oil when freshly broken” appearstion consists to be mainlyunconformably of dark coveredto medium by theand Lisama light grayFor (Wheeler 1929). A rich ammonite collection has[ ] been mationmudstone of Paleocene palynological age. The Umir Forma- gathered: Prionocycloceras, Protexanites, Miotexanites, Pe- ned muscovitic siltstone and sandstone in thin beds, incre- roniceras (Zuluiceras) represent the Coniacian, while Texa- asing in thickness, light gray and to abundancegreenish gray upsection. fine to medium Interspersed grai nites, Plesiotexanites and Cocuyites indicate the Santonian cuneiform coal beds up to 1.5 m thick, herringbone cross- (see Terraza, chap. 5, this book). lamination and oscillation ripples are conspicuous. Locally, gastropods, bivalve and ammonite remains are found (Pé- rez 2014). Sphenodicus pleurisepta (Conrad 1857) is relati- that the separation of the phosphatic and siliceous sequen- vely frequent (Morales and The Colombian Petroleum In- Lace—of Renta the Formation upper part (11); of the 45 Galembo—into m - 77 m. It has a been distinct concluded forma- dustry 1958, 656; Moreno-Sánchez 2019). According to - Petters (1955), “brackish and fresh water deposits of Maes- trichtian (sic) (Navarro) age were laid down along the wes- tionthere is were necessary. particular The oceanographic La Renta Formation conditions has greatthat favored paleo tern margin of the Bucaramanga Massif”. geographic significance because during the Campanian,

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