In the Cocinetas Basin, several fossiliferous stratigraphic units have been registered, providing an abundance of marine and continental vertebrate and invertebrate fossil fauna assemblages. The Uitpa, Jimol, Castilletes and Ware Formations contain numerous fossils of Neogene and Quaternary ages, both before and after the Great American Biotic Interchange (GABI), presenting new insights in the understanding of the variation in South American fauna related to the uplift of the Panama Block and the connection of North America and South America.
Description
The Serranía de Macuira, with its natural park, is the northern boundary of the Cocinetas Basin. The mountain range has a unique climate in the region, hosting the only dry forests in an overall desert environment.
The bounding fault to the south, the dextral Cuisa Fault with a lateral displacement of 15 kilometres (9.3 mi),[4] has an extension of approximately 80 kilometres (50 mi) along a roughly east–west axis and the fault continues to the east underneath the Gulf of Venezuela. The fault is partly covered by Oligocene sediments.[5] The northern boundary of the pull-apart basin is formed by the roughly northwest–southeast-trending Macuira Fault, with an extension of about 40 kilometres (25 mi). The sinistral oblique fault has a displacement of about 3 kilometres (1.9 mi) and uplifted the northeastern Serranía de Macuira.[6]
The basin is situated in its entirety in the municipalityUribia of the department of La Guajira. The southernmost tip of the basin borders the Venezuelan state of Zulia.[3] The villages of Uitpa, Castilletes and Puerto López are located inside the basin.[3][7][8]
The present-day climate in the basin is very dry and hot (Köppen: BSh), being in the desert of La Guajira. The temperature in tropical northern South America does not vary much across the year. July is the hottest month with an average temperature of 30.6 °C (87.1 °F) and January has a mean of 27.9 °C (82.2 °F). Rain is sparse throughout the year, except for October, the wettest month with 109 millimetres (4.3 in) of precipitation.[9] Alta Guajira is the driest region of Colombia and long periods of drought are common.[10]
Sedimentation in the basin started during the Middle to Late Eocene with the Macarao Formation and continued again during the Late Oligocene, when the Siamaná Formation, a sequence of conglomerates and thick carbonates, was deposited. Overlying the Siamaná Formation is the Early Miocene Uitpa Formation, a thick sequence of calcareous mudstone interbedded with lithic sandstones. The Uitpa Formation is covererd by the Miocene Jimol and Castilletes Formations, composed mostly of lithic sandstones and mudstones, that are in certain areas highly fossiliferous. The last phase of preserved sedimentation is represented by the Pliocene Ware Formation, defined in 2015 by Moreno et al.[15]
The Tertiary (Paleogene to Late Pleistocene) of South America is subdivided into an own stratigraphy; the South American land mammal ages, (SALMA). This subdivision is used throughout the continent to indicate certain geologic intervals based on the occurrences of specific land mammals.[16]
The lower part of the mostly Pliocene Ware Formation was deposited in a fluvio-deltaic coastal environment, where the carnivorous Chapalmalania foraged
The invertebrate fauna of the Castilletes Formation is highly similar not only to that of the underlying Jimol Formation, but also to the Cantaure Formation of Venezuela.[24] The Castilletes Formation was deposited in a shallow marine (estuarine, lagoonal, and shallow subtidal) to fluvio-deltaic environment with strong fluvial influence. The Castilletes Formation correlates with the upper Cerro Pelado and Querales Formations of the Venezuelan Falcón Basin. This unit is also correlative with the Cantaure Formation of the Paraguaná Peninsula in Venezuela.[25]
The marine invertebrate fauna of the Ware Formation shows a greater similarity with modern assemblages offshore of the Guajira Peninsula than with those of the
underlying units.[26] The base of the Ware Formation was deposited in a fluvio-deltaic environment, whereas the marine invertebrate assemblage at the top of the unit contains taxa typical of exposed open-ocean shoreface and nearshore settings, but with proximity to coral reef habitats. The Ware Formation correlates with the San Gregorio Formation in the Venezuelan Falcón Basin.[27]
The tectonic history of the Cocinetas Basin, a pull-apart basin formed on top of Mesozoicbasement underlain by oceanic crust, goes back to the Paleogene.[28] Farther to the south, in the Cesar-Ranchería Basin, the Paleocene, absent in the Cocinetas Basin, is represented by the first neotropic forest in the world, with megafauna as the largest recorded snake, Titanoboa cerrejonensis, with an estimated length of 14 metres (46 ft) and a weight of 1,135 kilograms (2,502 lb), today found in the Cerrejón Formation, dated to 60 to 58 Ma. It has been estimated on the basis of the fossil flora, pollen and large reptiles that the mean annual temperature was between 28.5 and 33 °C (83.3 and 91.4 °F) and yearly precipitation ranging from 2,260 to 4,640 millimetres (89 to 183 in) per year.[29]
North of the Oca Fault, the oldest sedimentary sequence of the Cocinetas Basin, the Macarao Formation, is the oldest sedimentary unit of both the higher La Guajira area (the Cocinetas Basin) as well as the lower La Guajira area. This formation was deposited in a phase that is informally called "rifting", because of the formation of half grabens in the Late Eocene, though no real rifting occurred in the area.[30] Shortly after deposition, during the Early Oligocene, the Macarao Formation was heavily deformed, creating the series of hills that today still surround the Cocinetas Basin.[31] This transtensional deformation was caused by the eastward movement of the Caribbean Plate along the South American Plate, when the Caribbean volcanic arc was located just north of the Cocinetas Basin.[32] The main fault movement forming the pull-apart basin of Cocinetas was caused by the dextral Cuisa Fault, active from the Paleocene to the Eocene.[28]
The transtensional phase of the Early Oligocene was followed by the deposition of the unconformably overlying Siamaná Formation, characterised by a basal sequence of conglomerates, indicating tectonic uplift in the provenance areas, followed by reefallimestones rich in corals and algae.[33] A new phase of transtension took place in the Early to Middle Miocene, when the Uitpa, Jimol and Castilletes Formations were deposited.[30] The initial phase of uplift of the Isthmus of Panama, has been dated to this period, at around 12 Ma.[34]
The Andean orogeny, represented by the tectonic uplift of the Colombian Eastern Ranges and its northern extension, the Serranía del Perijá, caused tilting and uplift in the Cocinetas Basin in the Late Miocene and Early Pliocene, when the Neogene hiatus separates the Castilletes Formation from the Ware Formation.[30] The end of the Neogene corresponded to a marine platform setting, interrupted by the presence of a series of highs; the present-day mountain ranges of the region. Between these elevated areas, reefal limestones were deposited in a relatively quiet marine environment.[35] During the Andean orogenic phase, the paleotemperatures in the basin dropped considerably; in the Baja Guajira area from 115 °C (239 °F) in the Early Miocene to 70 °C (158 °F) in the Late Miocene.[36] In the Late Miocene to Pliocene, the major faults to the southwest of the Cocinetas Basin, the Oca and Bucaramanga-Santa Marta Faults were tectonically active.[37]
Paleontology
The Uitpa Formation provided fossils of the kitefin shark (Dalatias licha)Fossils of Purussaurus were found in the Castilletes FormationNothrotherium is one of the many ground sloth genera found in the Ware Formation
The Cocinetas Basin has provided several new species and genera of vertebrates and invertebrates of which many are still studied in detail. The Uitpa, Jimol, Castilletes, and Ware Formations preserve both a diverse continental vertebrate and a rich marine invertebrate fossil record that documents paleoenvironmental change through the Neogene. This succession shows a broad pattern of changing depositional environments associated with the tectonic history of the Cocinetas Basin.[38] Paleobathymetric and paleoenvironmental analyses suggest that the lower Uitpa Formation accumulated in water depths ranging from 100 to 200 metres (330 to 660 ft), a deepening with respect to the underlying Siamaná Formation and leading to the collapse of coral reefs. This contrasts with an observed increase in sediment supply for the San Luis coral-reef ecosystems in the northwestern Falcón Basin.[39]
The Castilletes turtle fauna shares two taxa with the Middle Miocene La Venta Fauna (Chelus colombiana and Chelonoidis sp.), and one taxon with the Late Miocene of the Urumaco Formation and Western Amazonia areas. At least two hypotheses can be proposed to explain the early to middle Miocene geographical distribution of turtles in tropical South America. The first is based on the existence of the Pebas wetland system during the Middle Miocene, which could have served as a route for the dispersion of taxa facilitated by the connectivity between major and minor drainages, even with potential interruptions to this system due to the increasing uplifting of the Eastern Ranges of Colombia. Alternatively, the geographical distribution of tropical South American turtles during the Miocene can be explained as a relict of an extensive distribution reached during the Eocene or Oligocene and modified subsequently by the uplifting of the Andes and the changes in the pattern of the main river systems.[40]
The occurrence of Purussaurus and Mourasuchus in the early Middle Miocene Patajau and Kaitamana beds of the Castilletes Formation represent early records for lineages previously known from younger Laventan and Huayquerian faunas. These records expand the temporal range of high diversity gavialoid-caimanine assemblages into the early Middle Miocene. The Castilletes Formation record also expands the geographic range of Miocene endemic crocodilian faunas to latitudes equivalent to those of Central America.[41] The connections between hydrographic basins and the development of mega-wetland systems in equatorial South America allowed the long persistence of several lineages over an extensive geographical range. The extinction of gavialoids and specialized caimanines in equatorial South America was likely caused by the isolation and aridification of peripheral basins, together with the disappearance of mega-wetlands.[42]
The sloths from the Late Pliocene Ware Formation are represented by 12 specimens that belong to 5 taxa from the 4 families of ground sloths. Their body sizes span over two orders of magnitude, and they most likely featured various feeding strategies, documenting a highly diverse assemblage of sloths from the Neotropics. Although geographically close to the Isthmus of Panama, and temporally preceding the first phase of the Great American Biotic Interchange by only 200,000 to 400,000 years, the sloths for which unambiguous affinities were recovered are not closely related to the early immigrants found in North America before the first main pulse of the Great American Biotic interchange.[43] The registered giant capybaraHydrochoeropsis wayuu is the northernmost South American Pliocene hydrochoerine record and the nearest to the Panamanian bridge. The presence of this hydrochoerine, together with the fluvio-deltaic environment of the Ware Formation, suggests that during the Late Pliocene, the environment that dominated the Guajira Peninsula was more humid and with permanent water bodies, in contrast with its modern desert habitats.[44]
De Porta, Jaime (2003), "La formación del istmo de Panamá - su incidencia en Colombia", Revista de la Academia Colombiana de Ciencias Exactas, Físicas y Naturales, XXVII: 191–216
Wing, Scott L.; Herrera, Fabiany; Jaramillo, Carlos A.; Gómez Navarro, Carolina; Wilf, Peter; Labandeira, Conrad C. (2009), "Late Paleocene fossils from the Cerrejón Formation, Columbia ((sic)), are the earliest record of Neotropical rainforest", Proceedings of the National Academy of Sciences, 106 (44): 18627–18632, Bibcode:2009PNAS..10618627W, doi:10.1073/pnas.0905130106, PMC2762419, PMID19833876
Maps
Zuluaga, Carlos A.; Ochoa, Alberto; Muñoz, Carlos A.; Dorado, Camilo E.; Guerrero, Nathalia M.; Martínez, Ana M.; Medina, Paula A.; Ocampo, Edgar F.; Pinilla and Paula A. Ríos, Bibiana P. Rodríguez, Edward A. Salazar, Vladimir L. Zapata, Alejandro (2008), Plancha 3 - Puerto Estrella - 1:100,000, INGEOMINAS, p. 1, retrieved 2017-06-06{{citation}}: CS1 maint: multiple names: authors list (link)
Zuluaga, Carlos A.; Ochoa, Alberto; Muñoz, Carlos A.; Dorado, Camilo E.; Guerrero, Nathalia M.; Martínez, Ana M.; Medina, Paula A.; Ocampo, Edgar F.; Pinilla and Paula A. Ríos, Bibiana P. Rodríguez, Edward A. Salazar, Vladimir L. Zapata, Alejandro (2008), Plancha 5 - Bahía Portete - 1:100,000, INGEOMINAS, p. 1, retrieved 2017-06-06{{citation}}: CS1 maint: multiple names: authors list (link)
Zuluaga, Carlos A.; Ochoa, Alberto; Muñoz, Carlos A.; Dorado, Camilo E.; Guerrero, Nathalia M.; Martínez, Ana M.; Medina, Paula A.; Ocampo, Edgar F.; Pinilla and Paula A. Ríos, Bibiana P. Rodríguez, Edward A. Salazar, Vladimir L. Zapata, Alejandro (2008), Plancha 10 - Rancho Grande - 1:100,000, INGEOMINAS, p. 1, retrieved 2017-06-06{{citation}}: CS1 maint: multiple names: authors list (link)
Zuluaga, Carlos A.; Ochoa, Alberto; Muñoz, Carlos A.; Dorado, Camilo E.; Guerrero, Nathalia M.; Martínez, Ana M.; Medina, Paula A.; Ocampo, Edgar F.; Pinilla and Paula A. Ríos, Bibiana P. Rodríguez, Edward A. Salazar, Vladimir L. Zapata, Alejandro (2008), Plancha 10bis - Rancho Grande - 1:100,000, INGEOMINAS, p. 1, retrieved 2017-06-06{{citation}}: CS1 maint: multiple names: authors list (link)
Further reading
Bally, A.W.; Snelson, S. (1980), "Realms of subsidence", Canadian Society for Petroleum Geology Memoir, 6: 9–94
Barrero, Dario; Pardo, Andrés; Vargas, Carlos A.; Martínez, Juan F. (2007). Colombian Sedimentary Basins: Nomenclature, Boundaries and Petroleum Geology, a New Proposal. ANH. pp. 1–92.
