Changes

Very little is known about the pre-Late Jurassic history of the island except that the lower part of the San Cayetano clastics might be Lower Jurassic (163 Ma; [[:file:St58OverviewFG25.JPG|Figure 5]]). The San Cayetano must have been deposited over an initially [[rift]]ing [[basement]] that probably included fragments of continental crust as well as [http://geology.com/rocks/basalt.shtml basaltic] flows. This is supported by the sub-Neocomian [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000073 granodioritic] [[klippe]]n of La Rana, Tres Guanos, and Rancho Veloz and the occurrences of the El Sabalo and Nueva Maria [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?Term=tholeiite tholeitic basalt]s underlying the sedimentary section of the northern Rosario belt and Cifuentes* belt of the Sierra de Camajan.

Very little is known about the pre-Late Jurassic history of the island except that the lower part of the San Cayetano clastics might be Lower Jurassic (163 Ma; [[:file:St58OverviewFG25.JPG|Figure 5]]). The San Cayetano must have been deposited over an initially [[rift]]ing [[basement]] that probably included fragments of continental crust as well as [http://geology.com/rocks/basalt.shtml basaltic] flows. This is supported by the sub-Neocomian [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000073 granodioritic] [[klippe]]n of La Rana, Tres Guanos, and Rancho Veloz and the occurrences of the El Sabalo and Nueva Maria [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?Term=tholeiite tholeitic basalt]s underlying the sedimentary section of the northern Rosario belt and Cifuentes* belt of the Sierra de Camajan.

It can also be assumed that, prior to the deposition of the Upper Jurassic rocks, a large area of basement was exposed to the northwest, extending from Florida's Sarasota arch to the Maya Mountains. The nature of this basement is generally unknown, but it must have been of [http://geology.about.com/od/more_igrocks/a/granite.htm granitic] to [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000073 granodioritic] composition as indicated by the [[Arkose|arkosic]] nature of the San Cayetano Formation. In south Florida, several wells have penetrated an undifferentiated Jurassic–Triassic volcanic section and Paleozoic granite. The basement must also have included Paleozoic sediments known to outcrop in the Maya Mountains, present as fragments in San Cayetano conglomerates, and, perhaps, as exotics in the Cayo Coco Formation. The bulk of the San Cayetano Formation accumulated south of this basement high.

It can also be assumed that, prior to the deposition of the Upper Jurassic rocks, a large area of basement was exposed to the northwest, extending from Florida's Sarasota arch to the Maya Mountains. The nature of this basement is generally unknown, but it must have been of [http://geology.about.com/od/more_igrocks/a/granite.htm granitic] to [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000073 granodioritic] composition as indicated by the [[Arkose|arkosic]] nature of the San Cayetano Formation. In south Florida, several wells have penetrated an undifferentiated Jurassic–Triassic volcanic section and Paleozoic granite. The basement must also have included Paleozoic sediments known to outcrop in the Maya Mountains, present as fragments in San Cayetano [[conglomerate]]s, and, perhaps, as exotics in the Cayo Coco Formation. The bulk of the San Cayetano Formation accumulated south of this basement high.

The San Cayetano clastics could have originated from the Gulf of Mexico, as well as nearby South America. As already mentioned, some studies indicate that the southwestern part of the San Cayetano originated from the southwest, and the northeastern part originated from the northeast. Structural complexity makes source direction hard to evaluate.

The San Cayetano clastics could have originated from the Gulf of Mexico, as well as nearby South America. As already mentioned, some studies indicate that the southwestern part of the San Cayetano originated from the southwest, and the northeastern part originated from the northeast. Structural complexity makes source direction hard to evaluate.

Shallow-water platform carbonates, with some evaporites, continued to accumulate in the north (coastal area, [[Yaguajay belt|Yaguajay* belt]]). Elsewhere in central and western Cuba ([[Las Villas belt|Las Villas*]], southern [[Rosario belt]]s), the water was markedly deeper as indicated by the deposition of the [[Capitolio Formation|Capitolio*]] and [[Artemisa Formation]]s containing abundant [[nannoplankton]] (commonly rock forming) and other [http://www.merriam-webster.com/dictionary/pelagic pelagic] forms.

Shallow-water platform carbonates, with some evaporites, continued to accumulate in the north (coastal area, [[Yaguajay belt|Yaguajay* belt]]). Elsewhere in central and western Cuba ([[Las Villas belt|Las Villas*]], southern [[Rosario belt]]s), the water was markedly deeper as indicated by the deposition of the [[Capitolio Formation|Capitolio*]] and [[Artemisa Formation]]s containing abundant [[nannoplankton]] (commonly rock forming) and other [http://www.merriam-webster.com/dictionary/pelagic pelagic] forms.

Some tectonic activity extended into the [[Neocomian]] (132 Ma; see Figure 27), possibly associated with the rifting, and uplifted blocks south of the Yaguajay* belt. The result was denudation of previously deposited sediments as indicated by northward shedding of carbonate clastics ([[Sabanilla Fromation|Sabanilla* Formation]]), a southward increase in basement exposures (La Rana, Tres Guanos, Rancho Veloz), and deposition of the [[Jobosi]]* arkosic conglomerate. This basement could have been derived from a continental block, here named the La Rana block (after the best exposures) and similar to the Maya or Chortis blocks, that was overridden by later nappes.

Some tectonic activity extended into the [[Neocomian]] (132 Ma; see Figure 27), possibly associated with the rifting, and uplifted blocks south of the Yaguajay* belt. The result was denudation of previously deposited sediments as indicated by northward shedding of carbonate clastics ([[Sabanilla Fromation|Sabanilla* Formation]]), a southward increase in basement exposures (La Rana, Tres Guanos, Rancho Veloz), and deposition of the [[Jobosi]]* [[Arkose|arkosic]] [[conglomerate]]. This basement could have been derived from a continental block, here named the La Rana block (after the best exposures) and similar to the Maya or Chortis blocks, that was overridden by later nappes.

In central Cuba, the Upper Jurassic and Neocomian beds were only partially eroded. In western Cuba, shallow-bank carbonates, similar to those of the [[Vinas Group|Vinas* Group]], accumulated atop the La Rana [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000073 granodiorite] [http://en.wikipedia.org/wiki/Horst_%28geology%29 horst] and formed the Guajaibon–Sierra Azul belt. South of the La Rana basement horst, deep-water limestones of the Mayari, Collantes, and Cobrito Formations were deposited and preserved.

In central Cuba, the Upper Jurassic and Neocomian beds were only partially eroded. In western Cuba, shallow-bank carbonates, similar to those of the [[Vinas Group|Vinas* Group]], accumulated atop the La Rana [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000073 granodiorite] [http://en.wikipedia.org/wiki/Horst_%28geology%29 horst] and formed the Guajaibon–Sierra Azul belt. South of the La Rana basement horst, deep-water limestones of the Mayari, Collantes, and Cobrito Formations were deposited and preserved.

===Barremian===

===Barremian===

During the [[Barremian]], deposition of [[platform]] carbonates continued in the north, grading from shallow-water algal types, with fewer [[evaporite]]s, to [[breccia]]s. South, west, and possibly east of the Bahamas Platform, deep-water sedimentation of [http://www.merriam-webster.com/dictionary/pelagic pelagic] (nannoplankton) carbonates continued. However, because of the late Neocomian tectonic activity, conglomerates, derived from the previously deposited limestones in the Las Villas* belt and from the exposed granitic basement in the [[Cifuentes]]* belt to the south, became common. No Barremian sediments were deposited in some of the southern areas. However, the [http://geology.com/rocks/basalt.shtml basaltic] to intermediate flows possibly continued to accumulate over the southern part of the [[Wikipedia:Basic_rock|basic]] igneous basement.

During the [[Barremian]], deposition of [[platform]] carbonates continued in the north, grading from shallow-water algal types, with fewer [[evaporite]]s, to [[breccia]]s. South, west, and possibly east of the Bahamas Platform, deep-water sedimentation of [http://www.merriam-webster.com/dictionary/pelagic pelagic] (nannoplankton) carbonates continued. However, because of the late Neocomian tectonic activity, [[conglomerate]]s, derived from the previously deposited limestones in the Las Villas* belt and from the exposed granitic basement in the [[Cifuentes]]* belt to the south, became common. No Barremian sediments were deposited in some of the southern areas. However, the [http://geology.com/rocks/basalt.shtml basaltic] to intermediate flows possibly continued to accumulate over the southern part of the [[Wikipedia:Basic_rock|basic]] igneous basement.

===Aptian===

===Aptian===

During the [[Aptian]] (110 Ma; [[:file:St58OverviewFG28.JPG|Figure 8]]), deposition continued to be shallow-water marine along the north coast (Yaguajay* belt) with, farther to the north (Cayo Coco area) and as far as Oriente (Gibara area), some [http://www.merriam-webster.com/dictionary/pelagic pelagic] influence (Casablanca Group). Toward central and western Cuba, conditions continued to be pelagic. The pelagic and shallow-water conditions were separated by a conglomeratic breccia zone (Sagua la Chica* belt) representing a [[forereef]] facies, although reefs themselves are not common in outcrops.

During the [[Aptian]] (110 Ma; [[:file:St58OverviewFG28.JPG|Figure 8]]), deposition continued to be shallow-water marine along the north coast (Yaguajay* belt) with, farther to the north (Cayo Coco area) and as far as Oriente (Gibara area), some [http://www.merriam-webster.com/dictionary/pelagic pelagic] influence (Casablanca Group). Toward central and western Cuba, conditions continued to be pelagic. The pelagic and shallow-water conditions were separated by a [[Conglomerate|conglomeratic]] [[breccia]] zone (Sagua la Chica* belt) representing a [[forereef]] facies, although reefs themselves are not common in outcrops.

There was an influx of quartz- and mica-rich [[Turbidite|turbiditic]] detritus, possibly from the erosion of the previously formed basement high, which formed the La Esperanza, Polier, and Constancia* Formations. A southern Guajaibon–Sierra Azul carbonate bank may have been deposited.

There was an influx of quartz- and mica-rich [[Turbidite|turbiditic]] detritus, possibly from the erosion of the previously formed basement high, which formed the La Esperanza, Polier, and Constancia* Formations. A southern Guajaibon–Sierra Azul carbonate bank may have been deposited.

===Campanian-Maastrichtian===

===Campanian-Maastrichtian===

After the period of the [[Unconformity|disconformity]], [http://www.merriam-webster.com/dictionary/pelagic pelagic] conditions characterized the platform to deep-water province, which received massive, dominantly carbonate [[turbidite]] flows from the north (Lutgarda* Formation) and from the south (Amaro* and Cacarajicara formations) (67 Ma; [[:file:St58OverviewFG31.JPG|Figure 11]]). Over the [[Wikipedia:Basic_rock|basic]] igneous-volcanic province, local [http://www.merriam-webster.com/dictionary/provenance provenance] resulted in an abundance of fragmental rocks; that is, limestones toward the north (Penalver Formation) and volcanics toward the south. In the south, sedimentation was accompanied during the Maastrichtian by an outpouring of late orogenic [http://geology.com/rocks/basalt.shtml basaltic] flows and flow breccias (the Maastrichtian age of these flows disagrees with the current interpretation of most Cuban geologists, including Iturralde-Vinent, 1996). Toward the north, along the present outer line of clays, deposition of coarse [[Maastrichtian]] limestone conglomerate (Mayajigua* Formation) graded into fine-grained pelagic rocks. The basic igneous-volcanic province began its initial northward movement as indicated by [http://www.galleries.com/serpentine serpentine] detritus in the turbidites, by basic [http://www.geolsoc.org.uk/ks3/gsl/education/resources/rockcycle/page3598.html intrusive]-derived clastics (Miguel Formation) associated with the Domingo* thrust, as well as by the presence of large Maastrichtian [[Thrust fault|thrust]] sheets of [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000012 ultrabasics] in Oriente. Thrusting (and metamorphism) of ultrabasics began in the Escambray, and thrust sheets began to stack into the former basin that is today represented by the Guaniguanico Mountains. Northward-[[dip]]ping subduction to the south produced uplift of the [http://geology.com/nsta/convergent-plate-boundaries.shtml convergent margins]. The northward-moving thrust sheets or [[nappe]]s formed as the result of the sedimentary or volcanic cover sliding away from the uplifted areas.

After the period of the [[Unconformity|disconformity]], [http://www.merriam-webster.com/dictionary/pelagic pelagic] conditions characterized the platform to deep-water province, which received massive, dominantly carbonate [[turbidite]] flows from the north (Lutgarda* Formation) and from the south (Amaro* and Cacarajicara formations) (67 Ma; [[:file:St58OverviewFG31.JPG|Figure 11]]). Over the [[Wikipedia:Basic_rock|basic]] igneous-volcanic province, local [http://www.merriam-webster.com/dictionary/provenance provenance] resulted in an abundance of fragmental rocks; that is, limestones toward the north (Penalver Formation) and volcanics toward the south. In the south, sedimentation was accompanied during the Maastrichtian by an outpouring of late orogenic [http://geology.com/rocks/basalt.shtml basaltic] flows and flow breccias (the Maastrichtian age of these flows disagrees with the current interpretation of most Cuban geologists, including Iturralde-Vinent, 1996). Toward the north, along the present outer line of clays, deposition of coarse [[Maastrichtian]] limestone [[conglomerate]] (Mayajigua* Formation) graded into fine-grained pelagic rocks. The basic igneous-volcanic province began its initial northward movement as indicated by [http://www.galleries.com/serpentine serpentine] detritus in the turbidites, by basic [http://www.geolsoc.org.uk/ks3/gsl/education/resources/rockcycle/page3598.html intrusive]-derived clastics (Miguel Formation) associated with the Domingo* thrust, as well as by the presence of large Maastrichtian [[Thrust fault|thrust]] sheets of [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000012 ultrabasics] in Oriente. Thrusting (and metamorphism) of ultrabasics began in the Escambray, and thrust sheets began to stack into the former basin that is today represented by the Guaniguanico Mountains. Northward-[[dip]]ping subduction to the south produced uplift of the [http://geology.com/nsta/convergent-plate-boundaries.shtml convergent margins]. The northward-moving thrust sheets or [[nappe]]s formed as the result of the sedimentary or volcanic cover sliding away from the uplifted areas.

===Paleocene (Danian)===

===Paleocene (Danian)===