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Similar to the northeastern Cuban evaporites are Upper Jurassic(?) to Lower Cretaceous [[Maraval]] evaporites in the [[Paria Peninsula]] and [[Gulf of Paria]], in the southern Caribbean between [[Venezuela]] and [[Trinidad]]. The metamorphosed clastics and [[marble]]s of the Jurassic to Lower Cretaceous [[Caracas series]] in northern Venezuela have some similarities to Cuba's southern metamorphic massifs. In addition, the thick section of Upper Jurassic clastics of the [[Cosina Group]] (overlain by fossiliferous Neocomian carbonates of the [[Kesima]], [[Palare]], [[Moina]], and [[Yaruma]] Formations) in the [[Guajira Peninsula]] have similarities to the San Cayetano of Cuba's Pinar del Rio. Some similarity exists between the ''Orbitolina''-bearing reef carbonates of Cuba, Venezuela's Lower Cretaceous [[Cogollo Group]] and [[Cantil Formation]], and contemporaneous facies of the Florida-Bahamas Platform.

Similar to the northeastern Cuban evaporites are Upper Jurassic(?) to Lower Cretaceous [[Maraval]] evaporites in the [[Paria Peninsula]] and [[Gulf of Paria]], in the southern Caribbean between [[Venezuela]] and [[Trinidad]]. The metamorphosed clastics and [[marble]]s of the Jurassic to Lower Cretaceous [[Caracas series]] in northern Venezuela have some similarities to Cuba's southern metamorphic massifs. In addition, the thick section of Upper Jurassic clastics of the [[Cosina Group]] (overlain by fossiliferous Neocomian carbonates of the [[Kesima]], [[Palare]], [[Moina]], and [[Yaruma]] Formations) in the [[Guajira Peninsula]] have similarities to the San Cayetano of Cuba's Pinar del Rio. Some similarity exists between the ''Orbitolina''-bearing reef carbonates of Cuba, Venezuela's Lower Cretaceous [[Cogollo Group]] and [[Cantil Formation]], and contemporaneous facies of the Florida-Bahamas Platform.

Close similarities exist between the [[Mesozoic]] igneous intrusive and associated volcanic rocks of Cuba and those of the Caribbean.

Close similarities exist between the [[Mesozoic]] igneous [http://www.geolsoc.org.uk/ks3/gsl/education/resources/rockcycle/page3598.html intrusive] and associated volcanic rocks of Cuba and those of the Caribbean.

Ophiolites are common throughout the Caribbean and extend from the Motagua fault zone, between the Maya and Chortis block, to [[Puerto Rico]]. They also form the floor of the Cayman Trench. These rocks are also common along the northern coast of South America from [[Tobago]] to the Guajira Peninsula, although they are not as intensely [http://jersey.uoregon.edu/~mstrick/AskGeoMan/geoQuerry45.html serpentinized] as in the northern Caribbean. Cuba's outcrops of [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000012 ultrabasic] rocks are the most extensive in the region.

Ophiolites are common throughout the Caribbean and extend from the Motagua fault zone, between the Maya and Chortis block, to [[Puerto Rico]]. They also form the floor of the Cayman Trench. These rocks are also common along the northern coast of South America from [[Tobago]] to the Guajira Peninsula, although they are not as intensely [http://jersey.uoregon.edu/~mstrick/AskGeoMan/geoQuerry45.html serpentinized] as in the northern Caribbean. Cuba's outcrops of [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000012 ultrabasic] rocks are the most extensive in the region.

Similarities exist between the Caribbean and the Cuban Upper Cretaceous volcanic and associated intrusive rocks. The Cuban Upper Cretaceous [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000073 granodioritic] intrusion has counterparts outcropping in Hispaniola, Jamaica, and Puerto Rico in the north (where the intrusive's ages range into the [[Paleogene]]) and in [[Aruba]], the [[Venezuelan Antilles]], and the [[Aves Ridge]] in the south. Volcanics containing a characteristic fauna of ''Acteonella'', large rudists (''Hippurites''), and orbitoids are present in Cuba, Jamaica, Hispaniola, Puerto Rico, the [[Dutch West Indies]], and northern Venezuela, suggesting a connection between the various parts of the volcanic province.

Similarities exist between the Caribbean and the Cuban Upper Cretaceous volcanic and associated [http://www.geolsoc.org.uk/ks3/gsl/education/resources/rockcycle/page3598.html intrusive] rocks. The Cuban Upper Cretaceous [https://wwwf.imperial.ac.uk/earthscienceandengineering/rocklibrary/viewglossrecord.php?gID=00000000073 granodioritic] intrusion has counterparts outcropping in Hispaniola, Jamaica, and Puerto Rico in the north (where the intrusive's ages range into the [[Paleogene]]) and in [[Aruba]], the [[Venezuelan Antilles]], and the [[Aves Ridge]] in the south. Volcanics containing a characteristic fauna of ''Acteonella'', large rudists (''Hippurites''), and orbitoids are present in Cuba, Jamaica, Hispaniola, Puerto Rico, the [[Dutch West Indies]], and northern Venezuela, suggesting a connection between the various parts of the volcanic province.

Other than the Yucatan Basin, Cuba is probably the only place in the Caribbean with complete sections representative of the early Caribean region after the separation of North and South America and before the formation of the present Caribbean plate in the Paleogene.

Other than the Yucatan Basin, Cuba is probably the only place in the Caribbean with complete sections representative of the early Caribean region after the separation of North and South America and before the formation of the present Caribbean plate in the Paleogene.

===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 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)===

The early to middle [[Eocene]] was characterized by intense [[Orogeny|orogenic]] activity (50 Ma; [[:file:St58OverviewFG32.JPG|Figure 12]]). Early in the Eocene, the large-scale low-angle [[Thrust fault|thrust sheets]], or gravity [[nappe]]s, that first moved in the Maastrichtian began to move at a greater rate. The volcanic section, along with the [[Oceanic crust|oceanic basement]], rode over the platform to deep water province, probably along the line separating the [[Wikipedia:Basic_rock|basic]] igneous-volcanic province from the platform to deep basin province. As thrusting proceeded, additional thrusts formed within the carbonate section in front of and north of the basic igneous-volcanic front. As a result, the thrust sheets were generally arranged from older and more southerly sourced at the top of the stack to younger and more northerly sourced at the base.

The early to middle [[Eocene]] was characterized by intense [[Orogeny|orogenic]] activity (50 Ma; [[:file:St58OverviewFG32.JPG|Figure 12]]). Early in the Eocene, the large-scale low-angle [[Thrust fault|thrust sheets]], or gravity [[nappe]]s, that first moved in the Maastrichtian began to move at a greater rate. The volcanic section, along with the [[Oceanic crust|oceanic basement]], rode over the platform to deep water province, probably along the line separating the [[Wikipedia:Basic_rock|basic]] igneous-volcanic province from the platform to deep basin province. As thrusting proceeded, additional thrusts formed within the carbonate section in front of and north of the basic igneous-volcanic front. As a result, the thrust sheets were generally arranged from older and more southerly sourced at the top of the stack to younger and more northerly sourced at the base.

A large trough-shaped basin formed in front of the thrust sheets, deeper near the thrust front and shallower northward. Early to middle Eocene [[flysch]] deposition in the trough began with sediments derived from limestones, such as the Sagua* and San Martin* formations, followed by an increase in volcanic and intrusive-derived detritus, such as the lower Vega* and lower Manacas (Pica Pica) formations, and finally, capped by the intrusive and volcanic-derived coarse [[conglomerate]]s and [http://www.encyclopedia.com/doc/1O13-wildflysch.html wildflysch] of the upper Vega* (Rosas*) and upper Manacas (Vieja) Formations. In central Cuba, the rocks of the deep-water Vega* Formation became coarser grained through time. In western Cuba, the fine-grained clastics and other [http://www.merriam-webster.com/dictionary/pelagic pelagic] sediments of the Manacas Formation changed abruptly to the coarse [[breccia]]s of the Vieja Member. The breccia clasts reflect the lithology of the associated fault blocks. This suggests some subaerial [[erosion]] in central Cuba, whereas western Cuba was largely submarine.

A large trough-shaped basin formed in front of the thrust sheets, deeper near the thrust front and shallower northward. Early to middle Eocene [[flysch]] deposition in the trough began with sediments derived from limestones, such as the Sagua* and San Martin* formations, followed by an increase in volcanic and [http://www.geolsoc.org.uk/ks3/gsl/education/resources/rockcycle/page3598.html intrusive]-derived detritus, such as the lower Vega* and lower Manacas (Pica Pica) formations, and finally, capped by the intrusive and volcanic-derived coarse [[conglomerate]]s and [http://www.encyclopedia.com/doc/1O13-wildflysch.html wildflysch] of the upper Vega* (Rosas*) and upper Manacas (Vieja) Formations. In central Cuba, the rocks of the deep-water Vega* Formation became coarser grained through time. In western Cuba, the fine-grained clastics and other [http://www.merriam-webster.com/dictionary/pelagic pelagic] sediments of the Manacas Formation changed abruptly to the coarse [[breccia]]s of the Vieja Member. The breccia clasts reflect the lithology of the associated fault blocks. This suggests some subaerial [[erosion]] in central Cuba, whereas western Cuba was largely submarine.

South of the front of the advancing volcanic and basic intrusive-rock thrust plate, a second series of basins developed parallel to the northern trough. Within these basins, which were carried piggyback by the thrust plate, lower Eocene igneous-derived sediments accumulated, but under quieter tectonic conditions (the Taguasco*, Bijabo*, Santa Clara*, Alkazar, Bacunayagua, Capdevila, and Universidad Formations, for example).

South of the front of the advancing volcanic and basic intrusive-rock thrust plate, a second series of basins developed parallel to the northern trough. Within these basins, which were carried piggyback by the thrust plate, lower Eocene igneous-derived sediments accumulated, but under quieter tectonic conditions (the Taguasco*, Bijabo*, Santa Clara*, Alkazar, Bacunayagua, Capdevila, and Universidad Formations, for example).