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Journal articles on the topic 'Geology – Barbados'

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Published: 4 June 2021
Last updated: 1 February 2022

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1

Donovan, Stephen K., and David A. T. Harper. "Barbados." Geology Today 25, no. 4 (July 2009): 151–58. http://dx.doi.org/10.1111/j.1365-2451.2009.00724.x.

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2

Larue, D. K., and K. G. Provine. "Vacillatory turbidites, Barbados." Sedimentary Geology 57, no. 3-4 (June 1988): 211–19. http://dx.doi.org/10.1016/0037-0738(88)90028-0.

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3

MacDonald, William D. "Caribbean Geological Conference, Barbados." Geology 15, no. 1 (1987): 89. http://dx.doi.org/10.1130/0091-7613(1987)15<89:cgcb>2.0.co;2.

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4

Speed, R. C., L. H. Barker, and P. L. B. Payne. "GEOLOGIC AND HYDROCARBON EVOLUTION OF BARBADOS." Journal of Petroleum Geology 14, no. 2 (April 1991): 323–42. http://dx.doi.org/10.1111/j.1747-5457.1991.tb00315.x.

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5

Takizawa, Shigeru, and Yujiro Ogawa. "Dilatant clayey microstructure in the Barbados décollement zone." Journal of Structural Geology 21, no. 1 (January 1999): 117–22. http://dx.doi.org/10.1016/s0191-8141(98)00097-2.

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6

BURNS, STEPHEN J., and VICTOR ROSSINSKY. "Late Pleistocene mixing zone dolomitization, southeastern Barbados, West Indies." Sedimentology 36, no. 6 (December 1989): 1135–37. http://dx.doi.org/10.1111/j.1365-3091.1989.tb01547.x.

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7

HUMPHREY, JOHN D. "Late Pleistocene mixing zone dolomitization, southeastern Barbados, West Indies." Sedimentology 35, no. 2 (April 1988): 327–48. http://dx.doi.org/10.1111/j.1365-3091.1988.tb00951.x.

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8

Brown, K. M., and G. K. Westbrook. "The tectonic fabric of the Barbados Ridge accretionary complex." Marine and Petroleum Geology 4, no. 1 (February 1987): 71–81. http://dx.doi.org/10.1016/0264-8172(87)90022-5.

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9

Humphrey, J. D. "New Geochemical Support for Mixing-Zone Dolomitization at Golden Grove, Barbados." Journal of Sedimentary Research 70, no. 5 (September 1, 2000): 1160–70. http://dx.doi.org/10.1306/101399701160.

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10

Babaie, Hassan A., Robert C. Speed, David K. Larue, and George E. Claypool. "Source rock and maturation evaluation of the Barbados accretionary prism." Marine and Petroleum Geology 9, no. 6 (December 1992): 623–32. http://dx.doi.org/10.1016/0264-8172(92)90035-d.

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11

Faugères, J. C., E. Gonthier, L. Masse, M. Parra, J. C. Pons, and C. Pujol. "Quaternary deposits on the South Barbados accretionary prism." Marine Geology 96, no. 3-4 (January 1991): 247–67. http://dx.doi.org/10.1016/0025-3227(91)90150-3.

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12

Limonta, Mara, Eduardo Garzanti, Alberto Resentini, Sergio Andò, Maria Boni, and Thilo Bechstädt. "Multicyclic sediment transfer along and across convergent plate boundaries (Barbados, Lesser Antilles)." Basin Research 27, no. 6 (January 13, 2015): 696–713. http://dx.doi.org/10.1111/bre.12095.

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13

Huyghe, Pascale, Michel Foata, Eric Deville, Georges Mascle, and Caramba Working Group. "Channel profiles through the active thrust front of the southern Barbados prism." Geology 32, no. 5 (May 1, 2004): 429–32. http://dx.doi.org/10.1130/g20000.1.

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Abstract Submarine channels of the Orinoco River were analyzed using high-quality, dense- coverage bathymetric and seismic data provided by a recent marine survey on the southern Barbados prism. Analysis of the syntectonic sediments on seismic profiles shows that the four to five frontmost structures show evidence of recent tectonic movement. Slope analysis of the major channels was performed. From their headwaters to domains of little or no active tectonics, the channels display <0.2% slope and form levees. Slope and incision increase gradually in domains of moderate tectonics, but deep canyons with ∼2% mean slope form where the channels cross the active frontal folds of the prism. Detailed correlation between the active structures, their geometry, and canyon slope suggest that systematic variations in channel gradient highlight variations in substrate uplift rate. Steep slopes induced by uplift accelerate sediment flow and enhance incision. Nonetheless, such slope analysis is subject to complications introduced by variations in sediment flux and transient erosional conditions.
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14

FRIEDMAN, GERALD M. "Early submarine cementation in fore-reef carbonate sediments, Barbados, West Indies." Sedimentology 42, no. 4 (August 1995): 707. http://dx.doi.org/10.1111/j.1365-3091.1995.tb00402.x.

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15

STENTOFT, NIELS. "Early submarine cementation in fore-reef carbonate sediments, Barbados, West Indies." Sedimentology 41, no. 3 (June 1994): 585–604. http://dx.doi.org/10.1111/j.1365-3091.1994.tb02012.x.

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16

Humphrey, John D., and Eric M. Radjef. "Dolomite stoichiometric variability resulting from changing aquifer conditions, Barbados, West Indies." Sedimentary Geology 71, no. 3-4 (May 1991): 129–36. http://dx.doi.org/10.1016/0037-0738(91)90097-w.

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17

TORRINI, RUDOLPH, ROBERT C. SPEED, and GLEN S. MATTIOLI. "Tectonic relationships between forearc-basin strata and the accretionary complex at Bath, Barbados." Geological Society of America Bulletin 96, no. 7 (1985): 861. http://dx.doi.org/10.1130/0016-7606(1985)96<861:trbfsa>2.0.co;2.

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18

Wallace, G., J. C. Moore, and C. G. DiLeonardo. "Controls on localization and densification of a modern décollement: Northern Barbados accretionary prism." Geological Society of America Bulletin 115 (March 2003): 288–97. http://dx.doi.org/10.1130/0016-7606(2003)115<0288:colado>2.0.co;2.

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19

Speed, R. C., and H. Cheng. "Evolution of marine terraces and sea level in the last interglacial, Cave Hill, Barbados." Geological Society of America Bulletin 116, no. 1 (2004): 219. http://dx.doi.org/10.1130/b25167.1.

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20

Hearn, G. J., I. Hodgson, and S. Woddy. "GIS-based landslide hazard mapping in the Scotland District, Barbados." Geological Society, London, Engineering Geology Special Publications 18, no. 1 (2001): 151–57. http://dx.doi.org/10.1144/gsl.eng.2001.018.01.22.

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21

Larue, D. K., J. Schoonmaker, R. Torrini, J. Lucas-Clark, M. Clark, and R. Schneider. "Barbados: maturation, source rock potential and burial history within a Cenozoic accretionary complex." Marine and Petroleum Geology 2, no. 2 (May 1985): 96–110. http://dx.doi.org/10.1016/0264-8172(85)90001-7.

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22

Bard, E., B. Hamelin, and R. G. Fairbanks. "U/Th ages obtained by mass spectrometry in corals from Barbados." Chemical Geology 84, no. 1-4 (July 1990): 157–58. http://dx.doi.org/10.1016/0009-2541(90)90196-e.

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23

VROLIJK, PETER, and SIMON M. F. SHEPPARD. "Syntectonic carbonate veins from the Barbados accretionary prism (ODP Leg 110): record of palaeohydrology." Sedimentology 38, no. 4 (August 1991): 671–90. http://dx.doi.org/10.1111/j.1365-3091.1991.tb01014.x.

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24

Parnell, John, Geng Ansong, and Christopher Veale. "Petrology of the bitumen (manjak) deposits of Barbados: Hydrocarbon migration in an accretionary prism." Marine and Petroleum Geology 11, no. 6 (December 1994): 743–55. http://dx.doi.org/10.1016/0264-8172(94)90027-2.

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25

Cukur, Deniz, Gwang H. Lee, Jeong G. Um, Dae C. Kim, and Jin H. Kim. "Northern Barbados accretionary prism: Structure, deformation, and fluid flow interpreted from 3D seismic and well-log data." Island Arc 18, no. 4 (December 2009): 642–60. http://dx.doi.org/10.1111/j.1440-1738.2009.00679.x.

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26

Moore, J. C., T. H. Shipley, D. Goldberg, Y. Ogawa, F. Filice, A. Fisher, M. J. Jurado, et al. "Abnormal fluid pressures and fault-zone dilation in the Barbados accretionary prism: Evidence from logging while drilling." Geology 23, no. 7 (1995): 605. http://dx.doi.org/10.1130/0091-7613(1995)023<0605:afpafz>2.3.co;2.

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27

Larue, D. K. "Quartzose turbidites of the accretionary complex of Barbados, II: Variations in bedding styles, facies and sequences." Sedimentary Geology 42, no. 3-4 (March 1985): 217–53. http://dx.doi.org/10.1016/0037-0738(85)90046-6.

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28

Sumrall, Jonathan, John Mylroie, and Hans Machel. "Unusual polygenetic void and cave development in dolomitized Miocene chalks on Barbados, West Indies." International Journal of Speleology 42, no. 3 (September 2013): 247–55. http://dx.doi.org/10.5038/1827-806x.42.3.8.

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29

Behrmann, Jan H., Kevin Brown, J. Casey Moore, Alain Mascle, Elliott Taylor, Francis Alvarez, Patrick Andreieff, et al. "Evolution of structures and fabrics in the Barbados Accretionary Prism. Insights from leg 110 of the Ocean Drilling Program." Journal of Structural Geology 10, no. 6 (January 1988): 577–91. http://dx.doi.org/10.1016/0191-8141(88)90025-9.

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30

Faugères, Jean Claude, Eliane Gonthier, Roger Griboulard, and Laurent Masse. "Quaternary sandy deposits and canyons on the Venezuelan margin and south Barbados accretionary prism." Marine Geology 110, no. 1-2 (February 1993): 115–42. http://dx.doi.org/10.1016/0025-3227(93)90109-9.

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31

Machel, H. G., J. B. Sumrall, P. N. Kambesis, J. R. Mylroie, J. E. Mylroie, and M. J. Lace. "Episodic Fluid Flow and Dolomitization By Methane-Bearing Pore Water of Marine Parentage In An Accretionary Prism Setting, Barbados, West Indies." Journal of Sedimentary Research 84, no. 2 (February 24, 2014): 58–71. http://dx.doi.org/10.2110/jsr.2014.9.

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32

Hill, Ronald J., and Christopher J. Schenk. "Petroleum geochemistry of oil and gas from Barbados: Implications for distribution of Cretaceous source rocks and regional petroleum prospectivity." Marine and Petroleum Geology 22, no. 8 (September 2005): 917–43. http://dx.doi.org/10.1016/j.marpetgeo.2005.05.003.

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33

Aloisi, Giovanni, Catherine Pierre, Jean-Marie Rouchy, and Jean-Claude Faugères. "Isotopic evidence of methane-related diagenesis in the mud volcanic sediments of the Barbados Accretionary Prism." Continental Shelf Research 22, no. 16 (November 2002): 2355–72. http://dx.doi.org/10.1016/s0278-4343(02)00061-4.

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34

Jollivet, Didier, Jean-Claude Faugeres, Roger Griboulard, Daniel Desbruyers, and Gerard Blanc. "Composition and spatial organization of a cold seep community on the South Barbados accretionary prism: Tectonic, geochemical and sedimentary context." Progress in Oceanography 24, no. 1-4 (January 1990): 25–45. http://dx.doi.org/10.1016/0079-6611(90)90017-v.

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35

Mass�, L., J. C. Faug�res, and E. Gonthier. "Quaternary deposits and sediment fluxes at the toe of the Barbados Accretionary Prism." Geo-Marine Letters 15, no. 2 (June 1995): 99–105. http://dx.doi.org/10.1007/bf01275413.

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36

Kopf, A., and K. M. Brown. "Friction experiments on saturated sediments and their implications for the stress state of the Nankai and Barbados subduction thrusts." Marine Geology 202, no. 3-4 (November 2003): 193–210. http://dx.doi.org/10.1016/s0025-3227(03)00286-x.

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37

Ogawa, Y., and P. Vrolijk. "Control of internal structure and fluid-migration pathways within the Barbados Ridge decollement zone by strike-slip faulting: Evidence from coherence and three-dimensional seismic amplitude imaging: Discussion." Geological Society of America Bulletin 118, no. 1-2 (January 1, 2006): 253–54. http://dx.doi.org/10.1130/b25513.1.

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38

DiLeonardo, C., and J. C. Moore. "Control of internal structure and fluid-migration pathways within the Barbados Ridge decollement zone by strike-slip faulting: Evidence from coherence and three-dimensional seismic amplitude imaging: Reply." Geological Society of America Bulletin 118, no. 1-2 (January 1, 2006): 255–56. http://dx.doi.org/10.1130/b25793.1.

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39

Pindell, James L., Lorcan Kennan, David Wright, and Johan Erikson. "Clastic domains of sandstones in central/eastern Venezuela, Trinidad, and Barbados: heavy mineral and tectonic constraints on provenance and palaeogeography." Geological Society, London, Special Publications 328, no. 1 (2009): 743–97. http://dx.doi.org/10.1144/sp328.29.

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40

Vincent, Hasley, Grant Wach, and Yawooz Ketannah. "Heavy mineral record of Andean uplift and changing sediment sources across the NE margin of South America: a case study from Trinidad and Barbados." Geological Society, London, Special Publications 386, no. 1 (2014): 217–41. http://dx.doi.org/10.1144/sp386.19.

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41

Mangini, A., P. Blumbach, P. Verdes, C. Spötl, D. Scholz, H. Machel, and S. Mahon. "Combined records from a stalagmite from Barbados and from lake sediments in Haiti reveal variable seasonality in the Caribbean between 6.7 and 3ka BP." Quaternary Science Reviews 26, no. 9-10 (May 2007): 1332–43. http://dx.doi.org/10.1016/j.quascirev.2007.01.011.

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42

Wang, K. Y., and D. E. Shallcross. "A modelling study of tropospheric distributions of the trace gases CFCl<sub>3</sub> and CH<sub>3</sub>CCl<sub>3</sub> in the 1980s." Annales Geophysicae 18, no. 8 (August 31, 2000): 972–86. http://dx.doi.org/10.1007/s00585-000-0972-3.

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Abstract. Interhemispheric transport is a key process affecting the accuracy of source quantification for species such as methane by inverse modelling, and is a source of difference among global three-dimensional chemistry transport models (CTMs). Here we use long-term observations of the atmospheric concentration of long-lived species such as CH3CCl3 and CFCl3 for testing three-dimensional chemistry transport models (CTMs); notably their ability to model the interhemispheric transport, distribution, trend, and variability of trace gases in the troposphere. The very striking contrast between the inhomogeneous source distribution and the nearly homogeneous trend, observed in the global ALE/GAGE experiments for both CH3CCl3 and CFCl3 illustrates an efficient interhemispheric transport of atmospherically long-lived chemical species. Analysis of the modelling data at two tropical stations, Barbados (13° N, 59° W) and Samoa (14° S, 124° W), show the close relationship between inter-hemispheric transport and cross-equator Hadley circulations. We found that cross-equator Hadley circulations play a key role in producing the globally homogeneous observed trends. Chemically, the most rapid interaction between CH3CCl3 and OH occurs in the northern summer troposphere; while the most rapid photolysis of CH3CCl3 and CFCl3, and the chemical reactions between CFCl3 and O(1D), take place in the southern summer stratosphere. Therefore, the cross-equator Hadley circulation plays a key role which regulates the southward flux of chemical species. The regulation by the Hadley circulations hence determines the amount of air to be processed by OH, O(1D), and ultraviolet photolysis, in both hemispheres. In summary, the dynamic regulation of the Hadley circulations, and the chemical processing (which crucially depends on the concentration of OH, O(1D), and on the intensity of solar insolation) of the air contribute to the seasonal variability and homogeneous growth rate of observed CH3CCl3 and CFCl3.Key words: Atmospheric composition and structure (middle atmosphere - composition and chemistry; pollution - urban and regional) - Meteorology and atmospheric dynamics (convective processes)
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43

Hervouët, Yves, Leonardo Gonzalez-Montilla, Damien Dhont, Guillaume Backe, and José Tomas Castrillo-Delgado. "Deformation of the northeastern Venezuelan Andes. Relationships with the Caribbean overthrusts." Bulletin de la Société Géologique de France 176, no. 1 (January 1, 2005): 93–105. http://dx.doi.org/10.2113/176.1.93.

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Abstract Introduction The Mérida Andes (Venezuela) formed in the middle Miocene due to oblique convergence between the South American plate and the Maracaibo block [Audemard et al., 2002] (figs. 1A and 1B). The study area corresponds to the so-called “Barbacoas platform” [Renz, 1960], which constitutes the northeastern termination of the belt, NE of Valera (fig. 2). It is located in the northeastern part of Trujillo block [Hervouët et al., 2001], considered as an independent block separated from the main Maracaibo block along the Valera fault. According to Stéphan [1982], the N170°E-trending Caribbean compression developed in this area from late Cretaceous to Eocene. It was followed by a N105°E-trending compression older than middle Miocene, and finally by the NW-SE Andean compressional stage that lasted till now in most of the chain. However, east of El Empedrado fault, a NNE-SSW compression presently occurs that is oblique to the classical Andean stage. The tectonic evolution of the Andean stage is not well understood. The Mérida Andes are mainly composed of Precambrian and Paleozoic rocks. The northern part of the belt only comprises a complete and continuous Jurassic to Paleogene cover. This lithologic pattern is probably a consequence of the tectonic escape of the Maracaibo block, and more particularly of the smaller Trujillo block. The Mérida and Carribean belts being close to each other, the influence of the Andean deformation on the Caribbean allochthonous must be taken into account. In order to make a structural analysis at regional scale, we privileged the use of remote sensing data (Landsat, Spot and Radar images) and aerial photographs. This was complemented by structural data obtained in the field, allowing the study of geometric and chronological relationships between the tectonic structures. Lithostratigraphy of the northeastern Andes Andean formations The first Mesozoic deposits rest unconformably upon the marine Permian (Palmarito Fm.) [Gonzalez de Juana et al., 1980]. During the Jurassic, continental deposits of La Quinta Fm. were trapped in NE-SW grabens [Gonzalez de Juana et al., 1980] that opened due to rifting of the northern margin of the South-American plate. The first marine sediments are composed of thick sandstone layers at the bottom and limestone at the top, Barremian-Albian in age (Peñas Altas Fm). It is followed by Cenomanian-Campanian (La Luna Fm.) composed of euxinic black limestone and clay. Cretaceous ends with the Maastrichtian (Colon Fm.) composed of clay and limestone lenses with the intercalation of a white sandstone layer (Cujisal Member) [Renz, 1959; Pierce, 1960; Gonzalez de Juana et al., 1980]. Paleogene layers correspond to low depth deposits, such as the Paleocene-Eocene (Humocaro Fm.), and the upper Paleocene-early Eocene (Quebrada Arriba Fm). The Caribbean allochthonous The Caribbean series outcrop in the El Tocuyo area (fig. 3). The Barquisimeto Fm. (late Cretaceous) is composed of clay, clayey schist, marl, dark gray and black limestone, and phtanite [Bellizia, 1985; Stéphan, 1982; Lexico Estratigra-fico de Venezuela, 1997]. The Matatere Fm. (late Cretaceous-Paleocene) is composed of sandy turbidites involving sandy conglomerates. Tectonic structures of the northeastern Andes and adjacent plains The study area (figs. 3, 4) forms reliefs that can reach 3000 m. It is westerly and easterly surrounded by flat lying plains (La Pastora plain to the west ; El Tocuyo “synclinorium” [Stéphan, 1982] to the east) with elevations less than 500 m. To the north and east, it is overlain by the Lara overthrusts belonging to the Caribbean orogen. To the south, the Andean reliefs are mainly composed of Precambrian and Paleozoic rocks. This Barbacoas platform is westerly and easterly bounded by the San Pedro and Humocaro anticlines respectively, separated by the “Barbacoas synclinorium” [Renz, 1960] forming a flat-lying area. The Humocaro anticline: inversion of a Jurassic graben The 9 km width and 16 km length NE-trending Humocaro Bajo anticline is composed of a complete Meso-Cenozoic sedimentary sequence. It is overturned toward the SE (fig. 4). The Jurassic layers outcrop in the San Pedro and Humocaro Bajo anticlines whereas they are missing in the Barbacoas synclinorium, showing that the area was organized in horsts (Barbacoas) and grabens during the Jurassic. The western boundary of the Jurassic layers is not defined (El Empedrado fault?) compared to the eastern border where the layers overstep the Humocaro area. We interpret that the Humocaro anticline formed during inversion of a preexisting graben in the Andean stage. This led to formation of a wide anticline overturned outwards of the eastern graben. This is not the case of the San Pedro anticline overturned inwards of the western graben. The Barbacoas synclinorium: formation of flower structures Both the morphology and trend of the folds in the Barbacoas synclinorium (fig. 4) differ from those of the Humocaro anticline. Folds, trending ~N030°E, are narrow and well displayed on the remote sensing imagery. There are bounded by N030°E to N045°E trending left-lateral strike-slip faults juxtaposing contiguous anticlines. Numerous tectonic structures of various sizes affect these folds. In the field, we observed tension fractures striking N050°–060°E, N110°E and N150°E, an high-grade N030°–040°E deformation nearby strike-slip faults, fractures in various directions, and a field of flattened ammonites stretched in the N010°– to N030°E direction associated with a N010°E-striking cleavage. A N-S to NNE-SSW compression is well individualized (fig. 5, VE01–14, VE01–26, Ve02–30). It is responsible for left-lateral strike-slip motions along N030–045°E directed faults. Narrow anticlines, parallel to these faults, can be interpreted as flower structures. Nearby these tectonic irregularities, the compression turns from N-S to N110°E. The western area : associate pull-apart and buckling The western plain can be considered as a pull-apart basin that opened locally at the step-over of a NE-SW left-lateral fault (figs. 3, 5, VE03–12). The San Pedro anticline is parallel to and has the same length of the La Pastora plain. Since it is overturned toward the Jurassic graben (fig. 4), it cannot be related to a positive tectonic inversion. We interpret the San Pedro anticline as an extensional forced fold [Cosgrove and Ameen, 2000; Maurin and Nivière, 2000] because of (1) its position relative to the La Pastora graben; (2) the lack of internal flank; and (3) the 1500 m lowering between San Pedro and La Pastora. This deformation is associated to the NNE-SSW compressional stage (fig. 5; Ve03–12), which appears also in other areas of the northeastern Andes (figs. 5, 9). The allochthonous deformation West of El Tocuyo (figs. 3, 6), the Caribbean allochthonous, Upper Cretaceous in age (Barquisimeto Fm.), associated to the Paleocene-Eocene Morán Fm. is juxtaposed to the Andean autochthonous along vertical or sub-horizontal faults (fig. 6, 7). The Andean series are composed of the Peñas Altas and La Luna Fms. The Morán Fm. is highly folded comparatively to the underlying Cretaceous deposits. Moreover, since the intermediate deposits (Colon, Humocaro and Quebrada Arriba Fms.) do not outcrop, we interpret that the Morán Fm. is allochthonous in this area. To the south, in the Humocaro area, the Morán Fm. is slightly deformed and rests conformably upon the Quebrada Arriba Fm., showing that it is autochthonous in this southern area. In the El Tocuyo area, the Barquisimeto Fm. is represented as olistolites involved in the Morán Fm. (fig. 7B). In the Barquisimeto Fm., we observed N070°E- to N140°E-trending folds (fig. 8) with sub-horizontal axes that formed during the emplacement of the Caribbean overthrusts. These folds were reactivated during the Andean stage into recumbent folds trending N175°E to N050°E. In both the Barquisimeto and Morán Fms., we observed N000°– to N035°E-trending folds that can be sorted into two units corresponding (1) to sub-horizontal axes (plunges from 5°to 30°to the north) associated to a fracture or crenulation cleavage; and (2) to upright (45°to 64°to the north) axes. High-grade deformation develops at the bottom of the sedimentary units, showing that folding is related to ESE-ward displacement of these two formations. The upright fold axes, only observed on the borders of the El Tocuyo plain, characterize strike-slip motion of sub-meridian faults bounding this basin. Flat lying plains develop east and west of the northeastern Andes (figs. 3, 6, 7) and constitute an abrupt change in the topography. Our analysis of satellite imagery complemented by field observations show that the El Tocuyo plain (fig. 6) may be interpreted as a pull-apart basin that initiated along a left-lateral fault relay trending N000°E. The synclinal-like morphology of the basin results from the progressive breaking of the western fault, that locally buckles before vanishing in the south (fig. 7). This geometry greatly resembles to that of extensional forced folds initiating at the borders of grabens. Here, this deformation is associated to the NW-SE compressionnal Andean stage (fig. 9, VE01–49, VE02–54). Conclusions The northeastern part of the Mérida Andes recorded several tectonic stages that can be described as follows: – (1) the Jurassic rifting, corresponding to the formation of NE-trending grabens filled by La Quinta Fm.; – (2) the Caribbean orogen (upper Cretaceous-early Oligocene) associated with the emplacement of Caribbean overthrusts. The front of some units (Barquisimeto Fm.) can be partly involved into the Paleocene-Eocene Morán Fm. This stage is characterized by N070°E- to N150°E-trending folds; – (3) an ESE-WNW compression older than the middle Miocene, that may correspond to the N105°E-trending stage of Stéphan [1982], and related to ESE-ward displacement of the Morán Fm. and the Caribbean units; – (4) the NW- to NNW-directed Andean compression lasting from middle Miocene onwards. It is responsible for the formation of NE-SW folds, sometimes related to reactivation of the Jurassic grabens (Humocaro anticline); – (5) a NNE-SSW compression, younger than the Andean compression, and responsible for N-S right-lateral strike-slip faulting and NE-SW left-lateral strike-slip faulting. Relays along strike-slip faults locally created transtensional or transpressional areas, which localized flower structures (Barbacoas area for instance) and pull-apart basins (La Pastora) respectively. Important lowering along the pull-apart basins created the buckling of the sedimentary cover responsible for the formation of extensional forced folds. Near NE-SW strike-slip faults, the stress turns anti-clockwise to strike N100°E. North of the Boconó fault and east of the Valera fault, the Trujillo block [Hervouët et al., 2001] is composed of several compartments separated by sub-meridian left-lateral strike-slip faults. Our analysis of satellite imagery, structural observations in the field and slip vectors derived from focal mechanisms of earthquakes [Dhont et al., 2002; 2004] show that the Trujillo block tectonically escapes towards the north or north-east. However, between El Empedrado fault and Bocono fault, in front of the Carribean overthrusts, numerous focal mechanisms of earthquakes and structural observations in the field indicate that the Andean compressional stage is relieved by a NNE-SSW compression. North of the Trujillo block, the Caribbean overthrusts act as a barrier for the escape of this triangular block towards the north-east (fig. 1C).
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44

Blanc, G., J. M. Gieskes, P. J. Vrolijk, A. Mascle, C. J. Moore, E. Taylor, F. Alvarez, et al. "Advection de fluides interstitiels dans les series sedimentaires du complexe d'accretion de la Barbade (Leg 110 ODP)." Bulletin de la Société Géologique de France IV, no. 3 (May 1, 1988): 453–60. http://dx.doi.org/10.2113/gssgfbull.iv.3.453.

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45

Welshman, Rebecca. "Imagining the Ancient Britons: Victorian Adventures in Wye-Land." Victoriographies 2, no. 1 (May 2012): 31–43. http://dx.doi.org/10.3366/vic.2012.0058.

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Abstract:
Depicted in the mid to late nineteenth-century periodical press as wild, remote, and ‘intensely national’, Wales was perceived as a place of quiet mystery, geographically and socially distinct from the industrialisation of Victorian England. The borderland territory of the Wye Valley – what the Victorian journalist and historian, Barbara Hutton, called ‘Wye-Land’ – has been inhabited for over 12,000 years and preserves an ancient British identity in its rich archaeological landscapes. Developments in mid Victorian archaeology and anthropology precipitated a rise in the number of prehistoric excavations, which popularised knowledge of how ancient Britons lived and died. Drawing from articles in the late Victorian periodical press, and the activities of the Cardiff Naturalist's Society in the 1870s, which included the study of geology, botany and archaeology, this paper suggests that the observation of natural phenomena in the late nineteenth century was closely associated with the study of past human societies. I identify the changing interpretations of prehistoric sites – from early Victorian notions of barbarous druids, to more informed and sensitive appreciations of ancient British societies, whose sympathetic relation to the landscape fostered imaginative connections between late Victorians and their ancestors. This transition away from perceptions of being wholly distinct from prehistoric activity, shaped late Victorian pastoral journalism and encouraged a more integrated vision of the relationship between past and present human activity in the region.
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46

Beck, C., G. Blanc, A. Mascle, J. C. Moore, E. Taylor, F. Alvarez, Patrick Andreieff, et al. "Anatomie et physiologie d'un prisme d'accretion; premiers resultats des forages du complexe de la ride de la Barbade, Leg ODP 110." Bulletin de la Société Géologique de France IV, no. 1 (January 1, 1988): 129–40. http://dx.doi.org/10.2113/gssgfbull.iv.1.129.

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47

Thompson, Herb. "The ‘Barbarous Relic’ and the ‘Rim of Fire’: Gold in Papua New Guinea." Minerals & Energy - Raw Materials Report 6, no. 4 (January 1989): 20–31. http://dx.doi.org/10.1080/14041048909409934.

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48

King, Richard P., and Mfon T. Udo. "Vegetational succession - Mediated spatial heterogeneity in the environmental biology of Periophthalmus Barbaras (Gobiidae) in the estuarine swamps of Imo River, Nigeria." International Journal of Surface Mining, Reclamation and Environment 11, no. 3 (January 1997): 151–54. http://dx.doi.org/10.1080/09208119708944080.

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49

Schambach, L., S. T. Grilli, D. R. Tappin, M. D. Gangemi, and G. Barbaro. "Response to: Comment on “New simulations and understanding of the 1908 Messina tsunami for a dual seismic and deep submarine mass failure source” by L. Schambach, S.T. Grilli, D.R. Tappin, M.D. Gangemi, G. Barbaro [Marine Geology 421 (2020) 106093]." Marine Geology 442 (December 2021): 106636. http://dx.doi.org/10.1016/j.margeo.2021.106636.

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50

David C. Kasper, David K. Larue, Yv. "Fine-grained Paleogene Terrigenous Turbidites in Barbados." SEPM Journal of Sedimentary Research Vol. 57 (1987). http://dx.doi.org/10.1306/212f8b57-2b24-11d7-8648000102c1865d.

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