Hydraulic fracturing as a possible mechanism of dyke–sill transitions and horizontal discordant intrusions in trachytic tabular bodies of Arraial do Cabo, State of Rio de Janeiro, Brazil

A. Motoki¹* and S.E. Sichel²

¹ Departamento de Mineralogia e Petrologia Ígnea, Universidade do Estado do Rio de Janeiro. Rua São Francisco Xaveir 254, Bloco A, Sala 4023, Maracanã, Rio de Janeiro, 20550–990. Brazil. ^*Corresponding author: amotoki@pesquisador.cnpq.br

² Departamento de Geologia, Laboratory of Marine Geology, Universidade Federal Fluminense, Brazil.

Received: August 24, 2007 ]]> Accepted: October 30, 2007

Resumen

Este artículo presenta descripciones de campo y consideraciones genéticas acerca de la transición dique–sill y la intrusión subhorizontal discordante en un enjambre de diques alcalinos félsicos del Terciário inferior en el área de Arraial do Cabo, Estado de Río de Janeiro, Brasil. Dos ejemplos muestran el proceso íntegro de la transición de dique a sill: cerca del nivel del mar son verticales–discordantes y a media altura, oblicuos–concordantes; en la cima del barranco, horizontales–discordantes. Este último proceso no concuerda con el modelo tradicional de intrusión en fracturas preexistentes. Puede explicarse con un modelo de fracturamiento hidráulico: la presión magmática crea una nueva fractura normal a σ3, independientemente de la existencia de sistemas anteriores de fracturas. La transición de dique a sill ocurre a una profundidad tal que la dirección de σ3 cambia de horizontal a vertical. En el caso específico del área investigada, el cambio podría deberse a la intrusión y expansión del volumen del cuerpo sienítico de la Isla de Cabo Frío.

Palabras clave: Dique, sill, fracturamiento hidráulico, intrusión horizontal, Arraial do Cabo.

Abstract

This paper presents some field descriptions and genetic considerations about dyke–sill transitions and horizontal–discordant intrusions of the early Tertiary felsic alkaline dyke swarm at Arraial do Cabo, State of Rio de Janeiro, Brazil. Two examples show the entire process of dyke–sill transition. Near sea level they are vertical–discordant; at middle height, oblique–concordant; at the top of the cliff, horizontal–discordant. The latter process cannot be explained by a traditional model of magma intrusion along weaknesses in the host body. It can be accounted for by hydraulic fracturing: magma pressure creates a new fracture normal to σ₃, regardless of whether old fracture systems exist. The dyke–sill transition takes place at a depth such that σa₃ changes direction from horizontal to vertical. In the specific case described here, the stress change could be caused by intrusion and volume expansion of the Cabo Frio Island syenitic body.

Key words: Dyke, sill, hydraulic fracturing, horizontal intrusion, Arraial do Cabo

Dykes and sills are common tabular intrusives. Most textbooks (e.g., Billings, 1972; Best, 1982; Bates and Jackson, 1987; Hall, 1987) employ the term "dyke" to denote a tabular body that intrudes normally or obliquely to the bedding plane, the schistosity or the gneiss banding of the country rock, to be called "discordant intrusion", while "sill" indicates a sub–parallel or "concordant" intrusion.

Some other definitions exist. Bates and Jackson (1987) adopted the term "dyke" as meaning a vertical tabular intrusion and "sill", a horizontal one. Hatayama et al. (1980) define a "dyke" as a vertical intrusion, "sheet" as a horizontal one, and "sill" as a horizontal and concordant one. However, Billings (1972) commented that such definitions are "quite erroneous".

The traditional definition (Billings, 1972) appears to be based on the idea that magma intrusion is easier along pre–existent fractures systems or weaknesses, rather than by new fracture creation. The model of magma permeation along pre–existing fractures is widely accepted in Brazil, as old fracture systems in the Precambrian basement were considered to be an essential factor in Phanerozoic magmatic events (e.g., Almeida, 1986; Ricommini, 1997; Ricommini et al., 2004; Schmidt & Stanton, 2007). These authors assumed that the upper crust is highly fractured, and that the magma pressure is not sufficient to fracture the host rock. Some authors considered the fracture–fill model as an important dyke intrusion mechanism (e.g. Delaney et al., 1986; Bear et al., 1994; Delaney & Gartner, 1997; Valentine & Krogh, 2006).

It is widely known that most dykes of traditional definition crop out sub–vertically and that most sills crop out sub–horizontally. Dykes are more widely observed than sills even in a sub–horizontal sedimentary country rock. Sills are found mainly in sub–horizontal young sedimentary formations and rarely in steeply dipping Precambrian gneiss. The traditional fracture–fill model is unable to explain this tendency. Field observations of dyke–sill transitions and dyke fadeout could be important, though rarely described (Motoki, 1986; Motoki et al., 1988).

The magma intrusion mechanism in the upper crust and the process of dyke and sill formation represent an interesting geophysical subject. However, it has not interested many South American geologists. The present paper describes field observations of some peculiar forms of dyke–sill transition, discordant horizontal intrusions, and the fadeout of trachytic tabular rock bodies of Arraial do Cabo, State of Rio de Janeiro, Brazil. We propose a mechanism of formation of these features based on a hydraulic fracturing model involving magma pressure.

Geology of the studied area

The studied area covers the Atalaia Peninsula (Pontal da Atalaia) located about 22°58'S, 42°01'W, south of the town of do Cabo, about 120 km east of Rio de Janeiro city (Fig. 1). The area is underlain by a Pan–African metamorphic basement of orthogneiss, migmatites and amphibolites. The orthogneiss contains up to 10 m thick xenolith–like, sometimes dyke–like, anphibolitic enclaves. The metamorphic basement features a strike of N15°E to N15°W, dipping 20° to 40° to the east, with some local disturbances (Fig. 2A; Motoki et al., 1988). These rocks were metamorphosed during the continental collision between the São Francisco and Congo cratons in the Ribeira Belt (Campos Neto, 2000; Campos Neto & Caby, 2000; Trouw et al., 2000; Heilbron et al., 2000; Schmitt et al., 2004).

The basement is intruded by so–called "Jurassic diabase" dykes (Helmbold, 1967; 1978; Helmbold et al., 1965; Lima, 1974; 1976; Valença, 1976), that are actually early Cretaceous micro–gabbroes (Motoki et al., 1988; Motoki, 1994). Recent studies, such as Heilbron et al. (2007), showed that the mafic dyke swarms of the State of Rio de Janeiro are of high Ti type, and that the intrusion is 140 to 120 Ma old. They trend mainly NNE–SSW to NE–SW, with minor occurrences of NNW–SSE dykes. These dykes are usually very thick: they are 5 m to 15 m thick, straight and of vertical configuration. A horizontal columnar joint system is commonly observed. Grain–size variations are significant in the dykes. The 30 mafic dykes measured here trend N55°E, confirming earlier descriptions (Motoki et al., 1988; 1990; Valente et al., 2005). This dike orientation is completely discordant with the host gneiss structure (Fig. 2).

These dykes are believed to be feeders of a part of the Paraná Continental Flood Basalt (Bellieni et al., 1984; Hergt et al., 1991; Peate et al., 1992; Turner et al., 1994), aged 129 to 134 Ma (Peate, 1997; Deckart et al., 1998). However, recent ³⁹Ar–⁴⁰Ar dates for three tholeiitic dyke samples from the Arraial do Cabo area (Bennio et al., 2003) featured disturbed age spectra with some unexpectedly young ages, about 55 Ma. This means that some types of dykes are difficult to date even by the ³⁹Ar–⁴⁰Ar method.

The metamorphic basement and the mafic dykes are cut by late Cretaceous to early Tertiary alkaline felsic intrusives. About 2 km south–east of Arraial do Cabo, the Cabo Frio Island syenitic rock body occurs (Fig. 1). Around this body, there are many alkaline felsic dykes and some lamprophyre dykes, generally less than 2 m thick (Lima 1974; 1976; Valença, 1976; Motoki et al., 1988).

Motoki et al. (1988) observed 92 felsic alkaline tabular intrusives of which 61 were sub–vertical and 31 oblique or sub–horizontal. The outcrops suggest three different intrusive episodes for these tabular bodies. The youngest one corresponds to the N40°W group, which appears to belong to the radial dyke system originating from the Cabo Frio Island syenitic rock body. The second episode features intense deuteric alteration and related phenitization which affected the country rock along the contacts and pre–existing fractures.

Intrusion direction change

Some outcrops show a transition of felsic alkaline dykes of the second episode from sub–vertical to sub–horizontal. At the Boqueirão sea–cliff, near the south–west edge of the studied area (Loc. 1, 2; Fig. 1), we found two examples of complete transition (Fig. 2). Near sea level, these bodies strike NE–SW and dip steeply to the east, in discordance with the country gneiss (sub–vertical discordant stage). At mid–height, about 20 m above sea level, the dip and strike change to sub–parallel to the gneiss structure which trends N15E to 40E. They tend to show zigzag patterns and complex branching (oblique concordant stage). At the top of the cliff, about 40 m above sea–level, they become sub–horizontal and discordant to the host body (sub–horizontal discordant stage). The sub–horizontal part is generally thicker than the oblique one. Most transitions take place from 20 to 50 m above sea level, but they occur also at all elevations. In three dimensions these intrusive bodies show helical patterns. Outcrops that show transitions from oblique to sub–horizontal intrusion are more frequent (e.g. Loc. 3, 4; Fig. 1, 3, 4).

Tail–end of the tabular bodies

Field observations of fadeouts of dykes and sills are important for their interpretation and the problem of mechanism of intrusion. The traditional fracture–fill model assumes that a linear weakness such as a fault or joint is continuous along the dyke (Fig. 6A). However, few papers present field descriptions of dyke fadeouts. Motoki (1986) shows some examples of late Cretaceous trachytic and phonolithic dykes intruding the Vitória Island syenitic body, State of São Paulo, Brazil. They show a rounded fadeout and there is no continuous fracture in the host syenite as far as the extension of the dyke. In Arraial do Cabo there are also some examples (Fig. 6B, C). These outcrops show complex curved fadeouts where the host rock is deformed plastically without fractures. No faults or joints are found along the extension of the dykes. The examples suggest that intrusion took place by magma pressure, without any influence of pre–existing weaknesses in the host body.

Hydraulic fractiring

The transitions from oblique concordant bodies to sub–horizontal discordant ones and the rounded fadeouts in the studied area cannot be explained by a traditional dyke intrusion model. According to this model, magma should intrude along pre–existing weaknesses in the host body, such as faults, shear zones, tectonic lines, layered structures or parallel fractures (e.g. Almeida, 1986; Ricommini et al., 2004).

A model of fracture formation involving magma pressure in the brittle upper crust and a hydraulic fracturing mechanism is an attractive alternative. The idea of self–propagating fractures being referred to as dykes (Rubin, 1993; 1995) is little known in Brazil, yet it is assumed to be the most common mechanism for dyke intrusion (Valentine & Krogh, 2006).

This model originated in petroleum engineering. The actual water pressure for secondary oil recovery is known to be generally less than estimated from the overburden. Hubbert and Willis (1957) concluded that water is not intruding horizontally into the sedimentary formation, as in sills, but vertically as in a radial dyke system. If the deviator stress σ₁–σ₃ at the intrusion is higher than the stress needed for extensional fracture of the country rock, the water under pressure does not intrude along the stratification. Instead water pressure creates vertical tensile fractures normally to the minimum principal stress axis σ3. Hubbert and Willis suggested that dykes may intrude by hydraulic fracturing. An example is the Spanish Peak, Colorado radial dyke system (Ode, H., 1957). This idea was developed by Nakamura (1977), Nakamura et al. (1977), Phillips (1974), Hills (1975) and Haimson (1975) and was introduced to South America by Llambías (2003).

Under relatively low deviator stresses, less than four times the tensile strength of the host rock, hydraulic tensile fractures are formed normally to σ₃, that is, parallel to the σ₁–σ₂ plane, when the magma pressure exceeds σ₃ plus the host rock tensile strength (Fig. 7A).

Nakamura (1977) and Nakamura et al. (1977) estimated the direction of the horizontal compression stress axis from the alignment of parasitic cones of stratovolcanoes, a surface indication of the presence of underground radial dykes. Bacon et al., (1983) performed a similar estimation based on the distribution of monogenetic volcanoes. Haimson (1975), Kobayashi (1979a, b), Hori and Kobayashi (1980), Takeuchi (1980), Nicolas and Jackson (1982), Laughlin et al. (1983), Feraud and Campredon (1983), Southwick and Day (1983), Ui et al. (1984), Chevallier & Verwoerd (1987), and others applied the same theory to the problem of reconstructing palaeo stress–fields.

On the other hand, when the deviator stress is very high and the magma pressure is relatively low, the host body will fail with displacement along shear fractures. This is called "hydraulic shear fracturing", resulting in tabular intrusive rock bodies accompanied by wall displacement (Fig. 7B). Dykes are formed more easily than faults because of magma pressure. However, unlike in hydraulic tensile fracturing, dykes and faults become sub–parallel. In addition, the dykes are associated with fault–like displacements. Such types of dykes do occur, but examples are rarely described. Phillips (1974) proposed that cone sheets are formed at shallow depths by a dynamic process based on a combination of hydraulic tensile fracturing with hydraulic shear fracturing.

Preferred directions of dykes and faults

Based on observations of volcanoes, dyke swarms and fault systems, Nakamura (1977) and Nakamura et al. (1977) proposed a model relating volcanic eruption modes, preferred directions of dykes and faults, and regional stress field conditions, on the basis of the hydraulic tensile fracturing theory.

In a compressive stress field, rock is harder to fracture by magma pressure than in the case of an extensional stress field. Once a conduit is formed, the magma rises in it by many small pulses. Therefore, if a small volume erupts over a short time interval in a polygenetic eruption it form a large stratovolcano on the surface. The distance between stratovolcanoes is large. At deeper sites, σ₁ is vertical and σ₂ is parallel to the compression axis of the regional tectonic stress. Therefore, the volcano develops a radial dyke system with preferred direction parallel to the regional tectonic compression, that is, the main horizontal stress axis (Fig. 8A). Flank volcanoes, called parasitic cones, arise along a dyke, and the base of the main stratovolcano is elliptical. Contemporaneous fault systems are reverse and conjugated strike–slip systems. On a geologic map, reverse faults are normal to the preferred direction of the dyke swarm and strike–slip faults are oblique to it. Neither is parallel to the general dyke direction. The discordance between preferred directions of dykes and faults are attributed to different fracturing mechanisms. Dykes are formed by tensile fracturing by magma pressure and faults by shear fracturing. Because of tensile fracturing, dykes do not feature any host rock displacement. This case is mainly observed in active arcs. The active Chilean stratovolcanoes in the Southern Volcanic Zone, such as Villarica (Clavero & Moreno, 2004) and Osorno (Lara et al., 2001), are good examples. Some Pliocene volcanoes of the back–arc region, such as Cerro Nevado (Holmberg, 1973; Bermudez et al., 1993) in southern Mendoza, Argentina, also show these characteristics.

On the other hand, in an extensional stress field, new fractures open relatively easily and the magma in the chamber rises in a single pulse through a dyke. The eruptions are voluminous and occur at long time intervals. The rise of voluminous magma causes a large fissure eruption on the surface, while less voluminous ones generate many monogenetic cones along the dyke. The distance between cones is small. At deeper sites, σ1 is vertical and σ₂ is normal to the regional extension axis. Therefore, a parallel dyke system normal to the extension axis develops. The contemporary fault system is normal, and its trend is parallel to the dyke direction. Actually, however, the dykes and faults are not parallel, as dykes are vertical and faults show a high to low–angle dip (Fig. 8B). Also, dykes are formed by tensile fracturing and faults by shear fracturing. Thus a normal fault system forms a conjugate shear fault system with a vertical maximum compression axis. Because of magma pressure, hydraulic tensile fractures for dyke intrusion are formed more easily than normal faults. Therefore, the dykes intrude by means of this mechanism before the fault system is formed. In other words, magma does not fill the parallel normal faults in a given region. This case is mostly observed in active back–arc volcanoes and flood basalt eruptions in the initial stage of continental rifting. The Cretaceous parallel dyke system of the Ponta Grossa Arc, State of Paraná, Brazil, is a good example. Some very young back–arc monogenetic cones, such as Cerro Amarillo, Cerro Las Niñas, and Cerro Mancha Jarilla of the Mancha Jarilla Formation in southern Mendoza, Argentina (Bermudez et al., 1993), are other examples.

Dyke–sill transition mechanism

Valentine and Krogh (2006) proposed the following mechanisms of dyke–sill transitions in brittle host rock: (1) magma rising by buoyancy at deeper sites would accumulate at a level of neutral buoyancy (LNB) (e.g. Lister & Keer, 1991); (2) a change of orientation of σ₃ from vertical at deeper sites to horizontal at shallower sites (e.g. Parsons & Thompson, 1992).

The first mechanism is based on the traditional fracture–fill theory, as it assumes that heavy basaltic magma intrudes light sedimentary formations. In this case, the host rock must be less dense than the magma when the sites are shallower than the sill. At Arraial do Cabo, the trachytic magma intrudes gneissic host rock: thus the model is not applicable (Motoki, et al., 1988).

The second mechanism is based on the hydraulic tensile fracturing theory. Phillips (1974) and Hills (1975) explained the intrusion mechanism of sills (Fig. 9), and they stressed the importance of lateral compressive stress and shallow emplacement of the rock body. At deep sites, the vertical stress is large because of high overburden and because of the vertical stress σ₁ In such conditions, magma pressure can open a sub–vertical tensile fracture. At shallow sites, vertical stress is small. When the horizontal stress is high enough, the σ₃ becomes vertical, and horizontal tabular intrusion takes place. The horizontal stress is mainly due to magma pressure on dyke walls. At this level, the intrusion changes direction from vertical to horizontal, causing the dyke–sill transition (e.g. Parsons & Thompson, 1992). This transition can also occur in homogeneous country rock such as granite. Fracture analyses in the Arraial do Cabo area suggest that σ₃ was vertical at the time of fracture formation (Ferrari, 2001).

Hall (1987) pointed out that large sills can transgress the stratification of the host rock when mapped over a large area, showing abrupt steps rather than angular discordances. The author cited the example of Stirling coalfield (Dinham and Haldane, 1932), which shows that the general direction of sills over a large area may not be parallel to the sedimentary bedding planes, but to the surface of the ground. Thus the sill was not intruded according to the sedimentary stratification, but at a certain depth below the surface.

A specific case of Arraial do Cabo dykes

Fig. 3 may seem similar to Fig. 9. However, the dyke–sill transition at Arraial do Cabo is not easily explained by this model. The regional history of uplift and denudation may be reconstructed from a combination of fission track datings for apatite in the host gneiss. and of cooling ages of the intrusive rock bodies (e.g. Hackspacher, 2003; Motoki et al., 2007a). Thus the tabular intrusives are estimated to having been emplaced at a depth of 3 km. As compared to this intrusion depth, the vertical variation of outcrops is less than 100 m, which fails to account for the change in direction of the maximum stress axes ol and σ₃.

About 1 km to the south–east of the studied area is the syenitic intrusive body of Cabo Frio Island belonging to the same magmatic event. Earlier papers failed to define the precise mode of emplacement of this body. The lithology around Cabo Frio Island syenite suggests that the emplacement mode was similar to that of the Mendanha body in Nova Iguaçu (Motoki et al., 2007a), and of the Itaúna body in São Gonçalo (Motoki et al., 2007b; Fig. 1), both in the State of Rio de Janeiro. They correspond to the root of an upward mushrooming pluton. They could be stereotypes of the Cabo Frio Island syenitic intrusive.

The Cabo Frio Island intrusion and its horizontal ballooning expansion could have produced a transient but strong horizontal stress in radial directions, that might have included the study area situated on the same level. This horizontal stress could partly account for the change in σ₃ direction from horizontal to vertical (Fig. 10).

Fracture–fill and hydraulic fracturing

Field observations of tabular intrusives in the Arraial do Cabo area indicate that the self–propagating cracks originated from hydraulic fracturing by magma pressure. It is the main intrusion mechanism of the tabular rock bodies. Hydraulic fracturing occurs when σ₁, σ₂, and σ₃ are large enough, magma pressure is high enough in terms of the tensile strength of the host rock, and the deviator stress is adequate. If these conditions are not all fulfilled, magma intrusion may take place along pre–existing fractures. Motoki (1986) showed that small branches of phonolithic dykes, less than 5 cm wide, show intrusion along pre–existing fractures. This phenomenon might be due to insufficient magma pressure. Valentine and Krogh (2006) described dyke intrusions along host rock structures in very shallow subvolcanic sites. This may be due to insufficient lithostatic stress. At Arraial do Cabo, the intrusions along pre–existing host rock structure take place at the dyke–sill transition level (Fig. 3, 4).

Conclusion

The intrusion mode of alkaline felsic tabular bodies in the Arraial do Cabo area, State of Rio de Janeiro, Brazil, and especially the dyke–sill transitions, cannot be explained by a traditional intrusion model involving the filling of pre–existing fractures. The field observations fit a hydraulic fracturing model powered by magma pressure. According to this model, vertical intrusion takes place where σ₁ is vertical and σ₃ is horizontal, which happens ordinarily at deep sites. Horizontal intrusion occurs where σ₁ is horizontal and σ₃ is vertical, usually at shallow depth. Local plastic deformation of the host rock by hot magma is important in order to define the tapered shape of tabular intrusive bodies. Dyke–sill transitions occur at a depth where the vertical maximum stress axis changes from σ₁ to σ₃. In some cases within the studied area, the dyke–sill transition may not be related to intrusion depth variations. The horizontal stress needed for a transition could originate from the intrusion itself, and from horizontal ballooning of the Cabo Frio Island syenitic body. Magma intrusions along pre–existing fractures do also take place under certain conditions, such as insufficient magma pressure, very shallow depth, and the dyke–sill transition process.

Acknowledgements

The authors are grateful to Dr. Ciro Alexandre Ávila of Rio de Janeiro State University and Dr. Henrique Llacer Roig of Brasilia University for assistance in field work for their PhD thesis, and to Dr. Yoji Kobayashi of Tsukuba University (retired), Dr. Kazuaki Nakamura of the University of Tokyo (deceased), and Dr. Tadahide Ui of Hokkaido University (retired), for helpful discussions. The authors are grateful to Dr. Julio Cesar Horta de Almeida of Rio de Janeiro State University for his encouragement toward the conclusion of the present paper.

Bibliography

Almeida, F. F. M., 1986. Distribuição regional e relações tectônicas do magmatismo pós –Paleozóico no Brasil. Revista Brasileira de Geociências, 16, 325–349.        [ Links ]

Bacon, C. R., R. Macdonald, R. L. Smith and A. Baedecker, 1981. Pleistocene high silica rhyolites of the Coso volcanic field, Inyo Country, California. Journal of Geophysical Research, 86, 10223–10241.        [ Links ]

Bates, R. and J. A. Jackson, 1987. Glossary of Geology, 3rd edition. McGraw–Hill Book Company, 788 p.        [ Links ]

Bear, G., M. Beyth and Z. Reches, 1994. Dikes emplaced into fractured basement, Timna Igneous Complex, Israel. Journal of Geophysical Research, 99, 24039–24050.        [ Links ]

Bellieni, G., P. Comin–Chiarmonti, L. S. Marques, A. J. Melfi, E. M. Piccirillo, A. J. R. Nardy and A. Rosemberg, 1984. High– and low–TiO2 flood basalts from the Paraná plateau (Brazil): petrology and geochemical aspects bearing on their mantle origin. Neues Jahrbuch für Mineralogie–Abhandlungen, 150. 273–306.        [ Links ]

Bennio, L., P. Brotzu, M. D'Antonio, G. Feraud, C. B. Gomes, A. Marzoli, L. Melluso, L. Morbidelli, V. Morra, C. Rapaille and R. Excelso, 2003. The tholeiitic dyke swarm of the Arraial do Cabo peninsula (SE Brazil): ³⁹Ar/⁴⁰Ar ages, petrogenesis, and regional significance. Journal of South American Earth Sciences, 16–2, 163–176.        [ Links ]

Bermudez, A., D. Delpino, F. Frey and A. Sall, 1993. Los basaltos extraandinos. Relatorio del XII Congreso Geológico Argentino, 1, 161–172.        [ Links ]

Best, M. G., 1982. Igneous and metamorphic petrology. W.H. Freeman and Company, New York. 630 p.        [ Links ]

Billings, M. P., 1972. Structural Geology. Prentice–Hall Inc. Englewood Cliffs, New Jersey, USA. 606 p.        [ Links ]

Campos Neto, M. C. and R. Caby, 2000. Terrane accretion and upward extrusion of high–pressure granulites in the Neoproterozoic nappes of southeast Brazil: Petrologic and structural constraints. Tectonics, 19–4, 669–687.        [ Links ]

Campos Neto, M. C., 2000. Orogenic systems from SW–Gondwana: An approach to Brasiliano–Pan African Cycle and orogenic collage in SE–Brazil. In: U.G. Cordani, E.J. Milani., A. Thomáz Filho, D.A. Campos (Eds.), Tectonic Evolution of South America. 31th International Geological Congress, Rio de Janeiro, 335–365.        [ Links ]

Chevallier, L. and W. J. Verwoerd, 1987. A dynamic interpretation of Tristan da Cunha volcano, South Atlantic Ocean. Journal of Volcanology and Geothermal Research, 34, 35–49.        [ Links ]

Clavero, J. and H. Moreno, 2004. Evolution of Villarica Volcano. Boletín del Servicio Nacional de Geología y Minería, Gobierno de Chile, 61, –27.        [ Links ]

Decart, K., G. Feraud, L. S. Marques, and H. Bertrand, 1998. New time constrains on dyke swarms related to the Paraná–Etendeka magmatic province, and subsequent South Atlantic opening, southeast Brazil. Journal of Volcanology and Geothermal Research, 80, 68–83.        [ Links ]

Delaney, P. T. and A. E. Gartner, 1997. Physical processes of shallow mafic dike emplacement near the San Rafael Swell, Utha. Geologycal Society of America Bulletin, 109, 1117–1192.        [ Links ]

Delaney, P. T., D. D. Pollard, J. I. Ziony and E. H. Mckee, 1986. field relations between dikes and joints: emplacement processes and paleostress analyses. Journal of Geophysical Research, 91, 4920–4983.        [ Links ]

Dinham, C. H. and B. O. Haldane, 1932. The economic geology of the Stirling and Clackmannan Coalfield, Mem. Geol. Sur. Scotland, 242 p. (cited in Hall, 1987).        [ Links ]

Emerman, S. H. and R. Marrett, 1990. Why dikes? Geology, 18–3, 231–233.        [ Links ]

Feraud, G. and R. Campredon, 1983. Geochronology and structural study of Tertiary and Quartenary dikes in southern France and Sardinia: An example of utilization of dike swarms as paleostress indicators. Tectonophysics, 98, 297–325.        [ Links ]

Ferrari, A. L., 2001. Evolução Tectônica do Graben da Guanabara. Doctor Thesis. Instituto de Geociências da Universidade de São Paulo, 412 p. (unpublished)        [ Links ]

Hackspacher, P. C., L. F. B. Ribeiro, M. C. S. Ribeiro, A. H. Fetter, J. C. N. Hadler, C. A. S. Tello and E. L. S. Dantas, 2003. Consolidation and Break–up of the South American Platform in Southeastern Brazil: Tectonothermal and Denudation Histories. Gondwana Research, 7–1, 91–101.        [ Links ]

Haimson, B. C., 1975. Deep in–situ stress measurements by hydrofracturing. Tectonophysics, 29, 41–47.        [ Links ]

Hall, A., 1987. Igneous petrology. John Wiley & Sons, Inc. New York., 573 p.        [ Links ]

Hatayama, Y. and 344 coauthors, 1980. Chigaku Jiten (Geological Dictionary). The Association for Geological Collaboration. Heibonsha K.K., Tokyo, 1612 p. (in Japanese).        [ Links ]

Heilbron, M., W. Mohriak, C. M. Valeriano, E. Milani, J. C. A. Almeida, and M. Tupinambá, 2000. From collision to extension: the roots of the southeastern continental margin of Brazil. In: Mohriak, W.U. and Talwani, M. (Eds.), Geophysical Monograph, American Geophysical Union, 115: 1–32.        [ Links ]

Heilbron, M., S. Valente, P. Szatmari, J. C. H. Almeida, B. P. Duarte, J. Lobo, E. Guedes, A. Corval, M. Arena, T. Dutra, C. Valladares, C. Valeriano, L. Silveira, L. Sanchez and L. G. E. Silva, 2007. Episódios tectono–magamáticos de idade mesozóica e cenozóica na região SE brasileira e Bacias marginais: implicações e geodinâmicas. 11° Simpósio Nacional de Estudos Tectônicos, 5º International Symposium on Tectonics of Sociedade Brasileira de Geologia, Natal, 1p.        [ Links ]

Helmbold, R., 1967. Resumo da geologia do Estado da Guanabara. Relatório da Comissão Especial do CNPq, 5: 31–34.        [ Links ]

Helmbold, R., 1968. Basic and alkaline intrusions in the State of Guanabara, Brazil. Anais da Academia Brasileira de Ciências, 40, 183–185.        [ Links ]

Helmbold, R., J. G. Valença and O. H. L. Leonardos Jr., 1965. Mapa geológico do Estado da Guanabara, escala 1:50,000. MME/DNPM, Rio de Janeiro.        [ Links ]

Hergt, J. M., D. W. Peate and C. J. Hawkesworth, 1991. The petrogenesis of Mesozoic Gondwana low–Ti flood basalts. Earth and Planetary Science Letters, 105, 134–148.        [ Links ]

Hills, E. S., 1975. Elements of structural geology. Chapman and Hall. Ltd., London. 501 p.        [ Links ]

Holberg, E., 1973. Descripción geológica de la hoja 29d, Cerro Nevado. Pcia. de Mendoza. Dirección Nacional de Geología y Minería, República Argentina.        [ Links ]

Hori, K. and Y. Kobayashi, 1980. Determination of tectonic stress orientation in the Sunda Arc by means of dyke method. Bulletin of the Volcanological Society of Japan, 25–1, 33–44. (in Japanese).        [ Links ]

Hubbert, M. K. and D. G. Willis, 1957. Mechanics of hydraulic fracturing. Transactions of the American Institute of Mining, Metallurgical, and Petroleum Engineers, 210, 153–164.        [ Links ]

Kobayashi, Y., 1979a. Late Neogene dike swarms and regional tectonic stress field in the inner belt of southeast Japan. Bulletin of the Volcanological Society of Japan, 24, 153–168. (in Japanese).        [ Links ]

Kobayashi, Y., 1979b. Early and middle Miocene dike swarms and regional tectonic stress field in the southeast Japan. Bulletin of the Volcanological Society of Japan, 24, 203–212. (in Japanese).        [ Links ]

Lara, L., C. Rodríguez, Hugo Moreno and C. P. Arce, 2001. Geocronología K–Ar y geoquímica del volcanismo plioceno superior–pleistoceno de los Andes del sur (39–42°S). Revista Geológica de Chile, 28–1, 67–90.        [ Links ]

Laughlin, A. W., M. J. Aldrich and D. T. Vaniman, 1983. Tectonic implications of mid–Tertiary dikes in west–central New Mexico. Geology, 11, 45–48.        [ Links ]

Lima, P. R. A. S. 1974. Geologia da Ilha de Cabo Frio. Anais do 28° Congresso Brasileiro de Geologia, 1, 176–181.        [ Links ]

Lima, P.R.A.S., 1976. Geologia dos maciços alcalinos do Estado do Rio de Janeiro. Parte I – Localização e geologia dos maciços. Semana de Estudos Geológicos, Universidade Federal Rural do Rio de Janeiro, 205–245.        [ Links ]

Lister, J. R. and R. C. Kerr, 1991. Fluid–mechanical models of crack propagation and their application to magma transport in dykes. Journal of Geophysical Research, 96, 10049–10077.        [ Links ]

Llambías, E. J., 2003. Geología de los Cuerpos Ígneos. Asociación Geológica Argentina Serie B Didáctica y complementaria, 27, Buenos Aires. 182 p.        [ Links ]

Motoki A., C. A. Ávila and H. L. Roig, 1988. Estudos litológicos e geológicos dos corpos tabulares no município de Arraial do Cabo, RJ. Anais do 35° Congresso Brasileiro de Geologia, 6, 2727–2739.        [ Links ]

Motoki, A., 1986. Geologia e Petrologia do Maciço Alcalino da Ilha de Vitória, SP. PhD These, Instituto de Geociências da Universidade de São Paulo.        [ Links ]

Motoki, A., 1994. A possible fossil earthquake swarm? – Relationship between Mesozoic basaltic dykes and their linkage faults. Journal of Geography, 103–3, 548–557.        [ Links ]

Motoki, A., J. A. T. Leal, J. C. V. Campos, C. A. Ávila and H. L. Roig, 1990. Real relacionamento entre orientação dos diques basálticos e alcalinos leucocráticos e dos diaclasamentos da sua rocha encaixante metamórfica de Arraial do Cabo, RJ. Boletim de Resumos do 36° Congresso Brasileiro de Geologia, 281.        [ Links ]

Motoki, A., R. Soares, A. M. Netto, S. E. Sichel and J. R. Aires, 2007a. Reavaliação do modelo genético do Vulcão de Nova Iguaçu, RJ: origem eruptiva ou intrusão subvulcânica? Revista Escola de Minas. (in press).        [ Links ]

Motoki, A., R. Soares, A. M. Netto, S. E. Sichel, J. R. Aires, M. Lobato, 2007b. Mecanismo físico de soldamento e fluxo secundario no conduto subvulcánico piroclástico do Complexo Alcalino Intrusivo de maciço Itaúna, São Gonçalo, RJ. Bulletin of the 10th International Congress of the Brazilian Geophysical Society, Rio de Janeiro, CD, 6 p.        [ Links ]

Nakamura, K., 1977. Volcanoes as possible indicators of tectonic stress orientation; Principle and proposal, Journal of Volcanology and Geothermal Research, 2, 1–16.        [ Links ]

Nakamura, K., J. N. Jacob and K. H. Davies, 1977. Volcanoes as possible indicators of tectonic stress orientation; Aleutians and Alaska, Pure and Application Geophysics, 115, 87–112.        [ Links ]

Nicolas, A. and M. Jackson, 1982. High temperature dikes in peridotites: Origin by hydraulic fracturing. Journal of Petrology, 23–4, 568–582.        [ Links ]

Ode, H., 1957. Mechanical analysis of the dike pattern of the Spanish Peaks area, Colorado. Geological Society of America Bulletin, 68, 567–576.        [ Links ]

Parsons, T. and G. A. Thompson, 1992. The Role of magma overpressure in suppressing earthquakes and topography: worldwide examples. Science, 253, 1399–1402.        [ Links ]

Peate, D. W., 1997. The Paraná–Etendeka Province, In. Maboney J.J., Coffin, M.F. (Eds.) Large igneous provinces, American Geophysical Union Monograph, 100, 217–245.        [ Links ]

Peate, D. W., C. J. Hawkesorth and M. S. M. Mantovani, 1992. Chemical stratigraphy of the Paraná lavas (South America): classification of magma types and their spatial distribution. Bulletin of Volcanology, 55, 119–139.        [ Links ]

Phillips, W. J., 1974. The dynamic emplacement of cone sheets. Tectonophysics, 24, 69–84.        [ Links ]

Ricommini, C., L. G. Sant'anna and A. L. Ferrari, 2004. Evolução geológica do rift continental do Sudeste do Brasil. In Mantesso–Neto, V., Bartorelli, A., Carneiro, C.D.R., Brito–Neves, B.B. Ed. Geologia do Continente Sul–Americno: Evolução da obra de Fernando Flávio Marques de Almeida. São Paulo. Editora Beca, 385–405.        [ Links ]

Ricommini, C., 1997. Arcabouço estrutural e aspectos do tectonismo gerador e deformador da bacia Bauru no estado de São Paulo. Revista Brasileira de Geociências, 27–2, 153–162.        [ Links ]

Rubin, A. M., 1993. Tensile fracture of rock at high confining pressure: implications for dike propagation. Journal of Geophysical Researches, 98, 15919–15935.        [ Links ]

Rubin, A. M., 1995. Propagation of magma–filled cracks, Annual Review of Earth and Planetary Sciences, 23, 287–336.        [ Links ]

Schmitt, R. S., R. A. J. Trouw, W. R. Van Schmus and M. M. Pimentel, 2004. Late amalgamation in the central part of West Gondwana: new geochronological data and the characterization of a Cambrian collisional orogeny in the Ribeira Belt (SE Brazil). Precambrian Research, 133, 29–61.        [ Links ]

Schmitt, S. R. and N. Stanton, 2007. Cronologia relativa das estruturas rúpteis e diques meso–cenozóicos na porção onshore do alto do Cabo Frio – Região costeira e ilhas adjacentes, RJ. Anais do 11° Simpósio Nacional de Estudos Tectônicos, 5th Internacional Symposium on Tectonics of the SBG. 221–223.        [ Links ]

Southwick, D. L. and W. C. Day, 1983. Geology and petrology of Proterozoic mafic dikes, north central Minnesota and western Ontario. Canadian Journal of Earth Sciences, 20, 622–638.        [ Links ]

Takeuchi, A., 1980. Temporal changes of regional stress field and tectonics of sedimentary basin. Journal of the Geological Society of Japan. 87, 737–751. (in Japanese).        [ Links ]

Trouw R.A., M. Heilbron, A. Ribeiro, F. V. P. Paciullo, C. Valeriano, J. H. Almeida, M. Tupinambá, and R. Andreis, 2000. The Central Segment of the Ribeira belt. In: U.G. Cordani, E.J. Milani., A. Thomáz Filho, D.A. Campos (Eds), Tectonic Evolution of South America. 31st International Geological Congress, 297–310.        [ Links ]

Turner, S., M. Regelous, S. Kelley, C. Hawkesworth and M. Mantovani, 1994. Magmatism and continental break–up in the South Atlantic: high precision ⁴⁰Ar/³⁹Ar geochronology. Earth and Planetary Science Letters, 121, 333–348.        [ Links ]

Ui, T., M. Kono, Y. Hamano, F. Monge and Y. Aota, 1984, Reconstruction of a volcanic edifice using the dike swarm at Ocros, Peruvian Andes. Bullin of the Volcanological Society of Japan, 29–4, 285–296.        [ Links ]

Valença, J.G., 1976. Geologia dos maciços alcalinos do Estado do Rio de Janeiro. Parte II – Correlações geológicas. Semana de Estudos Geológicos, Universidade Federal Rural do Rio de Janeiro, 247–259. (unpublished).        [ Links ]

Valente, S., B. P. Duarte, M. Heilbron, J. C. H. Almeida, C. S. Valladares, E. Guedes, W. Tetzner, J. Lobo, A. Corval, T. Dutra, L. H. Soares, F. M. Souza, J. Vinha and N. Famalli, 2005. Mapa de enxame de diques da Serra do Mar. Anais do III Simpósio de Vulcanismo e Ambientes Associados, CD, 5 pp.        [ Links ]

Valentine, A. G. and K. E. C. Krogh, 2006. Emplacement of shallow dikes and sills beneath a small basaltic volcanic center – The role of pre–existing structure (Paiute Ridge, southern Nevada, USA). Earth and Planetary Science Letters, 246, 217–230.        [ Links ] ]]> 1986 16 16 325-349 1981 86 86 10223-10241 1987 3 788 1994 99 99 24039-24050 1984 150 150 273-306 2003 16-2 16-2 163-176 1993 1 161-172 1982 630 1972 606 2000 19-4 19-4 669-687 2000 Rio de Janeiro 335-365 1987 34 34 35-49 2004 61 27 1998 80 80 68-83 1997 109 109 1117-1192 1986 91 91 4920-4983 1932 242 1990 18-3 18-3 231-233 1983 98 98 297-325 2001 412 2003 7-1 7-1 91-101 1975 29 29 41-47 1987 573 1980 1612 2000 115 1-32 2007 1 1967 5 31-34 1968 40 40 183-185 1965 1991 105 105 134-148 1975 501 1973 1980 25-1 25-1 33-44 1957 210 210 153-164 1979 a 24 24 153-168 1979 b 24 24 203-212 2001 28-1 28-1 67-90 1983 11 11 45-48 1974 1 176-181 1976 205-245 1991 96 96 10049-10077 2003 27 182 1988 6 2727-2739 1986 1994 103-3 103-3 548-557 1990 281 2007 a 2007 b Rio de Janeiro 6 1977 2 2 1-16 1977 115 115 87-112 1982 23-4 23-4 568-582 1957 68 68 567-576 1992 253 253 1399-1402 1997 100 217-245 1992 55 55 119-139 1974 24 24 69-84 2004 385-405 1997 27-2 27-2 153-162 1993 98 98 15919-15935 1995 23 23 287-336 2004 133 133 29-61 2007 221-223 1983 20 20 622-638 1980 87 87 737-751 2000 297-310 1994 121 121 333-348 1984 29-4 29-4 285-296 1976 247-259 2005 5 2006 246 246 217-230