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The Baie Verte Lineament, Newfoundland: Ophiolite Complex Floor and Mafic Volcanic Fill of a Small Ordovician Marginal Basin

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The Baie Verte Lineament, Newfoundland: Ophiolite Complex Floor and Mafic Volcanic Fill of a Small Ordovician Marginal Basin Reprinted From Island Arcs, Deep Sea Trenches and Back-Arc Basins, Maurice Ewing Series, VolumeI © 1977 American Geophysical Union THE BAIE VERTE LINEAMENT, NEWFOUNDLAND: OPHIOLITE COMPLEX FLOOR AND MAFIC VOLCANIC FILL OF A SMALL ORDOVICIAN MARGINAL BASIN W. S.F. Kidd Department of Geological Sciences State University of New York at Albany, Albany, New York 12222 Abstract. The Baie Verte Lineament, located cline with subsequent moderate-angle overturning in the Burlington Peninsula, northwest Newfoundland, and eastward thrusting, followed by oversteepening is a steeply-dipping linear belt 90 km long by 1 to 5 of the main zone of the Lineament due to continued km wide containing a variably disrupted ophiolite convergence of the two rigid bounding blocks. This suite and other mainly mafic volcaniclastic and behavior, rather than subduction, was probably due volcanic rocks that originally overlay the ophiolite to the small width of the basin. The best present- complex. The ophiolite complex closely resembles day analogues to the Baie Verte basin can be found others interpreted as samples of oceanic crust and in the small basins in the upper mantle, although the thickness of the gabbro rear of the southern New Hebrides arc. It is sug- layer is less than 1 km. The overlying mafic gested that the rocks exposed in the Baie Verte volcaniclastic sediments show evidence of deposition Lineament provide useful information about parts of close to (and locally at) the base of a steep scarp present-day marginal basins that are mostly bounding the east side of the basin. Minor silicic inaccessible to direct observation. tuffs are found near the top of the preserved sequence. Mafic pillow lavas comprise from 0 to 80% of the sediment section whose total preserved Introduction thickness before deformation is estimated as 5 km. Lavas within the sediment section have a chemistry Wilson's [1966] suggestion that the Appalachian- closely resembling samples dredged from the Marianas Caledonian orogenic belt was the site of opening Basin, while the pillow lavas and dykes of the and subsequent closing of a major ocean basin has ophiolite complex are of a distinctly different been very fruitful both in the reinterpretation of composition and include some komatiites. its geology in terms of the effects of plate The rocks of the Lineament are tectonically tectonics [Dewey, 1969; Bird and Dewey, 1970; Dewey bounded on both sides by polyphase-deformed meta- and Bird, 1971; Stevens, 1970; Church and Stevens, sediments, metavolcanics and metaplutonic rocks, 1971] and for the interpretation of the geological generally of coarse-grained epidote-amphibolite corollaries of plate tectonics in general [Dewey metamorphic facies. These rocks were metamorphosed and Bird, 1970, 1971]. Although the quantitative and deformed prior to formation of the ophiolite plate motions responsible for the geology of complex and supplied some clearly identifiable Paleozoic and older orogenic belts will almost detritus to the lowest sediments to prove it. They certainly never be known, this situation is also behaved as rigid bounding blocks to the Lineament. true for many Mesozoic and Tertiary belts [Dewey et The local and regional structural, stratigraphic and al., 1973]. Therefore, even though the relative detrital derivation evidence shows that the plate motions responsible for parts of orogenic Lineament is best interpreted as belts are unlikely to be more precisely definable the remains of a small marginal basin. Its width was than having been convergent probably not more than 50 km (and probably less), or divergent, useful information about the geolog- after spreading in it ceased. It lay in the basement ical effects of plate tectonics may be obtained from to an Early Ordovician island arc, on the side remote any orogenic belt if the rocks concerned are well from the trench, on the American side of the exposed and were not severely disrupted and deformed Appalachian-Caledonian (Iapetus) Ocean. The basin during final closure of the ocean. In particular, remained undeformed until Middle Devonian time, when information may be obtained on features not readily it closed as a consequence of the Acadian continental accessible to sampling in the same tectonic collision that shut the Northern Appalachian Ocean. environment near present plate and continental Closure of the Baie Verte basin did not, it appears, margins. involve subduction, The northwestern Newfoundland Appalachians have but occurred by initial formation of a large syn- superb coastal exposures in a section across strike and are in an area that was relatively KIDD 407 little deformed during the Acadian collision that dence detailed below bears on this problem and is closed this sector of the ocean [Dewey and Kidd, discussed in a regional context; however, the main 1974]. They possess three sharply defined belts of purpose of this paper is to illustrate the rocks containing well-preserved ophiolite complexes evolution of a particular marginal basin and to (Fig. 1) that are of interest both as samples of draw some conclusions from it about marginal basins oceanic crust and mantle and for the nature of in general. their type of origin and mode of emplacement. This The rocks adjoining the western side and the paper deals with one of these ophiolitic belts, the northern part of the eastern side of the Baie Verte Baie Verte Lineament (Fig. 1). This is a steeply- Lineament are polyphase deformed, thoroughly dipping, linear belt 90 km long by 1 to 5 km wide recrystallized, generally epidote-amphibolite containing a variably disrupted ophiolite suite and facies metasedimentary and metavolcanic schists, other mostly mafic volcaniclastic and volcanic the Fleur de Lys Supergroup [Church, 1969], part rocks that originally overlay the ophiolite of the western margin clastic wedge of the New- complex. Several more or less plausible and foundland Appalachians (Fig. 1). These rocks, which comprehensive evolutionary schemes, seen in terms include some gneissic granitic basement to the west of the geologic corollaries of plate tectonics, [deWit, 1974] are lithologically correlated with the have been proposed for the development of the lower part of the autochthonous Cambro-Ordovician northwest Newfoundland Appalachians. Although these miogeocline of the Western Platform, and with the schemes differ considerably in various respects, Cambrian and older part of the allochthonous most workers now appear to agree with the view of sedimentary rocks of the Humber Arm and Hare Bay Dewey and Bird [1971] that the ophiolite complexes allochthons (Fig. 1). The latter and most of the and associated rocks were formed as the crust and Fleur de Lys Supergroup are interpreted as early fill to one or more early Ordovician marginal graben fill and overlying continental rise sediments basins. There is disagreement, however, over the developed on this margin of the opening Appalachian site or sites of origin of the basins with their ocean [Dewey, 1969; Stevens, 1970; ophiolite complex floor, and hence on the 'root Bird and Dewey, 1970]. Along most of its eastern zone" for the now allochthonous sheets of the Bay side, the Baie Verte Lineament is bounded by an of Islands and Hare Bay ophiolite complexes (Fig. extensive granodiorite, the Burlington Granodiorite. 1). Evi- This intruded rocks of the Fleur de Lys Supergroup early in, or prior to, their complex deformation [Kidd, 1974], and therefore belongs with the Fleur de Lys structural assemblage. The rocks it intrudes are mafic metavolcaniclastic and metavolcanic schists, which pass to the east conformably and transitionally upwards into an assemblage of silicic metavolcanic and metavolcaniclastic schists and subjacent plutonic rocks, the Grand Cove Group and Cape Brule porphyry [Church, 1969]. A suggestion [DeGrace et al., 1975] that the Grand Cove Group is equivalent to the late Ordovician or younger Cape St. John Group (also silicic volcanics and related rocks) has not yet, in the author's view, been satisfactorily demonstra- ted. The ophiolitic Baie Verte Lineament thus lies within a zone of complexly deformed and medium- grade metamorphic rocks while itself containing rocks that, although moderately to strongly deformed, are not metamorphosed beyond green- schist facies. The Baie Verte Group has not been directly dated, but is presumed to be Arenigian (early Ordovician) in age due to its very close lithological and stratigraphic resemblance to the fossil-dated Snooks Arm Group. The latter is found 30 km from the Baie Verte Lineament on the east cost of the Burlington Peninsula (Fig. 1). During the early and middle Ordovician, the rock assemblages found to the southeast of the Burlington Peninsula in the Notre Dame Bay region are interpreted [Dewey and Bird, 1971] as representing a volcanic island arc succeded to the southeast by an arc-trench gap, in turn adjoined by an extensive Fig. 1. Major tectonic zones of the Newfoundland melange (Dunnage) interpreted as a trench- Appalachians (black - ophiolites and related rocks; wall assemblage (Fig. 1). The spreading age of stippled - medium T/P metamorphic belts). the Bay of Island ophiolites is probably Trema- 408 KIDD docian (earliest Ordovician), and their obduction ophiolite complex pillow lavas stratigraphically into their present allochthonous position, in an below, and a further section of about 1 km exogeosyncline developed on the previous carbonate (probably at least 2 km before deformation) of miogeocline, occurred during medial Ordovician time pillow
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