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Petrogenesis of Siluro-Devonian Rhyolites of the Tobique Group In Downloaded from http://sp.lyellcollection.org/ by guest on January 13, 2021 Petrogenesis of Siluro-Devonian rhyolites of the Tobique Group in the northwestern Appalachians (northern New Brunswick, Canada): tectonic implications for the accretion history of peri-Gondwanan terranes along the Laurentian margin Jaroslav Dostal1*, Reginald A. Wilson2 and Pierre Jutras1 1Department of Geology, Saint Mary’s University, Halifax, Nova Scotia, Canada B3H 3C3 2235 Flemming Road, Fredericton, New Brunswick, Canada E3B 5J8 JD, 0000-0002-3110-4270 *Correspondence: [email protected] Abstract: Uppermost Silurian–Lower Devonian felsic rocks in the bimodal volcanic suite of the Tobique Group in the northwestern mainland Appalachians (northern New Brunswick, Canada) form part of an overstep sequence deposited across the accreted vestiges of Iapetus Ocean on composite Laurentia. Whereas the mafic rocks of the bimodal volcanic suite are continental tholeiites, the felsic rocks are peraluminous and possess geo- chemical characteristics of A2-type granites emplaced in post-collisional extensional settings. The major and trace element compositions of the felsic rocks indicate that they were generated by dehydration melting of late Precambrian granitoid rocks triggered by heat derived from the rising mafic magma. Unlike the basalts, which have positive εNd(t) values, the felsic rocks have values close to chondrites (−1.6 to +1.1), which is con- sistent with derivation from a crustal source. The rapid transition from compressional to extensional magmatism in latest Silurian–Early Devonian times in this part of Ganderia is probably due to Late Silurian Ganderia– Laurentia collision followed by slab breakoff. Based on Sm–Nd isotopic characteristics in their respective igne- ous rocks, both Ganderia and Avalonia are underlain by similar Neoproterozoic lower–middle crust and subcontinental lithospheric mantle. The Appalachian–Caledonide accretionary orogen Late Silurian Salinic Orogeny (c. 430–422 Ma) but was formed by the Paleozoic closure of the Iapetus, prior to the beginning of the Early–Middle Devonian Tornquist and Rheic oceans (e.g. Williams and Acadian Orogeny, which is attributed to the accre- Hatcher 1982). The northern Appalachian part of tion of the peri-Gondwanan microcontinent of Ava- this orogen records the closure of the early Paleozoic lonia (van Staal et al. 2009; Zagorevski et al. 2010; Iapetus Ocean, and the collision and accretion of Tremblay and Pinet 2016 and references therein). island arcs, seamounts and microcontinents that The abundant uppermost Silurian–Lower Devonian were located in the Iapetus Ocean between Laurentia volcanic rocks of the MCS in central and northern and Gondwana (e.g. van Staal et al. 2009, 2012). New Brunswick and southeastern Quebec occur However, the details of terrane accretion and defor- dominantly as bimodal suites. The mafic volcanic mational events are still under discussion. Much of types are considered to be rift-related (Dostal et al. the critical information on these processes can be 1989, 1993, 2016). However, as with many other obtained from the investigation of successor basins similar bimodal suites, the origin of the felsic mem- that overstep and link major elements of the orogen. bers has been under debate and, in fact, the petro- In the northwestern mainland Appalachians genetic aspects of the uppermost Silurian–Lower (Fig. 1), abundant uppermost Silurian–Lower Devonian felsic volcanic rocks in this part of Canada Devonian sedimentary and volcanic rocks form the have not yet been investigated in detail. The origin of upper part of an overstep sequence (the Matapedia the felsic rocks in bimodal suites is also an important cover sequence: MCS) deposited across the accreted key to the understanding of the evolution of the con- vestiges of Iapetus on composite Laurentia. These tinental crust (e.g. McBirney 2006). In this paper, we volcanic rocks can provide clues regarding the present whole-rock major and trace element data, as regional Late Silurian–Early Devonian geological well as Nd isotopic data, for volcanic rocks of the setting and the tectonic events that resulted in the Tobique Group in the MCS (Fig. 2). The focus of accretion of terranes to the eastern margin of Lauren- this paper is on the felsic rocks of the bimodal tia. The rocks were emplaced after the Middle–early suite; specifically, the aim is to (1) constrain their From: Murphy, J. B., Strachan, R. A. and Quesada, C. (eds) 2021. Pannotia to Pangaea: Neoproterozoic and Paleozoic Orogenic Cycles in the Circum-Atlantic Region. Geological Society, London, Special Publications, 503, 391–407. First published online June 1, 2020, https://doi.org/10.1144/SP503-2019-229 © 2020 The Author(s). Published by The Geological Society of London. All rights reserved. For permissions: http://www.geolsoc.org.uk/permissions. Publishing disclaimer: www.geolsoc.org.uk/pub_ethics Downloaded from http://sp.lyellcollection.org/ by guest on January 13, 2021 392 J. Dostal et al. Cover via Ganderia NORTH Greenland Scandina Carolinia AMERICA N Avalonia Red Indian Line Meguma realm Amorican Labrador Gondwanian terranes Gaspé Peninsula Great Laurentian realm Britain NB Craton Ireland New England Nova Scotia EUROPE Newfoundland Britttany AFRICA Iberia Fig. 1. The major lithotectonic units of the Appalachian–Caledonian orogenic belt in an Early Mesozoic restoration (modified after van Staal and Barr 2012; Dostal et al. 2016). evolution and origin, and, together with data on the the northern mainland Appalachians (Fig. 2). They associated mafic rocks, to (2) interpret their tectonic are primarily found in three volcanic belts in Maine setting and contribute to the debate on geodynamic and New Brunswick: the Piscataquis, Tobique- models for the closure of the Iapetus Ocean. The Chaleur and Coastal. The Piscataquis belt stretches investigation of the felsic rocks can also help to eval- discontinuously across north-central Maine (Osberg uate the nature of crustal basement. et al. 1989; Hon et al. 1992; Schoonmaker et al. 2011), whereas the Tobique-Chaleur belt extends in a SW–NE direction from west-central New Bruns- Geological setting wick to Chaleur Bay (Dostal et al. 1989, 2016; Wil- son and Kamo 2008, 2012; Wilson 2017), and As noted earlier, Upper Silurian–Lower Devonian farther to the NE in the Gaspé Peninsula of Québec volcanic rocks of northern New Brunswick are part (Dostal et al. 1993; D’hulst et al. 2008). The Coastal of the MCS (Fig. 2), which extends from the eastern belt extends for over 500 km along the coast of Mas- Gaspé Peninsula of Québec to northern and central sachusetts, Maine and New Brunswick but strikes Maine. The MCS is an Upper Ordovician–Lower inland in the vicinity of Saint John (Seaman et al. Devonian successor basin deposited unconformably 1999; Van Wagoner et al. 2002; Llamas and Hep- on Ordovician volcanic rocks of the Popelogan burn 2013). The volcanic centres are frequently asso- terrane, which in turn rests on Early Paleozoic and ciated with coeval intrusions. older continental substrate of Ganderia, a peri- The detailed stratigraphy and structural evolution Gondwanan microcontinent. Closure of the main of the MCS was presented by Wilson (2017). The tract of the Iapetus Ocean by southeasterly subduc- MCS has been divided into three structural zones, tion led to construction of the Andean-type Popelo- from NW to SE these are: the Connecticut Valley– gan arc, and culminated in accretion of Ganderia’s Gaspé Synclinorium, Aroostook–Percé Anticlino- leading edge to Laurentia in Late Ordovician time rium and Chaleur Bay Synclinorium (Wilson et al. (van Staal 1994; Wilson et al. 2004; van Staal 2004). The Chaleur Bay Synclinorium is subdivided et al. 2009, 2016; Zagorevski et al. 2010). Extension by the Rocky Brook–Millstream Fault into two parts and rifting of the Popelogan arc in the Middle Ordo- (Fig. 2): the Chaleur zone to the north and the Tobi- vician led to the opening of the Tetagouche back-arc que zone (the focus of this study) to the south. The basin and separation of Ganderia’s leading edge Tobique zone is mainly occupied by the Tobique from an outboard ‘trailing margin’ (van Staal et al. Group (Fig. 3), which is composed of marine sedi- 2016). NW-directed subduction of the Tetagouche mentary rocks (including turbidites) and bimodal back-arc basin between 450 and 425 Ma was accom- volcanic rocks that were emplaced in subaerial to panied by development of the Brunswick subduction submarine environments. The lower part of the Tobi- complex in northeastern New Brunswick, and culmi- que Group (the dominantly volcanic Costigan nated in the collision of Ganderia’s trailing margin Mountain, Cameron Mountain and Pentland Brook with composite Laurentia in the Middle–early Late formations) has been estimated to be as much as Silurian (Salinic Orogeny) (van Staal 1994; van 5000–6000 m thick, whereas the upper part of the Staal et al. 2009; Wilson et al. 2017). group (the dominantly sedimentary Wapske Forma- Upper Silurian–Lower Devonian volcanic rocks tion) is c. 8000 m thick (Wilson 2017). The felsic emplaced on Ganderian basement are widespread in rocks include rhyolite flows, felsic hyaloclastites, Downloaded from http://sp.lyellcollection.org/ by guest on January 13, 2021 Siluro-Devonian rhyolites, northern New Brunswick 393 Dalhousie 67°00’ 66°00’ Campbellton RS 48°00’ Québec Popelogan Inlier Elmtree Inlier N kilometres JRS 0102030 ult Fa stream Rocky Brook-Mill Bathurst CZ TZ Miramichi 47°30’ Inlier a C a n a d New Brunswick Québec Inliers of Cambrian to Dalhousie Group CG Ordovician rocks AP CB Tobique Group New Stratigraphic contact Mafic volcanic rocks Maine Fault USA Brunswick Felsic volcanic rocks Unconformity/disconformity Siliciclastic sedimentary rocks Dickie Cove Group Fig. 2. Simplified geology of the northern part of the Chaleur Bay Synclinorium (modified after Wilson et al. 2017). The Chaleur zone (CZ) is located north of the Rocky Brook–Millstream Fault and the Tobique zone (TZ) is south of the fault.
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