Igneous rock associations in Canada 3. Large Igneous Provinces in Canada and adjacent regions: 3 Ga to Present
Earth history is punctuated by numerous periods during which large volumes of mafic magma were emplaced. Such magmas not generated by a ‘normal’ spreading ridge or by subduction are termed Large Igneous Provinces (LIPs), and consist of continental flood basalts, volcanic rifted margins, oceanic plateaus, ocean basin flood basalts, submarine ridges, and seamount chains. Associated felsic rocks may also be present. LIPs of Mesozoic and Cenozoic age are typically the best preserved. Those of Paleozoic and Proterozoic age are usually more deeply eroded, and consist of flood basalt remnants and a deep-level plumbing system (of giant dyke swarms, sill provinces and layered intrusions). In the Archean the most promising LIP candidates are greenstone belts containing komatiites. Many LIPs have been linked to regional-scale uplift, continental rifting and breakup, and climatic crises. They can be used as precisely dated time markers in the stratigraphic record, and are key targets for Ni-Cu-PGE exploration. LIPs have also become a focus in the debate on the existence and nature of mantle plumes.
Canada has a rich record of LIPs. At least 80 candidates are recognized in Canada and adjacent regions, with ages ranging from 3100 to 17 Ma. We review proposed links between the LIP record of Canada and mantle plumes, continental breakup, regional uplift, and ore deposits. However, given that many mafic units in Canada remain poorly characterized, a concerted geochronology campaign with integrated paleomagnetism and geochemistry would be invaluable in expanding the application of the Canadian LIP record to solving major geological problems.
L’histoire de la Terre est ponctuee de nombreuses periodes de mise en place de forts volumes de magma mafiques. De tels magmas qui ne sont pas issus de zones d’expansion <> ou de subduction sont appeles Grandes provinces ignees (GPI), et celles-ci sont constituees de basaltes d’epanchements continentaux, de marges de fosse volcaniques, de plateaux oceaniques, d’epanchements de basaltes de bassins oceaniques, de cretes sous-marines, et de chaines de monts sous-marines. Peuvent egalement y etre associees des suites de roches felsiques. Generalement, les GPI du Mesozoique et du Cenozoique sont les mieux preservees. Celles du Proterozoique et du Paleozoique sont generalement plus fortement erodees et sont constituees de vestiges de basaltes d’epanchement et des reseaux de conduits d’origine (reseaux geants de dykes, provinces de filons-couches et d’intrusifs stratifiees). Dans l’Archeen, les meilleurs candidats sont representes par les bandes de roches vertes a komatiites. De nombreuses GPI ont ete associees a des episodes de soulevement regionaux, de derives ou de fragmentations continentales, ainsi qu a des crises climatiques. Elles peuvent servir de marqueurs temporels stratigraphiques et sont des cibles de premiere importance dans l’exploration de gisements de Cu-Ni-EGP. Les GPI sont aussi devenues des arguments tres consideres dans le debat sur l’existence et la nature des panaches mantelliques.
Le Canada possede de riches archives de GPI, et au moins 80 candidatures ont ete isolees sur le territoire canadien et dans les regions adjacentes, leur age delimitant une fourchette allant de 3 100 Ma a 17 Ma. Nous passons en revue les liens proposes entre la suite des GDI canadiennes d’une part, et celle des panaches mantelliques, des fragmentations continentales, des soulevements regionaux, et des gisements mineraux, d’autre part. Toutefois, vu le pietre etat de caracterisation des unites mafiques au Canada, une campagne de caracterisation geochronologique, paleomagnetique et geochimique serait d’une valeur inestimable pour favoriser l’utilisation des GDI canadiennes pour nous aider a solutionner de grands problemes geologiques.
Large Igneous Provinces (LIPs) represent voluminous magmatic events that were not generated by a ‘normal’ spreading ridge or by subduction (Coffin and Eldholm, 1994; 2001; Ernst et al., 2004). They may be emplaced as often as once every 10 Ma (e.g. Coffin and Eldholm, 2001), and time series analysis of the LIP record for the past 3.5 Ga suggests weak cyclicity (Isley and Abbott, 2002; Prokoph et al., 2004).
The most dramatic LIPs are emplaced rapidly (within <10 Ma and often within only a few Ma). These include continental flood basalts, seaward-dipping reflector sequences, oceanic plateaus, and ocean basin flood basalts. Continental flood basalts can be as large as several million cubic km (e.g. the Siberian Traps; Reichow et al., 2002). The largest LIP is the Ontong Java oceanic plateau, which has a volume of 44.4 million cubic km (Coffin and Eldholm, 2001) for combined extrusive (6 million cubic km) and intrusive components (Courtillot and Renne, 2003). The initial large-volume short-duration stage of magmatism of some LIPs has been linked to the arrival of a mantle plume (e.g. White and McKenzie, 1989; Campbell and Griffiths, 1990; Coffin and Eldholm, 1994; 2001; Campbell, 1998, 2001; Ernst and Buchan, 2001; Courtillot et al., 2003). Subsequent rifting/breakup is often associated with a second burst of volcanism (Campbell, 1998) by decompression melting (White and McKenzie, 1989). In addition, LIP magmatism can continue for prolonged periods after the initial outburst (or outbursts), in the form of seamount chains and ridges, which are usually explained as hotspot tracks associated with a plume tail. Other models invoke plate fracturing and 'edge convection' (upper mantle convection between thick and adjacent thin lithosphere), and have been suggested as an alternative to plume models for LIPs and hotspot chains (e.g. Anderson, 2001; Foulger and Natland, 2003).
The volcanic portion of older continental LIPs is largely removed by erosion and deformed during continental collision, whereas older oceanic LIPs are mostly lost during subduction and deformed during ocean closure. Therefore, in the Paleozoic and Proterozoic record, continental LIPs are typically recognized by their exposed plumbing system of giant dyke swarms, sill provinces, large layered intrusions, and remnants of flood basalts (Ernst and Buchan, 2001). The oceanic LIP record may be recognized in some accreted volcanic packages and ophiolite complexes (e.g., Coffin and Eldholm, 2001; Moores, 2002).
The extrapolation of the LIP record into the Archean is more speculative. There are erosional remnants of typical flood basalt provinces, namely the Fortescue sequence of the Pilbara craton of Australia and the Ventersdorp sequence of the Kaapvaal craton of southern Africa (Eriksson et al., 2002). However, most Archean volcanic rocks occur as deformed and fault-fragmented packages termed greenstone belts. Among these, the best candidates for LIPs are thick tholeiite sequences that contain komatiites. The nature of Archean LIPs is discussed in greater detail below.
LIPs are important 1) for testing plume and non-plume models for the generation of LIPs; 2) as precise time markers for stratigraphic correlations; 3) as an aid in reconstructing continents; and 4) as the hosts of major PGE deposits and as a potential tool in diamond exploration. In addition, they can be helpful in studying 5) climatic effects, and 6) regional uplift. We return to these topics after a review of the LIP record of Canada and adjacent regions.
PRELIMINARY LIP HISTORY OF CANADA AND ADJACENT REGIONS
Our compilation is based on a recent summary of the global LIP distribution (Ernst and Buchan, 2001) and a newly published compilation of dyke swarms and related magmatic units in Canada and adjacent regions (Buchan and Ernst, 2004). We currently recognize at least 80 LIPs and possible LIP remnants in and adjacent to Canada. The Proterozoic and Phanerozoic mafic magmatic record is reviewed first since its links with LIPs are better defined (Table 1, Fig. 1). The more speculative Archean LIP history follows (Table 2, Fig. 1).
The Proterozoic record relies heavily on diabase dyke swarms and sills (Fig. 2). Dykes injected laterally into the interior of continents have a preservation potential that is much greater than that of associated lavas, and therefore provide a robust record of cratonic LIP events (e.g. Halls, 1982; Fahrig, 1987; Buchan and Halls, 1990).
The compilation includes information on tectonic setting. Our criteria for determining setting rely heavily on dyke swarm geometry and its relationship to cratonic margins (Fig. 3, Table 3). Events are inferred to have a mantle plume origin if a giant radiating dyke swarm is present. Giant linear dyke swarms that extend into a craton (i.e. trend perpendicular to a cratonic margin) are inferred to represent an aulacogen-type swarm (‘failed-arm’ type in Fahrig, 1987), and can also be used to infer a plume origin with the plume centre situated at the edge of a craton. By contrast, linear swarms that parallel the edge of a craton may simply be rift/breakup related (Ernst and Buchan, 1997) or may possibly represent a back arc rifting setting (e.g. Rivers and Corrigan, 2000), or overriding of a spreading ridge (Gower and Krogh, 2002).
In addition (Table 3), those Archean greenstone belts containing komatiites are inferred to be plume-related on the basis of the elevated temperatures required for generation of komatiites (e.g. Campbell, 1998, 2001; Arndt et al., 1998; Condie, 2001). Finally, small, intraplate events not obviously linked to a cratonic boundary are categorized as ‘hotspots’.
Below (and in Tables 1 and 2) we summarize the main events, their age distribution and tectonic setting. It should be noted that referencing has been minimized in the text below because detailed referencing is available through Tables 1 and 2. Also note that we have included number-labels of the form [#14a] in order to facilitate easy cross-correlation with entries in Tables 1 and 2, and with the distribution of main units in Figure 1.
Proterozoic to Present
2.51-2.41 Ga: The earliest Proterozoic LIPs consist of dykes, layered intrusions and volcanic rocks and are mainly associated with the eastern and southern margin of Laurentia. Most notable are the ca. 2.5 Ga Mistassini [#1a] and 2.49-2.45 Ga Matachewan events [#1b] whose radiating diabase dyke swarms locate two plume centres about 800 km apart, and imply rifting of the southeast margin of Laurentia at this time. The conjugate margin may have been Baltica, which has a remarkably similar age range of magmatism (e.g. Heaman, 1997; Buchan et al., 2000), or the Hearne craton (Bleeker, 2004). Additional units in eastern and southwestern Laurentia, the 2.505 Ga Ptarmigan dykes [#1a, unit not displayed in Fig. 1] and the 2.408 Ga Du Chef dykes [#1a, unit not displayed in Fig. 1] have uncertain relationship with the events in the southeastern and southern parts of the Superior Province.
[FIGURE 1 OMITTED]
Elsewhere in Canada, there are additional events falling in this age range. These include the Kaminak dykes [#1c] in the Hearne Province, and the Mirond Lake dykes [#1d] in the Sask craron of the Trans Hudson orogen.
2.24-2.21 Ga: The next burst of activity in Laurentia was widespread in the North Atlantic (Nain), Superior, and Slave cratons [#2a-d]. The 2.235 Ga Kikkertavak swarm [#2a] has been linked with breakup along the southern margin of the North Atlantic Craton (lower Aillik Group) at 2.178 Ga (Ketchum et al., 2001) although the long interval between emplacement of the swarm and breakup 57 Ma later is problematic. The 2.21 Ga BN1 (and possibly correlative MD1) dykes [#2b] of western Greenland are also likely linked with North Atlantic Craron breakup.
Superior Province elements of this age include the 2.217-2.210 Ga Ungava giant radiating swarm [#2c] that spans the entire eastern half of the Superior Province (Buchan et al. 1998). The convergence point marks a plume centre and possible breakup of a continental fragment from the eastern margin of the Superior Province. Buchan et al. (1998) proposed that the Nipissing sills [#2c] of the Southern Province were fed laterally via the Ungava radiating swarm from the plume centre region >1000 km to the northeast.
The Slave Province is another node of activity in this age interval. The 2.23 Ga Malley and 2.21 Ga MacKay dyke swarms [#2d] are both roughly linear, and crosscut at a shallow angle. If they represent rift-parallel swarms (Fig. 3c) then they could be linked to breakup along the southeastern margin of the Slave Province (LeCheminant et al., 1996). However, if they represent an aulacogen (Failed-arm) type swarm (Fig. 3b), then the plume centre and locus of breakup would have to lie at one end of the swarms; i.e., either on the east or southwest margins of the Slave Province.
[FIGURE 3 OMITTED]
2.19-2.17 Ga: Widespread activity occurred during this age interval. The oldest activity is represented by the 2.19 Ga Dogrib dyke swarm [#3a] in the Slave Province and the similar age Tulematu-MacQuoid swarm [#3b] in the Hearne Province. While a connection would seem likely based on the age match, preliminary paleomagnetic data indicate that the Slave and Rae cratons were not in their present relative positions at this time (LeCheminant et at., 1997). Globally, a stage of Birimian magmatic activity in Western Africa has this age (event #187 in Ernst and Buchan, 2001). Magmatic activity in the Slave Craton continues to 2.18 Ga, the age of the Duck Lake sill [#3a, unit not displayed in Fig. 1].
The 2.17 Ga Biscotasing dyke swarm [#3c] is one of the most widespread in Canada, extending throughout much of the southern and central Superior Craton. Similar age activity [#3d] is present as the Payne River dykes in northern Ungava (Cape Smith Belt) and Cramolet Lake sills (part of “Cycle 1” magmatism) in the Labrador Trough. It seems unlikely that all these elements are part of a single event, but the association of Payne River dykes and “Cycle 1” magmatism in the Labrador Trough suggests a link to breakup along the eastern Superior Province. Globally, an identical age has also been obtained fiom a quartz diorite dyke in the Wyoming Province, although paleomagnetic data are inconclusive regarding the relative locations of the Wyoming and Superior provinces at this time (Harlan et al., 2003a).
2.12-2.07 Ga: In the Superior Province there are several distinct stages of activity during this time interval. The 2.12-2.10 Ga Marathon dyke swarm [#4a] is a broadly linear swarm that cuts northward across the Superior Province from Lake Superior. This is an aulacogen-type swarm, and therefore could be associated with a breakup margin at the end of the swarm. Since the swarm may reach the cratonic margin on its north end as well as its south end (c.f. Fig. 3b), then the applicable breakup margin may also be at either end, either to the north in Hudson Bay or to the south in Lake Superior.
Slightly younger is the 2.09-2.07 Ga Cauchon swarm [#4b], which has been linked with breakup along the northwest margin of the Superior Province (e.g. Halls and Heaman, 2000). Two other events are also of this age: the 2.077 Ga Fort Frances (Kenora-Kabetogama) dykes [#4c] that are linked with breakup along the southern margin of the Superior Province, and the 2.069 Ga Lac Esprit swarm [#4d] located east of James Bay. There are no obvious connections between these widely separated but coeval 2.07 Ga events. However, future identification of additional dykes of this age in intervening areas could suggest a link.
In the Hearne Province, the widespread 2.111 Ga Griffin gabbros (formerly Hurwitz gabbros) [#4e] are presumably linked to breakup along the Trans-Hudson margin (Aspler el al., 2002).
Finally, the Napaktok swarm [#4f] trends perpendicular to and extends along the Labrador coast for at least 200 km. These dykes have an uncertain age between 2.50 and 2.10 Ga, and uncertain tectonic setting. Although more than one age of dykes may be present, at least part of this activity is dated by the 2.121 Ga age for the Tikkigatsiagak dyke.
2.05-2.02 Ga: In the Nain Province, the 2.045 Ga Iglusuataliksuak dyke [#5a, unit not displayed in Fig. 1] is coeval with the Kangfimuit swarm [#5a] of adjacent southern Greenland. The combined 2.04-2.05 Ga event would be areally significant, and may represent a breakup event associated with the northern margin of the North Atlantic Craton. Korak sills associated with the lower Povungnituk sequence [#5b] in the Cape Smith Belt of the northeastern Superior Province are of the same age as the Iglusuataliksuak dyke. However, given that the North Atlantic Craton had not yet docked at this time, two independent events are probable. The younger Upper Povungnituk sequence [#6c] is discussed below in the next section.
The third locus of activity of this age is in the Slave Craton. The 2.038 Ga Hearne dykes [#5c] parallel the southern Slave margin, possibly representing breakup along that margin (cf. with evidence discussed above for an earlier 2.23-2.21 Ga breakup along that margin associated with the Malley/ MacKay swarms [#2d]). In contrast, the younger 2.030-2.023 Ga Lac de Gras swarm [#5d] is not easily linked to any margin. It is centred in the Slave province and slightly converges to the north toward the similar-aged Booth River Complex in the Kilohigok sedimentary basin. LeCheminant et at. (1996) suggest that the Lac de Gras swarm is coeval with rifting on the western margin of the Slave Province.
2.00-1.95 Ga: Magmatism of this age range is distributed along the circum-Superior margin (e.g. Baragar and Scoates 1987).
In the Belcher Islands there are two main volcanic suites, the Eskimo [#6a] and overlying Flaherty [#6b] volcanics. Based on paleomagnetic correlations, the Eskimo volcanics may be linked with Richmond Gulf, Persillon, Pachi and Nastapoka Group volcanics (Chandler and Schwarz, 1980; Schwarz and Fujiwara, 1981), and with 1.998 Ga Minto dykes (Buchan et at., 1998). The Minto dykes and correlated suites are also coeval and perhaps cogenetic with the precisely dated Watts Group ophiolitc. The Eskimo volcanics have been linked geochemically with the western Povungnituk [#6c] (Legault et al., 1994), but this link is now doubtful based on more extensive recent geochemical study (Modeland et al., 2003).
The overlying Flaherty Group [#6b] is essentially undated except for a very uncertain Pb-Pb age of 1960+/-80 Ma. However, paleomagnctic data suggest a link with the Haig and Sutton Inlier sills (Schwarz and Fujiwara, 1981). Geochemical correlations indicate that the Flaherty Group may be linked with the upper (eastern) Povungnituk [#6c] (Legault et al., 1994).
The Cape Smith Belt includes the tectonically juxtaposed 1.998 Ga Watts Group, 2.04-1.96 Ga Povungnituk suites [#5b & #6c], and ca. 1.87 Ga Chukotat Group volcanics [#8b]. (Note that the older 2.04 Ga portion of the Povungituk sequence [#5b] was discussed in the previous section.)
Additional magmatism in this age interval is present in the Nain Province. A 1.95 Ga plateau basalt sequence in the Mugford Mountains of Labrador [#6d] represents a rifting event (Wardle et al., 2002) that may be more widespread in the North Atlantic Craton based on possible correlations with the Ramah and Snyder groups.
1.90-1.88 Ga (Tram Hudson Orogen and Rae-Hearne Craton): Several non-arc packages are associated with the Trans Hudson during this age interval. These include the Sandy Bay assemblage of the Flin Flon Belt [#7a], which contains accreted oceanic crust of various affinities, including an oceanic plateau. In addition there are the Josland and related sills [#7b] in the Lynn Lake Belt of the Amisk collage, and the mafic magmatism in the Piling-Penhryn [#7c], and Lake Harbour [#7d] groups on Baffin Island.
1.88-1.86 Ga (Circum-Superior Province): 1.88-1.87 Ga mafic magmatism surrounds the Superior Province on all sides except the southeast where, if originally present, it has been obscured by the Grenville allochthon. This magmatism is present in the Labrador Trough (Montagnais sills belonging to New Quebec Orogen Cycle 2 [#8a]), Cape Smith Belt (Chukotat Group [#8b]), northwest Superior province (Fox River sill, Molson dykes, Thompson Nickel Belt, and Wmnipegosis komatiites [#8c]), and the Animikie Basin and Marquette Range Supergroup of the southern Province (Hemlock and Gunflint formations and associated Kiernan sills [#8d]). The 1.88 Ga event or events are of particular importance because they represent a metallotect; the major NiCu-PGE sulphide ores of both the Thompson Nickel Belt and the Raglan deposits of the Cape Smith Belt appear to be associated with this age of magmatism (e.g. Hulbert et al., 2004 for TNB; Wodicka, pers. comm. 2004 for Raglan).
1.88 Ga magmatism in the Cape Smith belt and Labrador Trough has been linked to rifting and possible separation of a microcontinent (St-Onge et al., 2000). However, the magmatism in both the Thompson belt and Animikie basin occurs within a broad period of ocean closure, and therefore may represent back-arc rifting. The recent discovery of a major ca. 1.88 Ga dyke, the NW-trending Pickle Crow dyke [#8c] crossing the interior of western Superior Province provides a link between the Animikie Basin and Thompson Belt magmatic activity, and may suggest a mantle plume model for the western part of the 1.88 Ga event (Buchan et al., 2003).
1.83-1.82 Ga: The Sparrow dyke swarm [#9a] of the western Rae Province is as yet uncorrelated with any volcanic sequences. Other units of similar age but uncertain relationship are 1) a meta-gabbro and two monzogabbros with U-Pb ages of 1.83-1.82 Ga in the Close Lake, Wollaston-Mudjatik Transition zone [#9a, unit not displayed in Fig. 1], and 2) the widespread Christopher Island formation volcanics of the Baker Basin region [#9a, unit not displayed in Fig. 1].
1.75-1.71 Ga: The Cleaver dykes in the Great Bear Magmatic Zone, the Hadley Bay sills on Victoria Island and MacRae Lake dykes in the northern Rae Province are coeval in age [#10a], suggesting a widespread event in northwestern Canada. This large region of 1.75 Ga activity could be associated with the generation of Wernecke sediments in the northwestern Cordillera, and the approximately 40 Ma younger 1.71 Ga Bonnet Plume River marie magmatism [#10a; unit not displayed in Fig. 1]. The Wernecke sediments are inferred to represent the earliest rift stage of activity associated with the Cordilleran margin (Cook et al. in Percival et al., 2004). The Pitz formation fclsic volcanics and Nueltin felsic intrusive suite [#10a, units not displayed in Fig. 1] of the Baker Basin region are similar in age.
Subhorizontal seismic reflectors interpreted as sills are present over a huge region (about 120,000 sq. km) in the basement underlying the Western Canada Basin. These Winagami sills [#10b] are roughly bracketed in age between 1.89 and 1.76 Ga, and have been tentatively linked with the Cleaver dykes by Ross and Eaton (1997).
1.64 Ga: The 1000 km long Melville Bugt swarm [#11a] is located in western Greenland. Although close to Baffin Island and other Canadian Arctic islands in a reconstructed Greeenland–North America configuration, Melville Bugt dykes have not yet been recognized in Canada.
1.47-1.44 Ga: There are two nodes of activity with this age. The Belt Basin of the western Cordillera contains extensive Moyie-Purcell sills and associated Purcell volcanics [#12a]. These may have been generated when a continent (perhaps Australia) was rifted from the western margin of Laurentia. It is also interesting that in the Wyoming Province there is an extensive linear dyke swarm (Tobacco Root–Group B; [#12a]) of the same age. Assuming that the dykes fed the volcanics and sills, we can infer that the magma source area was either on the western margin of Laurcntia in the vicinity of the Belt Basin, or far to the southeast on the southern margin of Laurentia with magma being transported laterally via the dykes to the Belt Basin. Long distance feeding of a sill province has been described above for the 2.22 Ga Ungava event, and may be a not uncommon consequence of the lateral flow pattern in giant dyke swarms (e.g. Ernst and Buchan, 1997).
A second node of this age is located in southeastern Laurentia. The Michael and Shabagamo gabbros [#12b] have an approximate age of 1.47-1.46 Ga and represent a significant event in the southeastern Laurentia. They are located in a back-arc setting to the evolving Grenville Orogen (Rivers et al. in Percival et al., 2004).
1.38 Ga: Hart River volcanic rocks and sills, and coeval sills from the Belt Basin region [#13a], may represent rift sequences (Abbott, 1997; Thorkelson et al., 2003).
1.28-1.27 Ga: One of the largest magmatic events in Canada occurred at 1.267 Ga [#14a]. Most prominently this event consists of the Mackenzie giant radiating dyke swarm. Mackenzie dykes (Fig. 2a) fan over an arc of 100[degrees] and cover almost 3 million sq. km of the Canadian Shield. Coeval Coppermine volcanics and the Muskox Intrusion are situated near the plume center, but additional volcanic and sill packages are distributed throughout the swarm and are inferred to be fed via lateral flow along dykes originating from near the plume center (e.g. Ernst and Baragar, 1992; Baragar et al., 1996). This LIP is presumed to be linked with continental breakup and formation of a northern ocean, which has been termed the Poseidon Ocean (G. Jackson cited in Fahrig, 1987). However, the missing rift block(s) has not yet been identified, although Siberia has been a repeated suggestion (see summary in Ernst et al., 2000; cf. Sears et al., 2004).
The North Atlantic Craton of North America and Greenland is another locus of magmatic activity during this time period [#14b]. The 1.280-1.277 Ga Nain-LP dykes of Labrador are correlative with the BD0 dykes of Greenland (Buchan et al., 1996). Also the 1.273 Ga Harp dykes of Labrador may be linked with Gardar (BD1, BD2, BD3) dykes of Greenland (Baragar, 1977). The setting of this 1.28-1.27 Ga activity is unknown, but it is clearly distinct in location, dyketrend, and probably in origin from the coeval Mackenzie event. Also widespread in Labrador are the anorthosites, granites, diorites and troctolites of the older and probably unrelated 1.35-1.29 Ga Nain plutonic suite (Ryan and James, 2004 and references therein).
Coeval activity of this age is represented globally by the Central Scandinavian Dolerite Complex (sills) of the Baltic Shield. Paleomagnetic data and geological evidence suggest a reconstructed location east of Greenland (Buchan et al., 2000, and references therein), which is supported by geological evidence (Bingen et al., 2002). Given its great spatial separation from Canada in this reconstruction, the Central Scandiuavian Dolerite Complex of Baltica must represent a separate event from the coeval Mackenzie (and also possibly the Nain Province) activity. The occurrence of multiple independent LIPs has been considered evidence for plume cluster events (Ernst and Buchan, 2002).
1.25-1.22 Ga: The Grenville Province and adjacent Superior Province contain widely separated packages of similar-aged magmatism. From southwest to northeast, these include 1.235 Ga Sudbury dykes [#15a], 1.25-1.225 Ga Seal Lake volcanic rocks and Naskaupi sills [#15b], and the 1.250 Ga Mealy dykes [#15b]. These 1.25-1.22 Ga events along the Grenville Orogen have not been previously linked to each other and more work is required to assess whether they represent disparate elements of the same event. They are situated in a back-arc setting with respect to the evolving Grenville orogen (e.g. Rivers and Corrigan, 2000; Rivers et al. in Percival et al., 2004). However a plume origin should not be ruled out. The Seal Lake suite has previously been considered analogous to a flood basalt sequence (“plateau basalt” is the term used in Baragar, 1977), and the aulacogen type geometry of the Sudbury dykes suggests derivation from a spreading center located to the southeast of the swarm (Fahrig, 1987).
1.18-1.14 Ga: Widely separated but possibly linked nodes of mafic magmatism of 1.18 Ga are distributed along the Grenville Orogen. Specifically, toward the northeast end of the Grenville Province the Davy Group sills and dykes [#16a] in the Wakeham Group have an age of 1.177 Ga. Similar ages are found in coronitic gabbros [#16a] in the Baie du Nord segment of Tshenukutish domain. Finally, the same age but with larger uncertainties applies to Algonquin metagabbros [#16a] in the Central Gneiss Belt, southwestern Grenville Province.
Late Gardar magmatism in South Greenland ranges in age from 1.18-1.14 Ga [#16b], and includes the 1.18 and 1.163 Ga Giant Tugtutoq Dykes.
The sparsely distributed 1.141 Ga Abitibi dyke swarm [#16c] of the Central Superior Province has a width of 400 km and extends for nearly 700 km across the southern and eastern Superior Province. This event has long been considered as a precursor to the 1.109-1.085 Ga Keweenawan event [#17a] located at the southwest end of the swarm (next entry). However, the broadly linear pattern of the Abitibi swarm does not eliminate a possible source at the other (northeast end) of the swarm.
1.11-1.08 Ga: One of the most dramatic flood basalt events in Canada and the United States is arguably the Keweenawan magmatism [#17a] of the Mid-Continent Rift (e.g. Ojakangas et al., 2001). It comprises at least 2 x [10.sup.6] cubic km of volcanic rocks and possibly an equal volume of intrusive rocks (Fig. 2b). The Mid-Continent Rift (and subsurface lavas) can be traced eastward through Michigan and southwestward into the central United States. A similar age of activity is found in the “Southwestern USA Diabase Province”, and in the Moores Lake sills of the Athabasca Basin (1000 km to the northwest). The Keweenawan activity consists of main pulses of activity at 1.109-1.105 Ga and 1.100-1.094 Ca, but activity is continuous to 1.085 Ca. Emplacement of the Keweenawan LIP is similar in age to that of terminal collision of the Grenville orogen (Rivers et al. in Percival et al., 2004). Although a back-arc rifting origin linked to the coeval Grenville orogeny has been suggested, the most widely accepted model links the event to a mantle plume on the basis of the great volume of tholeiitic magma generated in an intraplate setting (e.g. Ojakangas et al., 2001).
[FIGURE 2 OMITTED]
0.78 Ga: The Gunbarrel magmatte event [#18a] is distributed over a distance of 2400 km in western North America. Precise 0.780 Ga ages are found in the Hottah sheets of the Slave Province, the Mackenzie Mountains dykes and sills, the MacDonald dykes, and the Tobacco Root- Group B and Wolf Creek sills of the Wyoming Province (Harlan et al., 2003b). The Irene and Huckleberry volcanics of northwestern USA are also inferred to be of this age. The dykes define a radiating swarm with a convergence point in the southern Cordillera near Vancouver Island, indicating a mantle plume origin for this 0.78 Ga LIP (Park et al., 1995). The Windermere sedimentary/volcanic sequence starting at about 0.75 Ga may represent a passive margin associated with this 0.78 Ga plume. Both South China and Australia also contain magmatism dated at 0.78 Ga (events #67 and #64 in Ernst and Buchan, 2001, respectively) and both have been proposed as the rifted block(s).
0.72 Ga: Another major LIP event is represented by the Franklin dyke swarm [#19a] which extends throughout the southern Arctic Islands, but is most significant on Baffin Island, and also on reconstructed Greenland as the Thule swarm [#19a]. The convergence point marking the plume centre for this event is located north or northwest of Banks Island. Natkusiak volcanics, and Minto Inlier and Coronation sills [#19a] are also part of the Franklin event and are generally concentrated toward the plume centre region. The Franklin event may be linked with separation of an as yet unidentified continent.
Another possible locus of similar-aged activity is the Appalachians. A very approximate Rb-Sr age of 0.735 Ga has been suggested for coast-parallel dykes in basement inliers of the Appalachians of the United States (event #72 in Ernst and Buchan, 2001). This activity can been linked with additional magmatism and a stage of rifting along the Laurentian margin in the southern Appalachians (Aleinikoff et al., 1995).
0.62-0.56 Ga (Laurentian margin, Appalachians): The formation of the Iapetus Ocean was preceded by several distinct major magmatic events along the eastern margin of Laurentia. These include the 0.615 Ga Long Range dykes [#20a], the 0.590 Ga Grenville-Adirondack fanning swarm [#20b] and the 0.563 Ga Sept lies layered intrusion [#20c]. The latter is roughly coeval with the Catoctin flood basalts [#20c, unit not displayed in Fig. 1] situated in the southern Appalachians of the United States. Other basaltic units and syenitic intrusions with ages 0.56 to 0.55 Ga are widely distributed (Puffer, 2002; Higgins and van Breemen, 1998).
[FIGURE 1 OMITTED]
The oldest event, the 0.615 Ga dykes [#20a] may have been linked to similar-aged magmatism in Baltica, which is represented by the aulacogen-type Egersund dykes (Bingen et al., 1998) and the coast-parallel Baltoscandian breakup swarm (event #55 in Ernst and Buchan, 2001). Two younger rifting events are also recorded in Laurentia: an early separation of Amazonia, and a later separation of the peri-Laurentian Dashwoods microcontinent (Waldron and van Staal, 2001; cf. Cawood et al., 2001). Within this context, the 0.590 Ga radiating swarm [#20b] (associated with the St. Lawrence rift system) may presage the separation of Amazonia from Laurentia at 0.57 Ga to form the Iapetus Ocean, and the magmatism at 0.563 Ga [#20c] may similarly be linked to the separation of the Dashwoods terrane at 0.550-0.540 Ga.
0.62-0.55 Ga (Avalon zone, Appalachians): The ca. 0.62 Ga Harbour Main [#21a] and the 0.585-0.555 Ga Marystown events [#21b] are recorded in the Avalon zone, which had an uncertain relationship with Laurentia during this period and subsequently drifted with Gondwana before closure of the Iapetus Ocean in the early Paleozoic.
0.57-0.52 Ga (Cordillera): The 0.57 Ga Hamill-Gog Group magmatism [#22a] in the southern Cordillera has been linked with a breakup along this Laurentian margin (Colpron et al., 2002).
In the northern Cordillera lower Paleozoic alkalic and potassic mafic magmatism [#22b] is linked with rifting of the Selwyn Basin (Goodfellow et al., 1995). This magmatism includes the Demster, Menzie Creek, Niddery volcanics, and younger Fossil Creek volcanics. The only precise age is a 0.518 Ga U-Pb age from a Post-Hyland Group sill, probably representing a widespread set of sills (Abbott, 1997). However, a range of volcanic ages from Lower Cambrian to Early Devonian is suggested on biostratrigraphic grounds (Goodfellow et al., 1995; Abbott, 1997).
0.47-0.41 Ga (Dunnage, Gander, Avalon and Meguma zones, Appalachians): In Atlantic Canada several important mafic (and bimodal) magmatic suites include the 0.46 Ga Dunn Point [#23a], and 0.44-0.43 Ga Bayswater and Cape St. Mary’s suites of the Avalon zone [#23b], the Middle Ordovician Overstep Sequence of the Gander and Dunnage zones [#23a], the 0.44 Ga White Rock formation of the Meguma zone [#23b], and the early Silurian Overstep Sequence [#23b] of central Newfoundland (mainly in the Dunnage Zone). Much of this magmatism has been emplaced in a back-are setting. During this period the Iapetus Ocean was closing, but the spatial relationship between these Iapetan terranes is still under debate.
0.36-0.32 Ga: The Carboniferous Magdalen (or Maritimes) Basin is thought to have been underplated by a layer of mafic magma with an average thickness of 13 km based on geophysical modelling [#24a] (Marillier and Verhoef, 1989). In addition, volcanic rocks and intrusions of this age are distributed widely around the western and southern perimeter of the basin. The Magdalen Basin magmatic event [#24a] has been inferred to represent the final breakthrough of a plume that had been trapped beneath a subducting slab (Murphy et al., 1999).
0.27-0.21 Ga (Cordillera): The mid-Permian to upper Jurassic (ca. 0.27-0.20 Ga) Cache Creek terrane of the Cordillera may include some oceanic plateau and hotspot material [#25a], but this remains controversial (cf. Tardy et al., 2001 and Struik et al., 2001).
Wrangellia is an important accreted terrane of the Cordilleran orogen [#25b], consisting of Karmutsen and Nikolai volcanics and associated 0.232 Ga Maple Creek sills. These units originated as an oceanic plateau possibly formed atop an island arc before being accreted onto the Cordilleran orogen (e.g. Richards et al., 1991).
Note that the Wrangell Lavas (0.065-0.002 Ga) (event #331 in Buchan and Ernst 2004), which extend from the Yukon into Alaska for a distance of -430 km, are distinct from the much older Wrangellia flood basalts, despite the similar names. The extensive Wrangell lavas are not catalogued in Table 1 because they are linked to subduction along the Aleutian are.
Ramparts Group magmatism [#25c] of Alaska is poorly dated (ca. 0.21 Ga). It is located in the Tozima Belt of Alaska and is explained as a “parautochthonous rift assemblage” (p. 190, Dover, 1994).
0.20 Ga: The largest magmatic event on Earth in terms of areal distribution is the Central Atlantic Magmatic Province (CAMP) [#26a]. Found in North America, Europe, Africa and South America, it covers an area of nearly 7 million sq. km. It mainly consists of a giant radiating dyke swarm centred near Florida that was the precursor to the 0.175 Ga opening of the central Atlantic Ocean. Extensive sill provinces and volcanic packages are also found on all formerly adjacent blocks. In Atlantic Canada, this event is represented by several major dykes, as well as the North Mountain and Grand Manan volcanics [#26a].
A plume origin seems most likely based on the large scale and short duration of the event as well as presence of a giant radiating dyke swarm. However, a model involving “edge convection” has also been advocated mainly on the basis of ‘non-plume’ chemistry, and the suggestion that the dykes represent a superposition of distinct linear swarms rather than an overall single radiating swarm (e.g. several papers in Haines et al., 2003).
0.14-0.09 Ga: From 0.14 to 0.11 Ga there was extensive NEQ (New England-Quebec) magmatic activity [#27a] in the eastern United States and Quebec. The Monteregian Hills plutons and dykes of this magmatic event have been linked to a plume tail (the Great Meteor hotspot track) associated with the New England seamount chain (Heaman and Kjarsgaard, 2000). Problems with a plume origin for this magmatic province have been discussed by McHone (1996).
Another node of activity at this time is represented by the 400 km long Trap dyke swarm [#27b], which was emplaced along the southwestern coast of Greenland at 0.138 Ga. Given the proximity of Greenland to Labrador at this time, we would expect a continuation of this extensive magmatic event into eastern Canada. Globally, similar-aged magmatism is linked with two plume centres associated with the breakup of South America and Africa (Fig. 8 in Ernst and Buchan, 2002).
[FIGURE 8 OMITTED]
Magmatism on the Queen Elizabeth Islands [#27c] is part of the High Arctic Large Igneous Province (HALIP) [#27c]. This event is also present in northern Greenland, Svalbard and Franz Josef Land, as well as offshore (Tarduno et al., 1998; Maher, 2001). Precise dates of 0.095-0.092 Ga apply to both the Strand Fiord volcanics and the Wootton intrusion (Tarduno et al., 1998). However K-Ar and Rb-Sr dating as well as biostratigraphic control suggests that the magmatism may have begun at ca. 0.13 Ga. While a continuum of activity may be present, Maher (2001) interprets two pulses of activity, at ca. 0.13 and ca. 0.09 Ga. The identification of a radiating dyke swarm suggests a plume origin with a plume centre located near the Alpha Ridge (Embry and Osadetz, 1988; Ernst and Buchan, 1997; Maher, 2001).
0.07-0.05 Ga: The 0.070 Ga Carmacks volcanics [#28a1 of the northern Cordillera have a slightly more potassic composition than most of the other events discussed in this paper, but they have a large areal extent (about 60,000 sq. km) and were apparently emplaced in a short duration. The slightly younger 0.06-0.05 Ga Crescent Terrane volcanics [#28b] consist of thick basaltic sequences distributed over a ca. 600 km distance along the Coast Ranges of western North America. They are inferred to represent accreted seamounts. Both the Carmacks volcanics [#28a] as well as the Crescent Terrane volcanics [#28b] have been interpreted as originating from earlier stages of the Yellowstone plume, prior to its main expression as the Columbia River LIP at 0.017 Ga (see next entry, [#29b]) (e.g. Johnston et al., 1996; Murphy et al., 2003).
The North Atlantic igneous Province (NAIP) [#28c] is most voluminous in eastern Greenland and the UK, and adjacent offshore regions. Minor activity at Cape Dyer and Cape Searle on Baffin Island, as well as more substantial magmatism in west Greenland are linked with the NAIP. The NAIP LIP is linked to the present-day Icelandic hotspot.
0.025-0.015 Ga: An important intraplate event is the widespread Behm Canal event [#29a] of the Cordillera, which is also known as the Tertiary Lamprophyre Province. It consists of alkaline lamprophyres that are considered volatile-enriched equivalents of alkali basalts (Rock, 1991, p. 11-12, 122).
The voluminous Columbia River Basalt Group (CRBG) LIP [#29b] of the northwestern United States was mainly erupted from 0.017 to 0.015 Ga. It has been linked to the Yellowstone plume. The coeval Chilcotin Group volcanics [#29c] are located a short distance to the north in Canada, and although they arc areally extensive they are volumetrically minor.
Archean greenstone belts represent deformed and fragmented volcanic suites, and are of two main affinities: calc-alkaline and tholeiitic (e.g. de Wit and Ashwal, 1997; Condie, 2001; Blecker, 2002). The calc-alkaline suites are considered to be of arc origin whereas the tholeiitic suites, particularly those containing komatiites, are not. The presence of komatiites satisfies one requirement for the identification of LIPs, i.e. that they not be produced by subduction. In addition, greenstone belts with komatiites arc probably not produced by normal spreading ridge processes because komatiites indicate source region temperatures higher than those associated with normal spreading ridges. There is some controversy on this point since the Archean geotherm was hotter. The scale of Archean LIP candidates is also uncertain. In most cases deformation and faulting prevents the recognition of Archean tholeiitekomatiite greenstone belts over LIPscale distances. So the Archean LIP history, discussed below and summarized in Table 2 and Figure 1, remains speculative. Events are included in Table 2 on the basis of either the presence of komatiites, and/or inferred oceanic plateau setting.
[FIGURE 1 OMITTED]
3.11-2.98 Ga: The oldest known period of potential LIP activity is represented by komatiite-bearing greenstone belts (3.105 Ga Hunt River [#A1a] and 2.99-2.98 Ga Florence Lake [#A1b] belts) located in the Hopedale block of the Nain Province of the North Atlantic Craton. Another important magmatic event is associated with the ca. 2.99 Ga rifting [#A1c] of the ancient Archean nucleus in the western Superior Province comprising the North Caribou, Central Wabigoon and Marmion blocks (Tomlinson et al., 1999; Tomlinson and Condie, 2001).
2.93-2.92 Ga: A subsequent stage of komatiite-bearing greenstone belts [#A2a] at about 2.93-2.92 Ga is also widespread in the western Superior Province, but the setting and link with associated are-type greenstone belts is unclear.
2.86 Ga: The Pickle Crow greenstone belt [#A3a] in the Uchi subprovince is approximately dated at 2.86 Ga and contains komatiites.
2.79-2.77 Ga: The 2.786 Ga Vizien greenstone belt [#A4a] of northern Quebec contains komatiites and has been linked with formation of an oceanic plateau. Greenstone belt fragments (containing komatiites) within the Faribault-Thury Complex [#A4b] are also situated in northern Quebec, and are bracketed in age between 2.785 and 2.710 Ga. (Note that if future dating determines an age closer to the younger end of the age bracket, then the Faribault-Thury Complex event would be grouped in the next entry.)
The 2.775 Ga Fourbay sequence [#A4c] of the western Superior Province lacks komatiites, but is included in this LIP compilation because of its inferred oceanic plateau origin.
2.75-2.70 Ga: In various portions of the Canadian Shield there was widespread mafic magmatism falling in the age range 2.75-2.70 Ga. This is discussed in terms of three regional groupings.
It has been suggested that the Prince Albert Group [#A5a] can be correlated with the Woodburn and Mary River groups, thus defining a single event in the Rae Province of northern Canada, which is distributed over a lateral distance of nearly 1000 km. The magmatism which includes komatiites is interpreted to have initiated at 2.73 Ga and may be associated with plume-generated continental breakup.
The Kam Group [#A5b] has been traced across large parts of the Slave Province through a complicated deformation pattern (Bleeker, 2003, and references therein). The magmatism of the Kam Group ranges from 2.734-2.700 Ga, and was particularly voluminous from 2.72-2.70 Ga.
Magmatism in the Abitibi greenstone belt [#A5c] of the central Superior Province is widespread and consists of four distinct stages of komatiite-associated magmatism cmplaced during the interval 2.75-2.70 Ga (e.g. Sproule et al., 2002). The interspersed calc-alkaline magmatism suggests a plume arc association (e.g. Wyman, 1999). The Schreiber-Hemlo-White River-Dayohessarah packages found in the Wawa greenstone belt [#A5d], also contain significant komatiite-bearing tholeiitic magmatism with ages between 2.75 and 2.73 Ga. The Wawa belt is on strike with and is probably the continuation of the Abitibi belt.
As described above, Canada has a rich LIP history consisting of at least 80 possible events (Fig. 1, Tables 1 and 2). They range from Archean greenstone belts (containing komatiites) such as the Prince Albert Group and probable correlatives, which may extend for >1000 km along the Rae Province, through Proterozoic giant radiating dyke swarms, such as the Mackenzie swarm that covers nearly 3,000,000 sq. km of the Canadian Shield, to young flood basalts, such as the rift-related Keweenawan Group and the accreted oceanic plateau, Wrangellia, in the Cordillera. LIPs are key to resolving a number of important geological issues and processes. Here we apply our database of Canadian LIPs to several frontier issues.
Plume vs. Non-plume Origins
As mentioned earlier, there is currently an intense debate about plume versus non-plume origins for LIPs. This debate is occurring both on the web (e.g. www.mantleplumes.org; www.largeigneousprovinces.org) and in the scientific literature (e.g. Anderson, 2001; Foulger and Natland, 2003; DePaolo and Manga, 2003; Ernst et al., 2004). The Canadian LIP database can contribute to this debate in various ways. Giant radiating dyke swarms are strongly indicative of mantle plumes (e.g. Ernst and Buchan, 1997). Using this criteria, plumes would be inferred at 2.45, 1.27, 0.78, 0.72, 0.20 Ga. Furthermore, many Canadian swarms have a failed-arm (aulacogen setting) (Fig. 3b, Table 3), which also suggests plume involvement. In addition, Archean greenstone belts, which contain komatiites, are arguably plume-related. Finally, recognition of additional mantle plumes may also derive from studies of regional uplift patterns (see below). On the other hand, some LIPs having a linear distribution, such as those in a back-arc setting, may be consistent with non-plume origins. Those along a breakup margin may be generated by decompression melting accompanying rifting. Some LIPs may consist of two pulses, an initial burst of magmatism associated with plume arrival and a second caused by the onset of decompression melting associated with breakup.
[FIGURE 3 OMITTED]
Precise Time Markers for Stratigraphic Correlation
The wide distribution (potentially over millions of sq. km) and the typically short duration of events makes them ideal as precise stratigraphic markers (e.g. LeCheminant and Heaman, 1989; Harlan et al., 2003b). For instance, recognition of the same magmatic event within widely separated sedimentary sequences represents an ideal marker for inter-basin correlation. In Canada, the 1.27 Ga Mackenzie, 0.78 Ga Gunbarrel, and 0.72 Ga Franklin LIPs represent particularly good markers.
Reconstruction of Continents
Globally there is a clear link between young LIPs and breakup margins (e.g. Courtillot et al., 1999). The Canadian landmass preserves a history of continental breakup, and subsequent reassembly marked by sutures. Therefore, the Canadian LIP record is fertile ground for exploring links with breakup events. Archean continental fragments each contain a particular age distribution of mafic events (mostly Proterozoic dyke swarms) that represent a distinct “bar code” (Bleeker, 2003, 2004). Comparison of the “bar code” from the approximately 35 different Archean continental fragments (at least eight of which are in Canada) represents a key tool for proposing reconstructions between these fragments. Reconstructions can be tested by comparing the paleomagnetism of coeval mafic units on the different continental fragments (Buchan et al., 2000). In addition, linear (Fig. 4a) and radiating (Fig. 4b) dyke swarms can be used to constrain the reconstruction geometry. Some suggested correlations are given in Tables 1 and 2, and in the accompanying text.
[FIGURE 4 OMITTED]
Exploration (Ni-Cu-PGEs and Diamonds)
Ni-Cu-PGE deposits are commonly associated with LIPs. Notable examples include the Siberian Traps and the Bushveld Complex (e.g. Naldrett, 1999; Pirajno, 2000; Diakov et al., 2002; Hulbert, 2002). Ernst and Hulbert (2003) carried out a preliminary analysis of background PGE levels in about 60 Canadian LIPs and other intraplate mafic events in order to assess which are more likely to host such deposits. Events with elevated background PGE levels (>10 ppb Pt and Pd) are thought to have greater potential for enrichment during magmatic emplacement. Ernst and Hulbert (2003) found that events with high background levels include the 2.50-2.45 Ga Matachewan, 2.22-2.21 Ga Ungava-Nipissing, 1.27 Ga Mackenzie, 0.72 Ga Franklin, 0.59 Ga Grenville and portions of the 1.11-1.09 Ga Keweenawan and 0.13-0.09 Ga Sverdrup Basin events.
Some studies have proposed a direct link between kimberlites and underlying plumes (Haggerry, 1999; Heaman and Kjarsgaard, 2000; Schissel and Small, 2001). Recently it has also been suggested that some kimberlites might be preferentially localized along particular dyke swarms such as the 2.023 Ga Lac de Gras swarm of the Slave Province (Wilkinson et al., 2001; Stubley, 2003) and the 2.50-2.45 Ga Matachewan dykes of the Attawapiskat region in the James Bay lowlands (Stott and Halls, 2002). Further work is required to test the potential of fractures and zones of weakness represented by major dyke swarms to localize kimberlite magmas during their ascent through the crust.
Numerous studies have explored the link between LIPs and climate change (e.g. Condie, 2001; Isley and Abbott, 2002; Courtillot and Renne, 2003; Ernst and Buchan, 2003, Prokoph et al., 2003). The correlation between extinction events and LIPs is compelling (Courtillot et al., 1996; Courtillot and Renne, 2003) and suggests that some LIPs, perhaps acting in concert with meteorite impact events, may be the trigger for extinction events. Evaluation of a robust Canadian HP record can contribute to the global understanding of the effect of LIPs on climate. For instance, all other factors being equal, the largest LIP events should have the largest climatic effect. Some of the largest LIPs in Canada are the ca. 1.88 Ga Circum-Superior, 1.27 Ga Mackenzie, 0.72 Ga Franklin, 0.615-0.555 Ga Central Iapetus, and 0.20 Ga CAMP events. Only the climatic effect of the youngest of these events has been evaluated (Palfy 2003).
Regional Domal Uplift
LIPs linked to mantle plumes should be associated with regional domal uplift. The scale of uplift corresponds to the size of the plume head (e.g. Cox, 1989; Rainbird and Ernst, 2001; Campbell, 2001; Sengor, 2001; He et al., 2003). The largest plumes are thought to generate uplifts with a radius 1000 km and a peak elevation 1 to 2 km. Such uplifts should exert a first-order control on concurrent regional sedimentation patterns. Plume head related uplift has only received preliminary investigation in Canada, where it has been associated with 1.27 Ga Mackenzie, 0.72 Ga Franklin, and 0.615-0.555 Ga Central Iapetus events (e.g. Rainbird and Ernst, 2001). It is hoped that the LIP database for Canada will stimulate further investigation of regional uplift patterns.
EXPANDING THE LIP DATABASE TO ADDRESS FRONTIER ISSUES
The frontier issues discussed above can only be fully addressed using a more robust LIP record. Although an extensive database is presented in this paper, many major mafic and ultramafic units remain undated and poorly characterized. Rapid improvement in the LIP database can be achieved only through a concerted campaign of geochronology integrated with other fields such as paleomagnetism and geochemistry, as is being proposed for Canada by Bleeker (2004) and internationally by Ernst et al. (2004).
Table 1 Large Igneous Provinces (LIPs) and potential LIPs in Canada
and adjacent regions since 2.5 Ga. Names of the largest events are
underlined. Obsolete names in square brackets. Pre-2.5 Ga record is
discussed in Table 2. Anorthosites have not been included. Details
and full referencing on most events are available in compilations (=Ernst and Buchan, 2001) and  (=Buchan and Ernst, 2004), or
in the additional cited references. Abbreviations: se. = southeast,
ne. = northeast, c. = central, etc. Units in each entry are ordered
in terms of decreasing size. “REF.:” = key reference(s). SETTING
codes are explained in Table 3.
Event name Magmatic components (Age)
1 2.51-2.41 Ga
1a Mistassini (-2.5 Ga) DYKES: Mistassini (-2.5 Ga)
(e. Superior Prov.) REF.: #204 in ; #43 in [100,000 sq. km] COMMENT: ?Link with Ptarmigan
swarm (2.51 Ga [#35 in ]
of ne Superior Prov. ?Link with
Du Chef swarm (2.41 Ga) [#45 in
] along Grenville Front
SETTING: Plume (P1); Breakup
(B1; se. Superior Craton)
1b Matachewan DYKES: Matachewan [Hearst]
(2.49-2.45 Ga) (2.47 and 2.45 Ga)
(s. & e. Superior Prov.) LAYERED INTRUSIONS: East Bull[360,000 sq. km] Lake (2.48 Ga); Agnew (2.49 Ga);
River Valley (2.475 Ga);
Falconbridge Twp (2.44 Ga)
VOLCANIC ROCKS: Dollyberry;
Ellise Mountain; Copper Cliff
rhyolites (-2.45 Ga); Thessalon.
REF.: #206 in ; #42 in 
COMMENT: ? Link with Ptarmigan
swarm (2.51 Ga [#35 in ] of
ne. Superior Craton)
SETTING: Plume (P1); Breakup
(B1; s. Superior Craton)
1c Kaminak DYKES: Kaminak (-2.45 Ga)
(ca. 2.45 Ga REF.: #203 in ; #44 in 
(Hearne Prov.) SETTING: Plume (?P1); ?Breakup[18,000 sq. km] (Hearne Craton)
COMMENT: Linked with Matachewan
event [#1b] by Bleeker (2004)
1d Mirond Lake (2.49 Ga) DYKES: Mirond Lake (2.49 Ga)
(Trans Hudson) REF.: #41 in [two ‘windows’ into SETTING: ?Breakup (Sask Craton)
Archean basement about
120 km apart]
2 2.24-2.21 Ga
2a Kikkertavak DYKES: Kikkertavak (2.235 Ga)
(2.235 Ga) REF.: #47 in 
(Makkovik Prov.) COMMENT: Linked with Lower Aillik[6500 sq. km] Group (2.18 Ga) rift magmatism
[Ketchum et al., 2001]
SETTING: ?Breakup (s. North
Atlantic [Nain] Craton)
2b BN-1 (2.21 Ga) DYKES: BN-1 (norite) (2.21 Ga);
(s. Greenland) MD-1 undated but possibly similar[54,000 sq. km] in age
REF.: #193 in ; #40 in 
SETTING: ?Breakup (? North
Atlantic [Nain] Craton)
2c Ungava DYKES: Ungava radiating swarm =
(2.22-2.21 Ga) Senneterre (2.22 Ga), Maguire
(ne. and e. and Klotz (2.21 Ga)
Superior Prov.) SILLS: Nipissing (2.22 Ga)[500,000 sq. km] REF.: #191 in ; #50-52 in 
SETTING: Plume (P1); Breakup
(B1, e. Superior Craton)
2d Malley-MacKay DYKES: Malley NE trend
(2.23 and 2.21 Ga) (-2.23 Ga)]; MacKay ENE-E
(Slave Prov.) trend (-2.21 Ga)[35,000 sq. km] REF.: #192 and #197 in
; #48 and #57 in 
SETTING: Breakup (Slave Craton)
3 2.19-2.17 Ga
3a Dogrib (2.19 Ga) DYKES: Dogrib (2.19 Ga)
(Slave Prov.) SILLS: Duck Lake (2.18)[11,000 sq. km] REF.: #185 in ; #60 in
; Bleeker & Kamo, 2003
SETTING: Breakup (Slave Craton)
3b Tulemalu-MacQuoid DYKES: Tulemalu-MacQuoid (2.19 Ga)
(2.19 Ga) REF.: #186 in ; #61 in 
(Hearne Prov.) SETTING: Breakup (Hearne Craton)[15,000 sq. km]
3c Biscotasing (2.17 Ga) DYKES: Biscotasing (2.17 Ga)
(Superior Prov) REF.: #184 in ; #64 in ;[350,000 sq. km] Halls and Davis, 2004
SETTING: Plume (P3)
3d Cramolet MAGMATISM: ‘Cycle 1’, including
Lake-Payne River Cramolet Lake sill of basal
(2.17 Ga) Seward Subgroup (2.17 Ga)
(New Quebec Orogen) DYKES: Payne River -2.17 Ga[30,000 sq. km] [S. Pehrsson, pers. comm., 2000]
REF.: #63 in 
(B2, e. Superior Craton)
4 2.12-2.07 Ga
4a Marathon DYKES: Marathon-N (2.12 Ga);
(2.12-2.10 Ga) Marathon-R (2.10 Ga)
(c. Superior Prov.) REF.: #180 & 181 in ; #69 in [60,000 sq. km] SETTING: Plume (P2); Breakup
(B1, either nc. or sc. Superior
4b Cauchon Lake DYKES: Cauchon Lake
(2.09-2.07 Ga) (includes Birthday Rapids)
(nw. Superior Prov.) (2.09 and 2.07 Ga)
REF.: #175 in ; #72 in 
(B2, nw. Superior Craton)
4c Fort Frances DYKES: Fort Frances (2.08 Ga)
(2.075 Ga) REF.: #174 in [l]; #73 in 
(sw. Superior Prov.) SETTING: Plume (P2); Breakup[75,000 sq. km] (B1, sc. Superior Craton)
4d Lac Esprit (2.07 Ga) DYKES: Lac Esprit (2.07 Ga)
(ne. Superior Prov.) REF.: #74-75 in ,
Buchan et al., 2004
SETTING: Plume (P2); ?Breakup
(B1, nc. Superior Craton)
4e Griffin (2.11 Ga) SILLS: Griffin [Hurwitz] (2.11 Ga)
(Hearne Prov.) REF.: #179 in ; #70 in [80,000 sq. km] SETTING: Plume (P3); ?Breakup
4f Napaktok (?2.12 Ga) DYKES: Napaktok (<2.13 Ga);
(Labrador Coast) Tikkigatsiagak (2.12 Ga); ?Domes
REF.: #182 in ; #68 in 
5 2.05-2.02 Ga
5a Kangamuit DYKES: Kangamuit (of Greenland)
(2.05-2.04 Ga) (2.04-2.05 Ga); Iglusuataliksuak
(wc. Greenland; (2.05 Ga)
Nain Prov.) REF.: #170 in ; #80 in ;[20,000 sq. km] [#78 in 
SETTING: Breakup (?B2, n.
North Atlantic [Nain] Craton)
5b Lower Povungnituk VOLCANIC ROCKS: Lower Povungnituk
(2.04 or 1.96 Ga) SILLS: Korak [2.04 Ga)
(Cape Smith Belt, REF.: #169 in ;
ne. Superior Prov.) Modeland et al., 2003
(B3, n. Superior Craton)
5c Hearne (2.04 Ga) DYKES: Hearne (2.04 Ga)
(Slave Prov.) REF.: #168 in ; #81 in [15,000 sq. km] SETTING: Breakup
(B2, s. Slave Craton)
5d Lac de Gras DYKES: Lac de Gras (2.02-2.03 Ga)
(ca 2.025 Ga) LAYERED INTRUSION: Booth River
(Slave Prov.) Complex (2.02 Ga)[30,000 sq. km] REF.: #167 in , #82 in 
SETTING: ?Plume (P3)
6 2.00-1.95 Ga
6a Minto-Eskimo DYKES: Minto (2.00 Ga); Inukjuak
(2.00 Ga) VOLCANIC ROCKS: Eskimo; Persillon
(e. Hudson Bay, (Pachi); Nastapoka Group
ne. Superior Prov.) OPHIOLITE: Watts Group (2.00 Ga)[10,000 sq. km REF.: #162 in ; #88 and #92
for dykes only] in ; Scott et al., 1999
COMMENT: geochemically linked
with western Povungnituk (2.04
Ga) by Legault et al. (1994)
SETTING: Plume (P3); ?Breakup
(nc. Superior Craton)
6b Flaherty-Haig VOLCANIC ROCKS: Flaherty
(?1.96 Ga) (? -1.96 Ga)
(e. Hudson Bay) SILLS: Haig; Sutton
Inlier; Sleeper Island
REF.: #161 in ; Chandler and
Schwarz, 1980; Schwarz, and
COMMENT: linked with eastern
Povungituk (1.96 Ma) by Legault
et al. (1994)
(B3, nc. Superior Craton)
6c Upper Povungnituk VOLCANIC ROCKS: Upper Povungnituk
(ca. 1.96 Ca) (1.96 Ga)
(Cape Smith Belt, REF.: #169 in ; Pehrsson per.
ne. Superior Prov.) comm., 2000; Legault et al.,
1994; Modeland et al., 2003
SETTING: Breakup (B3, n.
Superior Prov. at 2.04 Ga)
6d Mugford (1.95 Ga) VOLCANIC ROCKS: Mugford
(Nain Prov.) (-1.95 Ga); ?Ramah; ?Snyder
400 sq. km 1.2 km thick REF.: #159 in ; Hamilton
pers. comm., 2000
SETTING: ? Rifting
7 1.90-1.88 Ga (in Trans Hudson and adjacent Rae-Hearne Craton)
7a Sandy Bay VOLCANIC ROCKS: oceanic plateau (Sandy
(1.90 Ga) Bay), oceanic island basalts and ocean
(Flip Flon belt) (Trans floor assemblages
Hudson Belt) REF.: #154 in ; Syme et al., 1999;
Stern et al., 1999
SETTING: ? Plume (P6)
7b Josland (1.88 Ga) SILLS: Josland Lake including Mikanagan
(Amisk collage, Trans Hudson) (1.89-1.88 Ga)
REF.: Stern et al. 1999; Zwanzig et al.,
2001; Turek et al. 2000
SETTING: Back-arc (A2)
7c Bravo Lake (1.90-1.88 Ga) VOLCANIC ROCKS AND SILLS: Bravo Lake
(Piling-Penhryn Group, Rae (1.90-1.88 Ga)
Prov.) REF.: Jackson and Taylor, 1972; Scott et
7d Lake Harbour VOLCANIC ROCKS AND SILLS: Lake Harbour
(-1.87 Ga) Group (~1.87 Ga)
(Lake Harbour Group, Rae REF.: St-Onge et al., 2000
Prov.) SETTING: Rifting and breakup of the
Meta Incognita microcontinent from the
Craton [St-Onge et al., 2000]
8 1.88-1.86 Ga (Circum-Superior events)
8a New Quebec-Cycle 2 VOLCANIC ROCKS AND SILLS: ‘Cycle 2’
(1.88 Ga) SILLS: Montagnais (1.88-1.87 Ga)
(New Quebec orogen) REF.: #151 in [30,000 sq. km] SETTING: Back Arc (A1)
8b Chukotat VOLCANIC ROCKS: Chukotat (lower portion
(1.89-1.87 Ga) are komatiitic basalt,) (1.87 Ga)
(Cape Smith Belt, ne. SILLS: Katniq sills (1.92 or ~1.89 Ga)
Superior Prov.) REF.: #153 in ; N. Wodicka, pers.
SETTING: Plume (P4)
8c Molson-Thompson DYKES: Molson (1.88 Ga); Pickle Crow
(1.88-1.86 Ga) (1.88 Ga)
(Thompson Belt; nw. Superior SILLS: Fox River (1.88 Ga); Thompson
Prov.) Nickel Belt magmatism[>30,000 sq. km] KOMATIITES: Winnipegosis (1.86 Ga)
REF.: #150 in [l]; #85 and #98 in ;
Hulbert et al., 1994; Buchan et al.,
2003; Hulbert er al., 2004
SETTING: Plume (?P1, P4); Back-arc (A1)
8d Hemlock VOLCANIC ROCKS: Hemlock put (1.87 Ga);
(1.88 Ga) Gunflint Fm. (1.88 Ga); Badwater
(Animikie Basin–Marquette Greenstone
Range, Southern Prov.) SILLS: Kiernan
REF.: Ueng et al., 1988; Schneider et
al., 2002; Fralick et al., 2002
SETTING: Rifting or Foredeep
9 1.83-1.82 Ga
9a Sparrow DYKES: Sparrow (1.83 Ga)
(1.83 Ga) GABBRO BODIES: In Wollaston-Mudjatik
(Rae Prov.) Transition zone (1.83-1.82 Ga)[100,000 sq. km] REF.: #146 in  & #101 ; Annesley et
COMMENT: Is there a link with
Christopher Island Fm (Baker Lake basin)
(Cousens er al., 2001; Peterson et al.,
SETTING: ? Breakup (Rae Craton)
10 1.75-1.71 Ga
l0a Cleaver (1.75-1.74 Ga) DYKES: Cleaver (1.74 Ga); Hadley Bay
(Bear and Rae Pov.) (~1.75 Ga) and MacRae Lake (~1.75 Ga)[three locations spanning an REF.: #105-107 in ; Irving et al.,
area of 300,000 sq. km] 2004
COMMENT: Is this event a precursor to
Bonnet River dykes and stocks, and Slab
volcanics (1.71 Ga), which have been
linked with Wernecke Supergroup
(Thorkelson et al., 2001)? Is there a
link to Pitz Fm and Nueltin Intrusive
Suite of Baker Lake area (Turner et al.,
2003; Peterson et al., 2002)?
SETTING: ? Plume (P3) Breakup
(preceeding breakup of nw. Laurentia)
10b Winagami (?1.89-1.76 Ga) SUBSURFACE SHEETS: Winagami (1.89-1.76
(Western Canada Basin) Ga).[120,000 sq. km] REF.: #149 in 
COMMENT: Imaged seismically; possible
link with Cleaver dykes suggested by
Ross and Eaton (1997)
SETTING: ? Plume (P3)
11 1.64 Ga
11a Melville Bugt (ca. DYKES: Melville Bugt (~1.64 Ga)
1.64 Ga) REF.: #132 in ; Hamilton et al., 2004
(w. Greenland) SETTING: ?[220,000 sq. km]
12 1.47-1.44 Ga
12a Moyie (1.47 Ga) SILLS: Moyie (Purcell) (1.47 Ga)
(Belt-Purcell basin, VOLCANIC ROCKS: Purcell
Cordillera) DYKES: Tobacco Root (Wyoming Block-1)[120,000 sq. km dykes only] (1.46 Ga)
REF.: #124 in ; #117 in 
SETTING: Plume (P2); Breakup (w. or sc.
12b Michael-Shabagamo (ca. SHEETS: Michael Gabbro (~1.47 Ga);
1.47 Ga) Shabagamo (~1.46, 1.45 Ga)
(ne. Grenville Prov.) REF.: Corrigan et al., 2000; Krogh, 1993[two regions spanning 50,000 in Gower and Krogh, 2002; #122 in ;
sq. km] #119-120 in 
SETTING: Back-arc (A1)
13 1.38 Ga
13a Hart River-Salmon River VOLCANIC ROCKS and SILLS: Hart River
Arch (1.38 Ga) of n. Cordillera; Salmon River
(1.38 Ga) Arch (1.38 Ga) of s. Belt Basin
(n. Cordillera and s. Belt REF.: entry in Table 4 of ; #121
Basin) in 
SETTING: ? Plume (P2) ? Breakup (nw.
14 1.28-1.27 Ga
14a Mackenzie (1.27 Ga) DYKES: Mackenzie (radiating swarm) (1.27
(Canadian Shield) Ga); Bear River (127 Ga); ‘305’[2,700,000 sq. km] VOLCANIC ROCKS: Coppermine; Ekalulia;
Nauyat; Hansen; Tweed Lake
SILLS: Christie Bay; Tremblay; Goding
LAYERED INTRUSIONS: Muskox (1.27 Ga)
REF.: #107 in ; 140, 142, 143 in ;
Sevigny et al., 1991; French et al.,
2002; Schwab et al., 2004
SETTING: Plume (P1); Breakup (B1, n.
14b Harp-Nain-Nutak-middle DYKES: Nain-LP (1.28 Ga); Nutak (1.27
Gardar Ga); Nain-HP; Harp (1.27 Ga) Gardar-BDO
1.28 and 1.27 Ga (~1.28 Ga) Gardar-BD1
(North Atlantic Craton) REF.: #108 in ; #132, #133, #137,
(Nain Prov. and s. Greenland) #138, #139 and #141 in [80,000 sq. km] SETTING: ?Breakup (se. Laurentia)
COMMENT: The anorthosites, diorites,
granites, and troctolites of the
1.35-1.29 Ga Nain Plutonic
Suite [e.g. Ryan and James, 2004] which
cover an area of 20,000 sq. km in
Labrador, are unrelated
15 1.25-1.225 Ga (Grenville Province)
15a Sudbury [dykes] (1.24 Ga) DYKES: Sudbury (1.24 Ga)
(Superior and Grenville REF.: #104 in ; #146 in 
Prov.) SETTING: Plume (P2); Back-arc (A1)[90,000 sq. km]
15b Seal Lake-Mealy (1.25 Ga) VOLCANIC ROCKS: Seal Lake
(Grenville Prov.) SILLS: Naskaupi (1.25 and 1.22 Ga)[20,000 sq. km] DYKES: Mealy (1.25 Ga) North West River.
REF.: #105 in ; #113, #144, & #144a
SETTING: Back-arc (A1)
16 1.18-1.14 Ga
16a Davy Group-Tshenukutish- SILLS AND DYKES: Davy Group in Wakeltam
Algonquin rift (1.18 Ga); Lillian Suite
(1.18-1.16) CORONITIC GABBRO: in Baie du Nord
(Grenville Prov.) segment of Tshenukutish domain (1.17 Ga)
METAGABBROS: Algonquin metagabbros in
Central Gneiss Belt (~1.17 Ga)
DYKES: Kingston (~1.16 Ga)
REF.: #97 in ; #145, #147 & #149
COMMENT: Widely separated events in
Grenville Prov. of the same age
SETTING: Back-arc (A1)
16b Late Gardar (1.16 Ga) DYKES: Tugtutoq Giant Dykes (1.18 and
(North Atlantic Craton, 1.16 Ga)
southern Greenland) REF.: Buchan et al., 2000; Upton et
SETTING: Breakup (?)
16c Abitibi [dykes] (1.14 Ga) DYKES: Abitibi (1.14 Ga)
(Superior Prop.) REF.: #94 in ; #155 in [240,000 sq. km] SETTING: Plume (P1); Breakup (?
precursor to Keweenawan)
17 1.11-1.09 Ga
17a Keweenawan (Mid-continent VOLCANIC ROCKS, SILLS AND DYKES:
rift system) Keweenawan (1.11-1.09 Ga; main pulses,
(1.11-1.09 Ga; main pulses: 1.107 and 1.097 Ga).
1.11, 1.10 Ga) REF.: #90 in ; #158-170 in 
(Southern Prov.) COMMENT: ?Relationship with Southwestern[160,000 sq. km] USA Diabase Province [#89 in ]; and
Moores Lake sills (1.11 Ga) in Athabasca
basin [French et al., 20021. ?Link with
Umkondo event of Africa [#91 in ;
Hanson er al., 2004]
SETTING: Plume (P3) Breakup (attempted
breakup of Laurentia)
18 0.78 Ga
18a Gunbarrel (0.78 Ga) SHEETS: Hottah (sheets) (0.78 Ga)
(Slave Prov; Mackenzie Mtns. VOLCANIC ROCKS: Huckleberry; Irene (ca.
of n. Cordillera; Wyoming 0.76 Ga)
Prov.) SILLS: Faber Lake Gabbro (0.78); Wolf[several areas spanning a Creek (0.78 Ga); Mackenzie Mountains
distance of about 2500 km] DYKES (0.78 Ga): MacDonald; Mackenzie
Mountains; Tobacco Root-Group B
REF.: #63 in ; #178-181 in ; Harlan
et al., 2003b
COMMENT: ?Link with Windermere rifting
[#77 in ]; Both South China and
Australia have been proposed as the
SETTING: Plume (P1); Breakup (B1, w.
19 0.72 Ga
19a Franklin-Thule (0.72 Ga) VOLCANIC ROCKS: Natkusiak
Arctic Islands, mainly Baffin DYKES: Franklin (0.72 Ga); Thule (of
Island also n. Superior Greenland)
Prov.) SILLS: (0.72 Ga) Minto Inlier;[1,100,000 sq. km for Coronation; Dybbol; Banks Island;
Canadian portion] Steensby Land (of Greenland)
REF.: #58 in  and #185-186 in 
COMMENT: Note 0.69 Ga Gataga and Hyland
Group volcanics of northern Cordillera
[Ferri et al., 1999; Colpron et al.,
2002]. Do these represent subsequent
rifting associated with the
SETTING: Plume (P1); ?Breakup (B1, n.
20 0.615-0.56 Ga Central Iapetus
(Laurentian margin, Event [Puffer 2002]
20a Long Range (0.62 Ga) DYKES: Long Range (0.62 Ga)
(e. North America) VOLCANIC ROCKS: Lighthouse Cove[105,000 sq. km] REF.: #54 in ; #192 in 
SETTING: ?Plume ?Breakup (B2, e.
Laurentia from Baltica)
20b Grenville-Rideau (0.59 DYKES: Grenville (0.59 Ga)-Rideau-
Ga) Adirondack (fanning swarm)
(e. North America) REF.: #53 in ; #194-196 in [140,000 sq. km] SETTING: Plume (P1); ?Breakup (B1, e.
Laurentia from ?Amazonia)
20c Sept-Iles-Catoctin (0.56 LAYERED INTRUSION: Sept-Iles (0.56 Ga)
Ga) VOLCANIC ROCKS: Skinner Cove; Catoctin
(e. North America) (in US Appalachians) (0.56 Ga)
REF.: #52 in 
SETTING: ?Plume (P3); ?Breakup (e.
Laurentia from Dashwoods Terrane)
21 0.62-0.55 Ga (Avalon terrane, Appalachians)
21a Harbour Main VOLCANIC ROCKS: part of Harbour Main
(ca. 0.62 Ga) Group (0.63-0.59 Ga)
(Avalon Zone, Appalachians) INTRUSIONS: Holyrood granite suite (0.62
Ga); Connaigre Bay Group (0.63 Ga);
Simmons Brook suite (0.62 Ga); Cap au
Miquelon Group (ca. [greater than or
equal to] 6.2 Ga); East Bay Hills Belt
(ca. 0.62 Ga); Coxheath Hills Belt (ca.
REF.: Rabu et al., 1996; Bevier et al.,
21b Marystown VOLCANIC ROCKS: Marystown Group
(0.59-0.55 Ga) (0.59-0.575 Ga); Long Harbour Group
Avalon Zone, Appalachians) (0.57-0.55 Ga); St. Pierre Group (0.58
Ga); Belle Riviere Group (0. 57 Ga);
part of Harbour Main Group (0.63-0.59
Ga); Coastal Belt (0.58 Ga)
REF.: p. 15, O’Brien et al., 1996; Rabu
et al., 1996; Bevier et al., 1993; Fig.
3 in McNamara et al., 2001
SETTING: Arc/ back-arc
22 0.57-0.52 Ga (Cordillera)
22a Hamill-Gog (0.57 Ga) VOLCANIC ROCKS: Hamill-Gog Group
(SE Canadian Cordillera) (0.57 Ga)
REF.: Colpron et al., 2002
22b Selwyn Basin (0.54-0.45 SILLS: Post-Hyland Group (0.52 Ga)
Ga) VOLCANIC ROCKS: Alkali and potassic
(Cordillera, n. of and within mafic volcanism
Selwyn Basin) REF.: #218 in ; Goodfellow et al.,
1995; Abbott, 1997
SETTING: Selwyn Basin rifting
23 0.47- 0.42 Ga (Appalachians)
23a Middle Ordovician VOLCANIC ROCKS: Middle Ordovican
‘Overstep’ Sequence Overstep Sequence’ includes bimodal
(0.47-0.45 Ga) magmatism (in Exploits subzone of
(Gander Zone-Dunnage Zone) Newfoundland, Bathurst area of New
Brunswick, Maine, and United Kingdom)
REF.: van Staal et al., 1996
COMMENT: Coeval Dunn Point bimodal volc.
(0.46 Ga) occur in the Avalon terrane,
Nova Scotia (Hamilton and Murphy, 2004)
23b Late Ordovician-Silurian GANDER ZONE-DUNNAGE ZONE (of New
magmatism of Atlantic Canada Brunswick, Quebec and Maine) (0.43-0.41
(11.44-11.41 Ga) Ga)
(e. Newfoundland and VOLCANIC ROCKS: Tobique and Piscataquis
Maritimes) volcanic belts
REF.: Keppie and Dostal, 1994
AVALON ZONE (of Nfld. and New Brunswick)
SILLS: Cape St. Mary’s (0.44 Ga)
VOLCANIC ROCKS: Bayswater Group (0.44
Ga); Coastal Volcanic Belt (0.43-0.42
DYKES: Kingston Terrane dyke complex
(0.44-0.41 Ga); Passamaquoddy Bay
REF.: Van Wagoner et al., 2001; Barr et
al., 1999; Hodych and Buchan, 1998
MEGUMA ZONE (of Nova Scotia) (0.44 Ga)
VOLCANIC ROCKS: White Rock Fm (0.44 Ga)
INTRUSION: Brenton monzogranite (0.44
REF.: MacDonald et al., 2002; Keppie and
OVERSTEP SEQUENCE OF NEWFOUNDLAND
VOLCANIC ROCKS: bimodal volc. such as
King George IV (0.43 Ga); Springdale
(0.42 Ga), and Botwood groups; and
mainly felsic volc. such as Sops Arm and
La Poile groups
INTRUSION: Taylor Brook (0.43 Ga); Main
Gut (0.43 Ga)
REF.: Chandler et al., 1987; Heaman et
24 0.36-0.32 Ga
24a Magdalen (Maritimes) INTRUSIONS: magmatic underplate
Basin underlying entire Magdalen (Maritimes)
(0.36-0.32 Ga) Basin, interpreted from gravity;
(Maritimes) Wentworth and Wyvern gabbros
VOLCANIC ROCKS: Cape an Diable; Fountain
Lake (mafic to felsic)
REF.: Pe-Piper and Piper, 1998; Murphy et
25 0.27-0.20 Ga (Cordillera)
25a Cache Creek VOLCANIC ROCKS: Late Triassic volcanics
(Late Triassic and interpreted to represent oceanic plateau
mid-Permian) (Cordillera) (Tardy et al., 2001). Overlies[~1500 km long, 50-100 km mid-Permian magmatism interpreted to
wide] represent underlying Permian Crust
Alternative, more complex model
suggested by Struik et al. (2001)
REF.: #38 in 
SETTING: ?Plume (?P6)
25b Wrangellia (0.23 Ga) VOLCANIC ROCKS: Karmutsen; Nikolai
(Cordillera) INTRUSIONS: Kluane[1,000,000 cu. km] SILLS: Maple Creek (0.23 Ga)
REF.: #34 in ; #303-304 in 
SETTING: Plume (P6)
25c Ramparts Group (0.21 Ga) SILLS AND VOLCANIC ROCKS: Ramparts Group
(Alaska) (0.21 Ga)[100,000 sq. km] REF.: #306 in 
26 0.20 Ga
26a ENA (Eastern North VOLCANIC ROCKS: North Mountain Basalt;
America) portion of Grand Manan
CAMP (Central Atlantic DYKES: ENA (0.20 Ga)
Magmatic Province) (0.20 Ga) COMMENT: Rest of CAMP event is located
(Atlantic Canada) along east coast of US and also in[7,000,000 sq. km for entire Europe, NW Africa and South America
event] REF.: #32 in ; #307 in 
SETTING: Plume (P1); Breakup (B1,
forming Atlantic Ocean)
27 0.14-0.09 Ga
27a New England-Quebec (NEQ); INTRUSIONS AND PLUTONS: Monteregian
Monteregian) Hills intrusions of Quebec and related
(0.14-0.11 Ga) plutons of[60,000 sq. km] New England) (0.14-0.11 Ga)
REF.: #323 in 
27b Trap (sw. Greenland) DYKES: Trap (0.14 Ga)[20,000 sq. km] REF.: #30 in ; #322 in 
SETTING: ? Breakup (B2, Linked to
subsequent breakup of Greenland from
Laurentia to form Labrador Sea)
27c Sverdrup Basin Magmatic VOLCANIC ROCKS AND SILLS: including
Province Strand Fiord pot (0.13-0.09 Ga; major
(part of High Arctic Large pulse at 0.095 Ga); Alpha Ridge
Igneous Province; HALIP) DYKES: Queen Elizabeth Islands (inludes
(0.13-0.09 Ga) (Arctic Hazen Strait); Lightfoot River
Islands) INTRUSIONS: Wootton (0.092 Ga)[550,0110 sq. km] REF.: #12 in ; #325 in ; Tarduno
et al., 1998; Trettin and Parrish, 1987
COMMENT: Part of Large Igneous Province
that includes Svalbard and Franz Josef
Land (Maher, 2001
SETTING: Plume (P1); Breakup
28 0.07-0.05 Ga
28a Carmacks VOLCANIC ROCKS: Carmacks (0.07 Ga)
(n. Cordillera) RER: #9 in [63,000 sq. km] SETTING: Plume (? P6)
28b Crescent (0.06-0.05 Ga) VOLCANIC ROCKS: Crescent Terrane (“Coast
(western margin of North Range Basalt Province”) (0.06-0.05 Ga)
America) REF.: #339 in ; Murphy et al., 2003
SETTING: Plume (? P6)
28c North Atlantic Igneous VOLCANIC ROCKS: Cape Dyer; West
Province (NAIP) Greenland
(0.06 Ga) DYKES: Cape Searle; West Greenland
(Baffin Island, w. Greenland) RER: #334 and 335 in ; #5 in [1,300,000 sq. km for entire COMMENT: Part of Noah Atlantic Igneous
NAIP event] Province of Greenland, United Kingdom
(0.062-0.052 Ga), and linked to
present-day Iceland hotspot
SETTING: Plume Breakup (Europe from
29 0.025-0.015 Ga
29a Behm Canal (Tertiary DYKES: Behm Canal (0.023-005 Ga)
‘Lamprophyre’ Province) REF.: #348 in 
(ca. 0.023-0.005 Ga) COMMENT: alkalic lamprophyres
(c. British Columbia) SETTING: Hotspot (H1)[25,000 sq. km]
29b Columbia River Basalt VOLCANIC ROCKS, DYKES AND SILLS:
Group Columbia River Basalt Group (CRBG)
(mainly 0.017-0.0150 Ga) REF.: #1 in 
(nw. US) SETTING: Plume (P1, P7)[165,000 sq. km]
29c Chilcotin (Neogene- VOLCANIC ROCKS: Chilcotin Group basalts;
Paleogene; mainly Miocene) Anahim volcanic belt; Cheslatta Lake
(c. and sc. British Columbia) suite; Masset Fm[25,000 sq. km] REF.: Anderson et al., 2001
COMMENT: Nearby to and potentially
linked to Columbia River Basalt Group
SETTING: Hotspot (H1) Back-arc (partial
Table 2 Archean greenstone belts in Canada interpreted to have a plume
origin (i.e. tholeiitic sequences containing komatiites and/ or those
interpreted as oceanic plateaus). Details and full referencing on most
events is available in compilations  (=Ernst and Buchan 2001) and 
(=Buchan and Ernst 2004), and Tomlinson and Condie (2001), or in the
additional cited references. “REF.:” = key reference(s). SETTING
codes are explained in Table 3.
Event name Magmatic components (Age)
A1 3.11-2.98 Ga
A1a Hunt River GREENSTONE BELTS: Hunt River (3.11 Ga)
(3.11 Ga) REF.: James et al., 2002
(Hopedale block, North COMMENT: Includes komatiites
Atlantic Craton) SETTING: ?Plume (P4)
A1b Florence Lake GREENSTONE BELTS: Florence Lake
(2.99-2.98 Ga) (2.99-2.98 Ga)
(Hopedale block, North REF.: James et al., 2002
Atlantic Craton) COMMENT: Includes komatiites
SETTING: ?Plume (P4)
A1c North Caribou GREENSTONE BELTS: Balmer Assemblage (Red
(2.99 Ga) Lake greenstone belt) (2.99 Ga)
(n. Caribou Terrane, nw. REF.: #256 in ; Tomlinson et al.,
Superior Prov.) 1998; Hollings et al., 1999 “plume
COMMENT: Includes komatiites
SETTING: ?Plume (P4)
A2 2.93-2.92 Ga
A2a Western Superior GREENSTONE BELTS: Steep Rock; Finlayson;
(2.93 Gal North Rim Unit of McGruer Assemblage
(Wabigoon subprov., w. (2.93 Ga) Lumby Lake 2963-2898 Ma, ?
Superior Prov.) Heaven Lake [U 2954 Ma]
REF.: #252 in 
COMMENT: Includes komatiites. Rifting or
impingement of plume in subduction
setting (Hollings et al. 1999)
SETTING: ?Plume (P4) Back-arc (A2)
A3 2.86 Ga
A3a Pickle Crow GREENSTONE BELTS: Pickle Crow Assemblage
(2.86 Ga) (~2.86 Ga)
(Uchi subprov., nw. Superior REF.: #244 in 
Prov.) COMMENT: Includes komatiites
SETTING: ?Plume (P4)
A4 2.79-2.78 Ga
A4a Vizien GREENSTONE BELTS: Vizien (2.79 Ga)
(2.79 Ga) REF.: #236 in 
(Minto Block, ne. Superior COMMENT: Includes komatiites
Prov.) SETTING: ?Plume (P4, P6)
A4b Faribault-Thury GREENSTONE BELTS: greenstone belt
(ca. 2.88-2.71 Ga) remnants in Faribault-Thury Complex
(Minto Block, ne. Superior (~2.88-2.71 Ga)
Prov.) REF.: Maurice et al., 2003
SETTING: ?Plume (P4)
A4c Fourbay GREENSTONE BELTS: Fourbay Sequence in
(2.78 Ga) Savant Lake and Sturgeon Lake (2.78 Ga)
(Wabigoon subprov, w. REF.: Sanborn-Barrie and Skulski, 1999
Superior Prov.) COMMENT: Possible oceanic plateau
SETTING: ?Plume (P6)
A5 2.75-2.70 Ga
A5a Prince Albert-Woodburn GREENSTONE BELTS: (~2.73 Ga): Prince
(2.73 Ga) Albert Group; Woodburn Group; Mary River
(Rae Prov.) Group, ?Murmac Bay Group[>1000 km. long belt] REF.: #220 in ; Schau, 1997; Aspler et
al., 1999; Zaleski et al., 2001;
Hartlaub et al., 2002; Skulski et al.,
COMMENT: Includes komatiites
SETTING: ?Plume (P4) ?Breakup Rae Craton
A5b Kam VOLCANIC ROCKS and DYKES: Kam Group and
(2.73-2.70 Ga) early dykes (2.73-2.70 Ga).
(Slave Prov.) REF.: #227 in 
COMMENT: Widespread tholeiitic cover
SETTING: ?Plume (?P3)
A5c Abitibi GREENSTONE BELTS: includes komatiites:
(2.75-2.70 Ga) Pacaud (2750-2735 Ma); Stoughton-
(Abitibi belt, Superior Roquemaure (2725-2720 Ma); Kidd-Munro
Prov.) (2718-2710 Ma); Tisdale (2710-2703 Ma)
REF.: #224 in ; Ayer et al., 2002;
Sproule et al., 2002
COMMENT: Includes komatiites
SETTING: ?Plume (P4); Back-arc (A2)
A5d Wawa GREENSTONE BELTS: Schreiber-Hemlo-White
(2.75-2.74 Ga) River-Dayohessarah (2.75-2.74 Ga)
(Wawa belt, Superior Prov.) REF.: #230 in [1)
COMMENT: Includes komatiites
SETTING: ?Plume (P4)
Table 3 Selected criteria for interpreting origin and setting of LIPs
and smaller intraplate mafic events.
MANTLE PLUME LINK
P1 Radiating dyke swarm
P2 Linear dyke swarm (or belt of mafic magmatism) perpendicular to
cratonic margin (failed-arm type of Fahrig, 1987; could also be
P3 Large event, distal from cratonic boundary
P4 Presence of high-Mg rocks, e.g. komatiites in Archean greenstone
P5 Geochemistry: OIB or FOZO signature
P6 Accreted oceanic plateaus
P7 Link to present-day hotspot
B1 Radiating swarm or failed-arm type swarm (Fahrig, 1987) with
convergence point near cratonic margin of similar age
B2 Linear dyke swarm, parallel to and nearby cratonic margin of
similar age. This is termed passive margin type swarm by Fahrig
B3 LIP situated nearby cratonic margin of similar age
A1 Location in a back-arc setting relative to concurrent orogenic
activity. However, this does not necessarily require back-arc
extension processes. (See Note 1, below)
A2 Coexisting with arc magmatism
HOTSPOT (OF UNSPECIFIED ORIGIN)
H1 Small (sub-LIP scale) region of anomalous intraplate mafic
Note 1: The Keweenawan rift activity is arguably in a back-arc setting
with respect to the Grenville orogen, yet it is generally viewed that
the Keweenawan magmatism is plume-related (see discussion in text).
John Morgan helped compile information on the link between Canadian HPs and breakup events. Discussions with Tom Skulski and Wouter Bleeker have been invaluable in guiding our application of LIP concepts to Archean greenstone belts. Mike Hamilton, Tony LeCheminant and Henry Halls are acknowledged for numerous discussions on the nature and setting of Proterozoic dyke swarms of Canada. Thoughtful reviews were provided by Wouter Bleeker, Michael Higgins and Peter Lightfoot. Figure 2a (portion of aerial photograph #A14233-138) [c] 2004, Her Majesty the Queen in Right of Canada, reproduced from the collection of the National Air Photo Library with permission of Natural Resources Canada. Figure 2b (archive number 202781) is reproduced with the permission of the Minister of Public Works and Government Services Canada, 2004, and courtesy of Natural Resources Canada, Geological Survey of Canada.
[FIGURE 2 OMITTED]
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R.E. Ernst and K.L. Buchan
Geological Survey of Canada
601 Booth Street
Ottawa, Ontario K1A OE8
Geological Survey of Canada publication no. 2004026
Accepted as revised 30 June 2004
COPYRIGHT 2004 Geological Association of Canada
COPYRIGHT 2004 Gale Group