Taking the pulse of planet earth: a proposal for a new multi-disciplinary flagship project in Canadian solid earth sciences.
Herein I propose a vision for a new multidisciplinary "big science" project for Canada's solid earth sciences. I call this proposed project: "Taking the Pulse of Planet Earth". At a modest cost, and over a 5 to 10 year life-span, it would aim at providing the most comprehensive and multidisciplinary knowledge base of the complete record of mafic magmatism in and around Canada, and through stimulating international cooperation, around the world.
A complete record of mafic magmatism (spatial distribution, ages, periodicities, rates, volume estimates, estimated geochemical fluxes to atmosphere and hydrosphere, tectonic settings, structural trends, sequence stratigraphic framework, evolving major and trace element compositions, evolving isotopic ratios, paleomagnetic information, paleo-intensities, associated ore deposits, etc.) constitutes critical input data for numerous first-order questions about the past and present evolution of our planet. Many of such questions relate to issues that are currently a focus of attention: global change, past climate extremes, complex Earth systems, planetary evolution, extinction events, flood volcanism, potential relationships with large impact events, and the discovery of new ore resources.
The proposed project is a focused, "smart", and highly efficient approach to solve a large number of these seemingly unrelated but first-order questions in contemporary earth science. At its core, it would have a large dating program, aiming to provide approximately 200 new, high-precision ages of mafic magmatic events across Canada and adjacent regions. A Supporting Geoscience grant system would ensure that other aspects of the magmatic record receive equal attention. Finally, I illustrate the impact this project would have on paleo-continental reconstructions. As part of this illustration, I synthesize existing data on two dyke swarms, the ca. 2.45 Ga Matachewan and Kaminak swarms, respectively, and propose a novel Superior-Hearne reconstruction within supercraton Superia.
Je propose ci-contre l'idee d'un nouveau projet multidisciplinaire de grande envergure dans le domaine des sciences des roches solides au Canada. J'ai nomme ce projet << Prendre le pouls de la planete Terre>>. D'un cout modeste et s'echelonnant sur cinq a dix ans, ce projet constituerait la base de connaissances multidisciplinaire la plus complete de tout le repertoire des evenements magmatiques mafiques au Canada et a son pourtour, cela, en profitant des effets stimulant de la cooperation internationale.
Un repertoire complet des evenements magmatiques mafiques (distribution spatiale, ages, periodicites, taux, estimations des volumes, estimations geochimiques des flux dans l'atmosphere et l'hydrosphere, cadres tectoniques, styles structuraux, cadres stratigraphiques des sequences, compositions des suites evolutives des elements majeurs et en trace, evolution des ratios isotopiques, donnees paleomagnetiques, paleo-intensites, gisements associes, etc.) constitue un registre de donees de base cruciales pour nombres de grandes questions sur revolution passee et actuelle de notre planete. Plusieurs de ces grandes questions sont liees a des problemes actuels qui mobilisent l'attention, tels: les changements a l'echelle planetaire, les evenements climatiques extremes du passe, les systemes planetaires complexes, l'evolution de la planete, les grandes extinctions biotiques, les grands epanchements volcaniques, les liens eventuels avec de grands impacts meteoritiques, ainsi que la decouverte de nouvelles sources de minerai.
Le projet propose constitue une approche ciblee, << habile >>, et tres efficace permettant de solutionner un grand nombre de ces grands problemes, sans liens apparents, des geosciences contemporaines. Au coeur du projet on retrouve un grand programme de datation visant a etablir quelques 200 nouvelles datations de grande precision d'evenements magmatiques au Canada et dans les regions peripheriques. Un systeme de subvention d'appoint permettrait d'assurer que d'autres aspects de la problematique magmatique recoivent autant d'attention. Finalement, a titre d'illustration, je decris les repercussions escomptees d'un tel projet sur les reconstitutions paleo-continentales. Dans le cadre de cette illustration, je presente une synthese des donnees disponibles concernant deux reseaux de dykes, soit les reseaux de Matachewan et de Kaminak de 2,45 Ga, respectivement, et propose une nouvelle reconstitution Superieur-Hearne dans le super-craton Superia.
LITHOPROBE, for more than two decades the premier flagship project of Canada's solid earth sciences, is winding down. Lithosphere-scale cross-sections have been gathered across the Canadian landmass and final syntheses are now being prepared (e.g., Percival et al., 2004). The inevitable ending of this project, on the heels of its success, will leave a growing vacuum across the Canadian earth science community at a time when competition for significant science funding is stronger than ever. Much of this competition revolves around highly visible "big science" projects in such fields as physics, astronomy, biochemistry and material science. Hence, we need to position ourselves to compete in this arena--we need a new flagship project. Here I will outline my vision for such a project, which I call "Taking the Pulse of Planet Earth" and which has at its core a large multidisciplinary study of all mafic magmatism through time. I use "mafic magmatism" as a shorthand here, but mean to include all mantle-derived magmatic activity other than steady-state arc magmatism; that is, all basalt ([+ or -] komatiite)-dominated and (or) bimodal magmatism associated with divergent margins, or more generally extensional regimes, intraplate magmatic provinces, mantle plumes, anorogenic provinces, kimberlite and alkaline provinces.
Before describing this vision in some detail, it is important to understand the key reasons why LITHOPROBE was successful as a "big science" project, so that we may emulate some of the same proven formulae in any future project. First of all, proponents of LITHOPROBE had a grand vision (e.g., Keen, 1981; Clowes et al., 1984)--to understand the fundamental architecture of the Canadian crust and lithosphere from coast to coast, in the third dimension, and through time. Second, rapid advances in seismic reflection and deep probing electromagnetic techniques, largely made possible by rapid growth in modern electronics and computing power, opened an entirely new observational window into the crystalline crust and, increasingly over the last decade, into the lithospheric mantle (e.g., Calvert et al., 1995; Cook et al., 1999). Third, the transect approach divided the overall project up into manageable chunks, linking regional expertise pertinent to particular transects with thematic expertise from across the country. Fourth, the Supporting Geoscience grant system assured "buy-in" from a multi-disciplinary science community, bringing together the best minds from different disciplines and organizations to work together on cross-sections through the Canadian lithosphere. And finally, competent leadership and management made it all happen. Of course, favourable timing of these and other factors (e.g., funding sources and cycles, willingness of the Geological Survey of Canada to be a significant partner, industry interest), all coming together at the right time, was equally critical.
Although all of the reasons above are necessary for a successful "big science" project, the first two--a grand vision, and a powerful new observational window--are undoubtedly the most important at a conceptual stage of any new project, and hence I will focus on those. The "vision" I propose is to understand the first-order pulse of the Earth, as reflected in its record of mafic magmatic events, at a global scale and over 4.5 billion years of Earth history. The "new observational window" is provided by ever increasing precision, accuracy, and resolving power in a broad range of disciplines and techniques: geochronology, isotope and trace element geochemistry, paleomagnetism, sequence stratigraphy, and geophysical approaches such as tomography, receiver function analysis, and geodynamic modeling.
THE PULSE OF PLANET EARTH
Silicate planets regulate their internal thermal state through melting events in their mantles; through transport of these melts and entrained heat to their surfaces; through creation of new lithosphere; and through recycling of cold crust and lithosphere back into their hot convective interiors (e.g., Davies, 1999). Today, on Earth, plate tectonics is the dominant process and is driven to a large extent by the negative buoyancy of aged, and therefore cool, rigid, and relatively dense slabs of oceanic lithosphere (i.e., the upper thermal boundary layer of the convective mantle). Mantle plumes (e.g., Morgan, 1971; Ritsema and Allen, 2003; Montelli et al., 2004), originating from instabilities at deeper thermal boundary layers (i.e., the core-mantle boundary in whole-mantle convection, e.g., Campbell, 2001), are thought to contribute about 10% of the global heat loss (Davies, 1999). Plate tectonics and mantle plumes are two independent manifestations of mantle convection, one strongly controlled by the mechanical behaviour of the cold upper boundary layer (e.g., Anderson, 2002a), the other by the fluid dynamics of a hot deep boundary layer. Each process produces voluminous mafic magmas, but on different and independent time scales and with different characteristic plan forms.
At longer time-scales, plate tectonic activity appears quasi-periodic and self-organizes into the supercontinent cycle (e.g., Schuiling, 1973; Anderson, 1982; Gurnis, 1988). There are subtle indications that the periodicity between successive supercontinent cycles is getting shorter (Fig. 1), perhaps primarily because the average size of continental plates has increased, allowing less time lag between break-up and subsequent aggregation events (Bleeker, 2003; see also Hoffman, 1997).
[FIGURE 1 OMITTED]
Running time forward into the future, average plate size may grow further while the overall vigour of mantle convection will decrease as a result of secular heat loss and exponential decay of heat-producing elements. At some point in the future, plates will seize up (e.g., Anderson, 2002b) and ultimately planet Earth will die a "thermal death", a state long reached by our much smaller neighbouring planet, Mars. There will be a transient era, in which heat production will still exceed conductive heat loss so that the mantle underneath the seized-up lithosphere will heat up, and transient plume activity or mantle overturn events may temporarily bring back mobility to the lithosphere, resulting in significant resurfacing. This is the probable state of our closest sister planet, Venus. Smaller neighbouring planets, although each having unique attributes, provide to some extent future snapshots of planet Earth as the rate of thermal evolution scales inversely with planetary radius (but, see also Stevenson, 2003). In this sense, Venus, with a radius 0.95 that of Earth, is marginally ahead of us, whereas our much smaller Moon, after initial cooling of its magma ocean, may never have had a mobile lithosphere, although the 3.9-3.1 Ga mare basalts suggest significant transient heating and possibly one or more mantle overturn events (e.g., Hess and Parmentier, 1995; Stegman et al., 2003).
Going back in time, it is possible that mantle plumes may have played a more significant role, although this remains uncertain. Perhaps plume activity was highly episodic, in response to strong spikes in heat flow across the core-mantle boundary due to tidal resonances in the fluid outer core (Greff-Lefftz and Legros, 1999; see Fig. 1). Increased core heat flow would have temporarily destabilized the boundary layer (D") at the base of the mantle and sharply increased plume activity. Because past rates of deceleration of the Earth's spin (due to tidal drag) are variable and not very well known (e.g., Denis et al., 2002, and references therein), the absolute timing of these resonances are poorly constrained but are estimated at ca. 3.0[+ or -]0.2 Ga and 1.8[+ or -]0.2 Ga (Greff-Lefftz and Legros, 1999). Could this explain the post-Archean spike in komatiite magmatism at ca. 1.9 Ga, as observed in circum-Superior belts?
In the past, plate tectonic recycling must have operated faster (e.g., Burke et al., 1976; Hargraves, 1986) to keep pace with significantly higher heat production and a still significantly higher primordial heat budget retained from the era of accretion and internal differentiation (e.g., Richter, 1988; Pollack, 1997; Davies, 1999). Thermal arguments suggest that at some point in the distant past, plate tectonics may not have been able to keep pace with the required rate of heat loss (e.g., Davies, 1992, 1999) for the simple reason that oceanic lithosphere, on reaching a nearby trench, was on average too young (hence too buoyant to subduct), and too thin (and hence less capable of cooling the mantle). Therefore, other and less familiar geodynamic processes must have mediated the required heat loss, perhaps involving 1) catastrophic mantle overturn and melting events (Davies, 1995; Condie, 1998; e.g., the 2.72-2.70 Ga basalt-komatiite-rhyolite magmatism documented in virtually every fragment of Archean crust around the world?); and 2) a less organized return flow of lithospheric material into the deep mantle in the form of delamination or "drip" (e.g., Davies, 1992) of subcreted mafic and ultramafic material after its partial transformation into dense, refractory eclogite. As part of the transformation into dense eclogite, aqueous fluids and fusible tonalite-trondjhemite-granodiorite (TTG) components were extracted from the subcreted mafic-ultramafic material and ascended into the overlying crust to contribute to the formation of granite-greenstone terrains. Numerous questions remain, but these less familiar, non-uniformitarian processes explain in part why Archean cratons do not look like modern continental plates, even though many of the second-order processes were similar (e.g., Vlaar, 1986; Zegers and van Keken, 2001; Bleeker, 2002; Hamilton, 2003). Certainly there was great mobility, involving both horizontal and vertical tectonics, but not necessarily in the form of plate tectonics sensu stricta, driven by strongly asymmetrical subduction of rigid, negatively buoyant slabs.
Most importantly for the present purpose, all these processes of first-order geodynamic interaction between core, mantle, and lithosphere, and of planetary evolution in general, leave a record in the form of mafic magmatic events. The products of these mafic magmatic events are preserved in the continental geological record through time, and for the last 180 million years also in the oceanic record. With increasing precision and accuracy these mafic magmatic events can be dated (e.g., Krogh et al., 1987; Harlan et al., 2003), while at the same time the mafic magmas provide chemical probes into the evolution of the lithosphere and convective mantle (e.g., Sylvester et al., 1997; Campbell, 2003). Some of them entrain deep crustal and mantle xenoliths to the surface, providing the only direct rock samples of the lithosphere available to us. Remanent magnetism of mafic magmatic rocks, if primary, can provide paleo-intensities of the geomagnetic field at the time of crystallization (e.g., Macouin et al., 2003), thus providing constraints on processes in the liquid outer core. When did the inner core start to form (e.g., Labrosse et al., 2001)? And when did the geodynamo ignite?
The very presence of these mafic magmatic events signifies extension, rifting and break-up, and arrival of mantle plumes or astheno-spheric upwellings. Some of the largest mafic magmatic events may be related to catastrophic mantle overturn events or slab avalanches. Basalt flows, dykes, and sills signify critical events on rifted margins and in the evolution of many sedimentary basins and, where they can be dated, allow time calibration of basin evolution. Some of the largest events are capable of venting enough C[O.sub.2], other volcanic gases, and (or) ash into the atmosphere to result in major environmental deterioration and upsets of the greenhouse balance. Although ultimate causes are still being debated (e.g., Courtillot and Renne, 2003), the two largest Phanerozoic extinction events, the Permo-Triassic and K-T boundaries, overlap in time or immediately follow the extrusion of some of the largest continental flood basalt sequences, the Siberian (e.g., Kamo et al., 2003) and Deccan (Hofmann et al., 2000) traps, respectively. Collectively, mafic magmatic events provide perhaps the most important record of "the pulse of the Earth" (e.g., Larson, 1991) in its overall thermal evolution from a hot, young planet to a cold, dead planet.
DATING ALL MAFIC MAGMATIC EVENTS THROUGH TIME
Many mafic magmatic events have been precisely dated (e.g., see Ernst and Buchan, 2001 for a recent compilation; see also Ernst and Buchan, 2004); however, many others remain undated or have yielded imprecise, less robust, or questionable ages (e.g., many old K-Ar ages). A few mafic magmatic events may not be datable directly, although with continuing advances in U-Pb and [sup.40][Ar-.sup.39]Ar dating, their number is shrinking. Hence, given the significance of mafic magmatic events to nearly all first-order geodynamic processes, either as direct manifestations of these processes, or as time calibrators, it is surprising that no concerted national or international effort has yet been made to date all such events and obtain a complete time series of mafic magmatism and its critical attributes. Perhaps this deficiency is more conspicuous now then ever, at a time when highly capable robotic rovers are investigating the surface of a neighbouring planet, yet key elements of the much more readily available terrestrial record remain poorly known.
Significant interest in a complete record of all terrestrial mafic magmatism exists in Canada and, indeed, Canadian geochronologists have been leading efforts to date such rocks. There is equal interest in this around the world, and a Canadian initiative may be the critical impetus for a global initiative (e.g., see plans for an international dating campaign on pre-Mesozoic large igneous provinces being developed by the Large Igneous Provinces Commission, at www.largeigneousprovinces.org). A comprehensive study of all mafic magmatism on Earth would have major impacts across numerous earth science disciplines, ranging from the study of ancient tectonic regimes, and the chemical and dynamic evolution of the core and mantle, to testing putative links between major flood volcanism, impacts, and extinctions, and the study of what triggers major climatic excursions. It is beyond the scope of this paper to do equal justice to all these disciplines and questions; below, I will merely illustrate potential impacts on two related fields: Precambrian evolution and paleo-continental reconstructions.
Let us examine plate tectonic reconstructions of various times in the past and the impact a global dating program would have on such reconstructions.
The extant record of Archean crust is highly fragmented and scattered around the globe in about 35 significant pieces, the "Archean cratons" (Bleeker, 2003). Each of these cratons is crosscut by numerous mafic dykes swarms, the precise ages of which provide a "bar code" (Fig. 2) that identifies that piece of crust and which can be expected to match, at least in part, the "bar code" from a distant craton that has since rifted off and been dispersed around the globe. For example, from the time of its formation in an ancestral landmass (Kenorland or Superia? see Bleeker, 2003), up to its incorporation into the Laurentian collage (Hoffman, 1988, 1989), the Superior craton was cut by as many as 20 mafic dyke swarms and intrusive events (Buchan and Ernst, 2004). To date, only about half of these events have been dated precisely. In contrast, the Slave craton in northwestern Canada was intruded, over a similar time interval, by about 10 dyke swarms, few if any of which match those in the Superior. Hence, these two distinct pieces of Archean crust were never close neighbours and likely originated from different ancestral supercratons (Bleeker, 2003). Only by 1.9-1.8 Ga were these crustal fragments brought into relative proximity during their amalgamation into Laurentia (Hoffman, 1988).
[FIGURE 2 OMITTED]
Subsequently, both cratons were cut by radiating dykes of the giant Mackenzie swarm at 1267 Ma (LeCheminant and Heaman, 1989), which fan out from a focal point along the northern edge of the Slave craton to the southeast, as far as the northwestern Superior craton (e.g., Ernst and Baragar, 1992; Baragar et al., 1996). Were Laurentia to break up, it would be the shared record of the Mackenzie swarm dykes, and their inherent paleomagnetic record, that would allow reconstruction of Laurentia and reveal, most conclusively, a shared, transient, residence of the Slave and Superior cratons in this continent from some time prior to 1267 Ma to the time of breakup.
Although correlation of platformal sequences on dispersed cratons is one of the more definitive tools to track initially adjacent pieces of crust (e.g., the sequence stratigraphic correlation of the Transvaal Supergroup, overlying the Kaapvaal craton, with that of the Mount Bruce Supergroup, overlying the Pilbara craton; e.g., Cheney, 1996), it is not the most generally applicable tool, because it relies on good preservation. During collision and orogenesis, platformal sequences may be entirely removed by uplift and erosion. Even where platformal sequences are preserved and potential sequence stratigraphic correlations can be made, they may not provide the detailed spatial and directional information to tightly constrain past configurations.
Mafic dyke swarms, on the other hand, have a significant aerial and depth extent and commonly survive significant uplift. Equally important, they provide a trend and thus directional information, as well as potentially precise piercing points (Park et al., 1995; Buchan and Ernst, 1997). In theory, an analysis of flow direction (e.g., from magnetic fabrics or imbrication of tabular plagioclase phenocrysts in the laminar flow regime near dyke margins) can provide unique azimuthal directions. Integrated mapping, high-precision age dating, fabric studies, and paleomagnetism of mafic magmatic events and their dyke swarms thus allow continental fragments to be placed:
1) at a specific latitude;
2) at a specific time;
3) with a known orientation;
4) in an position that optimizes geological continuity prior to break up and dispersal; and
5) that satisfies the specific requirements of precise piercing points.
In an ideal case, information from multiple dyke swarms (e.g., all dyke swarms of the Superior, precisely dated) would allow definition of improved apparent polar wander paths, providing additional information on how a certain continental fragment arrived at a specific location and which other blocks were fellow travelers. When a supercraton breaks up, apparent polar wander paths bifurcate; when two cratons are joined by collision, two previously independent paths merge into a common path. Better-defined and more densely populated polar wander paths can greatly reduce or even eliminate the ambiguities due to polarity. They may also contribute to the understanding of true polar wander events (e.g., Evans, 2003).
None of these various approaches is strictly new and various pioneers have applied them successfully, particularly over the last two decades. However, their scale of application and integration, under the proposed project, would be new. As recent examples, Wingate et al. (2002) have shown the power of every new precisely dated mafic event and associated paleopole in testing the putative Laurentia-Australia connection in the mid-Proteozoic, whereas Buchan et al. (2000) have applied similar tests to Laurentia-Baltica connections. However, no comprehensive effort has been made to address these questions for all mafic magmatic events across Canada. For instance, about half of the mafic magmatic events in the Slave and Superior, two of the best-studied cratons worldwide, remain to be dated precisely. Worse, few if any mafic dyke swarms have been dated from the Rae craton and, hence, the ancestry of this second-largest building block of Laurentia remains entirely unknown.
Given the improved precision in many of the underlying techniques, and the growing awareness that mafic magmatic events and their inherent information (precise age, composition, causative tectonic event, orientation, paleolatitude and polar wander path) provide the most efficient, robust, and generally applicable tools to unravel past plate configurations, the time seems right for a national and international effort.
AN EXAMPLE: A SUGGESTED SUPERIOR-HEARNE CORRELATION AT 2.45 GA
As one further illustration of the power of this approach, I will present a possible reconstruction of the Hearne and Superior cratons prior to their breakup and dispersal sometime before 2.0 Ga. The Superior craton is cut by the large Matachewan dyke swarm (e.g., Halls and Zhang 1998, and references therein), which radiates from an apparent focal point along its Huronian margin--a probable break-up margin that was later obscured by younger Grenvillian overthrusts. Although complicated by the presence of two age populations, the younger Matachewan dykes have been dated precisely at 2446 Ma (e.g., Heaman, 1997). Many of these dykes contain abundant, large plagioclase megacrysts (Fig. 3a, b, c), which set these dykes apart petrographically from many other dyke swarms. I estimate that such an abundance of large plagioclase megacrysts occurs in fewer than 10% of mafic dyke swarms worldwide. Following up on earlier suggestions of similar dykes in the Kaminak area of the Hearne craton (Christie et al., 1975), Heaman (1994) showed that these dykes, characterized by a similar abundance of large plagioclase megacrysts (Fig. 3d, e), are essentially identical in age (ca. 2.45 Ga, Heaman, 1994). Remarkably, both dyke swarms trend in a northerly direction, at high angles to dominant late Archean tectonic trends in each craton.
[FIGURE 3 OMITTED]
Existing paleomagnetic data (Christie et al., 1975) allow the Hearne craton to be placed, at ca. 2.45 Ga, just to the south of the Huronian margin of the Superior craton (Fig. 4a, b, c)--a position that could equate the Kaminak dykes with a southern continuation of the younger age population of the Matachewan dykes, perhaps as another branch of a giant radiating dyke swarm associated with a triple junction along the Huronian margin (Fig. 4d). This configuration (Fig. 4d) suggests that dyke intrusion, rifting, and eventual break-up of supercraton Superia may have occurred in response to the arrival of a mantle plume head--the Matachewan plume of Heaman (1994). The proposed reconstruction would suggest a more or less direct correlation between the partly glaciogenic Huronian Supergroup (e.g., Young et al., 2001) and Hurwitz Group (e.g., Young, 1973, 1975), perhaps on either side of a large continental rift (Fig. 5). By 2218 Ma, the age of the Nipissing diabase sills in the Huronian Supergroup (Corfu and Andrews, 1986; Krogh et al., 1987), this rift was evidently wide enough to impede southward propagation of Nipissing magmas across the rift into the Hurwitz basin. Nipissing sill magmas are thought to be derived, via a radiating swarm of feeder dykes, from a focal point northeast of the Superior craton (Buchan et al., 1998).
[FIGURES 4-5 OMITTED]
This Superior-Hearne reconstruction (Fig. 4d), prior to Paleoproterozoic break-up and dispersal of these cratonic fragments, is arguably one of the most specific, and testable, pre-2.0 Ga plate reconstructions proposed to date, although the Kaminak swarm paleomagnetic pole (Christie et al., 1975) and age need to be improved. An immediate and straightforward test would be to investigate the flow direction in Kaminak dykes, as the reconstruction of Figure 4 would predict a north-to-south magma flow in these dykes, away from a northerly plume source.
If correct, the new reconstruction would further suggest that Hearne crust and its large, juvenile Kaminak greenstone belt represent a continuum of the belt-like crustal growth observed in the southern Superior craton. Alternatively, if refined 2.45 Ga paleopoles for both the Kaminak and Matachewan swarms would prove to be statistically identical (i.e., the original interpretation of Christie et al., 1975), it would place both cratons in approximately their current relative position at ca. 2.45 Ca. This alternate result may require a radical re-interpretation of Trans-Hudson Orogen in terms of being the product of opening and closure of a narrow "intra-cratonic" ocean rather than the prevailing view of a wide Manikewan ocean (Stauffer, 1984; see also Symons, 1998; Halls and Hanes, 1999). These first-order questions about the fundamental architecture and evolution of Laurentia have presented themselves loud and clear since the 1975 paper of Christie et al., yet they remain unresolved. A related question is the identity and significance of the two or more age populations among the dykes of the composite Matachewan swarm.
PALEOGEOGRAPHY AT CA. 1885 MA: WHERE ARE THE CONJUGATE MARGINS OF THE SUPERIOR?
Although possibly distracting the discussion from the specific late Archean Superior-Hearne reconstruction proposed above, it is worth pointing out that very similar paleogeographic questions present themselves again when we consider the distribution of ca. 1883 Ma mafic-ultramafic magmatism around the margins of the Superior craton (e.g., Molson dykes, Fox River Sill). If this widespread magmatism is related to rifting and break-up of the Superior craton, perhaps related to arrival of a mantle plume underneath the western part of this craton, why do we find mafic sills of identical age (1883 [+ or -] 5 Ma; R. Parrish, unpublished date; mentioned in Van Kranendonk et al., 1993) in the Piling Group on the southern flank of the Rae craton? Are these identical ages mere coincidence, or a product of insufficient age accuracy? Or do they suggest proximity of the Piling Group basin, and by inference the Rae margin, to the Superior craton and the Molson plume centered on this latter craton?
In general, which margins were conjugate to the circum-Superior margin at ca. 1.88 Ga and where are they now? Given the presence of world-class mineral deposits along the western and northern Superior margin (e.g, Thompson, at 80 Mtonnes the largest komatiite-associated Ni-Cu-PGE deposit in the world), this question is of more than scientific interest. Again, all these questions are most clearly and critically addressed by a comprehensive survey of the record of ca. 1.88 Ga mafic magmatism around the Superior and other cratons and the information inherent therein: spatial distribution, sequence stratigraphic framework, high-resolution age data, and paleomagnetic information.
The time is right for a comprehensive, multidisciplinary, Canada-wide study of all mafic and intraplate magmatic events through time, their precise ages, their tectonic settings, and other inherent information, which not only addresses critical paleogeographic questions but has the potential to illuminate secular evolution of the mantle and the core.
Results from such a project would produce a quantum leap in the understanding of Precambrian terrains, younger break-up margins, and past plate configurations such as the Superior-Hearne reconstruction proposed herein, particularly if a Canadian project would help stimulate similar initiatives on other continents (e.g., Australia, southern Africa, Europe, Russia and China). More complete "bar codes" for a significant number of Precambrian crustal fragments would immediately lead to more robust reconstructions of past crustal aggregations, including that of Rodinia (e.g., Hoffman, 1991) and Nuna, as well as the first outlines of Archean supercratons. Equally important, with a complete time series of mafic magmatic events, we can investigate apparent periodicities (e.g., Prokoph et al., 2004), pulses and gaps, and their ultimate causes--i.e, the pulse of planet Earth. With volume estimates, we can address production rates over time. Is there a connection with climate and extinctions (e.g., Courtillot and Renne, 2003)? Is there a connection with large impacts (Abbott and Isley, 2002; Glikson, 2003; Becker et al., 2004)?
The overall price tag of the proposed project would be substantial but modest compared to that of LITHOPROBE. Funding on the order of 10 MS over 10 years would allow many of the goals to be achieved, including approximately 200 new high-precision ages. Of course, increased funding would allow more supporting geoscience and hence assure broader buy-in from a wider spectrum of disciplines.
Naturally, high-precision geochronology would be a lead discipline, as precise ages are critical to the ordering of events in their correct sequence, the unraveling of cause and effect, and the determination of rates. However, the following disciplines would all be natural and equal partners in this potential "big science" project: major and trace element geochemistry, isotope geochemistry, paleomagnetism, paleo-intensity studies and insights into core dynamics, structural geology and tectonics, regional mapping, sequence stratigraphy and basin analysis, petrology and xenolith studies, geophysics, geodynamic modeling, economic geology (Ni-Cu-PGEs, Cr, diamonds), Earth systems science and the study of extinction events.
A strategic link with the Integrated Oceanic Drilling Program (IODP; http://www.iodp.org) would extend the scope into the marine and oceanic realm. Finally, this project would aim to understand the evolution of planet Earth in its true natural context--the dynamic evolution of the Solar System. Hence it would seek close links with the planetary science community. Perhaps more so than for LITHOPROBE, international participation should be encouraged, to benefit from expertise not currently resident within Canada.
Major industry players around the world are spending considerable time and money on the understanding and exploration of mafic magmatic provinces, with the potential rewards of world-class mineral deposits such as those of Norilsk, Thompson, or a Merensky Reef. Even other deposit types, not traditionally related to mafic magmatic events (VMS, SEDEX), may owe their ultimate origin to mafic or ultramafic intrusions, i.e. as the heat engines that drove hydrothermal circulation (e.g., Pirajno, 2000). Key examples would be the 2716-2710 Ma, giant Kidd Creek Cu-Zn-Ag deposit, closely associated with ultramafic flows and intrusions (Bleeker, 1999; Hannington and Barrie, 1999), or the Sullivan Pb-Zn deposit in the Belt-Purcell basin, closely associated with the 1468 Ma Moyie sills (e.g., Anderson and Davis, 1995). Hence, there is no doubt that industry would be a supportive partner, allowing significant opportunities for matching funding.
Finally, the same tectonic questions that control mafic magmatic events are also relevant to the triggering and emplacement of kimberlite provinces. Indeed, as emphasized in the introduction, this project should include all intra-plate magmatic events as they reflect equally on the tectonic pulse of the Earth. This project will clearly look into the mantle, and in some ways even into the core. In this sense it is a logical follow-up on LITHOPROBE, which had a definite crustal and lithospheric perspective. Through its mantle perspective there is potential for synergies with the POLARIS project already underway in the geophysical community.
"Taking the Pulse of Planet Earth", by means of a comprehensive multidisciplinary study of the complete record of mafic magmatism, including a large dating program, is a "smart" and highly efficient approach to address a number of first-order questions in contemporary Earth science over the next 5 to 10 years.
A complete record of mafic magmatism (ages, periodicities, rates, volume estimates, geochemical fluxes, spatial distribution, structural trends, evolving isotope and trace element ratios, paleomagnetic information, associated ore deposits, etc.) will provide critical constraints on issues as diverse as paleogeographic reconstructions and the supercontinent cycle; the triggers of past climate extremes; complex Earth systems through time; crustal growth, core and mantle evolution; evolution of the core dynamo; causes of flood volcanism, and the potential relationships with extinction events; the hypothesized relationship between flood volcanism and large impact events; and, last but not least, the discovery of new ore deposits of strategic minerals.
The proposed project is certain to stimulate a quantum leap in the understanding of Precambrian terrains and their paleogeographic distribution through time. More importantly, a more complete understanding of mafic magmatism through time will provide new insights into the evolution of planet Earth. Finally, this project would promote, at a modest cost, new links between numerous earth science disciplines and facilitate further integration between earth and planetary sciences.
Ideas discussed herein were first presented at the 2002 GAC conference in Saskatoon and have since developed through discussions with many, in particular Ken Buchan, Richard Ernst, Don Davis, Sandra Kamo, Bill Davis, Cees van Staal, Simon Hanmer, Bob Barager, Tom Skulski, John Waldron, Paul Sylvester, Larry Heaman, Henry Halls, Keith Sircombe, John Ketchum, Kevin Cassidy, Dave Evans, Ian Dalziel, and many others. Many of these scientists share my vision, although individual approaches or emphases would naturally differ somewhat--this is to be expected. At a minimum, I hope this paper will stimulate discussion on the future of the Solid Earth Sciences in Canada. More so, I hope to convince fellow scientists that mafic magmatism is a first-order process and diagnostic of both long-term and short-term planetary evolution. As a tool, its enormous potential remains grossly underutilized. I thank Ken Buchan for kindly assisting with the plotting of Figure 4. The two field photos of Kaminak dykes were provided by Simon Hanmer. Bob Baragar suggested the flow direction test of the Superior-Hearne reconstruction. Geological Survey of Canada contribution number 2003305.
[FIGURE 4 OMITTED]
Abbott, D.H. and Isley, A.E., 2002, Extraterrestrial influences on mantle plume activity: Earth and Planetary Science Letters, v. 205 (1-2), p. 53-62.
Anderson, D.L., 1982, Hotspots, polar wander, Mesozoic convection and the geoid: Nature, 297 (5865), 391-393.
Anderson, D.L., 2002a, How many plates?: Geology, v. 30 (5), p. 411-414.
Anderson, D.L., 2002b, Plate tectonics as a far-from-equilibrium self-organized system, in Stein, S. and Freymueller, J.T., eds., Plate Boundary Zones: American Geophysical Union, Geodynamics Series, v. 30, p. 411-425.
Anderson, H.E. and Davis, D.W., 1995, U-Pb geochronology of the Moyie Sills, Purcell Supergroup, southeastern British Columbia; implications for the Mesoproterozoic geological history of the Purcell (Belt) Basin: Canadian Journal of Earth Sciences, v. 32 (8), p. 1180-1193.
Ayers, J., Amelin, Y., Corfu, F., Kamo, S., Ketchum, J., Kwok, and Trowell, N., 2002, Evolution of the southern Abitibi greenstone belt based on U-Pb geochronology: autochthonous volcanic construction followed by plutonism, regional deformation, and sedimentation: Precambrian Research, v. 115, p. 63-95.
Baragar, W.R.A., Ernst, R.E., Hulbert, L. and Peterson, T., 1996, Longitudinal petrochemical variation in the Mackenzie dyke swarm, northwestern Canadian Shield: Journal of Petrology, v. 37 (2), p. 317-359.
Bates, M.P. and Halls, H.C., 1990, Regional variation in paleomagnetic polarity of the Matachewan dykes swarm related to the Kapuskasing Structural Zone, Ontario: Canadian Journal of Earth Sciences, v. 27, p. 200-211.
Becker, L., Poreda, R.J., Basu, A.R., Pope, K.O., Harrison, T.M., Nicholson, T.M., and Iasky, R., 2004, Bedout: A possible end-Permian impact crater offshore of northwestern Australia: Science, 13 May 2004 (10.1126/science. 1093925).
Bleeker, W., 1999, Structure, stratigraphy, and primary setting of the Kidd Creek volcanogenic massive sulphide deposits: a semiquantitative reconstruction, in Hannington, M.D. and Barrie, C.T., eds., The giant Kidd Creek Volcanogenic Massive Sulfide Deposit, Western Abitibi Subprovince, Canada: Economic Geology Monograph 10, p. 71-121.
Bleeker, W., 2002, Archaean tectonics: a review, with illustrations from the Slave craton, in Fowler, C.M.R., Ebinger, C.J. and Hawkesworth, C.J., eds., The Early Earth: Physical, Chemical and Biological Development: Geological Society Special Publications, v. 199, p. 151-181.
Bleeker, W., 2003, The late Archean record: a puzzle in ca. 35 pieces: Lithos, v. 71 (2-4), 99-134.
Bleeker, W and Davis, W.J., 1999, The 1991-1996 NATMAP Slave Province Project: Introduction: Canadian Journal of Earth Sciences, v. 36 (7), p. 1033-1042.
Buchan, K.L. and Ernst, R.E., 1997, Restoration of the primary geometry of giant dyke swarms: constraints on paleocontinental reconstructions [abstract]: Geological Association of Canada, Annual Meeting, May 19-21, 1997, Abstract volume, p. A-20.
Buchan, K.L. and Ernst, R.E., 2004, Diabase dyke swarms and related units in Canada and adjacent regions: Geological Survey of Canada, Map 2022A, scale 1:5,000,000.
Buchan, K.L., Mortensen, J.K., Card, K.D. and Percival, J.A., 1998, Paleomagnetism and U-Pb geochronology of diabase dyke swarms of Minto block, Superior Province, Quebec, Canada: Canadian Journal of Earth Sciences, v. 35, p. 1054-1069.
Buchan, K.L., Mertanen, S., Park, R.G., Pesonen, L.J., Elming, S.A., Abrahamsen, N. and Bylund, G., 2000, Comparing the drift of Laurentia and Baltica in the Proterozoic; the importance of key palaeomagnetic poles: Tectonophysics, v. 319 (3), p. 167-198.
Burke, K., Dewey, J.F. and Kidd, W.S.F., 1976, Dominance of horizontal movements, arc and microcontinental collisions during the later permobile regime, in Windley, B.F., ed., The Early History of the Earth: John Wiley & Sons, New York, USA p. 113-129.
Calvert, A.J., Sawyer, E.W., Davis, W.J. and Ludden, J.N., 1995, Archaean subduction inferred from seismic images of a mantle suture in the Superior Province: Nature, v. 375 (6533), p. 670-674.
Campbell, I.H., 200 I, Identification of ancient mantle plumes, in Ernst, R.E. and Buchan, K.L., eds., Mantle plumes: Their Identification Through Time: Geological Society of America, Special Paper 352, p. 5-21.
Campbell, I.H., 2003, Constraints on continental growth models from Nb/U ratios in the 3.5 Ga Barberton and other Archaean basalt-komatiite suites: American Journal of Science, v. 303, p. 319-351.
Card, K.D., 1990, A review of the Superior Province of the Canadian Shield, a product of Archean accretion: Precambrian Research, v. 48 (1-2), p. 99-156.
Cheney, E.S., 1996, Sequence stratigraphy and plate tectonic significance of the Transvaal succession of Southern Africa and its equivalent in Western Australia: Precambrian Research, v. 79 (1-2), p. 3-24.
Christie, K.W., Davidson, A. and Fahrig, W.F., 1975, The paleomagnetism of Kaminak dikes; no evidence of significant Hudsonian plate motion: Canadian Journal of Earth Sciences, v. 12 (12), p. 2048-2064.
Clowes, R.M., Green, A.G., Yorath, C.J., Kanasewich, E.R., West, G.E and Garland, G.D., 1984, Lithoprobe; a national program for studying the third dimension of geology: Journal of the Canadian Society of Exploration Geophysicists, v. 20 (1), p. 23-39.
Condie, K.C., 1998, Episodic continental growth and supercontinents: a mantle avalanche connection?: Earth and Planetary Science Letters, v. 163 (1-4), p. 97-108.
Condie, K.C., 2001, Mantle plumes and their record in Earth history: Cambridge University Press, New York, USA, 306 p.
Cook, F.A., van der Velden, A.J., Hall, K.W. and Roberts, B.J., 1999, Frozen subduction in Canada's Northwest Territories; Lithoprobe deep lithospheric reflection profiling of the western Canadian Shield: Tectonics, v. 18 (1), p. 1-24.
Corfu, F., 1993, The evolution of the southern Abitibi greenstone belt in light of precise U-Pb geochronology: Economic Geology, v. 88 (6), p. 1323-1340.
Corfu, F. and Andrews, A.J., 1986, A U-Pb age for mineralized Nipissing Diabase, Gowganda, Ontario; Canadian Journal of Earth, v. 23 (1), p. 107-109.
Courtillot, V.E. and Renne, P.R., 2003, On the ages of flood basalt events: Comptes Rendus, Geoscience, v. 335 (1), p. 113-140.
Davies, G.F., 1992, On the emergence of plate tectonics: Geology, v. 20, p. 963-966.
Davies, G.F., 1995, Punctuated tectonic evolution of the Earth: Earth and Planetary Science Letters, v. 136 (3-4), p. 363-379.
Davies, G.F., 1999, Dynamic Earth: Cambridge University Press, Cambridge, United Kingdom, 458 p.
Denis, C., Schreiber, A.A., Varga, P., and Zavoti, J., 2002, Despinning of the earth rotation in the geological past and geomagnetic paleointensities: Journal of Geodynamics, v. 34, p. 667-685.
Ernst, R.E. and Baragar, W.R.A., 1992, Evidence from magnetic fabric for the flow pattern of magma in the Mackenzie giant radiating dyke swarm: Nature, v. 356, p. 511-513.
Ernst, R.E. and Buchan, K.L., 2004, Igneous rocks associations in Canada 3. Large igneous provinces (LIPs) in Canada and adjacent regions: 3 Ga to present: Geoscience Canada, v. 31, p. 103-126.
Ernst, R.E. and Buchan, K.L., 2001, Large mafic magmatic events through time and links to mantle-plume heads, in Ernst, R.E. and Buchan, K.L., eds., Mantle Plumes: Their Identification Through Time: Geological Society of America, Special Paper 352, p. 483-575.
Evans, D.A., 2000, Stratigraphic, geochronological, and paleomagnetic constraints upon the Neoproterozoic climatic paradox: American Journal of Science, v. 300, p. 347-433.
Evans, D.A.D., 2003, True polar wander and supercontinents: Tectonophysics, v. 362, p. 303-320.
Evans, D.A., Beukes, N.J., and Kirschvink, J.L., 1997, Low-latitude glaciation in the Paleoproterozoic era. Nature, v. 386 (6622), p. 262-266.
Glikson, A., 2003, Comment on "Extraterrestrial influences on mantle plume activity": Earth and Planetary Science Letters, v. 215, p. 425-427.
Greff-Lefftz, M. and Legros, H., 1999, Core rotational dynamics and geological events: Science, v. 286 (5445), p. 1707-1709.
Gurnis, M., 1988, Large-scale mantle convection and the aggregation and dispersal of supercontinents: Nature, v. 332 (6166), p. 695-699.
Halls, H.C. and Hanes, J.A., 1999, Paleomagnetism, anisotropy of magnetic susceptibility, and argon-argon geochronology of the Clearwater anorthosite, Saskatchewan, Canada: Tectonophysics, v. 312, p. 235-248.
Halls, H.C. and Zhang, B., 1998, Uplift structure of the southern Kapuskasing zone from 2.45 Ga dike swarm displacement: Geology, v. 26, p. 67-70.
Hamilton, W.B., 2003, An alternative Earth: GSA Today, 13 (11), 4-12.
Hannington, M.D. and Barrie, C.T., 1999, The giant Kidd Creek volcanogenic massive sulfide deposit, western Abitibi Subprovince, Canada. Economic Geology, Monograph 10, 672 p.
Hargraves, R.B., 1986, Faster spreading or greater ridge length in the Archean: Geology, v. 14, p. 750-752.
Harlan, S.S., Heaman, L., LeCheminant, A.N. and Premo, W.R., 2003, Gunbarrel mafic magmatic event: a key 780 Ma time marker for Rodinia plate reconstructions: Geology, v. 31, p. 1053-1056.
Heaman, L.M., 1994, 2.45 Ga global mafic magmatism: Earth's oldest superplume? [abstract]: Eighth International Conference on Geochronology, Cosmochronology, and Isotope Geology; Program with Abstracts; U.S. Geological Survey Circular 1107, p. 132.
Heaman, L.M., 1997, Global mafic magmatism at 2.45 Ga; remnants of an ancient large igneous province?: Geology, v. 25 (4), p. 299-302.
Hess, P.C. and Parmentier, E.M., 1995, A model for the thermal and chemical evolution of the Moon's interior; implications for the onset of mare volcanism: Earth and Planetary Science Letters, v. 134 (3-4), p. 501-514.
Hoffman, P.F., 1988, United plates of America, the birth of a craton: early Proterozoic assembly and growth of Laurentia: Annual Review of Earth and Planetary Sciences, v. 16, p. 543-603.
Hoffman, P.F., 1989, Precambrian geology and tectonic history of North America, in Bally, A.W. and Palmer, A.R., eds., The Geology of North America: An Overview: Geological Society of America, Boulder, Colorado, p. 447-512.
Hoffman, P.F., 1991, Did the breakout of Laurentia turn Gondwanaland inside-out?: Science, v. 252 (5011), p. 1409-1412.
Hoffman, P.F., 1997, Tectonic genealogy of North America, in van der Pluijm, B.A. and Marshak, S., eds., Earth Structure and Introduction to Structural Geology and Tectonics: McGraw Hill, New York, USA, p. 459-464.
Hoffman, P.F., Kaufman, A.J., Halverson, G.P. and Schrag, D.P., 1998, A Neoproterozoic snowball Earth: Science, v. 281, p. 1342-1346.
Hofmann, C., Feraud, G. and Courtillot, V., 2000, 40Ar/39Ar dating of mineral separates and whole rock from the Western Ghats lava pile: further constraints on duration and age of the Deccan traps: Earth and Planetary Science Letters, v. 180, p. 13-27.
Keen, C.E., 1981, Lithoprobe; geoscience studies on the third dimension; a coordinated national geoscience project for the 1980s: Geoscience Canada, v. 8 (3), p. 117-125.
Krogh, T.E., Corfu, F., Davis, D.W., Dunning, G.R., Heaman, L.M., Kamo, S.L., Machado, N., Greenhough, J.D., and Nakamura, E., 1987, Precise U-Pb isotopic ages of diabase dykes and mafic to ultramafic rocks using trace amounts of baddeleyite and zircon, in Halls, H.C. and Fahrig, W.F., eds., Mafic Dyke Swarms: Geological Association of Canada, Special Paper 34, p. 147-152.
Kamo, S.L., Czamanske, G.K., Amelin, Y., Fedorenko, V.A., Davis, D.W. and Trofimov, V.R., 2003, Rapid eruption of Siberian flood-volcanic rocks and evidence for coincidence with the Permian-Triassic boundary and mass extinction at 251 Ma: Earth and Planetary Science Letters, v. 214 (1-2), p. 75-91.
Labrosse, S., Poirier, J.P. and Le, M.J.L., 2001, The age of the inner core: Earth and Planetary Science Letters, v. 190 (3-4), p. 111-123.
Larson, R.L., 1991, The latest pulse of the Earth. Geology, v. 19, p. 547-550.
LeCheminant, A.N. and Heaman, L.M., 1989, Mackenzie igneous events, Canada: middle Proterozoic hotspot magmatism associated with ocean opening: Earth and Planetary Science Letters, v. 96 (1-2), p. 38-48.
Macouin, M., Valet, J.P., Besse, J., Buchan, K., Ernst, R., LeGoff, M. and Sharer, U., 2003, Low paleointensities recorded in 1 to 2.4 Ga Proterozoic dykes, Superior Province, Canada: Earth and Planetary Science Letters, v. 213, p. 79-95.
Mertanen, S., Halls, H.C., Vuollo, J.I., Personen, P.J., Stepanov, V.S., 1999, Paleomagnetism of 2.44 Ga mafic dykes in Russian Karelia, eastern Fennoscandian Shield--implications for continental reconstructions: Precambrian Research, v. 98, p. 197-221.
Montelli, R., Nolet, G., Dahlen, F.A., Masters, G., Engdahl, E.R. and Hung, S-H., 2004, Finite frequence tomography reveals a variety of plumes in the mantle: Science, v. 303, p. 338-342.
Morgan, W.J., 1971, Convection plumes in the lower mantle: Nature, v. 230 (5288), p. 42-43.
Ojakangas, R.W., 1988, Glaciation: an uncommon "mega-event" as a key to intracontinental and intercontinental correlation of early Proterozoic basin fill, North American and Baltic cratons, in Kleinspehn, K.L. and Paola, C., eds., New Perspectives in Basin Analysis: Springer-Verlag, New York, USA, p. 431-444.
Park, J.K., Buchan, K.L. and Harlan, S.S., 1995, A proposed giant radiating dyke swarm fragmented by the separation of Laurentia and Australia based on paleomagnetism of ca. 780 Ma mafic intrusions in western North America: Earth and Planetary Science Letters, v. 132, p. 129-139.
Percival, J.A, Bleeker, W., Cook, F.A., Rivers, T., Ross, G. and van Staal, C., 2004, Pan-LITHOPROBE workshop IV: Intraorogen correlations and comparative orogenic anatomy: Geoscience Canada, v. 31, p. 23-39.
Pirajno, F., 2000, Ore Deposits and Mantle Plumes: Kluwer Academic Publishers, Dordrecht, The Netherlands, 556 p.
Pollack, H.N., 1997, Thermal characteristics of the Archaean, in de Wit, M.J. and Ashwal, L.D. eds., Greenstone Belts: Oxford Monographs on Geology and Geophysics 35, p. 223-232.
Prokoph, A., Ernst, R.E. and Buchan, K.L., 2004, Time-series analysis of large igneous provinces: 3500 Ma to present: The Journal of Geology, v. 112, p. 1-22.
Richter, F.M., 1988, A major change in the thermal state of the Earth at the Archean-Proterozoic boundary: consequences for the nature and preservation of continental lithosphere, in Menzies, M.A. and Cox, K.G., eds., Oceanic and Continental Lithospheres: Similarities and Differences: Journal of Petrology, Special Lithosphere Issue, p. 39-52.
Ritsema, J. and Allen, R.M., 2003, The elusive mantle plume: Earth and Planetary Science Letters, v. 207 (1-4), p. 1-12.
Schuiling, R.D., 1973, Active role of continents in tectonic evolution--geothermal models, in de Jong, K. and Scholten, R., eds., Gravity and Tectonics: John Wiley and Sons, New York, USA, p. 35-47.
Sircombe, K.N., Bleeker, W., and Stern, R.A., 2001, Detrital zircon geochronology and grain-size analysis of ~2800 Ma Mesoarchean proto-cratonic cover succession, Slave Province, Canada: Earth and Planetary Science Letters, v. 189 (3-4), p. 207-220.
Stauffer, M.R., 1984, Manikewan: an early Proterozoic ocean in central Canada, its igneous history and orogenic closure: Precambrian Research, v. 25 (1-3), p. 257-281.
Stegman, D.R., Jellinek, A.M., Zatman, S.A., Baumgardner, J.R. and Richards, M.A., 2003, An early lunar core dynamo driven by thermomechanical mantle convection: Nature, v. 421 (6919), p. 143-146.
Stevenson, D.J., 2003, Styles of mantle convection and their influence on planetary evolution: Comptes Rendus Geoscience, v. 335, p. 99-111.
Sylvester, P.J., Campbell, I.H., and Bowyer, D.A., 1997, Niobium/uranium evidence for early formation of the continental crust: Science, v. 275, p. 521-523.
Symons, D.T.A., 1998, Precambrian plate tectonic models: shifting the paleomagnetic paradigm for orogens such as the Trans-Hudson in Canada: Physics and Chemistry of the Earth, v. 23 (7), p. 753-759.
Van Kranendonk, M.J., St-Onge, M.R. and Henderson, J.R., 1993, Paleoproterozoic tectonic assembly of Northeast Laurentia through multiple indentations: Precambrian Research, v. 63, p. 325-347.
Vlaar, N.J., 1986, Archean global dynamics: Geologie and Mijnbouw, v. 65, p. 91-101.
Wingate, M.T.D., Pisarevsky, S.A., and Evans, D.A.D., 2002, Rodinia connection between Australia and Laurentia: no SWEAT, no AUSWUS?: Terra Nova, v. 14 (2), p. 121-128.
Young, G.M., 1973, Tillites and aluminous quartzites as possible time marker for middle Precambrian (Aphebian) rocks of North America, in Young, G.M., ed., Huronian Stratigraphy and Sedimentation: Geological Association of Canada, Special Paper 12, p. 97-127.
Young, G.M., 1975, Geochronology of Archean and Proterozoic rocks in the southern District of Keewatin: Discussion: Canadian Journal of Earth Sciences, v. 12, p. 1250-1254.
Young, G.M., Long, D.G.F., Fedo, C.M., and Nesbitt, H.W., 2001, Paleoproterozoic Huronian basin: product of a Wilson cycle punctuated by glaciations and a meteorite impact: Sedimentary Geology, v. 141-142, p. 233-254.
Zegers, T.E. and van Keken, P.E., 2001, Middle Archean continent formation by crustal delamination: Geology, v. 29, p. 1083-1086.
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Accepted as revised 7 August 2004
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