Cratons: stress melting during the Shock Dynamics event
Cratons are considered to be the oldest parts of continents, but are they? This page will present detailed information from professional geologic journals, and then offer a Shock Dynamics perspective. While all the material is useful, that which is highlighted in red is most important for the new interpretation.In the geologic time scale, the oldest eon is called the Archean, with an assigned age of 2.5 billion years ago and older. The Proterozoic eon is the next younger on the time scale, with assigned age range of 2.5 billion to 542 million years ago. The Archean and Proterozoic eons together make up the Precambrian; all the rest of the geologic time scale is Phanerozoic. Most cratons are considered to have formed during the Archean. "Archean cratons are relatively flat, stable regions of the crust that have remained undeformed since the Precambrian, forming the ancient cores of the continents."23
Sometimes a shortened name is used:
Archon=Archean+craton; Proton=Proterozoic+craton. "Archons are areas
where the last major tectonothermal event to affect the upper crust was >2.5
billion years ago; Protons experienced their last ... event between 2.5 and 1.0
billion years ago; and Tectons are typically underlain by different types of
[sub-continental lithospheric mantle] SCLM... toward less depleted SCLM through time."15 SCLM
is the lowermost part of a plate below a continent. From Archean to
Proterozoic to Phanerozoic time, SCLM has become progressively less depleted in
terms of Al, Ca, Mg# and Fe/Al.9
However, this view has fundamental problems:
Studies of peridotites from Kaapvaal craton do not follow the expected density-with-depth curve: shallow ones are less dense, while deep (>120 km) high-temperature ones are denser than isopycnic predictions. Peridotite xenoliths from Slave and Tanzanian cratons show a steeper-than-predicted density increase with depth.21
Furthermore, the neutral buoyancy of cratons has been challenged. "After subtracting pure crustal isostasy from observed topography, we find that cratons are generally depressed by about 300 to 1500 meters."30 Northern Eurasia is strongly depressed; large parts of Eurasia, South America, and North America are depressed by about 300 meters. Western North America, southern Africa, western Europe, Greenland, and eastern Asia are not.30
Even if it were correct, the "isopycnic hypothesis provides no direct insight into craton origin."25
Chemical buoyancy cannot prevent recycling.27 "Numerical studies have clearly demonstrated that neutral buoyancy is not sufficient to stabilize cratonic keels from the shearing of mantle flow.23 Buoyancy alone is ineffective to deter entrainment. "The chemical layer of lithosphere needs to be significantly more viscous... than the underlying mantle to remain stable."36
"Melt depletion... leaves the mantle lithosphere depleted in radioactive heat producing elements and in water... low temperature and low water content of cratonic mantle lithosphere can lead it to have a viscosity as much as 3-4 orders of magnitude higher than warm, wet asthenospheric mantle."5 Yet "stabilizing the cratonic root requires it to be significantly more viscous than can be explained by dehydration or melt depletion alone."23
Research is challenging the neat definitions of cratons. "Generalizations of Archean cratons do not capture the variability between cratonic regions or the complexity within a single craton assemblage. For example, not every craton is underlain by high-velocity roots, and the deepest roots do not always occur under Archean cratons."23 "There is [as] yet no clear theory for why some cratonic roots appear to be deformed during rifting or compressional events while other cratonic roots appear to resist similar deformation events."23 "Other questions regarding cratons and mantle dynamics that remain unsolved are how cratons form, when cratonic roots formed, and why cratons appear to have formed early in Earth evolution and not now."21,23,26,36
"Cratonal lithosphere is significantly thicker than old oceanic lithosphere, yet much thinner than it would be if it had simply cooled from above by conduction since the Archean."36 While the thickness of thermal boundary layers of Archean cratons (>2.5 billion years old) is 200-300 km, the thickness predicted by conductive cooling is 400-500 km.26 "If the mantle cooled significantly, ~150 K, since the Archean... the vigor of convection should wane over time and the lithospheric thickness... should increase."36 Conductive cooling would also require subsidence of the surface to the point that the cratons should either be under water or should have overlying sedimentary layers more than ~5 km thick, neither of which is observed."22
There are 3 main ideas for
the formation of cratons:
The main problem with the oceanic accretion hypothesis is that oceanic lithosphere gets denser as it cools, and is subductable after only 20 million years.25
If chemical boundary layers form beneath continents from oceanic lithosphere or arcs, and "if these lithospheric segments are initially dry, a paradox arises because they should be strong and not easily deformed. If they are wet or rehydrated to make them weak enough to deform and make cratons, another paradox arises because a chemically buoyant boundary layer, without being intrinsically stronger, would eventually thin out gravitationally."26
Also, "there has been much debate in recent years on the existence, configuration and evolution of the supercontinent Rodinia."24 Paleomagnetic data do not support the idea. For example, one study concluded that "African, southern Indian, and South American cratons were not part of the Rodinia supercontinent."24
2) Another common model involves stacking subducted slabs of oceanic or arc-related mantle under continents. This fails because modern examples are not compositionally like Archean SCLM, and there is no evidence that Phanerozoic SCLM is made that way.16 This model requires the SCLM to be deformable at the time of formation, and soon afterward become strong enough to resist shearing.23 It is also not clear why stacked subducted crust "would lead to roots between 200-300 km deep and no deeper, or why there appears to be a unique period in Earth history when cratonic roots formed."23 "The geochemical evidence is consistent with the hypothesis that the roots are the residue of partial melting, which is difficult to reconcile with the stacked subducted slab hypothesis."23
3) The thick, depleted chemical boundary layer
beneath cratons implies formation by melting of upwelling mantle much hotter
than that found today.26
The entire craton could be formed in one
large heating event, such as a plume-melt. "A thick, strong, and chemically
buoyant mantle keel can be generated by one seemingly simple and elegant
"Recent models of crustal evolution are based on the belief that the thickness of the continental crust is proportional to its age, with ancient crust being the thickest." One hypothesis for crustal growth is "that the crust is thickened by repeated episodes of basaltic underplating." "A worldwide review of seismic structure contradicts this belief and falsifies these models, at least for the Archean." "Proterozoic crust has a thickness of 40-50 km and a substantial high-velocity (>7 km/s) layer at its base, while Archean crust is only 27-40 km thick... and lacks the basal high-velocity layer."10
"Accumulating evidence suggests that in many areas, later reworking of the deep crust is more widespread than previously recognized."44 "A comparison of average Proterozoic crustal structure with highly evolved Phanerozoic crust that has undergone the full range of plate tectonic processes (from island arc to continental-arc volcanism) reveals a remarkable similarity."10
South African studies "indicate that the Archean crust was composed of granite (~70%) and a mafic component (up to 30%) which probably was komatiite." Compared to Proterozoic crust, "Archean rocks are depleted in Si and K and enriched in Na, Ca, and Mg. There is also a marked change in the Eu/Eu ratio." "Archean crust develops above mantle lithosphere (garnet lherzolite) that is depleted in FeO and intrinsically bouyant." "Proterozoic crust develops above fertile (normal FeO) mantle lithosphere (spinel herzolite)."10
Crust formation is getting granite from basalt.2 Primitive mantle differentiates to form continental crust, which is Al and Si rich, and so less dense, plus depleted mantle, which is Mg and Fe rich and denser.1 After mafic magmas differentiate, the crust and mantle segregate. Partial melting of the crust then refines the material, and further segregates the crust. This results in mature continental crust of intermediate to felsic material.3 Low-temperature liquid is extracted at each step, leaving a larger volume of solid residue.2
Upper crustal sediments are the source of
S-type granites; M-type granites are from mantle-derived basalts. But though
I-type granites are abundant, widely distributed, and diverse, origin is
uncertain. They make up a large portion of the continental crust.12
"Continental crust is thought to be formed as a result of arc
magmatism." "A fundamental problem is that the majority of magmas erupted on
Earth are basaltic and yet the continents do not have a basaltic bulk
composition." Those that are silicic (dacitic to andesitic) lavas are evolved,
with lower Mg#s than continental crust.20
Forming continental crust makes much residue. Crust is made by 20% partial melt. Residue from crust formation is about 5 times the volume of continental crust. So a 40 km thick crust leaves a 200 km thick restite. Restite is Fe-rich pyroxene/amphibole plus garnet, and has high density.2 "To generate bulk crust with a high Mg# andesite composition, some process is required to remove the cumulates and residues formed during generation of the silicic, "granitic" end-member."20
"Komatiites are not found in all cratons, and where they occur, basalts are a more common lithology."19 If komatiites form from ~25-50% melting of pyrolitic mantle, and the residues are in ~100km-thick (or more) cratonic roots, then ~35-100 km of complementary Archean crust should have been produced. "Where is all the komatiite?" "We have a paradox of mass balance requirement and geological observation." "The easiest way to resolve this paradox is by elimination of komatiite from the geological record."19 That is, to submerge it into the mantle.
Crustal foundering builds continental crust. In continental crust we find Si, Al, incompatible enriched gabbro, and low density. Dense lower crustal ultramafic cumulates, carrying contaminants from the lower crust, find their way to the mantle.3
Intracrustal melting produces granitoid magmas and dense mafic restites that return to the mantle. The foundering of mafic restites from granitoid magmas is likely a major process.3
High temperature is required for dense lower crustal mafic-ultramafic cumulates to sink into the mantle. Results of experiments show that "an initial strain rate can significantly reduce the Moho temperature required for an instability to develop." "Instability times decrease because the initial effective viscosity is lower."20
Foundering in the crust is an alternative to proposals calling for the ascent of contamination up to the lithospheric mantle.3
Moho and sub-Moho boundary layer
"There is still no scientific consensus about its origin, petrologic significance, and structural context."11 One hypothesis "posits mechanical decoupling of the crust and uppermost mantle as a result of structural detachment at (or near) the Moho." "Under exceptionally hot conditions, lower crustal channel-flow behaviour can result in nearly complete decoupling of the... crust from the upper mantle."11 There could even be "a differential horizontal movement or decoupling of crust and upper mantle at the level of the Moho."13
"For a large majority of cases, the Moho transition is sharp (across only a few kilometers)." If the transition is due to the gabbro-to-eclogite transition, it should be gradual. It is "more likely a break between mafic crustal compositions and underlying ultramafic mantle."20 "We can then ask, if the Moho depth is not simply the result of a pressure sensitive phase transition from gabbro to eclogite, why does the thickness of the crust vary only between 25 and 40 km worldwide?"20
High-resolution seismic observations show a sub-Moho boundary layer (SMBL) at the top of the lithospheric mantle. SMBL thickness is 60-100 km. "High-frequency seismic phases traverse geological provinces of various age, heat flow, crustal thickness, and tectonic regimes. Their propagation appears to be independent of age, temperature, pressure, and stress."14 The SMBL acts as a waveguide. It is connected to the Mohorovicic discontinuity, a global phenomenon.14 "Differential horizontal deformation between crust and mantle near the Moho is the most likely explanation for the creation of seismic velocity fluctuations within the SMBL."14
Several Precambrian massive outpourings or intrusions of continental flood basalts occurred in southern Africa. Ventersdorp covers much of Kaapvaal. Bushveld is the world's largest layered igneous intrusion, and was injected rapidly. The 500-km-long Great Dyke is likely the remnant of a large igneous province covering 60,000 km2. Eruptive basalts of the Soutpanberg Group are over 3 km thick, and are probably the eroded remnants of a Proterozoic Large Igneous Province.34
The rifting characteristics found at these places show that they are related to "collisional orogens." They were caused by "stress perturbations" in the lithosphere, "not melting due to deep-seated, high-temperature mantle plumes." Nor were they likely due to lithospheric thinning by thinning or delamination.34 "It is very difficult to find any evidence for delamination from the xenolith record of any cratonic environment worldwide." The only clear evidence is for the North China Craton.34
"We thus conclude that the presently accepted mechanisms for flood basalts - mantle plumes and lithospheric thinning - are incapable of accounting for the southern African Precambrian magmatic events."34 Cratonic flood basalts erupted quickly, perhaps from "abrupt stress change in the lithosphere", leading to "propagation of lithospheric dikes". This implies large reservoirs of magma.34
Low-Velocity Zones (low seismic velocity, indicating rock that is less-dense, perhaps hot)
"Low-velocity zones beneath stable [i.e. cratonic] continental regions tend to be either extremely weak or entirely absent. As a result the base of the continental lithosphere is not well defined by seismological data. With increasing depth the high seismic velocities of the stable lithosphere gradually" merge into mantle velocities.5
"A low-velocity zone at depths below ~100 km is a global feature of the continental mantle."37 "This zone may be caused by a partial melting, globally initiated at equal depth in the continental mantle. Solid state is again attained at the Lehmann discontinuity [220 km] in cold, stable areas, whereas the zone extends to near the 400-kilometer discontinuity in hot, tectonically active areas."37
"Low-velocity zones beneath cratonic lithosphere are not uncommon." They appear below the Kaapvaal craton, Canadian Shield, and Australian shield. "The low-velocity anomalies below these lithospheric roots, however, do not reach shear wave velocities below 4.4 km/s. By comparison, the dramatic excursion to β=4.20+0.05 km/s at 200-250 km below the surface of the Tanzanian craton is unique. These velocities are lower than velocities found at comparable depths beneath the East Pacific Rise spreading center and require unusually high temperatures and perhaps partial melting."42 Also, "the volume of igneous basalt in the eastern branch of the East African Rift system [is] estimated at greater than 900,000 km3."42
There is "evidence of a super-deep low-velocity layer in [both] the upper mantle of southern Africa and the Tunguska basin of the Siberian platform." "Three regions with evidence of this layer are remarkable for large-scale eruptions of continental flood basalts:" the Karoo flood basalt province in southern Africa, the Siberian traps in the Tunguska Basin (>2.5 million km2), and extensive flood basalts in Ethiopia and on the Arabian plate (30-20 million years ago (Ma)).40 "A correlation between the locations of the low-velocity layer and of the continental flood basalts up to 250 Ma old suggests that the layer migrates with the plates. While this is very surprising with respect to conventional wisdom, a similar conclusion was derived [for]... the Parana flood basalts 137-127 Ma old in South America."40 "A low velocity anomaly in the southern part of the Parana basin suggests that the Parana LIP might have been related to the upwelling of several plumes." However, why traces of them are still there "remains unclear".18
"Dehydration can lead to several order of magnitude increase in viscosity, relative to mantle at the same pressure and tempereature conditions." Cratonic keels could be the depleted residue from a large melting event.23 The entire craton could be formed in one large heating event, such as a plume-melt. "A thick, strong, and chemically buoyant mantle keel can be generated by one seemingly simple and elegant process."25
"In contrast to the varied and scattered major element systematics of cratonic peridotites in general, their heavy rare-earth element concentrations vary in a much more systematic and more easily interpreted manner." "Mildly incompatible trace elements offer much more promise in terms of providing geodynamic information about the original Archean melting regime. The very low, systematically varying heavy rare-earth element abundances in the North Atlantic Craton whole-rock peridotites and in peridotites from all other cratons where high-quality data are available provide ubiquitous evidence for a shallow melting regime in the absence of, or to the exhaustion of garnet. This finding explicitly excludes large extents of deep... melting." "This and all other craton locations investigated so far contain peridotites that experienced melting in shallow environments."43
The data show that "peridotites whose history is dominated by shallow melt extraction [are] dispersed throughout the entire depth of the deep cratonic root." "Our conclusions... for the North Atlantic Cratonic lithosphere agree with those of other workers who have concentrated on the Kaapvaal craton." "We can extend these conclusions to other cratons where reasonably large numbers of major and trace element data are available such as the Siberian, Slave, Rae province, Wyoming and Tanzanian cratons."43
"Heavy rare-earth element concentrations of North Atlantic Craton whole-rock peridotites are consistently lower than those of primitive mantle. In order to reproduce these low heavy rare-earth element concentrations, modelling demands that polybaric fractional partial melting took place in the absence or in the presence of only small amounts of garnet (<3 GPa), similar to shallow melting regimes currently operating in the Earth's mantle." "The abundant heavy rare-earth element-enriched peridotites predicted for plume-melting are not observed in the North Atlantic Craton or any other craton." The North Atlantic Cratonic sub-continental lithospheric mantle and all other cratonic continental mantle roots studied here are the product of extreme melt extraction at relatively shallow depths (~90 km or less)."43
High degrees of melting can be generated by adiabatically decompressing mantle to shallow pressures without extremely high temperatures. Large amounts of complementary komatiitic magmas are not required.25
"Most geochemical characteristics of lithospheric mantle peridotites are most easily reconciled with a relatively low-pressure melting origin, albeit in the case of cratonic peridotites one taken to very high degrees of melting."5 Interestingly, Al2O3-MgO systematics of cratonic peridotites "are largely indistinguishable" from that of Phanerozoic spinel peridotites, and are easily explained by melting between 1-4 Gpa. Low Al2O3 contents of Archean cratonic peridotites means they may have melted at lower pressures than at their current depth.25
"V, Sc, Y and the heavy rare-earth elements in peridotites almost always preserve original melting systematics, while highly incompatible elements do not." Cratonic mantle peridotites from Tanzania, South Africa, and Siberia have Sc systematics nearly indistinguishable from Phanerozoic spinel peridotites. Thus there is no indication from Sc that cratonic peridotites melted at 7 Gpa. This study of Sc systematics showed that cratonic peridotites could not have formed by high-pressure melting.25 V-MgO systematics give the same conclusion.25
Major and moderately incompatible trace element systematics of cratonic peridotites are very similar to that of Phanerozoic spinel peridotites: 30-50% melt residues at pressures <~4GPa. "It thus seems likely that the majority of cratonic peridotites melted on average anywhere between 1 and 4 Gpa" (in the spinel stability field).25 Most cratonic peridotites probably melted at low pressures and were transported deeper (90-220 km) to about 7 GPa. Melting temperatures would likely have been 1400-1650°C, near that estimated for modern plumes (1450-1650°C). On the other hand, some cratonic peridotites have low FeO, which usually signifies very high melting pressure.25
A study of the Vredefort dome indicated "that as much as 40% of the crust, chiefly the lower crust, was re-melted" "during a craton-wide thermal event at 3.11 Ga." "The very large degree of crustal melting proposed... is sufficient to form something resembling an 'ocean' of melt in the cratonic lower crust near the crust-mantle boundary. The magmatic differentiation and layering accompanying the crystallization of that lower crustal melt 'ocean' is one possible means for producing... a flat and sharp Moho."32
Petrological studies show cratonic lithospheric depletion decreases with depth. The compositional density anomaly is highest just below the Moho.21
"Mid-crustal reflections resembling "shingles" are interpreted as imbricates and/or tectonically underplated material. These reflection patterns occur in Neoarchean cratons worldwide and are remarkably similar to reflection patterns beneath Proterozoic and Phanerozoic orogens. Thus, Neoarchean cratons appear to be products of rigid plate behavior in which horizontal forces were dominant."38
The assumptions of plate tectonics are often applied to Archean or Paleoproterozoic orogens. However, many of these ancient deformation belts differ by being mainly flat with steep (vertical) transpressive zones. They may result from hot, weak lithosphere spreading horizontally rather than thickening during convergence towards more resistant lithosphere.4
Cratonic mantle lithosphere must be highly viscous "so that the depleted mantle does not flow horizontally across terrain boundaries to spread out widely beneath the crust."5
A study of a section of the Western Superior craton shows that in much of the section "significant mass anomalies occur only in the upper crust and at the crust-mantle boundary."31 The absence of mass anomalies at deep crustal levels may be related to mass redistribution processes resulting from "a major episode of intracrustal softening and crustal differentiation", "indicated by voluminous late orogenic granitic magmatism" around 2.71-2.66 Ga.31 In the Slave craton, an "intense craton-wide 'granite bloom' argues for a widespread thermal disturbance, the exact cause of which remains speculative."7
An alternative explanation for
In this model, the weight, movement, and melting of the overlying crust determines the nature and features of the lithosphere below. At large (continental) scale, gravity is the dominant force, not material cohesion. Oceanic crust 4-7 km thick has an effect down to 60-80 km; continental crust 35 km thick has a lithospheric effect down to 150 km. Cratonic melt products reach down to 200-250 km. The isostatic (buoyancy displacement) depth of a continental mass below sea level is an indicator that this mass of crust is compacting the mantle below it. When the overlying weight is removed, the lithosphere or lithospheric effect disappears or is reduced to whatever remains above it. So when continents move, their continental lithosphere only appears to go with them. Thus characteristics of lithosphere below the crust are a consequence of the crust above it: oceanic crust gives shallow lithosphere; a spreading center produces adiabatic partial melting at depth; regular continental crust produces typical sub-continental lithosphere; the leading edges of moving continents produce thick lithosphere, mountains, and benioff ("subduction") zones; shock waves in the crust freeze at the threshold energy level, forming "subduction zones" in oceanic lithosphere.
By far, most crustal activity occurred during the Shock Dynamics event. Actions were initiated at the surface, not in the mantle. For example, the Hawaiian chain eruptions were due to tension fracturing of oceanic crust. The evidence from cratons points to widespread melting near the surface rather than from below by a plume. Plate tectonics theory has no mechanism to make that happen. However, in the Shock Dynamics model, lateral stress (pivoting or compression followed by extension) melted continental crust, and the residue foundered, producing a mantle root.
A study of thermal diffusivity
of rock from the middle to lower crust shows that this region is
a much better thermal insulator than previously thought. "The
deformation of the crust in response to tectonic forces is commonly
accompanied by strain localization: that is, by the formation of
narrow, ductile shear zones. During deformation at high stress
levels, mechanical energy is transformed into heat (a process called
strain heating), which is dissipated from the shear zone by conduction.
Reduced thermal conductivity at high temperature would limit
heat dissipation, resulting in much hotter shear zones than commonly
assumed." "This may even lead to melting inside
the shear zone, causing further localization of the deformation
within the shear zone." "Enhanced strain heating
could also explain the formation of larger than expected volumes
of granitic magmas produced by partial melting of deep crustal rocks."--
Braun, Jean. 19 March 2009. Hot blanket in Earth's deep crust. Nature,
Vol. 458, pp. 292-293.
Thus all cratons would be a consequence of the Shock Dynamics event. Although stress on the protocontinent led to craton and proton formation, melting and founder of dense residue must have occurred after the motion of the continents (which lasted only about 26 hours) had ceased. The correlation of apparent isotopic age with the degree of melting (Proton=high, Archon=highest) suggests that widespread, intense melting during the Shock Dynamics event accelerated apparent aging, perhaps through transmutation by neutron capture (explained below).
Artificial radioisotope ages
* * * * * * * * * * *
1. Amelin, Yuri. 23 December 2005. A Tale of Early Earth Told in Zircons. Science, Vol. 310, pp. 1914-1915.
2. Arndt, Nicholas T., Eric Lewin, Francis Albarede. 2002. Strange partners: formation and survival of continental crust and lithospheric mantle. in The Early Earth: Physical, Chemical and Biological Development, editors C.M.R. Fowler, C.J. Ebinger, C.J. Hawkesworth, Geological Society, London, Special Publications, 199, pp. 91-103.
3. Arndt, Nicholas T., Steven L. Goldstein. 1989. An open boundary between lower continental crust and mantle: its role in crust formation and crustal recycling. Tectonophysics, Vol. 161, pp. 201-212.
4. Cagnard, Florence, Nicolas Durrieu, Denis Gapais, Jean-Pierre Brun, Carl Ehlers. 2006. Crustal thickening and lateral flow during compression of hot lithospheres, with particular reference to Precambrian times. Terra Nova, Vol. 18, No. 1, pp. 72-78.
5. Carlson, Richard W., D. Graham Pearson, David E. James. 2005. Physical, chemical, and chronological characteristics of continental mantle. Reviews of Geophysics, Vol. 43, RG1001, pp. 1-24.
6. Cook, Melvin A. 1966. Prehistory and Earth Models. Max Parrish and Co. Ltd., London.
7. Davis, W.J., A.G. Jones, W. Bleeker, H. Grutter. 2003. Lithosphere development in the Slave craton: a linked crustal and mantle perspective. Lithos, Vol. 71, pp. 575-589.
8. Dixon, Jacqueline E., T.H. Dixon, D.R. Bell, R. Malservisi. 2004. Lateral variation in upper mantle viscosity: role of water. Earth and Planetary Science Letters, Vol. 222, pp. 451-467.
9. Djomani, Yvette H. Poudjom, Suzanne Y. O'Reilly, W.L. Griffin, P. Morgan. 2001. The density structure of subcontinental lithosphere through time. Earth and Planetary Science Letters, Vol. 184, pp. 605-621.
10. Durrheim, Raymond J., Walter D. Mooney. August 10, 1994. Journal of Geophysical Research, Vol. 99, No. B8, pp. 15,359-15,374.
11. Eaton, David W. 2005. Multi-genetic origin of the continental Moho: insights from Lithoprobe. Terra Nova, Vol. 18, No. 1, pp. 34-43.
12. Eiler, John M. 16 February 2007. On the Origins of Granites. Science, Vol. 315, pp. 951-952.
13. Enderle, U., M. Tittgemeyer, M. Itzin, C. Prodehl, K. Fuchs. 1997. Scales of structure in the lithosphere -- images of processes. Tectonophysics, Vol. 275, pp. 165-198.
14. Fuchs, Karl, Marc Tittgemeyer, Trond Ryberg, Friedemann Wenzel, Walter Mooney. 2002. International Geology Review, Vol. 44, pp. 671-685.
15. Griffin, W.L., Suzanne Y. O'Reilly, B.J. Doyle, N.J. Pearson, H. Coopersmith, K. Kivi, V. Malkovets, N. Pokhilenko. 2004. Lithosphere mapping beneath the North American plate. Lithos, Vol. 77, pp. 873-922.
16. Griffin, W.L., S. Y. O'Reilly, N. Abe, S. Aulbach, R.M. Davies, N.J. Pearson, B.J. Doyle, K. Kivi. 2003. The origin and evolution of Archean lithospheric mantle. Precambrian Research, Vol. 127, pp. 19-41.
17. Handy, M.R., J.-P. Brun. 2004. Seismicity, structure and strength of the continental lithosphere. Earth and Planetary Science Letters, Vol. 223, pp. 427-441.
18. Heintz, Maggy, Eric Debayle, Alain Vauchez. 2005. Upper mantle structure of the South American continent and neighboring oceans from surface wave tomography. Tectonophysics, Vol. 406, pp. 115-139.
19. Herzberg, Claude. 1999. Phase equilibrium constraints on the formation of cratonic mantle. in Mantle Petrology: Field Observations and High Pressure Experimentation: A Tribute to Francis R. (Joe) Boyd, editors Yingwei Fei, Constance M. Bertka, Bjorn O. Mysen, The Geochemical Society, Special Publication No. 6, pp. 241-257.
20. Jull, M., P.B. Kelemen. April 10, 2001. On the conditions for lower crustal convective instability. Journal of Geophysical Research, Vol. 106, No. B4, pp. 6423-6446.
21. Kaban, Mikhail K., Peter Schwintzer, Irina M. Artemieva, Walter D. Mooney. 2003. Density of the continental roots: compositional and thermal contributions. Earth and Planetary Science Letters, Vol. 209, pp. 53-69.
22. Kelly, Robyn K., Peter B. Kelemen, Matthew Jull. 18 February 2003. Buoyancy of the continental upper mantle. Geochemistry Geophysics Geosystems, Vol. 4, No. 2, pp. 1-24.
23. King, Scott D. 2005. Archean cratons and mantle dynamics. Earth and Planetary Science Letters, Vol. 234, pp. 1-14.
24. Kroner, Alfred, Umberto Cordani. 2003. African, southern Indian and South American cratons were not part of the Rodinia supercontinent: evidence from field relationships and geochronology. Tectonophysics, Vol. 375, pp. 325-352.
25. Lee, Cin-Ty Aeolus. 2006. Geochemical/Petrologic Constraints on the Origin of Cratonic Mantle. in Archean Geodynamics and Environments, Geophysical Monograph Series 164, editors Keith Benn, Jean-Claude Mareschal, Kent C. Condie, pp. 89-114.
26. Lee, Cin-Ty Aeolus, Adrian Lenardic, Catherine M. Cooper, Fenglin Niu, Alan Levander. 2005. The role of chemical boundary layers in regulating the thickness of continental and oceanic thermal boundary layers. Earth and Planetary Science Letters, Vol. 230, pp. 379-395.
27. Lenardic, A., L.-N. Moresi, H. Muhlhaus. 2003. Longevity and stability of cratonic lithosphere: Insights from numerical simulations of coupled mantle convection and continental tectonics. Journal of Geophysical Research, Vol. 108, No. B6, pp. ETG 9 - 1-15.
28. Meert Joseph G., Trond H. Torsvik. 2003. The making and unmaking of a supercontinent: Rodinia revisited. Tectonophysics, Vol. 375, pp. 261-288.
29. Milton, Richard. 1997. Shattering the Myths of Darwinism. Park Street Press, Rochester, Vermont.
30. Mooney, Walter D., John E. Vidale. 2003. Thermal and chemical variations in subcrustal cratonic lithosphere: evidence from crustal isostasy. Lithos, Vol. 71, pp. 185-193.
31. Nitescu, B., A.R. Cruden, R.C. Bailey. 2006. Crustal structure and implications for the tectonic evolution of the Archean Western Superior craton from forward and inverse gravity modeling. Tectonics, Vol. 25, TC1009, pp. 1-16.
32 Niu, Fenglin, David E. James. 2002. Fine structure of the lowermost crust beneath the Kaapvaal craton and its implications for crustal formation and evolution. Earth and Planetary Science Letters, Vol. 200, pp. 121-130.
33. Kochemasov, G.G. 1983. The Congo craton: an old impact structure? Lunar and Planetary Institute, NASA Astrophysics Data System.
34. Silver, Paul G., Mark D. Behn, Katherine Kelley, Mark Schmitz, Brian Savage. 2006. Understanding cratonic flood basalts. Earth and Planetary Science Letters, Vol. 245, pp. 190-201.
35. Sleep, Norman H. 2005. Evolution of the Continental Lithosphere. Annual Review of Earth and Planetary Science, Vol. 33, pp. 369-393.
36. Sleep, Norman H. 2003. Survival of Archean cratonal lithosphere. Journal of Geophysical Research, Vol. 108, No. B6, pp. ETG 8 - 1-29.
37. Thybo, H., E. Perchuc. 14 March 1997. The Seismic 8° Discontinuity and Partial Melting in Continental Mantle. Science, Vol. 275, pp. 1626-1629.
38. Van der Velden, Arie J., Frederick A. Cook, Barry J. Drummond, Bruce R. Goleby. 2006. Reflections of the neoarchean: A global perspective. Archean geodynamics and environments, Vol. 164, pp. 255-265.
39. Vigneresse, Jean Louis. 2004. A new paradigm for granite generation. Transactions of the Royal Society of Edinburgh: Earth Sciences, Vol. 95, pp. 11-22.
40. Vinnik, Lev, Veronique Farra. 2002. Subcratonic low-velocity layer and flood basalts. Geophysical Research Letters, Vol. 29, No. 4, pp. 8 - 1-4.
41. Watson, E.B., T.M. Harrison. 6 May 2005. Zircon Thermometer Reveals Minimum Melting Conditions on Earliest Earth. Science, Vol. 308, pp. 841-844.
42. Weeraratne, Dayanthie S., Donald W. Forsyth, Karen M. Fischer, Andrew A. Nyblade. 2003. Evidence for an upper mantle plume beneath the Tanzanian craton from Rayleigh wave tomography. Journal of Geophysical Research, Vol. 108, No. B9, pp. ESE 10 - 1-17.
43. Wittig, N., D.G. Pearson, M. Webb, C.J. Ottley, G.J. Irvine, M. Kopylova, S.M. Jensen, G.M. Nowell. 2008. Origin of cratonic lithospheric mantle roots: A geochemical study of peridotites from the North Atlantic Craton, West Greenland. Earth and Planetary Science Letters, Vol. 274, pp. 24-33.
44. Zheng, Jianping, W.L. Griffin, Suzanne Y. O'Reilly, Ming Zhang, Norman Pearson, Yuanming Pan. June 2006. Widespread Archean basement beneath the Yangtze craton. Geology, Vol. 34, No. 6, pp. 417-420.