Earlier - forming continental crust
Most of the Pacific seafloor was not affected by the Shock Dynamics event, and there are features on it that point to an extraordinary past. Using the assumptions and evidence upon which the Shock Dynamics theory is based plus current ideas about the formation of the Moon, it is possible to piece together a series of major events on Earth prior to the Shock Dynamics event.
The Earth began with a uniform basaltic crust, typical of oceanic crust.
A moderately large impact struck the Earth near where Japan is today.
The melting and mixing of basaltic crust and upper mantle differentiated into continental crust in the impact area, which I will call Antar.
The collision of a Mars-size planetesimal ejected material that coalesced to form the Moon, according to current mainstream thinking. In this reconstruction, the impact also struck the northern portion of Antar, splitting it and sending the pieces skimming across the basaltic crust. The pulling away of the largest piece, which became East Antarctica, left an extension that became Alaska and the Chukchi Peninsula following the Shock Dynamics impact (see Alaska view). The collision likely gave Earth its 23.45 degree tilt.
The largest piece came to rest near the South Pole (white dot). As with the first impact, the melting and mixing of basaltic crust and upper mantle differentiated into continental crust in the large area hit by the planetesimal, becoming the protocontinent.
Next, the Shock Dynamics meteorite struck Earth. South America rushed away from Africa. On its southern end was an extended arm that had wrapped around what is today South Africa, reaching all the way to Madagascar.
The extended arm collided with the center of the largest piece of Antar, what is today East Antarctica, turning and pushing it in the direction of South America's movement. The arm pulled off of South America, and the two ends dragged to make the Scotia/Sandwich Trench/Ridges (purple). Initial motion of East Antarctica opened the oceanic crust under its former leading edge. The outpouring of flood basalts became the Kerguelen Plateau.
The high cliffs that run along the left edge of East Antarctica in the image below are an unusual mountain range. These Transantarctic Mountains were not formed by lateral compression but by curling up.13 It suggests that East Antarctica was formerly part of a larger whole that was clipped along the line of the mountains, as proposed in this scenario. Also, the big difference in thickness between West (25 km) and East (40 km) Antarctica12, clearly apparent in this image, suggests that they did not originate together but were brought together.
At the center of East Antarctica are the Gamburtsev Subglacial Mountains (GSM). In a study using seismic tomography, "no evidence is found for a significant thermal anomaly beneath the GSM, precluding the existence of a Cenozoic hotspot". The data "indicate little change in lithospheric thickness beneath the GSM and surrounding regions." In the opinion of the researchers, "uplift is attributed to one or more Proterozoic compressional orogenic events". "For example, the Petermann Range in central Australia represents the remnants of a... compressional intraplate orogeny".4 In other words, a strong compressive force in ancient times raised the mountains in central Antarctica, similar to what happened to Australia. Presentation 6 shows how the Shock Dynamics meteorite impact formed the Petermann Range and the Bight in Australia. In the same way, the impact of the planetesimal on Antar formed the Gamburtsev Subglacial Mountains.
The reasoning behind it
In the Shock Dynamics theory, features on the face of the Earth are primarily made by action on the surface. That applies to the spreading ridges that encompass the Earth like the seam of a baseball. When continental crust divides and moves over oceanic crust, the top of the oceanic crust melts and follows the moving continental crust in the manner demonstrated with parafin wax experiments. The most well-known of these was published in 1972, and is described below.
"A tray of melted paraffin was cooled by a variable-speed fan until a film of solidified wax formed between one end of the pan and a movable stick. The stick... was drawn at a uniform rate through the wax by a variable-speed a-c motor". The pattern of spreading ridge segments with transform faults between them was produced. "The upwelling of material is a result only of hydrostatic forces in the fluid caused by the separation of the plates." "The ridge crest has moved at one-half the spreading velocity." "Typical values for the velocity of the stick are a few millimeters per second." "The thickness of the solidified wax is typically less then 0.5 mm near the ridge crest and may increase up to a few millimeters near the plate boundaries." If the separation speed was too slow, the ridge crest solidified and a new ridge opened up in the same segment.7 Another experiment with spreading wax plates found that fast rates of separation produced longer transform faults and larger distances between ridge segments.10
The Atlantic ridge is an example of slow spreading.
The Pacific is an example of fast spreading.
Plate tectonics, on the other hand, states that entire plates are separating. "As the oceanic plates separate at the mid-ocean ridge spreading centers, partial melting of the upwelling mantle creates enough magma to form a layer of basaltic crust 6 to 7 km thick."2
Whether that is so can be determined by a look at the melt regions beneath the spreading ridges. The popular notion is that magma is rising up all along the ridge. However, "no magma chamber reflectors have been imaged at slow-spreading ridges"1,5,9 such as the Mid-Atlantic Ridge, although there are random volcanic eruptions. At fast-spreading ridges such as the East Pacific Rise, magma chambers are found in segments along the ridge, but they are quite small and only in the upper crust. A column of partial melt is below them in the lower crust. "Models of oceanic crustal generation must account for the efficient delivery of melt through the lower crust to a small upper crustal magma chamber."15 A tomographic study shows that globally, low-velocity zones (indicating at least partial melt) beneath mid-ocean ridges extend only to about 100 km depth.3 For the Mid-Atlantic Ridge, "the melt source region lies at a depth of 50-100 km below sea level", and there is "no evidence... of any clear conduit or connection between the mantle melt source and the crustal magma body"8 where volcanism occurs. "Basaltic melt is present beneath the East Pacific Rise spreading center in a broad region several hundred kilometers across..., not just in a narrow region".2 This region of melt is skewed to the west. "The lowest velocities do not lie directly under the ridge".2
"Mantle melting beneath ocean ridges is caused by decompression as mantle adiabatically upwells". "More melt is produced from a given parcel of mantle beneath fast-spreading ridges than beneath slow-spreading ridges." "Spreading rate variation is the primary variable that determines both the extent of mantle melting beneath ocean ridges and mid-ocean ridge basalt chemistry."6 This seems odd, considering that the difference in speeds is between 2.5 and 11 centimeters per year.6 And yet "all these types of ridges produce crust of 6-7 km thickness, except for those with extremely low half-spreading rates (less than 0.5 cm per year), where it is thinner"11 such as in the Arctic.
Geologists talk about oceanic crust in 3 layers. Layer 1 is fairly thin sediment. The upper part of Layer 2 (called 2A) is 0.5 km-thick basaltic lava in the form of 'pillow basalt' (fine-crystal or glassy basalt that cooled quickly). The lower part (called 2B) is 1.5 km-thick diabase (medium-size crystal basalt that cooled more slowly) intrusive dikes (fairly vertical sheets of solidified magma). Layer 3 is 4-5 km-thick gabbro (coarse crystal basalt that cooled slowly).
"Basaltic dikes are nearly 1 meter wide, on average, across all oceanic spreading centers"9 regardless of spreading speed. This seems odd because dike width "should scale with... ridge spreading rate." "The most feasible explanation for this discrepancy is that the magma supply from the magma chamber is limited, so that the magma pressure drops as the dike propagates."9
The evidence of tiny or non-existent magma chambers under spreading ridges that encompass the world suggests that spreading ridges are the remains of past events, things that formed long ago and are not great seams of upwelling today. As weak zones in the oceanic crust, they are subject to stress from differential rotation between the lithosphere and mantle, as well as from other forces, producing limited volcanism and earthquakes. In the Shock Dynamics paradigm, the speed of Antar was considerably faster, because of the greater force-to-mass ratio, than that of continents separating after the Shock Dynamics impact. This produced the distinct "fast spreading" ridge with extremely long transform faults and higher melt volume. But since both events were limited to altering the surface of the oceanic crust, Layer 3 was undisturbed and the magma supply to dikes was universally small for both, being surface melt from pressure and pressure-relief melting.
The ridge reaching from the East Pacific Rise to the Southeast Indian Rise is illustrated below. The bars show the directions that transform faults extend from the ridge, and thus the trend of spreading. Following this scenario, the white bars indicate parts of the ridge where side strips of Antar passed over the seafloor. Those that went east are now accreted (attached by collision) to the west coast of North America. Those that went south are now accreted to South America. This material would have ended up west of Africa. Accretion to North and South America would have occurred as these landmasses moved west following the Shock Dynamics impact, accumulating the material like bugs on a car grill. A strip of this material on North America's west coast, from Vancouver Island to Baja California, appears to have slid north a few hundred miles with North America's slight counterclockwise rotation.
The red bars mark the likely path of the largest part of Antar, which became East Antarctica. These sections of the ridge are by far the most dramatic in the world for length and definition of transform faults, and are associated with so-called megatrends of seamount chains and fracture zones. Two prominent megatrends are shown in yellow below.
There are many thousands of seamounts on the Pacific seafloor. Crudely speaking, they are pimples where hot magma has pushed to the surface. On a small scale, one can compare them to bubbles of boiling mud above hot springs.
Following this scenario, the portion of the Pacific seafloor nearest to the impact of the planetesimal was heated the most, producing the most seamounts. The largest piece of Antar (East Antarctica) pulled a film of hot surface seafloor crust behind it, so seamounts should follow its path in diminishing numbers. The map (below) of seamount density14 on the Pacific plate shows that to be so, with a northwest-southeast axis.
Together, these features suggest a path for East Antarctica represented by the shaded area below. Note that the Shock Dynamics event happened much later, and thrust new landmasses and features into the western part of the shaded area, such as the Izu-Bonin and Marianas Trenches, Japan, parts of Asia and Southeast Asia, Australia, New Zealand, the Tonga-Kermadec Trench, etc. The Emperor-Hawaiian chain is also associated with the Shock Dynamics event, in particular the movement of Alaska along the line of the Aleutian Trench.
East Antarctica (Antar) fits the bulge in the East Pacific Rise nicely, as shown below.
It is plausible that the force of impact of the planetesimal was sufficient to tip the Earth 23.5 ° from the plane of the ecliptic. Because this was the same impact that set Antar in motion, the sudden tipping may have led to the bend in Antar's path.
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2. Forsyth, D.W., and the MELT Seismic Team. 22 May 1998. Imaging the Deep Seismic Structure Beneath a Mid-Ocean Ridge: The MELT Experiment. Science, Vol. 280, pp. 1215-1218.
3. Lebedev, Sergei, Rob D. van der Hilst. 2008. Global upper-mantle tomography with the automated multimode inversion of surface and S-wave forms. Geophysical Journal International, Vol. 173, pp. 505-518.
4. Lloyd, Andrew J., Andrew A. Nyblade, Douglas A. Wiens, Patrick J. Shore, Samantha E. Hansen, Masaki Kanao, Dapeng Zhao. 2013. Upper mantle seismic structure beneath central East Antarctica from body wave tomography: Implications for the origin of the Gamburtsev Subglacial Mountains. Geochemistry, Geophysics, Geosystems, Vol. 14, pp. 1-19, doi: 10.1002/ggge.20098, ISSN: 1525-2027.
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6. Niu, Yaoling, Roger Hékinian. 23 January 1997. Spreading-rate dependence of the extent of mantle melting beneath ocean ridges. Nature, Vol. 385, pp. 326-329.
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9. Qin, Ran, W. Roger Buck. 2008. Why meter-wide dikes at oceanic spreading centers? Earth and Planetary Science Letters, Vol. 265, pp. 466-474.
10. Ragnarsson, Rolf, J. Lewis Ford, Christian D. Santangelo, Eberhard Bodenschatz. 29 April 1996. Rifts in Spreading Wax Layers. Physical Review Letters, Vol. 76, No. 18, pp. 3456-3459.
11. Ruedas, Thomas, Harro Schmeling. 2008. Kinematic models for the thickness of oceanic crust at and near mid-oceanic spreading centers. Journal of Geophysical Research, Vol. 113, B01402, 21 pages.
12. Sieminski, Anne, Eric Debayle, Jean-Jacques Lévêque. 2003. Seismic evidence for deep low-velocity anomalies in the transition zone beneath West Antarctica. Earth and Planetary Science Letters, Vol. 216, pp. 645-661.
13. ten Brink, Uri S., Ron I. Hackney, Stephen Bannister, Tim A. Stern, Yizhaq Makovsky. December 10, 1997. Uplift of the Transantarctic Mountains and the bedrock beneath the East Antarctic ice sheet. Journal of Geophysical Research, Vol. 102, No. B12, pp. 27,603-27,621.
14. Wessel, Paul, Suzanne Lyons. October 10, 1997. Distribution of large Pacific seamounts from Geosat/ERS-1: Implications for the history of intraplate volcanism. Journal of Geophysical Research, Vol. 102, No. B10, pp. 22,459-22,475.
15. Wilcock, William S.D., Sean C. Solomon, G.M. Purdy, Douglas R. Toomey. 27 November 1992. The Seismic Attenuation Structure of a Fast-Spreading Mid-Ocean Ridge. Science, Vol. 258, pp. 1470-1474.
John Michael Fischer, 2008 - 2013