Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
Table of Contents
Summary 1
Geology of Rockall Plateau and Basin 2
First model of Atlantis slide 3
Friction of sedimentary novaculite quartz went to zero 5
Second model of Atlantis slide 6
Separation from continental shelf 8
Reconstruction of Atlantis before sinking 11
Bibliography 13
Summary
Rockall Plateau is 650 km long, 450 km wide and 2 km high; its top averages a kilometer below
sea level, while its bottom rests on the flat surface of Rockall Basin, 3 km deep. Its eastern edge
matches the continental shelf of Ireland, 218 km away.
The plateau consists of two overlapping sedimentary layers, a top half and a bottom half. By
sliding the top half 175 km east over the bottom half, Atlantis pops out of the sea, about 400 m
high. A mountain range crosses the north; in the center, farm lands measure 3000 stadia long by
2000 stadia wide from sea to sea. Its area measures in size between Libya and Asia as they were
defined in 600 BC. Any trace of agricultural canals has vanished, but a feature in the southwest
looks like a ship channel that ends in a circular lake.
In Egypt, 4000 km away, shepherds in the mountains recalled the sequence: a terrible earthquake
followed by a catastrophic flood that penetrated the Mediterranean Sea and lasted a day and a
night. The earthquake resulted from an extra-terrestrial strike in Karelia by a satellite of Nibiru.
Page 1
Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
A separate satellite struck Atlantis, most likely killing everyone. Shock from the strike turned
two horizontal layers of quartz into a frictionless surface. The top half slid west into Rockall
Basin, gathering speed as it went. It slid 175 km, lost 1.5 km of elevation, and reached 422 kph.
Suddenly the sliding top regained friction and latched onto the bottom half. Momentum jerked
the two pieces away from the continental shelf and across the Atlantic. As the plateau moved like
a sheet of plywood through the sea, it lost energy from raising the sea. It finally stopped when the
front edge dug into the bottom of the basin and rotated the plateau counter-clockwise 6 degrees.
Above an area the size of Britain, the slide raised sea level an average of 1.5 km with a peak of
2.1 km.
Figure 1: Atlantis west of Eire.
Page 2
First model of Atlantis slide
First model of Atlantis slide
Cross section across Rockall Plateau show s the top half slipped w est
A cross section across Rockall Plateau reveals two pieces, an eastern base and a western top that
slid off the base (Figures 2 and 3). Both Rockall Plateau and the continental shelf are
sedimentary deposits, 4 to 6 km thick for the continental shelf. When a satellite of Nibiru
disintegrated and struck the Scandinavian ice sheet, one piece landed near or on Atlantis. The
resultant shock converted a sloping sedimentary layer of quartz beneath the island into a
frictionless material (see below). Without friction, the top half slid west into Rockall Basin.
Figure 2: Initial concept of the sinking of Atlantis. Cross section across Rockall Plateau shows
how the upper part of the island might have slid into Rockall Basin. The problem is lack of a
horizontal frictionless layer.
To reconstruct the slide, first push the plateau back to the mainland (Figures 4 and 5).
Page 3
Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
Figure 4: Rockall Plateau shoved up against the continental shelf of Ireland. This preliminary
model does not push the plateau far enough.
Next slide the western half back to its original position (Figure 5). Atlantis rises out of the sea.
Figure 5: Preliminary model of Atlantis before sinking. Problem is that Atlantis is too narrow.
Without accounting for loss due to raising sea level, Atlantis would have accelerated down a
1.34% slope for 120 km and reached 475 kph in 26 minutes (Figure 6). But this model has
problems.
Page 4
Friction of sedimentary novaculite quartz w ent to zero
Figure 6: Preliminary model of the Atlantis slide created a tsunami 2.1 km high.
Page 5
Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
Figure 7: Coefficient of friction for novaculite quartz drops to zero above 1.2 m/s.
Coefficient of dynamic friction vs sliding velocity
0.8 Novaculite at 5 Mpa (49 atmospheres)
0.7 Source: Giulio Di Toro (2004)
Coefficient of friction 0.6 Friction goes to zero at 1.2 m/s
0.5
0.4
0.3
Arkansas Novaculite is a quartz rock
0.2 of meta-sedimentary origin with a grain
0.1 size of 1 to 5 microns.
0.0
0.000001 0.00001 0.0001 0.001 0.01 0.1 1 10
Sliding velocity - m/s
Page 6
Second model of Atlantis slide
Figure 8: Cross-section of Atlantis attached to the continental shelf west of Ireland. Two slopes,
east and west, supplied energy to propel Atlantis into Rockall Basin. Two frictionless, horizontal
surfaces offered no resistance. Mass above the slopes contributed to acceleration, while raising
water above sea level subtracted from acceleration.
2.1 km
Atlantis cross section
2 km
1 km
0 km
43 min
Ireland
-1 km
135 km
-2 km
366 kph
Rockall Basin
-3 km
1100 1000 900 800 700 600 500 400 300 200 100 0
Distance from center of Ireland - km S Harris May 2018
Page 7
Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
Figure 9: Acceleration of Atlantis from two slopes of the continental shelf less force to lift the
sea. The eastern slope provided the initial force, barely offsetting the force required to lift the
sea. Once the slide started, the western slope provided most of the force.
Acceleration - m/sec2 Acceleration of east slope, west slope and sea slope
0.08
0.00
175 150 125 100 75 50 25 0
-0.02
-0.04
-0.06
West East
-0.08
Distance moved by top of Atlantis - km
Subtracting the force required to lift the sea slowed final velocity to 385 kph. (Figure 10).
Figure 10: Velocity versus time for Atlantis to plunge into Rockall Basin.
Velocity vs Time
In 56 minutes, the top half of Atlantis traveled 175 km and reached 385 kph
450
400 385
350
Velocity - kph
300
250
200
150
100
50
0
0 10 20 30 40 50 60
Time - minutes
Page 8
Separation from continental shelf
Momentum of sliding top carries island w est
The interface between Rockall Plateau and Rockall Basin exhibited close to zero friction. Any
friction at all would have brought the plateau to a quick stop, but instead, it went on until the
leading edge caught on the southwest corner, spun the plateau 6 degrees counterclockwise, and
rebounded slightly. Water resistance had little impact because of how thin the plateau was in
relation to its width, thinner than a knife, but raising the sea 1½ km did cause drag. A volcano in
the north-east corner remained anchored to the basin floor.
Figure 11: Model of plateau travel across Rockall Basin. Kinetic Energy of the plateau was
converted to Potential Energy of raised sea water.
Both pieces moved as a unit across Rockall Basin for 218 km. The gain in Potential Energy
equaled the loss in Kinetic Energy.
d(PE) = d(KE) H = height of raised sea = 1.6 km
d(PE) = ½ H g Mw g = gravity = 9.8 m/s2
= ½ H g (ρWHLx) ρW = density of water = 1
d(KE) = ½ MP (v02-vx2) ρP = density of plateau = 2.55
2 2
= ½ (ρP A L)(v0 – vx ) L = length of plateau = 650 km
x = distance slide has traveled, in km
A = cross section area of plateau = 575 km2
v0 = initial velocity of plateau = 70 m/s, 253 kph
vx = velocity at distance x, in m/s
Setting the two sides equal, crossing out identical items, and letting the density of water = 1,
H2 g x = ρP A(v02 – vx2)
Solving for velocity,
vx2 = v02 – g H2 x/ρP A m2/s2
= (70 m/s)2 – [(9.8 m/s2)(1.62 km2/575 km2)(1000 m/km)/2.55](x km)
= 4900 – [(9.8*1.6*1.6*1000)/(575*2.55)]x
= 4900 – 17.1x
= 17.1(286 – x) m2/s2
Taking the square root gives meters per second, while multiplying by 3.6 gives kph.
vx = 4.13(286 - x)½ m/s, or 14.9(286 - x)½ kph
For x = 218 km, velocity = 123 kph
To calculate time, use the equation: distance = (average velocity)*(time)
x = ½ (v0 + vx)t
t = 120 x/(v0+vx) minutes, with x in km, v in kph
For x = 218 km, vo = 253 kph, vx = 123 kph
t = 120*218/(253+123) = 70 minutes
Page 9
Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
Figure 12: Separation of Rockall Plateau from Ireland. In seventy minutes, the plateau moved
218 km. Inrush from north and south began to fill Rockall Trough. Above the plateau, sea level
rose an average of 1.6 km across an area of 400 km by 650 km, with a maximum height of 2100
m.
Page 10
Reconstruction of Atlantis before sinking
Figure 14: A half hour later, the tsunami began to cross Ireland at 410 kph, its average height
still about 1.6 km because of run-up.
Page 11
Sinking of Atlantis by Nibiru in 9577 BC: Part 2, Mechanics of Sinking
Figure 16: Move mountain range to continental shelf.
Page 12
Bibliography
Figure 19: Assembled island moved back to the continental shelf. The volcano in the north-east
corner did not move. A large central plain is ringed by mountains.
Bibliography
Balsillie, James H. (1946-1960) and Joseph F. Donoghue (2004); High resolution sea-level
history for the Gulf of Mexico since the last glacial maximum; Florida Geological Survey.
Di Toro, Giulio, David L Goldsby, Terry E Tullis (2004); Friction falls to zero in quartz rock as
slip velocity approaches seismic rates; Letters to Nature, V427, Jan 29, 2004. Discovery of zero
coefficient of friction property of quartz at high pressure and slip speeds greater than 1.2 m per s.
Page 13