Earth has internal energy stores larger than 1027 J
The infographic’s first takeaway
Earth’s spin alone holds 2.1 × 1029 J [4], and the heat in the mantle and the latent heat of the liquid core are each of order 1030 J [2][5][6]. See section 1.
Evidence review · Earth’s interior
The disaster-cycle video says Earth turns over 90° in a day [1]. Several of Earth’s internal energy stores hold more than such a slide would need, but none can release it within a day, and if its base resisted with 1 MPa or more, friction would cost several times more than the motion itself. We re-derived every value on the infographic that asks the question.
Our analysis marks our own reasoning and calculations, and the verdicts are our assessment. Everything else comes from the numbered sources.
7 × 1026 J
to turn a 100-km-thick lithosphere 90° in 24 hours at a steady rate, our calculation [2]
108 ×
Earth’s whole heat flow, 47 TW, is what delivering even the infographic’s smaller figure in a day would take [3]
4 × 1027 J
lost to friction for each megapascal of resistance at the base, five times the kinetic energy of a 100-km lithosphere’s slide, our estimate
The claims about Earth’s energy
The infographic’s first takeaway
Earth’s spin alone holds 2.1 × 1029 J [4], and the heat in the mantle and the latent heat of the liquid core are each of order 1030 J [2][5][6]. See section 1.
“in one day during the magnetic pole shift, Earth turns over 90°”
The disaster-cycle video [1]
A 90° slide of the lithosphere in a day needs 4–7 × 1026 J of motion, all within the day, and more if its base resists: each megapascal of drag adds about 4 × 1027 J. No store can release energy that fast: heat leaves Earth at 47 TW, about 4 × 1018 J a day [3]. See sections 3 and 4.
The infographic’s mechanism box and third takeaway
They are the only stores of roughly the right size, but buoyancy is released over millions of years, the stress needed exceeds the strength of rock, and no evidence points to a day-long instability combining them. See section 5.
“global coherent stresses of the required size are unproven”
The infographic, on elastic pre-stress
Storing that energy would take about 1 GPa throughout a 100-km lithosphere, more than the few hundred megapascals rock can hold [7]; earthquakes relieve a median of about 4 MPa of stress [8]. “Unproven” makes a physical limit sound like an open question. See section 3.
1 · The stores
We re-derived every value on the infographic from published constants. Four follow directly; the other eight need inputs the infographic doesn’t state, which we reconstructed (section 2). The original chart printed 1026 twice and placed five points 0.7 to 1.9 powers of ten from their values, so it is redrawn here.
1.7 × 1018 J Radiogenic heat produced in one day, at 20 TW
1.1 × 1021 J Magnetic energy in the outer core, at 4 mT
4.2 × 1022 J Elastic strain, 10 MPa throughout a 100-km shell
2.6 × 1023 J Spin energy freed by moving all of Greenland’s ice to the equator
4.2 × 1024 J Elastic strain, 100 MPa
4.2 × 1026 J Elastic strain, 1 GPa
5 × 1026 J Buoyancy of a large dense patch in the deep mantle
2.1 × 1029 J Earth’s spin
1.35 × 1030 J Latent heat if the whole outer core froze
4.8 × 1030 J Mantle heat released by 1,000 K of cooling (illustrative)
Energy, joules (logarithmic scale: each step is ten times the last)
| Value | On the infographic | Ours | With other published inputs | Result |
|---|---|---|---|---|
| Radiogenic heat in one day (20 TW) | 1.7 × 1018 J | 1.7 × 1018 J | 9.8 × 1017 to 3.3 × 1018 J | Reproduced |
| Magnetic energy in the outer core (4 mT) | 1.1 × 1021 J | 1.1 × 1021 J | 4.2 × 1020 to 1.1 × 1021 J | Reproduced |
| Elastic strain (10 MPa) | 4.2 × 1022 J | 4.2 × 1022 J | 1.6–4.6 × 1022 J | Reproduced with our assumptions |
| Elastic strain (100 MPa) | 4.2 × 1024 J | 4.2 × 1024 J | 1.6–4.6 × 1024 J | Reproduced with our assumptions |
| Elastic strain (1 GPa) | 4.2 × 1026 J | 4.2 × 1026 J | 1.6–4.6 × 1026 J | Reproduced with our assumptions |
| Greenland ice comparison | 2.6 × 1023 J | 2.6 × 1023 J | 1.7–2.6 × 1023 J | Reproduced with our assumptions |
| Gravitational buoyancy | 5 × 1026 J | 5.0 × 1026 J | — | Reproduced with our assumptions |
| K0, minimum peak kinetic energy of the slide | 4.1 × 1026 J | 4.1 × 1026 J (a 58-km shell) | 7.1 × 1026 J for a 100-km lithosphere (5.5–9.5 × 1026 J) | Reproduced only with a thin shell |
| Smoothstep peak | 9.2 × 1026 J | 9.2 × 1026 J | 1.6 × 1027 J for a 100-km lithosphere | Reproduced |
| Earth’s spin | 2.1 × 1029 J | 2.1 × 1029 J | — | Reproduced |
| Latent heat if the outer core froze | 1.35 × 1030 J | 1.3 × 1030 J | 1.1–2.2 × 1030 J | Reproduced with our assumptions |
| Mantle heat, 1,000 K of cooling | 4.8 × 1030 J | 4.8 × 1030 J | 4.8–5.1 × 1030 J | Reproduced with our assumptions |
Inputs: Earth’s structure from the reference Earth model [2], its rotation from the IERS Conventions [4], heat flow [3], radiogenic heat [9][13][10], the core field [12][11], Greenland’s ice, 7.42 m of sea level [14], deep-mantle structures [15][16], latent heat [5] and mantle heat capacity [6].
2 · The inputs
Each can be reproduced, but only by guessing a thickness, a stiffness or a distance. The most important is the slide’s own energy, which implies a thinner shell than the usual 100-km lithosphere.
| On the infographic | What reproduces it | With standard inputs |
|---|---|---|
| K0, the slide’s minimum peak kinetic energy: 4.1 × 1026 J | A shell about 58 km thick turned 90° in 24 hours, or a 100-km shell turned 68° | A 100-km lithosphere turned 90°: 7.1 × 1026 J; turned 104°: 9.5 × 1026 J [2] |
| Smoothstep peak: 9.2 × 1026 J | 2.25 times K0, exactly what the smoothstep curve gives | 1.6 × 1027 J for a 100-km lithosphere |
| Elastic strain at 10 MPa, 100 MPa and 1 GPa: 4.2 × 1022, 4.2 × 1024 and 4.2 × 1026 J | That stress everywhere in a global 100-km shell, with a stiffness of 60 GPa, the model’s average shear modulus there | Using the Young’s modulus instead gives 2.6 times less [2] |
| Greenland ice comparison: 2.6 × 1023 J | Spin energy freed if all of Greenland’s ice, 7.42 m of sea level, moved from 72°N to the equator [14] | Melted into the ocean instead: 1.7 × 1023 J |
| Gravitational buoyancy: 5 × 1026 J | 109 km3 of mantle 50 kg/m3 denser than its surroundings, moving 1,000 km | The two large dense-bottomed patches at the base of the mantle hold more mass, but they already rest on the core, so little of it can still sink [15][16] |
| Core latent heat: 1.35 × 1030 J | A latent heat of 733 kJ per kilogram for the outer core’s 1.84 × 1024 kg [2] | Published range 600–1,200 kJ/kg: 1.1–2.2 × 1030 J, so three significant figures overstate it [5] |
| Mantle heat: 4.8 × 1030 J | A heat capacity of 1,200 J/kg/K for 4.0 × 1024 kg of mantle cooled by 1,000 K | 1,265 J/kg/K gives 5.1 × 1030 J [6] |
Radiogenic heat in a day, 20 TW × 86,400 s = 1.7 × 1018 J; the magnetic energy of a 4 mT field filling the outer core, 1.1 × 1021 J; Earth’s spin, ½Cω² = 2.1 × 1029 J; and the smoothstep peak, 2.25 × K0 [12][4]. The 20 TW is one estimate among several: Earth models and geoneutrino measurements run from about 11 to 38 TW, and Earth’s total heat loss, radiogenic heat plus slow cooling, is 46–47 TW [9][10][3].
3 · How fast
The infographic’s table points the right way, but softly: “not demonstrated”, “unproven” and “no known mechanism” describe limits that physics sets.
Earth’s heat loss
4 × 1018 J a day
47 TW, all the heat leaving Earth, radiogenic and primordial; the slide needs 108 times that rate [3]
From Earth’s spin
Our analysis0.19%
rise in Earth’s moment of inertia needed to free 4 × 1026 J: 2.7 oceans’ worth of mass moved from the poles to the equator [4]
Stored in rock
Our analysis1 GPa
throughout a 100-km lithosphere to hold the slide’s energy as strain, above what rock can bear [7]
| Store | The infographic | What sets the limit |
|---|---|---|
| Mantle heat | “Huge inventory, but heat must be transported and converted into mechanical work.” | Heat leaves Earth at 46–47 TW, about 10−12 of this inventory a day, and only part of any heat flow can become work [3]. |
| Core latent heat | “Very large long-term source, not demonstrated as a one-day releasable reservoir.” | It is released only as the inner core grows: about 6.9 × 1028 J over some 670 million years, roughly 3 TW [17]. Freezing the outer core in a day would mean drawing 1.6 × 1025 W through the core’s surface. |
| Earth’s spin | “Large total energy, but only a small accessible fraction becomes available unless inertia changes along a real path.” | Right. Without an outside pull such as the tides, only a change in the moment of inertia frees spin energy; moving all of Greenland’s ice to the equator frees 2.6 × 1023 J, a sixteen-hundredth of the slide’s kinetic energy [14]. |
| Gravitational buoyancy | “Mechanically relevant and close to the target scale in large anomaly examples; requires a real mass redistribution and torque pathway.” | The size is right, but buoyancy works against the viscosity of the lower mantle, about 1022 Pa s [18 p. 4]. A 109 km3 anomaly sinks about 13 cm a year and takes some 7 million years to release 5 × 1026 J. |
| Elastic pre-stress | “Can release quickly, but global coherent stresses of the required size are unproven.” | It would take about 1 GPa throughout the lithosphere. Laboratory experiments put the strength of rock at “a few hundred megapascals for relatively dry rocks” [7]. Earthquake stress drops run from 0.3 to 50 MPa, with a median of about 4 [8]; the largest ever recorded, magnitude 9.5, released about 1019 J [19]. |
| Magnetic energy | “Too small, in this inferred core-field model, to power the target motion.” | Too small by a factor of about 400,000; a field several times stronger would change nothing [12]. |
| Radiogenic heat | “Real long-term source, but no known mechanism releases it coherently in one day.” | Radioactive decay sets the rate. A day’s output is about four billionths of the slide’s kinetic energy [9]. |
Rates and ratios without a reference are our calculations from the values above.
4 · Friction
The infographic compares the stores only with the slide’s kinetic energy. But a lithosphere turned 90° slides an average of about 7,700 km over the layer beneath it, and every metre against resistance turns energy into heat.
| Resistance at the base | Energy lost | Times the infographic’s K0 | Times a 100-km slide’s | Average power |
|---|---|---|---|---|
| 0.1 MPa | 3.8 × 1026 J | 0.9 | 0.5 | 4.4 × 1021 W |
| 1 MPa | 3.8 × 1027 J | 9.3 | 5.4 | 4.4 × 1022 W |
| 4 MPa (median earthquake stress drop) | 1.5 × 1028 J | 37 | 21 | 1.8 × 1023 W |
| 10 MPa | 3.8 × 1028 J | 93 | 54 | 4.4 × 1023 W |
| 100 MPa | 3.8 × 1029 J | 932 | 536 | 4.4 × 1024 W |
Our estimate: resistance × base area × average slip. K0 is the infographic’s 4.1 × 1026 J; a 100-km lithosphere’s slide needs 7.1 × 1026 J [2].
Friction alone matches the slide’s kinetic energy at a resistance of about 0.1 to 0.2 MPa, a twentieth to a fortieth of a typical earthquake’s stress drop [8]. At 1–10 MPa the slide loses 4 × 1027 to 4 × 1028 J, more than every store on the infographic except Earth’s spin, the core’s latent heat and the mantle’s heat, the three whose release in a day it already doubts. That heat would soon melt the slip zone, which may be the “weakening” in its mechanism box. Melt would lower the resistance, so friction is not a firm limit. Even with no friction, the motion alone needs about 5 × 1021 W, a hundred million times Earth’s heat flow [3].
The layer under the lithosphere flows with a viscosity of about 1017 to 1019 Pa s [18 p. 5]. Sheared that fast, it would resist with stresses of 1014 Pa or more, and over a single day it would behave as a solid and break rather than flow. Keeping the losses below the kinetic energy would need about 108 Pa s, a billion times lower than the lowest of those values. Just getting the shell moving within the day takes a push of a few megapascals across its whole base. Only a layer of melt could slide that easily.
5 · The mechanism box
The infographic names “coupled buoyancy + pre-stress + weakening instability” as the “most promising mechanistic direction” and suggests a research path that would “calculate accessible energy as displacement proceeds, rather than assuming the motion in advance”.
Buoyancy and pre-stress are the only stores of roughly the right size, which is all the box shows. Buoyancy is released at the pace of mantle flow, millions of years for this much energy; pre-stress at that level exceeds the strength of rock; and weakening by melting is untested at this scale (section 4). We found no observations or models of a day-scale instability that combines them. The picture under the box shows two plates converging, not a whole shell sliding.
Calculating the energy that becomes available as the motion proceeds, instead of assuming the motion, is the right way to test the idea. Such a calculation would also have to include friction, the strength of rock and the rate at which each store can release energy, the three things that rule a one-day slide out here. The box’s heading, “most promising”, still suggests a one-day slide is a live option; these limits say it isn’t.
6 · A faster flip
The ECDO hypothesis proposes a 104° turn of the mantle and crust together [20]. Its main article captions the turn “a violent 48 hours” [20]; another exhibit puts it at six to eight hours [21]. Our page on ECDO checks its other claims.
Lithosphere, 104° in 8 hours
Our analysis8.6 × 1027 J
of kinetic energy at a steady rate; in 6 hours, 1.5 × 1028 J [2]
Our analysis Over 48 hours, the mantle and crust would need about 4 × 1027 J, a fiftieth of Earth’s spin energy and ten times the infographic’s one-day slide [2].
7 · Read with care
Where our numbers rest on our own assumptions, and what we couldn’t read.
The research summary behind the infographic wasn’t available, so the shell, stiffness, distance and latent heat behind eight values are our reconstructions. Each reproduces the printed value, but other combinations might too.
It treats the lithosphere as one rigid shell sliding over a uniform base, and doesn’t model melting faults, real plate shapes or a lithosphere that bends. It shows the size of the problem, not a precise figure.
The infographic’s footer rightly warns that some values are total inventories, one is a day’s output and others are examples. Its chart marked some kinds in its labels but didn’t sort them; ours names the kind in every label.
Several papers were read as abstracts or summaries, including those on the core field, rock strength, stress drops and deep-mantle structures [12][11][7][8][15][16]. The reference Earth model was entered by hand and checked against published totals [2][4].
Bottom line: Earth has the energy, but no way to spend it in a day.
The infographic’s numbers hold up and its instinct is right: total energy isn’t the problem. Release is. The stores big enough to matter give up their energy over millions to billions of years, and even 1 MPa of resistance at the base would cost several times the motion’s energy. A 90° turn in a day is not an open research question but one these limits close.
Bracketed numbers refer to this list; p. gives a page of the published article. Values without a reference are our calculations from the cited inputs. Links checked October 19, 2026.
SpaceWeatherNews (S0) (2026). THE DISASTER CYCLE – The Evidence. YouTube video, quoted from the transcript behind our check of the video; the line is at 1:22:26.
Dziewonski, A. M., and Anderson, D. L. (1981). Preliminary reference Earth model. Physics of the Earth and Planetary Interiors 25(4), 297–356. Its density and elastic profiles give the masses, volumes, moments of inertia and moduli we use.
Davies, J. H., and Davies, D. R. (2010). Earth’s surface heat flux. Solid Earth 1(1), 5–24. CC BY 3.0.
Petit, G., and Luzum, B. (eds.) (2010). IERS Conventions (2010), IERS Technical Note 36, chapter 1 (updated version): Earth’s rotation rate, flattening and gravity field, from which its moment of inertia follows.
Deguen, R., Alboussière, T., and Cardin, P. (2013). Thermal convection in Earth’s inner core with phase change at its boundary. Geophysical Journal International 194(3), 1310–1334. We read the version on arXiv.
Barnes, R., et al. (2020). VPLanet: the virtual planet simulator. Publications of the Astronomical Society of the Pacific 132(1008), 024502. We read the version on arXiv.
Kohlstedt, D. L., Evans, B., and Mackwell, S. J. (1995). Strength of the lithosphere: constraints imposed by laboratory experiments. Journal of Geophysical Research 100(B9), 17,587–17,602. We read the abstract.
Allmann, B. P., and Shearer, P. M. (2009). Global variations of stress drop for moderate to large earthquakes. Journal of Geophysical Research 114(B1), B01310. We read the abstract.
Borexino Collaboration (Agostini, M., et al.) (2020). Comprehensive geoneutrino analysis with Borexino. Physical Review D 101(1), 012009. CC BY 4.0.
KamLAND Collaboration (Abe, S., et al.) (2022). Abundances of uranium and thorium elements in Earth estimated by geoneutrino spectroscopy. Geophysical Research Letters 49(16), e2022GL099566. CC BY-NC-ND 4.0. We read the version on arXiv.
Buffett, B. A. (2010). Tidal dissipation and the strength of the Earth’s internal magnetic field. Nature 468(7326), 952–954. We read the University of California, Berkeley’s release about it.
Gillet, N., Jault, D., Canet, E., and Fournier, A. (2010). Fast torsional waves and strong magnetic field within the Earth’s core. Nature 465(7294), 74–77. We read the abstract.
KamLAND Collaboration (2011). Partial radiogenic heat model for Earth revealed by geoneutrino measurements. Nature Geoscience 4(9), 647–651. We read the abstract.
Morlighem, M., et al. (2017). BedMachine v3: complete bed topography and ocean bathymetry mapping of Greenland from multibeam echo sounding combined with mass conservation. Geophysical Research Letters 44(21), 11,051–11,061. CC BY 3.0. We read the abstract.
Cottaar, S., and Lekic, V. (2016). Morphology of seismically slow lower-mantle structures. Geophysical Journal International 207(2), 1122–1136. We read the abstract.
Lau, H. C. P., Mitrovica, J. X., Davis, J. L., Tromp, J., Yang, H.-Y., and Al-Attar, D. (2017). Tidal tomography constrains Earth’s deep-mantle buoyancy. Nature 551(7680), 321–326. We read the abstract.
Li, W.-J., Li, Z., Shi, Y.-B., He, X.-T., Wang, C., and Zhang, P. (2020). Ab initio determination on the thermal evolution of the Earth’s core. arXiv:2010.05423, a preprint not peer reviewed.
Cathles, L., Fjeldskar, W., Lenardic, A., Romanowicz, B., Seales, J., and Richards, M. (2023). Influence of the asthenosphere on earth dynamics and evolution. Scientific Reports 13, 13367. CC BY 4.0.
Hanks, T. C., and Kanamori, H. (1979). A moment magnitude scale. Journal of Geophysical Research 84(B5), 2348–2350; and Kanamori, H. (1977). The energy release in great earthquakes. Journal of Geophysical Research 82(20), 2981–2987. The standard relations between magnitude, seismic moment and energy.
The Ethical Skeptic (pseudonym). Exothermic Core-Mantle Decoupling – Dzhanibekov Oscillation (ECDO) Theory. Blog article, May 12, 2024, as modified October 8, 2026; read October 19, 2026.
The Ethical Skeptic (pseudonym). Hidden in Plain Sight. Blog article, December 18, 2023, as modified July 3, 2026; read October 19, 2026 (Exhibit K4).
Method
On October 19, 2026, we checked every value and statement on the original infographic, 38 items, against published constants and studies: the reference Earth model, the IERS conventions, heat-flow and geoneutrino measurements, estimates of the core’s field and latent heat, laboratory rock strength, earthquake stress drops and mantle viscosity. We re-derived all twelve values, measured the original chart against its axis and estimated the friction a sliding lithosphere would meet. The check corrected several statements; the change log lists them.
The verdicts and the items tagged “Our analysis” are our own assessment, built on the cited sources: the re-derivations, release rates and the friction estimate. The chart is redrawn by factchecked.science from the infographic’s values, and the video is quoted from the transcript behind our check of it [1].
After the page was built, a second reviewer who hadn’t seen the drafting recomputed every value with its own model of Earth’s structure, all of which matched, checked the chart against its values and checked every quotation and reference. The changes that followed: the friction comparison is now conditional, about 4 × 10²⁷ J lost per megapascal of resistance at the base, five times a 100-km lithosphere’s kinetic energy, and melt in the slip zone could lower it; the release-rate limit, which rules out a one-day slide on its own, leads; ECDO’s own “48 hours” is given beside its six to eight hours; the deep-mantle patches no longer count as buoyancy that could still be released; the K0 row says it reproduces only with a thin shell; the change log gives the right cause for the original chart’s errors; and several sources and wordings were corrected.
This page was researched and written with Claude, an AI assistant made by Anthropic, and then re-checked against its sources in a separate verification pass.
Corrections
If we get something wrong, we fix it and record the change below with the date. If a correction changes a verdict, the log says what the old verdict was.