SOME FIGURES FOR UNFINISHED MANUSCRIPTS (CONDENSED; FULL VERSION CAN BE REQUESTED VIA DROPBOX)

1. SOME FIGURES FOR UNFINISHED MANUSCRIPTS (CONDENSED; FULL VERSION CAN BE REQUESTED VIA DROPBOX)

2. ridge Ridge-normal profile OIB B TZ MORB source Birch’s Transitional Layer Density barrier D’ D”

3. eclogite harzburgite 410 cold 650 cold

4. RIDGE Shear wavespeed Temperature OIB 1 1600 C adiabat BL VSH>VSV Observed Seismic profile High-T conduction geotherm 2 5 220 km ~1600 C 6 VSV>VSH 3 Vs for self-compressed solid along adiabat Subadiabatic geotherm 4 7 Tp=~1300 C 650 km disconnect A mantle circulation model based on anisotropy, anharmonicity, absolute wavespeeds & gradients, allows for, and predicts, non adiabaticity

5. ridge hotspots Tp LIL Sheared mélange 200 400 km LIL LVZ UPPER MANTLE Ancient eclogite cumulates TZ Modern slab fragments ‘cold’ THE “NEW” PARADIGM “the canonical box”

6. SUMMARY SCHEMATIC* Intraplate volcanoes Midocean ridges Sediments volatiles Residual slab components LOWER MANTLE *Essentially the classical model of Birch, Tatsumoto, Wilson…

7. The Eureka Solution Pebbles Old Greeks Slabs Physics-Based Archimedian Paradigm* Shear-driven magma segregation OIB Shear strain Super-adiabatic boundary layer REGION B squeezing squeezing Hawaii source “fixed” Thermal max 300 km Sources deeper than ~ 150-200 km are effectively fixed (e.g.J.T.Wilson) Tp decreases with depth Narrow downwellings Broad passive upwellings MORB source k(T), a(V,T), TCMB(t), n(V,T), U(z,t), Th(z,t)… TRANSITION ZONE (TZ) Archimedes & Birch 600 km 600 km (RIP) 200 Myr of oceanic crust accumulation (* Birch, Tatsumoto, J. Tuzo Wilson)

8. STANDARD CONCEPTUAL MODEL (1988) No physics, no seismology jet ISOTHERM 100 km ADIABATIC ISOTHERMAL HOMOGENEOUS ISOTHERM No U, Th, K No secular cooling Ambient T constrained (<1600K) (used as reference model; Herzberg, Asimow, Humphreys, Schmandt, Victor Camp…e.g…)

9. LID LLAMA subadiabat BOUNDARY LAYER T (oC) Negative Vs gradient 1600 1200 800 400 0 Tp(max)~1600o Tp=1280o Cambridge nomenclature Lithosphere Mechanical boundary layer Thermal boundary layer Adiabatic interior 0 100 200 300 Depth (km)

10. European, African, Asian (Changbai), Yellowstone & most continental intra-plate volcanoes (“hotspots”) are underlain by slabs Cold slab Cooled mantle UPPER MANTLE & LOWER MANTLE ARE COOLED BY LONG-LIVED FLAT (STAGNANT) SLABS 49

11. Fixed hotspot paradox STAGNANT SLABS–A FIXED REFERENCE FRAME Ridges & hotspots No hotspots REGION B LVA 410 WARM TZ COLD 650 COOL SLIP-FREE BOUNDARY There may be a concentration of CaO, Al2O3, K…U, Th…in the upper mantle…Birch 50

12. Illustrating the thermal bump and subadiabaticity Midplate bump 1600 1400 (& backarc) Ridge adiabat Boundary layer UPPER MANTLE T oC LLAMA(shearing) midplate ridge TZ 400 200 D” Plate (conducting) T LOWER MANTLE B CMB Depth Depth The highest potential temperature in the mantle is near 200 km. Tectonic processes (shear, delamination) are required to access this.

13. U, Th, K and other LIL are concentrated in the crust & the upper mantle boundary layer during the radial zone refining associated with accretion (Birch, Tatsumoto…). This accentuates the thermal bump. (Lubimova, MacDonald, Ness)

14. SUMMARY Ridges are fed by broad 3D upwellings plus lateral flow along & toward ridges ridge OIB LID LVZ LLAMA 200 400 subadiabatic Mesosphere (TZ) km Cold slabs Intraplate (delamination, CRB, Deccan, Karoo, Siberia) magmas are shear-driven from the 200 km thick shear BL (LLAMA)