Seismic and geochemical observations indicate a compositionally heterogeneous mantle in the lower mantle, suggesting a layered mantle. The volume and composition of each layer, however, remain poorly constrained. This study seeks to constrain the layered mantle model from observed plume excess temperature, plume heat flux, and upper mantle temperature. Three-dimensional spherical models of whole mantle and layered mantle convection are computed for different Rayleigh number, internal heat generation, buoyancy number, and bottom layer thickness for layered mantle models. The model results show that these observations are controlled by internal heating rate in the layer overlying the thermal boundary layer from which mantle plumes are originated. To reproduce the observations, internal heating rate needs similar to 65% for whole mantle convection, but for layered mantle models, the internal heating rate for the top layer is similar to 60-65% for averaged bottom layer thicknesses <similar to 1100 km. The heat flux at the core-mantle boundary (CMB) is constrained to be similar to 12.6 TW for whole mantle convection. For layered mantle, an upper bound on the CMB heat flux is similar to 14.4 TW. For mantle secular cooling rate of similar to 80 K/Ga, the current study suggests that the top layer of a layered mantle is relatively thick (>2520 km) and has radiogenic heat generation rate >2.82x10(-12) W/kg that is >3 times of that for the depleted mantle source for mid-ocean ridge basalts (DMM). For the top layer to have the radiogenic heat generation of the DMM, mantle secular cooling rate needs to exceed 145 K/Ga. The current study also shows that plume temperature in the upper mantle is about half of the CMB temperature for whole mantle convection or similar to 0.6 of temperature at compositional boundary for a layered mantle, independent of internal heating rate and Rayleigh number. Finally, the model calculations confirm that mantle plumes accounts for the majority (similar to 80%) of CMB heat flux in whole mantle convection models. However, plume heat flux decreases significantly by as much as a factor of 3, as plumes ascend through the mantle to the upper mantle, owing to the adiabatic and possibly diffusive cooling of the plumes and owing to slight (similar to 180 K) subadiabaticity in mantle geotherm.

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plume excess temperature plume heat flux ridge generation mantle secular cooling rate bottom layer coremantle boundary cmb upper mantle temperature layered mantle convection rayleigh number internal heat generation buoyancy number internal heating rate

Zhong, SJ,.Constraints on thermochemical convection of the mantle from plume heat flux, plume excess temperature, and upper mantle temperature. 111 (),18.

Zhong, SJ,"Constraints on thermochemical convection of the mantle from plume heat flux, plume excess temperature, and upper mantle temperature" 111

Zhong, SJ,"Constraints on thermochemical convection of the mantle from plume heat flux, plume excess temperature, and upper mantle temperature"