TY - JOUR

T1 - Thermal structure and evolution of Precambrian lithosphere

T2 - a global study

AU - Artemieva, Irina

AU - Mooney, Walter D.

PY - 2001

Y1 - 2001

N2 - The thermal thickness of Precambrian lithosphere is modeled and comparedwith estimates from seismic tomography and xenolith data. We use the steady state thermal conductivity equation with the same geothermal constraints for all of the Precambrian cratons (except Antarctica) to calculate the temperature distribution in the stable continental lithosphere. The modeling is based on the global compilation of heat flow data by Pollack et al. [1993] and more recent data. The depth distribution of heat producing elements is estimated using regional models for ;300 blocks with sizes varying from 18 3 18 to about 58 3 58 in latitude and longitude and is constrained by laboratory, seismic and petrologic data and, where applicable, empirical heat flow/heat productionrelationships. Maps of the lateral temperature distribution at depths 50, 100, and 150 km are presented for all continents except Antarctica. The thermal thickness of the lithosphere is calculated assuming a conductive layer overlying the mantle with an adiabat of 13008C. The Archean and early Proterozoic lithosphere is found to have two typical thicknesses, 200–220 km and 300–350 km. In general, thin (;220 km) roots are found for Archean and early Proterozoic cratons in the Southern Hemisphere (South Africa, Western Australia, South America, and India) and thicker (.300 km) roots are found in the Northern Hemisphere (Baltic Shield, Siberian Platform, West Africa, and possibly theCanadian Shield). We find that the thickness of continental lithosphere generallydecreases with age from .200 km beneath Archean cratons to intermediate values of 200 6 50 km in early Proterozoic lithosphere, to about 140 6 50 km in middle and late Proterozoic cratons. Using known crustal thickness, our calculated geotherms, and assuming that isostatic balance is achieved at the base of the lithosphere, we find that Archean and early Proterozoic mantle lithosphere is 1.5% less dense (chemically depleted) than the underlying asthenosphere, while middle and late Proterozoic subcrustal lithosphere should be depleted by ;0.6–0.7%. Our results suggest three contrasting stagesof lithosphere formation at the following ages: .2.5 Ga, 2.5–1.8 Ga, and ,1.8 Ga. Ages of komatiites, greenstone belts, and giant dike swarms broadly define similar stages and apparently reflect secular changes in mantle temperature and, possibly, convection patterns.

AB - The thermal thickness of Precambrian lithosphere is modeled and comparedwith estimates from seismic tomography and xenolith data. We use the steady state thermal conductivity equation with the same geothermal constraints for all of the Precambrian cratons (except Antarctica) to calculate the temperature distribution in the stable continental lithosphere. The modeling is based on the global compilation of heat flow data by Pollack et al. [1993] and more recent data. The depth distribution of heat producing elements is estimated using regional models for ;300 blocks with sizes varying from 18 3 18 to about 58 3 58 in latitude and longitude and is constrained by laboratory, seismic and petrologic data and, where applicable, empirical heat flow/heat productionrelationships. Maps of the lateral temperature distribution at depths 50, 100, and 150 km are presented for all continents except Antarctica. The thermal thickness of the lithosphere is calculated assuming a conductive layer overlying the mantle with an adiabat of 13008C. The Archean and early Proterozoic lithosphere is found to have two typical thicknesses, 200–220 km and 300–350 km. In general, thin (;220 km) roots are found for Archean and early Proterozoic cratons in the Southern Hemisphere (South Africa, Western Australia, South America, and India) and thicker (.300 km) roots are found in the Northern Hemisphere (Baltic Shield, Siberian Platform, West Africa, and possibly theCanadian Shield). We find that the thickness of continental lithosphere generallydecreases with age from .200 km beneath Archean cratons to intermediate values of 200 6 50 km in early Proterozoic lithosphere, to about 140 6 50 km in middle and late Proterozoic cratons. Using known crustal thickness, our calculated geotherms, and assuming that isostatic balance is achieved at the base of the lithosphere, we find that Archean and early Proterozoic mantle lithosphere is 1.5% less dense (chemically depleted) than the underlying asthenosphere, while middle and late Proterozoic subcrustal lithosphere should be depleted by ;0.6–0.7%. Our results suggest three contrasting stagesof lithosphere formation at the following ages: .2.5 Ga, 2.5–1.8 Ga, and ,1.8 Ga. Ages of komatiites, greenstone belts, and giant dike swarms broadly define similar stages and apparently reflect secular changes in mantle temperature and, possibly, convection patterns.

U2 - 10.1029/2000JB900439

DO - 10.1029/2000JB900439

M3 - Journal article

VL - 106

SP - 16387

EP - 16414

JO - Journal of Geophysical Research: Solid Earth

JF - Journal of Geophysical Research: Solid Earth

SN - 0148-0227

IS - B8

ER -