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NARROW
GeoRef Subject
-
all geography including DSDP/ODP Sites and Legs
-
Africa
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Central Africa
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Burundi (1)
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Gabon
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Oklo (1)
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Madagascar (1)
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Southern Africa
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South Africa
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Asia
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China
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South Atlantic (1)
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Australasia
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Canada
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Al-26 (6)
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He-4 (1)
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alkali metals
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potassium
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alkaline earth metals
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barium (1)
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beryllium
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Be-10 (6)
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calcium (2)
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magnesium
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Mg-25/Mg-24 (1)
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radium
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Ra-226 (9)
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Ra-228 (1)
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Th-230/Ra-226 (1)
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strontium (2)
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aluminum
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Al-26 (6)
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lead
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Pb-206/Pb-204 (2)
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polonium
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oxygen
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fossils
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Invertebrata
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Plantae
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geologic age
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Tertiary
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uranium minerals (2)
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-
Primary terms
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absolute age (27)
-
Africa
-
Central Africa
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Burundi (1)
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Gabon
-
Oklo (1)
-
-
-
Madagascar (1)
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Southern Africa
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South Africa
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Bushveld Complex (1)
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Transvaal region (1)
-
-
-
-
Asia
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Far East
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China
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Xizang China
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Gangdese Belt (1)
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Yunnan China (1)
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Japan
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Lake Baikal (1)
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atmosphere (1)
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Australasia
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Australia
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Olympic Dam Deposit (1)
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Tasmania Australia (1)
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biography (1)
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boron
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brines (1)
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Canada
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Quebec
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Matagami (1)
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-
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Western Canada
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Athabasca Basin (1)
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Manitoba
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Lac du Bonnet Batholith (1)
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Pinawa Manitoba (1)
-
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Saskatchewan (1)
-
-
-
carbon
-
C-13/C-12 (1)
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C-14 (1)
-
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Cenozoic
-
Quaternary
-
Holocene (2)
-
Pleistocene
-
upper Pleistocene (1)
-
-
upper Quaternary (1)
-
-
Tertiary
-
Neogene
-
Miocene
-
Paintbrush Tuff (1)
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Topopah Spring Member (1)
-
-
Pliocene
-
upper Pliocene (1)
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-
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Paleogene (1)
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climate change (2)
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continental drift (1)
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crust (4)
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crystal structure (8)
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Earth (3)
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education (1)
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Europe
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-
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Ukraine (1)
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Scandinavia
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-
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faults (2)
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geochemistry (14)
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ground water (6)
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heat flow (4)
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hydrology (2)
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igneous rocks
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granites (4)
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pegmatite (2)
-
syenites
-
nepheline syenite (1)
-
-
ultramafics
-
chromitite (1)
-
-
-
volcanic rocks
-
basalts
-
mid-ocean ridge basalts (1)
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ocean-island basalts (1)
-
-
pyroclastics
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tuff (1)
-
-
-
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impact statements (1)
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Indian Ocean Islands
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interplanetary space (1)
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Invertebrata
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Mollusca (1)
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Protista
-
Foraminifera
-
Rotaliina
-
Globigerinacea
-
Neogloboquadrina
-
Neogloboquadrina pachyderma (1)
-
-
-
-
-
-
-
isotopes
-
radioactive isotopes
-
Al-26 (6)
-
Ar-39 (1)
-
Be-10 (6)
-
C-14 (1)
-
Cs-134 (1)
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Cs-137 (3)
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I-129 (2)
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I-131 (1)
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K-40 (1)
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Pa-231 (2)
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Pb-206/Pb-204 (2)
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Pb-207/Pb-204 (1)
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Pb-208/Pb-204 (1)
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Pb-210 (5)
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Po-210 (1)
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Pu-239 (1)
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Pu-244 (2)
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Ra-226 (9)
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U-235 (5)
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U-238 (9)
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U-238/Th-232 (1)
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U-238/U-235 (1)
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stable isotopes
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Ar-40 (1)
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B-11/B-10 (1)
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C-13/C-12 (1)
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He-3 (2)
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He-4 (1)
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Mg-25/Mg-24 (1)
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O-18/O-16 (2)
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Mediterranean region
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Mesozoic
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Cretaceous
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Jurassic
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Upper Jurassic
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Thermophysical properties and geochemical characteristics of granites in the Tengchong area: indications for resource potential of hot dry rocks
Soil gases in mineral exploration: a review and the potential for future developments
(U-Th)/He chronology: Part 1. Data, uncertainty, and reporting
A Date for Odysseus
Noble Gas Thermochronology of Extraterrestrial Materials
Noble Gases Deliver Cool Dates from Hot Rocks
Abiotic Sources of Molecular Hydrogen on Earth
REE-, Sr-, Ca-aluminum-phosphate-sulfate minerals of the alunite supergroup and their role as hosts for radionuclides
222 Rn and 220 Rn Emanations from Zircon Crystals As a Function of Absorbed α-Doses
Geological Disposal of Nuclear Waste: a Primer
Mechanical properties of natural radiation-damaged titanite and temperature-induced structural reorganization: A nanoindentation and Raman spectroscopic study
The subsidence of an aging seafloor starts to slow down at ~70 m.y. old with respect to that expected from simple half-space cooling, and this phenomenon has long been known as seafloor flattening. The flattening signal remains even after removal of the influence of the emplacement of hotspot islands and oceanic plateaus. The combination of small-scale convection and radiogenic heating has been suggested as a mechanism to explain seafloor flattening, and this study explores the possibility of using the magnitude of seafloor flattening to constrain the amount of radiogenic heating in the convecting mantle. By comparison of properly scaled geodynamic expectations with the observed age-depth relation of the normal seafloor, the mantle heat production is estimated to be ~12 ± 3 TW, which supports geochemistry-based estimates. A widely held notion that small-scale convection enhances cooling, thus being unable to explain seafloor flattening, is suggested to be incorrect. The ability to accurately interpret the age-depth relation of seafloor based on the thermal budget of Earth has an important bearing on the future theoretical study of early Earth evolution.
Geochronology and Thermochronology Using Apatite: Time and Temperature, Lower Crust to Surface
Possible new Ca-REE-Bi phosphate minerals from a tungsten-rich calcsilicate skarn, Sierra Nevada Mountains, California
Abstract Determining the timescales of magma degassing is essential for understanding the mechanisms controlling the eruption style and the dynamics of magmatic systems. Towards this end, we measured 210 Pb– 226 Ra disequilibria in andesite lavas erupted from Volcán de Colima between 1998 and 2010. ( 210 Pb/ 226 Ra) 0 activity ratios range from 0.86 to 1.09, and are best explained in terms of 222 Rn degassing and accumulation. The range in 210 Pb deficits indicates that the timescales of 222 Rn degassing did not exceed 11 years. 210 Pb excesses are rare and small (<10%), which signifies that 222 Rn degassing is more effective than 210 Pb accumulation in this intermediate system despite the relatively low gas output at the surface. The absence of significant 210 Pb excesses strongly suggests that the volcanic activity results from episodic ascent of small magma batches through the vapour-saturated section of the magmatic system. Overall, the degassing models based on 210 Pb– 226 Ra disequilibrium suggest an open and complex subvolcanic magmatic system comprising several conduits in which multiple magma batches reside for up to 10 years. Shifts from effusive to explosive Vulcanian eruptive phases are not related to changes in degassing mode on timescales resolvable using 210 Pb– 226 Ra disequilibria.
“Silicified” pyrochlore from nepheline syenite (mariupolite) of the Mariupol Massif, SE Ukraine: A new insight into the role of silicon in the pyrochlore structure
1896 marked the beginning of a decade that spawned both modern physics and the science of geochronology based on radioactive decay. The decade started with the discovery of radioactivity by Henri Becquerel in 1896, and ended with the formal publication of ages for natural mineral samples by Ernest Rutherford in 1906. The next fifty years witnessed the discovery of isotopes and nuclear fission; the development of the mass spectrograph and the mass spectrometer; application of the isotope dilution method to dating trace, accessory, and major minerals in typical crustal rocks; and publication of the ca. 4.55 Ga age for the Earth. Yet, after all this, geochronology was still viewed with suspicion by some geologists. In the past fifty years, with additional major advances in instrumentation, technique, and interpretation, geochronology is fully integrated into almost all fields of geology. The three major dating methods from the 1950s and 1960s, U-Pb, K-Ar, and Rb-Sr, have been refined repeatedly. In particular, U-Pb and Ar-Ar, a modern variant of K-Ar, are now capable of <0.1% precisions, with spectacular results in recent studies of crucial problems such as the exact timing and duration of mass extinctions. Many new methods are now available to attack problems ranging from rates of metamorphic mineral growth to rates of uplift and erosion, to the time of surface exposure of geomorphic surfaces. It is a good time to be a geochronologist, or to collaborate with one or more. The future looks very bright.