Transition from infrastructure to suprastructure in the northern Ruby Mountains, Nevada

1980 ◽  
pp. 287-334 ◽  
Author(s):  
Arthur W. Snoke
Keyword(s):  
Ruby Mountains

CLIMATE CHANGE DURING DEGLACIATION OF THE OVERLAND CREEK VALLEY, RUBY MOUNTAINS, NEVADA, U.S.A

2016 ◽  
Author(s):  
Hannah Sackett ◽  
◽  
Benjamin J.C. Laabs ◽  
Jeffrey S. Munroe ◽  
Samantha W. Eckes
Keyword(s):  
Climate Change ◽  
Ruby Mountains

Mammals of the Ruby Mountains Region of North-Eastern Nevada

1934 ◽  
Vol 15 (1) ◽  
pp. 12 ◽  
Author(s):  
Adrey E. Borell ◽  
Ralph Ellis
Keyword(s):  
Ruby Mountains ◽  
North Eastern

scholarly journals Petrogenesis of Mesozoic, Peraluminous Granites in the Lamoille Canyon Area, Ruby Mountains, Nevada, USA

2003 ◽  
Vol 44 (4) ◽  
pp. 713-732 ◽  
Author(s):  
Sang-Yun Lee ◽  
Calvin G. Barnes ◽  
Arthur W. Snoke ◽  
Keith A. Howard ◽  
Carol D. Frost
Keyword(s):  
Great Basin ◽  
Late Cretaceous ◽  
Heat Input ◽  
Crustal Thickening ◽  
Dehydration Melting ◽  
Granitic Gneiss ◽  
Peraluminous Granites ◽  
Ruby Mountains ◽  
Sevier Orogeny ◽  
Biotite Dehydration Melting

Abstract Two groups of closely associated, peraluminous, two-mica granitic gneiss were identified in the area. The older, sparsely distributed unit is equigranular (EG) with initial εNd ∼ − 8·8 and initial 87Sr/86Sr ∼0·7098. Its age is uncertain. The younger unit is Late Cretaceous (∼80 Ma), pegmatitic, and sillimanite-bearing (KPG), with εNd from −15·8 to −17·3 and initial 87Sr/86Sr from 0·7157 to 0·7198. The concentrations of Fe, Mg, Na, Ca, Sr, V, Zr, Zn and Hf are higher, and K, Rb and Th are lower in the EG. Major- and trace-element models indicate that the KPG was derived by muscovite dehydration melting (<35 km depth) of Neoproterozoic metapelitic rocks that are widespread in the eastern Great Basin. The models are broadly consistent with anatexis of crust tectonically thickened during the Sevier orogeny; no mantle mass or heat contribution was necessary. As such, this unit represents one crustal end-member of regional Late Cretaceous peraluminous granites. The EG was produced by biotite dehydration melting at greater depths, with garnet stable in the residue. The source of the EG was probably Paleoproterozoic metagraywacke. Because EG magmatism probably pre-dated Late Cretaceous crustal thickening, it required heat input from the mantle or from mantle-derived magma.

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