FRINK Linked Data Fragments server

Matches in SemOpenAlex for { <https://semopenalex.org/work/W1560172911> ?p ?o ?g. }

• W1560172911 endingPage "21" @default.
• W1560172911 startingPage "7" @default.
• W1560172911 abstract "Sedimentary and volcanic rocks of Late Proterozoic to Cambrian age from the lower part of a miogeoclinal wedge that thickens generally towards the west, and extends for about 4500 km along the inner edge of the North American Cordillera between eastern Alaska and northern Mexico. The rocks overlie crystalline basement of Archean to early Middle Proterozoic age and in places as much as several thousand metres of relatively unmetamorphosed sedimentary rocks of Middle to earliest Late Proterozoic age. The contact with the overlying miogeocline ranges from one of angular unconfonnity or nonconfonnity to an ill-defined transition within a relatively conformable succession. The age of this transition is not well constrained, but from dating in western Canada and northeastern Washington it appears to be younger than 770 Ma and older than 720 Ma. An especially distinctive feature of the lower part of the miogeocline throughout the Cordillera is the presence of diamictite, in part of glacial origin. Overlying rocks of Late Proterozoic to Cambrian age are predominantly siliciclastic, although carbonate rocks are abundant locally, especially in the Mackenzie Mountains of northwestern Canada and in the southern part of the Cordillera between eastern California and Sonora, Mexico. The upper part of the miogeocline consists largely of platformal carbonate rocks and mudstones of Cambrian to Devonian age. The transition from siliciclasticdominated to carbonate-dominated rocks is typically in the Lower to Middle Cambrian part of the section, with the age of the transition younging toward the east. It is generally recognized that as a whole the Upper Proterozoic and Lower Paleozoic strata record a transition from intracontinental rifting to the development of a passive continental margin, but the precise location of the transition within the stratigraphy is controversial. Quantitative analysis of tectonic subsidence mainly for strata of Cambrian and Ordovician age between British Columbia and eastern California indicates that thermally driven subsidence of the passive margin began after about 590 Ma, that is, in latest Proterozoic or Early Cambrian time, and this is corroborated by limited stratigraphic evidence for rifting through much of the lower part of the miogeoclinal wedge. An alternative view is that the transition from rift to post-rift phases is well within the lower part of the miogeocline, stratigraphically as much as several kilometres below the base of the Cambrian. This view stems mainly from the fact that most of the geological evidence for rifting is concentrated near the base of the miogeocline, which is some 100–200 m.y. older than the estimated time of onset of the rapid thennal subsidence characterizing the early part of the Paleozoic. The results of subsidence analysis and the geological data may be reconciled by supposing that the region experienced at least two extensional events in LateProterozoic and Early Cambrian time, and that for the later event either 1) all of the areas studied are continentward of the hinge zone between stretched and relatively unstretched lithosphere, or 2) the lithosphere extended in a heterogeneous manner, perhaps in association with regional detachment faults. It is not known whether the region was internal to a supercontinent prior to about 800 Ma, or near a passive continental margin of Middle Proterozoic age, leaving open the possibility that the Late Proterozoic counterpart may consist of one or more relatively narrow slivers rather than a large continental fragment. The Upper Proterozoic and Paleozoic miogeoclinal rocks were affected by several orogenic events beginning in late Devonian time, and in places the rocks were buried by thick successions of younger Paleozoic strata. Much of the defonnation, metamorphism and igneous activity observed within the miogeoclinal belt is related to collision in Mesozoic and Cenozoic time of North America with exotic or suspect terranes of varying affmity, to associated largescale strike-slip deformation, and especially in the western United States to mid- to late Cenozoic lithospheric extension." @default.
• W1560172911 created "2016-06-24" @default.
• W1560172911 creator A5003452705 @default.
• W1560172911 creator A5050492047 @default.
• W1560172911 date "1989-01-01" @default.
• W1560172911 modified "2023-10-03" @default.
• W1560172911 title "Stratigraphic and tectonic framework of Upper Proterozoic and Cambrian rocks in the western United States" @default.
• W1560172911 cites W119862345 @default.
• W1560172911 cites W1644631706 @default.
• W1560172911 cites W1908442502 @default.
• W1560172911 cites W1963827929 @default.
• W1560172911 cites W1968439712 @default.
• W1560172911 cites W1968752174 @default.
• W1560172911 cites W1969566004 @default.
• W1560172911 cites W1973535425 @default.
• W1560172911 cites W1976895386 @default.
• W1560172911 cites W1977106657 @default.
• W1560172911 cites W1977151267 @default.
• W1560172911 cites W1979331501 @default.
• W1560172911 cites W1980506837 @default.
• W1560172911 cites W1982118449 @default.
• W1560172911 cites W1983596468 @default.
• W1560172911 cites W1983829740 @default.
• W1560172911 cites W1986764082 @default.
• W1560172911 cites W1987125108 @default.
• W1560172911 cites W1987135569 @default.
• W1560172911 cites W1988925446 @default.
• W1560172911 cites W1989072731 @default.
• W1560172911 cites W1989242057 @default.
• W1560172911 cites W1989701796 @default.
• W1560172911 cites W1990947892 @default.
• W1560172911 cites W1992918921 @default.
• W1560172911 cites W1993508061 @default.
• W1560172911 cites W1993524516 @default.
• W1560172911 cites W1993775609 @default.
• W1560172911 cites W1993804022 @default.
• W1560172911 cites W1994182127 @default.
• W1560172911 cites W1994587751 @default.
• W1560172911 cites W1994917745 @default.
• W1560172911 cites W1995712304 @default.
• W1560172911 cites W1995983326 @default.
• W1560172911 cites W1997252211 @default.
• W1560172911 cites W1997759594 @default.
• W1560172911 cites W2000414042 @default.
• W1560172911 cites W2000606644 @default.
• W1560172911 cites W2000871075 @default.
• W1560172911 cites W2002180431 @default.
• W1560172911 cites W2002566645 @default.
• W1560172911 cites W2004468553 @default.
• W1560172911 cites W2005535021 @default.
• W1560172911 cites W2005936492 @default.
• W1560172911 cites W2006031023 @default.
• W1560172911 cites W2006263788 @default.
• W1560172911 cites W2007417704 @default.
• W1560172911 cites W2009004065 @default.
• W1560172911 cites W2014696764 @default.
• W1560172911 cites W2015500663 @default.
• W1560172911 cites W2016562641 @default.
• W1560172911 cites W2017950482 @default.
• W1560172911 cites W2018843945 @default.
• W1560172911 cites W2019093746 @default.
• W1560172911 cites W2019987698 @default.
• W1560172911 cites W2020286870 @default.
• W1560172911 cites W2023667913 @default.
• W1560172911 cites W2024332563 @default.
• W1560172911 cites W2025010591 @default.
• W1560172911 cites W2025329049 @default.
• W1560172911 cites W2026414118 @default.
• W1560172911 cites W2026951827 @default.
• W1560172911 cites W2027614909 @default.
• W1560172911 cites W2028812913 @default.
• W1560172911 cites W2030474253 @default.
• W1560172911 cites W2034275980 @default.
• W1560172911 cites W2034651217 @default.
• W1560172911 cites W2034753142 @default.
• W1560172911 cites W2037240729 @default.
• W1560172911 cites W2037582493 @default.
• W1560172911 cites W2038899995 @default.
• W1560172911 cites W2043756665 @default.
• W1560172911 cites W2044021650 @default.
• W1560172911 cites W2047244068 @default.
• W1560172911 cites W2048827124 @default.
• W1560172911 cites W2050442970 @default.
• W1560172911 cites W2050535665 @default.
• W1560172911 cites W2051521766 @default.
• W1560172911 cites W2052044539 @default.
• W1560172911 cites W205236894 @default.
• W1560172911 cites W2053913791 @default.
• W1560172911 cites W2054064647 @default.
• W1560172911 cites W2057239933 @default.
• W1560172911 cites W2061116240 @default.
• W1560172911 cites W2062227426 @default.
• W1560172911 cites W2066907116 @default.
• W1560172911 cites W2073153084 @default.
• W1560172911 cites W2073205970 @default.
• W1560172911 cites W2073501080 @default.
• W1560172911 cites W2073671350 @default.
• W1560172911 cites W2075817993 @default.

• next