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NARROW
GeoRef Subject
-
all geography including DSDP/ODP Sites and Legs
-
Africa
-
North Africa
-
Algeria
-
Great Kabylia (1)
-
-
Atlas Mountains
-
Moroccan Atlas Mountains
-
High Atlas (4)
-
-
-
Maghreb (1)
-
Morocco
-
Moroccan Atlas Mountains
-
High Atlas (4)
-
-
Rif (1)
-
-
Tunisia (1)
-
-
Southern Africa
-
Karoo Basin (1)
-
Lesotho (1)
-
South Africa (1)
-
-
-
Arctic Ocean
-
Barents Sea (1)
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Norwegian Sea
-
Haltenbanken (1)
-
-
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Arctic region
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Greenland
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East Greenland (1)
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Asia
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Arabian Peninsula
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Kuwait (1)
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Saudi Arabia (1)
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Central Asia
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Pamirs (1)
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Far East
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China
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Fujian China (1)
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Hunan China (1)
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Sichuan China (1)
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Indian Peninsula
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India
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Andhra Pradesh India (1)
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Middle East
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Turkey
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Antalya Turkey (1)
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Taz Basin (1)
-
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West Siberia (1)
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Atlantic Ocean
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Europe
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Alps (3)
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Italy
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Scotland
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Highland region Scotland
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Wales
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oxygen
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sulfur
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S-34/S-32 (2)
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fossils
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Chordata
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Vertebrata
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Labyrinthodontia
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Mammalia (1)
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Thecodontia
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Synapsida
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ichnofossils (1)
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Invertebrata
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Plantae
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middle Liassic (17)
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Portlandian (2)
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Triassic
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Triassic-Jurassic boundary (1)
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Paleozoic
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upper Precambrian
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igneous rocks
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sheet silicates (1)
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Primary terms
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absolute age (4)
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Africa
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North Africa
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Algeria
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Great Kabylia (1)
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Atlas Mountains
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High Atlas (4)
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Maghreb (1)
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High Atlas (4)
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Rif (1)
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Tunisia (1)
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Southern Africa
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Arctic Ocean
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West Siberia (1)
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biogeography (3)
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Canada
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Whitehorse Trough (1)
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carbon
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C-13/C-12 (6)
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Cenozoic
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Quaternary
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Holocene
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Boreal (1)
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Tertiary
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Paleogene (1)
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-
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Chordata
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Vertebrata
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Amphibia
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Labyrinthodontia
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Temnospondyli (1)
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Mammalia (1)
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Reptilia
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Diapsida
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Archosauria
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dinosaurs
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Ornithischia (1)
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Theropoda (2)
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-
-
Pterosauria (1)
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Thecodontia
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Ichthyosauria
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Synapsida
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Cynodontia (2)
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Western Europe
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Scotland
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-
-
-
Highland region Scotland
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Raasay (1)
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Wales
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faults (6)
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geochemistry (4)
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geophysical methods (1)
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government agencies
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survey organizations (1)
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igneous rocks
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plutonic rocks
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ultramafics (1)
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volcanic rocks
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pyroclastics
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tuff (1)
-
-
-
-
Indian Ocean
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-
Exmouth Plateau (1)
-
-
Invertebrata
-
Brachiopoda (1)
-
Cnidaria
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Anthozoa
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Zoantharia
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Rugosa (1)
-
-
-
-
Mollusca
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Bivalvia
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Ostreoidea
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Gryphaea (1)
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Pterioida
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Pectinacea
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-
-
-
-
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Cephalopoda
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Ammonites (4)
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Psiloceratida (2)
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-
-
-
Protista
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Foraminifera
-
Miliolina
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Miliolacea (1)
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Rotaliina
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Nodosariacea (1)
-
-
Textulariina
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Ammodiscacea (1)
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-
-
Radiolaria (2)
-
-
-
isotopes
-
stable isotopes
-
C-13/C-12 (6)
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N-15/N-14 (1)
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Nd-144/Nd-143 (1)
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O-18/O-16 (4)
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Os-188/Os-187 (1)
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S-34/S-32 (2)
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Sr-87/Sr-86 (1)
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lava (1)
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Mesozoic
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Antalya Complex (1)
-
Cretaceous
-
Lower Cretaceous
-
Neocomian (1)
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Valanginian (1)
-
-
-
Jurassic
-
Clarens Formation (1)
-
Fernie Formation (1)
-
Lower Jurassic
-
Carixian (2)
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Domerian (2)
-
Dunlin Group (1)
-
Hettangian (21)
-
Laberge Group (1)
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Lotharingian (1)
-
lower Liassic (64)
-
middle Liassic (17)
-
Nordegg Member (1)
-
Pliensbachian (23)
-
Sinemurian (77)
-
Sunrise Formation (1)
-
Toarcian
-
lower Toarcian (1)
-
-
Triassic-Jurassic boundary (1)
-
upper Liassic (10)
-
-
Middle Jurassic
-
Aalenian (5)
-
Bajocian (3)
-
Bathonian (2)
-
Callovian (4)
-
Dogger (1)
-
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Sinemurian
Abstract The most prolific reservoir package in the SW Barents Sea is currently the Upper Triassic–Middle Jurassic Realgrunnen Subgroup, comprising the main hydrocarbon accumulations in the Goliat, Snøhvit and Johan Castberg fields and the Wisting discovery. The interval continues to be the main target as hydrocarbon exploration ventures further into this region. However, the package varies considerably in thickness and reservoir quality throughout the basin, and it is therefore very important to understand how this package developed and what has affected it in the time since it was deposited. Here we review controls on the tectonostratigraphic evolution and facies distribution within the Realgrunnen Subgroup, and exemplify the variability in reservoir characteristics within the subgroup by comparing some key wells in relation to their depositional environment and provenance. New provenance data that record a turnover from reworked Triassic- to Caledonian-sourced mature sediment support facies observations which suggest temporal changes in the depositional environment from marine to fluvial. Much of the variability within the subgroup is attributed the tectonostratigraphic development of the basin that controlled accommodation, facies transitions and sediment distribution. This variability is reflected in subtle differences in reservoir quality important both for exploration and production in the remaining underexplored basin.
High-resolution record of multiple organic carbon-isotope excursions in lacustrine deposits of Upper Sinemurian through Pliensbachian (Early Jurassic) from the Sichuan Basin, China
The Hettangian–Sinemurian (Lower Jurassic) strata of Redcar, Cleveland Basin, NE England: facies and palaeoecology
Tethyan carbonate platform transformations during the Early Jurassic (Sinemurian–Pliensbachian, Southern Alps): Comparison with the Late Triassic Carnian Pluvial Episode
ABSTRACT Lower Mesozoic clastic rocks that unconformably overlie Paleozoic rocks within the Northern Sierra terrane provide clues regarding the evolution of the terrane during a 60 m.y. interval spanning the late Carnian through Bajocian. New detrital-zircon data provide fresh insights into the ages and provenance of these clastic rocks, together with new inferences about the Mesozoic tectonic evolution of the terrane. Previous studies have shown that from the late Carnian to the Sinemurian (~40 m.y.), a 1-km-thick section of subaerial to shallow-marine clastic arc-derived sediment accumulated and shallow-marine carbonate was deposited. At the base of this section, detrital-zircon results suggest the Northern Sierra terrane was located near a source area, possibly the El Paso terrane, containing Permian igneous rocks ranging in age from 270 to 254 Ma. By the earliest Jurassic, the detrital-zircon data suggest the Northern Sierra terrane was located near a source containing latest Triassic–earliest Jurassic igneous rocks spanning 209–186 Ma. The source of this material may have been the Happy Creek volcanic complex of the Black Rock terrane. A deep-marine, anoxic basin developed within the Northern Sierra terrane ca. 187–168 Ma. Approximately 3.5 km of distal turbidites were deposited in this basin. Previously reported geochemical characteristics of these turbidites link the Northern Sierra terrane with arc rock of the Black Rock terrane during this interval, except for a short time in the late Toarcian, when the terrane received an influx of quartz-rich sediment, likely derived from Mesozoic erg deposits now exposed on the Colorado Plateau. Clastic deposition within the Northern Sierra terrane ended in the Bajocian. Eruption of proximal-facies, mafic volcanic rocks and intrusion of hypabyssal rock and 168–163 Ma plutons reflect development of a magmatic arc within the terrane. These igneous rocks represent the first unequivocal evidence that the Northern Sierra terrane was located within a convergent-margin arc during the Triassic and Jurassic. Because detrital-zircon data from Lower Mesozoic strata within the Northern Sierra terrane indicate that it was depositionally linked with differing source areas through time early in the Mesozoic, the terrane may have been mobile along the western margin of Laurentia. There is little evidence from sediment within the Lower Mesozoic section of the terrane that can clearly be tied to the craton or the continental-margin Triassic arc prior to the late Toarcian. The absence of Upper Triassic or Lower Jurassic plutonic rocks within the terrane prior to the mid-Bajocian is also consistent with some form of isolation from the continental-margin arc system. While new detrital-zircon results place the Northern Sierra terrane proximal to the western margin of Laurentia in the late Toarcian, the current location of the terrane likely reflects Early Cretaceous offset along the Mojave–Snow Lake fault.
Detrital zircon U-Pb geochronology of the Sierra de Santa Rosa Formation, Sonora, Mexico, and implications for an Early Jurassic retroarc basin
Carbon-isotope anomalies and demise of carbonate platforms in the Sinemurian (Early Jurassic) of the Tethyan region: evidence from the Southern Alps (Northern Italy)
The evolution of growth patterns in mammalian versus nonmammalian cynodonts
POST-EXTINCTION BIOFACIES OF THE FIRST CARBONATE RAMP OF THE EARLY JURASSIC (SINEMURIAN) IN NE PANTHALASSA (NEW YORK CANYON, NEVADA, USA)
Calcareous nannofossil zonation and sequence stratigraphy of the Jurassic System, onshore Kuwait
EVALUATING TAPHONOMIC BIAS IN A STORM-DISTURBED CARBONATE PLATFORM: EFFECTS OF COMPOSITIONAL AND ENVIRONMENTAL FACTORS IN LOWER JURASSIC BRACHIOPOD ACCUMULATIONS (EASTERN SUBBETIC BASIN, SPAIN)
DINOSAUR FOOTPRINTS AS ULTIMATE EVIDENCE FOR A TERRESTRIAL ENVIRONMENT IN THE LATE SINEMURIAN TRENTO CARBONATE PLATFORM
Jurassic rifting evolution of the Apennines and Southern Alps (Italy): Parallels and differences
The palynology of the Pabay Shale Formation (Lower Jurassic) of SW Raasay, northern Scotland
Major perturbation in sulfur cycling at the Triassic-Jurassic boundary
A Dominant Tectonic Signal in High-Frequency, Peritidal Carbonate Cycles? A Regional Analysis of Liassic Platforms from Western Tethys
Early Jurassic normal faulting in a carbonate extensional basin: characterization of tectonically driven platform drowning (High Atlas rift, Morocco)
Gryphaea beds (upper Scunthorpe Mudstone Formation; Lower Jurassic) at Scunthorpe, North Lincolnshire, north-east England
BASAL SAUROPODOMORPHS (DINOSAURIA: SAURISCHIA) FROM THE LOWER JURASSIC OF INDIA: THEIR ANATOMY AND RELATIONSHIPS
The restricted Gemuk Group: A Triassic to Lower Cretaceous succession in southwestern Alaska
New data from an Upper Triassic to Lower Cretaceous deep marine succession—the herein reinstated and restricted Gemuk Group—provide a vital piece of the puzzle for unraveling southwestern Alaska's tectonic history. First defined by Cady et al. in 1955 , the Gemuk Group soon became a regional catchall unit that ended up as part of at least four different terranes. In this paper we provide the first new data in nearly half a century from the Gemuk Group in the original type area in Taylor Mountains quadrangle and from contiguous rocks to the north in Sleetmute quadrangle. Discontinuous exposure, hints of complex structure, the reconnaissance level of our mapping, and spotty age constraints together permit definition of only a rough stratigraphy. The restricted Gemuk Group is at least 2250 m thick, and could easily be at least twice as thick. The age range of the restricted Gemuk Group is tightened on the basis of ten radiolarian ages, two new bivalve ages, one conodont age, two U-Pb zircon ages on tuff, and U-Pb ages of 110 detrital zircons from two sandstones. The Triassic part of the restricted Gemuk Group, which consists of intermediate pillow lavas interbedded with siltstone, chert, and rare limestone, produced radiolarians, bivalves, and conodonts of Carnian and Norian ages. The Jurassic part appears to be mostly siltstone and chert, and yielded radiolarians of Hettangian-Sinemurian, Pliensbachian-Toarcian, and Oxfordian ages. Two tuffs near the Jurassic-Cretaceous boundary record nearby arc volcanism: one at 146 Ma is interbedded with red and green siltstone, and a second at ca. 137 Ma is interbedded with graywacke turbidites. Graywacke appears to be the dominant rock type in the Lower Cretaceous part of the restricted Gemuk Group. Detrital zircon analyses were performed on two sandstone samples using SHRIMP. One sandstone yielded a dominant age cluster of 133–180 Ma; the oldest grain is only 316 Ma. The second sample is dominated by zircons of 130–154 Ma; the oldest grain is 292 Ma. The youngest zircons are probably not much older than the sandstone itself. Point counts of restricted Gemuk Group sandstones yield average ratios of 24/29/47 for Q/F/L, 15/83/2 for Ls/Lv/Lm, and 41/48/11 for Qm/P/K. In the field, sandstones of the restricted Gemuk Group are not easily distinguished from sandstones of the overlying Upper Cretaceous turbidite-dominated Kuskokwim Group. Petrographically, however, the restricted Gemuk Group has modal K-feldspar, whereas the Kuskokwim Group generally does not (average Qm/P/K of 64/36/0). Some K-feldspar-bearing graywacke that was previously mapped as Kuskokwim Group ( Cady et al., 1955 ) is here reassigned to the restricted Gemuk Group. Major- and trace-element geochemistry of shales from the restricted Gemuk Group and the Kuskokwim Group show distinct differences. The chemical index of alteration (CIA) is distinctly higherforshales of the Kuskokwim Group than forthose of the restricted Gemuk Group, suggesting more intense weathering during deposition of the Kuskokwim Group. The restricted Gemuk Group represents an estimated 90–100 m.y. of deep-water sedimentation, first accompanied by submarine volcanism and later by nearby explosive arc activity. Two hypotheses are presented for the tectonic setting. One model that needs additional testing is that the restricted Gemuk Group consists of imbricated oceanic plate stratigraphy. Based on available information, our preferred model is that it was deposited in a back-arc, intra-arc, or forearc basin that was subsequently deformed. The terrane affinity of the restricted Gemuk Group is uncertain. The rocks of this area were formerly assigned to the Hagemeister subterrane of the Togiak terrane—a Late Triassic to Early Cretaceous arc—but our data show this to be a poor match. None of the other possibilities (e.g., Nukluk and Tikchik subterranes of the Goodnews terrane) is viable; hence, the terrane subdivision and distribution in southwestern Alaska may need to be revisited. The geologic history revealed by our study of the restricted Gemuk Group gives us a solid toehold in unraveling the Mesozoic paleogeography of this part of the northern Cordillera.