Geologic Map of the Yukon-Koyukuk Basin, Alaska

Patton, W.W.; Wilson, Frederic H.; Labay, Keith A.; Shew, Nora B.

doi:10.3133/sim2909

Cited by 9 publications

(10 citation statements)

References 32 publications

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“…4I -800 L). Based upon field/petrographic observations, the Type 3 sediments of this study are 801 similar to lithologic descriptions of the uppermost conglomerate and non-marine 802 sandstone unit of Patton et al (2009) andDillon (1989). Fossil flora reported from these 803 types of sediments are Albian to Cenomanian in age (Dillon, 1989, Nilsen, 1989.…”

Section: Basin 796mentioning

confidence: 52%

“…4 -6). The correlation of the Type 1 sediments with mafic-to 704 ultramafic-rich units of Patton et al (2009) suggests that the Type 1 sediments may 705 represent the lowermost sedimentary rock unit in the Kobuk Koyukuk sub-basin. Type 1 706 sample BRJR13-K8a yields a maximum depositional age of 107 Ma.…”

Section: Unroofing Of the Brooks Range And Ruby Terrane 696mentioning

confidence: 97%

“…Regional tectonic interpretations of the basin have been influenced by the 90 occurrence of arc-affinity volcanic rocks that form the base of the Yukon Koyukuk 91 sedimentary succession within the interior of the Yukon-Koyukuk Basin (Figs. 1 and 2) 92 7 Patton et al, 2009;Dillon, 1989;Nilsen, 1989). 139…”

Section: Basin 87mentioning

confidence: 99%

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Provenance, U-Pb detrital zircon geochronology, Hf isotopic analyses, and Cr-spinel geochemistry of the northeast Yukon-Koyukuk Basin: Implications for interior basin development and sedimentation in Alaska

et al. 2017

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21The Yukon Koyukuk Basin is a large depression that covers ~118,000 sq. km in 22 western interior Alaska that is divided into two sub-basins by a volcanic arc assemblage. Sedimentary basins that flank orogenic belts serve as archives that record the 58 long-term deformational and uplift history of orogenic systems. When associated with a 59 topographic effect, the kinematic evolution of an orogen affects the geometry, filling 60 pattern, and provenance signature of the adjacent synorogenic sedimentary basins 61 (Bayona, et al., 2008). Processes such as tectonic uplift and surficial denudation, rainfall, 62 sediment supply, sediment transport and dispersal have direct implications on the 63 evolution of synorogenic sediment routing systems (Whitchurch et al., 2011). As 64 observed in several Cenozoic orogenic belts (e.g. Himalayas and Andes), differences in 65 sedimentary filling patterns are recognizable by variations in large-scale axial and 66 transverse river systems and smaller transverse rivers observed draining into and within 67 the foreland and hinterland basins separated by an orogenic high (Burbank et al., 1996; 68 Clark et al., 2004; DeCelles, 2012; Dietze et al., 2014; Hessler and Fildani, 2015). This 69 4 variation in drainage systems leads to differences in provenance signatures recorded 70 within the basin sediments (Lease et al., 2007; Bayona, et al., 2008; Cina, et al., 2009; 71 DeCelles et al., 2014). Therefore, the provenance signature of the sediments that occupy 72 these basins should help in understanding the evolution of the synorogenic sediment 73 routing systems on either side of the orogen. 74In northern Alaska, the latest Jurassic -Early Cretaceous Brooks Range orogen is 75 flanked by two synorogenic sedimentary basins, the northern Colville foreland basin and 76 southern Yukon Koyukuk Basin (Fig. 1). Renewed deposition of thick successions of 77 clastic rocks in the Colville Basin occurred coincidently with the formation of Yukon 78Koyukuk Basin, which led authors to conclude that these events were the result of 79 orogenic uplift of the Brooks Range (Molenaar et al., 1984(Molenaar et al., , 1986 Miller and Hudson, 80 1991;Till, 1992). Seismic reflection data collected within the Colville Basin delineate a 81 series of turbidite-dominated sedimentary packages that longitudinally filled the basin 82 from west to northeast from the late Early Cretaceous to the Cenozoic (Houseknecht et 83 al., 2009; Houseknecht and Wartes, 2013). Despite all the work performed in 84 characterizing the clastic rocks of the Colville Basin, little emphasis has been paid to 85 understanding the formation and sedimentary evolution of the southern Yukon Koyukuk 86 Basin. 87The Yukon Koyukuk Basin is a large wedge-shaped physiographic depression, 88 underlain by volcanic and marine sedimentary rock units, that covers ~118,000 sq. km 89 (Fig. 1) formed in a syn-collisional forearc setting (Till et al., 1993) to its formation during post-95 accretion lithospheric extension of the hinterlan...

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Section: Basin 796mentioning

confidence: 52%

Section: Unroofing Of the Brooks Range And Ruby Terrane 696mentioning

confidence: 97%

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Provenance, U-Pb detrital zircon geochronology, Hf isotopic analyses, and Cr-spinel geochemistry of the northeast Yukon-Koyukuk Basin: Implications for interior basin development and sedimentation in Alaska

et al. 2017

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“…Quaternary deposits of the study area comprise Holocene floodplain deposits and undivided Holocene and Pleistocene deposits, including alluvial, colluvial, glacial and aeolian deposits (Patton et al ., ). Within the Yukon‐Koyukuk lowland, Weber and Péwé () distinguished floodplain alluvium, younger (low) and older (high) terrace deposits, aeolian sand dunes and loess deposits in the foothills.…”

Section: Study Areamentioning

confidence: 97%

Cryostratigraphy and Permafrost Evolution in the Lacustrine Lowlands of West‐Central Alaska

Kanevskiy

Jorgenson

Shur

et al. 2014

Permafrost & Periglacial

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The influence of permafrost growth and thaw on the evolution of ice-rich lowland terrain in the Koyukuk-Innoko region of interior Alaska is fundamental but poorly understood. To elucidate this influence, the cryostratigraphy and properties of perennially frozen sediments from three areas in this region are described and interpreted in terms of permafrost history. The upper part of the late Quaternary sediments at the Koyukuk and Innoko Flats comprise frozen organic soils up to 4.5 m thick underlain by ice-rich silt characterised by layered and reticulate cryostructures. The volume of visible segregated ice in silt locally reaches 50 per cent, with ice lenses up to 10 cm thick. A conceptual model of terrain evolution from the Late Pleistocene to the present day identifies four stages of yedoma degradation and five stages of subsequent permafrost aggradation-degradation: (1) partial thawing of the upper ice wedges and the formation of small shallow ponds in the troughs above the wedges; (2) formation of shallow thermokarst lakes above the polygons; (3) deepening of thermokarst lakes and yedoma degradation beneath the lakes; (4) complete thawing of yedoma beneath the lakes; (5) lake drainage; (6) peat accumulation; (7) permafrost aggradation in drained lake basins; (8) formation of permafrost plateaus; and (9) formation and expansion of a new generation of thermokarst features. These stages can occur in differing places and times, creating a highly complex mosaic of terrain conditions, complicating predictions of landscape response to future climatic changes or human impact.

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“…A large granodiorite body (Kgd) is located SW and up valley from the hot springs. The granodiorites range in age from 89-78 Ma in the Yukon-Koyukuk basin 2 . Seismic activity in the region is documented with the Kobuk fault to the north having a 4.6M earthquake in 1980 3 .…”

Section: Geologic Backgroundmentioning

confidence: 99%

NANA Geothermal Assessment Program Final Report

Hermanson¹

2010

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Geologic Map of the Yukon-Koyukuk Basin, Alaska

Cited by 9 publications

References 32 publications

Provenance, U-Pb detrital zircon geochronology, Hf isotopic analyses, and Cr-spinel geochemistry of the northeast Yukon-Koyukuk Basin: Implications for interior basin development and sedimentation in Alaska

Provenance, U-Pb detrital zircon geochronology, Hf isotopic analyses, and Cr-spinel geochemistry of the northeast Yukon-Koyukuk Basin: Implications for interior basin development and sedimentation in Alaska

Cryostratigraphy and Permafrost Evolution in the Lacustrine Lowlands of West‐Central Alaska

NANA Geothermal Assessment Program Final Report

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