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Journal articles on the topic 'Cassiar Mountains British Columbia'

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Published: 4 June 2021

Last updated: 16 February 2022

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1

Grice, J. D., and R. A. Gault. "Jade, Gold, and TOPAZ:From the Cassiar Mountains, British Columbia/Yukon Territory, Canada." Rocks & Minerals 60, no. 1 (January 1985): 9–13. http://dx.doi.org/10.1080/00357529.1985.11764360.

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2

Butler, R. F., T. A. Harms, and H. Gabrielse. "Cretaceous remagnetization in the Sylvester Allochthon: limits to post-105 Ma northward displacement of north-central British Columbia." Canadian Journal of Earth Sciences 25, no. 8 (August 1, 1988): 1316–22. http://dx.doi.org/10.1139/e88-126.

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The Sylvester Allochthon of the Slide Mountain Terrane in northern British Columbia is a structurally interleaved assemblage of ocean-floor lithologies ranging in age from Late Devonian to Late Triassic. It is the most inboard of oceanic suspect terranes and rests as a vast klippe on miogeoclinal strata of the Cassiar Terrane. The Sylvester Allochton and the Cassiar Terrane lie west of the Northern Rocky Mountain Trench Fault. Both the Sylvester Allochthon and the Cassiar Terrane are intruded by mid-Cretaceous (105 Ma) granite of the Cassiar Batholith. Six oriented cores were collected at each of 12 sites in Guadalupian Parafusulina-bearing limestone of the Sylvester Allochthon at a location 4 km from the batholith. Isothermal remanent magnetization (IRM) acquisition and subsequent thermal demagnetization indicate that pyrrhotite is the dominant ferrimagnetic mineral. Least-squares line fitting to four thermal demagnetization steps between 150 and 310 °C was used to determine the characteristic natural remanent magnetization (NRM) directions that fail the fold test at the 99.5% confidence level. We interpret these observations as indicating that the NRM is a thermoremanent or thermochemical remanent magnetism associated with intrusion of the Cassiar Batholith. The resulting paleomagnetic pole location is latitude = 75.7°N, longitude = 171.7°E, α95 = 8.5°. When compared with the mid-Cretaceous pole for cratonic North America, a small but significant clockwise rotation (R ± ΔR = 23.9 ± 18.1 °) is evident, but poleward translation (p ± Δp = 5.3 ± 9.2°) is not significant at the 95% confidence level. The paleomagnetic results are consistent with geological evidence for moderate (700 km) northward transport of the Cassiar Terrane (along with the previously emplaced overlying Sylvester Allochthon) during mid-Cretaceous to Tertiary dextral transcurrent faulting.

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3

Pyle, Leanne J., and Christopher R. Barnes. "Conodonts from the Kechika Formation and Road River Group (Lower to Upper Ordovician) of the Cassiar Terrane, northern British Columbia." Canadian Journal of Earth Sciences 38, no. 10 (October 1, 2001): 1387–401. http://dx.doi.org/10.1139/e01-033.

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This study examines the lower Paleozoic stratigraphy of the Cassiar Terrane from three key sections comprising an east-west transect across the terrane. The Cassiar Terrane, west of the Northern Rocky Mountain Trench, consists of a Neoproterozoic to Triassic succession and is a fragment of the Cordilleran Miogeocline that has been displaced northward. The amount of displacement from its original position remains controversial. Conodonts from the Cassiar Terrane have been previously reported from only a few reconnaissance studies. More than 3000 m of strata have been measured and examined in detail and 85 conodont samples collected. A total of 926 identifiable conodont elements are assigned to 31 species representing 21 genera. The conodonts are mainly representative of the Midcontinent Faunal Realm, but some also represent the Atlantic Realm. Conodonts from the upper Kechika Formation and base of the Road River Group are Early Ordovician (Tremadocian) in age, and those from the upper Road River Group range into the Upper Ordovician (Caradocian). The detailed Ordovician stratigraphy and temporal constraints established by conodont biostratigraphy provide for correlation to coeval facies of ancestral North America. The onset of Road River sedimentation in the mid-Tremadocian is, however, older than that in the Macdonald Platform to the east (early Arenigian). This onset timing may help link the Cassiar Terrane to a specific part of the miogeocline from which it was transported.

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4

Nelson, JoAnne, and Richard Friedman. "Superimposed Quesnel (late PaleozoicJurassic) and YukonTanana (DevonianMississippian) arc assemblages, Cassiar Mountains, northern British Columbia: field, UPb, and igneous petrochemical evidence." Canadian Journal of Earth Sciences 41, no. 10 (October 1, 2004): 1201–35. http://dx.doi.org/10.1139/e04-028.

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Allochthons in the Cassiar Mountains of northern British Columbia contain assemblages belonging to two distinct Canadian Cordilleran terranes, YukonTanana (YTT) and Quesnellia. These assemblages, of pre-Late Devonian, DevonianMississippian, PennsylvanianPermian, and Early Jurassic age, occur in intrusive and depositional, as well as structural, contact with each other. The allochthons are gently dipping thrust panels, interrupted by the mid-Cretaceous Cassiar Batholith. A key element for correlation across the batholith is the Mississippian and older pericratonic Dorsey Complex. New DevonianMississippian UPb ages for deformed plutons within it document an igneous suite like those in type YukonTanana exposures farther north. Other characteristics of the Dorsey Complex that ally it with YTT are orthoquartzites and grits, and amphibolite bodies with transitional mid-ocean ridge basalt (MORB) to ocean-island basalt (OIB) petrochemical signatures. Unconformities, deformed clasts in the late Paleozoic sequences, and a shared mid-Permian intrusive suite show that later arcs onlapped the mid-Paleozoic and older YTT assemblage. The Early Jurassic intrusive suite cuts all major contacts and fabrics except the terrane-bounding fault between the Slide Mountain and combined YTTQuesnel terranes. It represents a northern continuation of a plutonic belt that extends the length of the Mesozoic Quesnel magmatic arc. These relationships carry important implications for Cordilleran terrane history and the tectonic evolution of the North American margin. At least some of the major terranes were not unrelated entities prior to their accretion to the continent, but a system of superimposed and interconnected arcs that developed over a protracted time interval, with complex and evolving paleogeographic configurations much like the modern western Pacific province.

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5

Nelson, JoAnne L. "The Sylvester Allochthon: upper Paleozoic marginal-basin and island-arc terranes in northern British Columbia." Canadian Journal of Earth Sciences 30, no. 3 (March 1, 1993): 631–43. http://dx.doi.org/10.1139/e93-048.

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The Sylvester Allochthon is a composite klippe of upper Paleozoic ophiolitic, island-arc, and pericratonic assemblages, which rests directly on the Cassiar terrane, a displaced sliver of Ancestral North America. Each tectonic assemblage occurs at a distinct and consistent structural level within the allochthon. They are assigned, respectively, to the Slide Mountain, Harper Ranch, and Yukon–Tanana terranes. The Sylvester Allochthon provides a view of the structural relationships between these terranes prior to Early Cretaceous – early Tertiary strike-slip dismemberment, as well as possible sedimentological links to late Paleozoic North America. Slide Mountain Terrane assemblages, designated divisions I and II, form the lowest structural panels. Chert – quartz sandstones are interbedded with Lower Mississippian deep-water sediments in division I and ocean-floor basalts and deep-water sediments in division II. They are similar in age and character to sandstones in the autochthonous Earn Group. Division II assemblages represent atypical oceanic crust and upper mantle assemblages. Continuous basalt–sedimentary sequences, well dated by conodont faunas, span Early Mississippian to mid-Permian time. Feeders for the basalts are sills rather than sheeted dyke swarms, suggesting very slow spreading and high(?) sedimentation rates in a marginal-basin setting. These supracrustal sequences are thrust-imbricated with ultramafite–gabbro panels. Division II is in part overlain by a Triassic siliciclastic and limy sedimentary sequence, which resembles the basal Takla Group, Slocan Group, and autochthonous Triassic units. Division III occupies the highest structural levels in the allochthon. With one exception, thrust sheets within it consist of Pennsylvanian to Upper Permian mixed calc-alkaline volcanic and plutonic rocks, chert, tuff, and limestone, assigned to the Harper Ranch Terrane. One panel, assigned to the Yukon–Tanana Terrane, consists of an Early Mississippian quartz diorite pluton with Precambrian inheritance that intrudes older volcanogenic sediments, pyroclastics, limestone, and siliciclastic sediments. Preferred pre-Mesozoic restoration of these terrane elements shows a Harper Ranch arc, built partly on pericratonic Yukon–Tanana and partly on primitive oceanic basement (division III), which is separated from North America by the Slide Mountain marginal basin (divisions I and II).

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6

Pyle, Leanne J., and Christopher R. Barnes. "Lower Paleozoic stratigraphic and biostratigraphic correlations in the Canadian Cordillera: implications for the tectonic evolution of the Laurentian margin." Canadian Journal of Earth Sciences 40, no. 12 (December 1, 2003): 1739–53. http://dx.doi.org/10.1139/e03-049.

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The ancient Laurentian margin rifted in the latest Neoproterozoic to early Cambrian but appears not to have developed as a simple passive margin through a long, post-rift, drift phase. Stratigraphic and conodont biostratigraphic information from four platform-to-basin transects across the margin has advanced our knowledge of the early Paleozoic evolution of the margin. In northeastern British Columbia, two northern transects span the Macdonald Platform to Kechika Trough and Ospika Embayment, and a third transect spans the parautochthonous Cassiar Terrane. In the southern Rocky Mountains, new conodont biostratigraphic data for the Ordovician succession of the Bow Platform is correlated to coeval basinal facies of the White River Trough. In total, from 26 stratigraphic sections, over 25 km of strata were measured and > 1200 conodont samples were collected that yielded over 100 000 conodont elements. Key zonal species were used for regional correlation of uppermost Cambrian to Middle Devonian strata along the Cordillera. The biostratigraphy temporally constrains at least two periods of renewed extension along the margin, in the latest Cambrian and late Early Ordovician. Alkalic volcanics associated with abrupt facies changes across the ancient shelf break, intervals of slope debris breccia deposits, and distal turbidite flows suggest the margin was characterized by intervals of volcanism, basin foundering, and platform flooding. Siliciclastics in the succession were sourced by a reactivation of tectonic highs, such as the Peace River Arch. Prominent hiatuses punctuate the succession, including unconformities of early Late Ordovician, sub-Llandovery, possibly Early to Middle Silurian and Early Devonian ages.

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7

Ferri, Filippo. "Nina Creek Group and Lay Range Assemblage, north-central British Columbia: remnants of late Paleozoic oceanic and arc terranes." Canadian Journal of Earth Sciences 34, no. 6 (June 1, 1997): 854–74. http://dx.doi.org/10.1139/e17-070.

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In north-central British Columbia, a belt of upper Paleozoic volcanic and sedimentary rocks lies between Mesozoic arc rocks of Quesnellia and Ancestral North America. These rocks belong to two distinct terranes: the Nina Creek Group of the Slide Mountain terrane and the Lay Range Assemblage of the Quesnel terrane. The Nina Creek Group is composed of Mississippian to Late Permian argillite, chert, and mid-ocean-ridge tholeiitic basalt, formed in an ocean-floor setting. The sedimentary and volcanic rocks, the Mount Howell and Pillow Ridge successions, respectively, form discrete, generally coeval sequences interpreted as facies equivalents that have been interleaved by thrusting. The entire assemblage has been faulted against the Cassiar terrane of the North American miogeocline. West of the Nina Creek Group is the Lay Range Assemblage, correlated with the Harper Ranch subterrane of Quesnellia. It includes a lower division of Mississippian to Early Pennsylvanian sedimentary and volcanic rocks, some with continental affinity, and an upper division of Permian island-arc, basaltic tuffs and lavas containing detrital quartz and zircons of Proterozoic age. Tuffaceous horizons in the Nina Creek Group imply stratigraphic links to a volcanic-arc terrane, which is inferred to be the Lay Range Assemblage. Similarly, gritty horizons in the lower part of the Nina Creek Group suggest links to the paleocontinental margin to the east. It is assumed that the Lay Range Assemblage accumulated on a piece of continental crust that rifted away from ancestral North America in the Late Devonian to Early Mississippian by the westward migration of a west-facing arc. The back-arc extension produced the Slide Mountain marginal basin in which the Nina Creek Group was deposited. Arc volcanism in the Lay Range Assemblage and other members of the Harper Ranch subterrane was episodic rather than continuous, as was ocean-floor volcanism in the marginal basin. The basin probably grew to a width of hundreds rather than thousands of kilometres.

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8

Anderson, P. G., and C. Jay Hodgson. "The structure and geological development of the Erickson gold mine, Cassiar District, British Columbia, with implications for the origin of mother-lode-type gold deposits." Canadian Journal of Earth Sciences 26, no. 12 (December 1, 1989): 2645–60. http://dx.doi.org/10.1139/e89-225.

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The Erickson gold mine is a typical gold quartz vein deposit. The veins are hosted by a thrust-imbricated, gently dipping, synformal allochthon of low-grade metamorphic, Devonian to Upper Triassic basalts, argillites, and peridotites of oceancrustal origin belonging to the Sylvester Group, part of the Slide Mountain assemblage. The Sylvester allochthon lies concordantly on Devonian miogeoclinal sedimentary rocks of the North American continental margin and was emplaced in the Middle Jurassic as a result of the collision of the Quesnel arc with North America. The veins in the mine are hosted mainly by a moderately dipping system of shear zones with approximately orthorhombic symmetry, indicating a triaxial bulk, inhomogeneous strain pattern superimposed on the earlier formed, gently dipping thrusts. Steeply dipping extension veinlets, rotation of schistosity, and downdip slickenlines indicate the maximum shortening axis was subvertical. The veins display complex superimposed ribbon and breccia textures, indicating incremental growth. Most of the gold occurs in association with tetrahedrite, sphalerite, and chalcopyrite in steeply dipping, late, grey quartz veinlets localized within and striking perpendicular to the main veins. The vein-forming event, dated at 130 Ma, appears to have been related to extension and high heat flow associated with the rise of the Omenica geanticline, in turn the result of crustal thickening caused by the collision of the amalgamated Quesnel arc – North America plate with Stikinia in the Middle Jurassic.

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9

Sketchley, Dale A., A. J. Sinclair, and C. I. Godwin. "Early Cretaceous gold–silver mineralization in the Sylvester allochthon, near Cassiar, north central British Columbia." Canadian Journal of Earth Sciences 23, no. 9 (September 1, 1986): 1455–58. http://dx.doi.org/10.1139/e86-139.

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K–Ar dates on sericite from several gold–silver bearing white quartz veins in the Cassiar area indicate that mineralization occurred in the Early Cretaceous at about 130 Ma. Thus, these veins predate the mid-Cretaceous Cassiar batholith and Late Cretaceous and early Tertiary plutons in the immediate area. The Early Cretaceous date probably represents either a thermal precursor to emplacement of the Cassiar batholith or a structurally related event associated with allochthonous emplacement of the Sylvester Group. Either of these events may have caused circulation of the meteoric fluids responsible for the veins.

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10

Erdmer, P., and H. Baadsgaard. "2.2 Ga age of zircons in three occurrences of Upper Proterozoic clastic rocks of the northern Cassiar terrane, Yukon and British Columbia." Canadian Journal of Earth Sciences 24, no. 9 (September 1, 1987): 1919–24. http://dx.doi.org/10.1139/e87-182.

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Analyses of detrital zircons from three occurrences of Upper Proterozoic clastic rocks of the northern Cassiar terrane in Yukon and northern British Columbia yield a U–Pb age of 2224 ± 22 Ma. The zircons apparently belong to a single population similar in age to zircons in stratigraphically equivalent rocks of the southern Cassiar terrane and to zircons in rocks in the Yukon–Tanana terrane of Alaska. A source terrane or area of the required age and extent has not yet been identified.

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11

Pope, Michael C., and James W. Sears. "Cassiar platform, north-central British Columbia: A miogeoclinal fragment from Idaho." Geology 25, no. 6 (1997): 515. http://dx.doi.org/10.1130/0091-7613(1997)025<0515:cpncbc>2.3.co;2.

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12

Sketchley, D. A., and A. J. Sinclair. "Carbonate alteration in basalt, Total Erickson gold mine, Cassiar, northern British Columbia, Canada." Economic Geology 86, no. 3 (May 1, 1991): 570–87. http://dx.doi.org/10.2113/gsecongeo.86.3.570.

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13

Apps, Clayton D., Bruce N. McLellan, Trevor A. Kinley, and John P. Flaa. "Scale-Dependent Habitat Selection by Mountain Caribou, Columbia Mountains, British Columbia." Journal of Wildlife Management 65, no. 1 (January 2001): 65. http://dx.doi.org/10.2307/3803278.

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14

Hägeli, Pascal, and David M. McClung. "Avalanche characteristics of a transitional snow climate—Columbia Mountains, British Columbia, Canada." Cold Regions Science and Technology 37, no. 3 (November 2003): 255–76. http://dx.doi.org/10.1016/s0165-232x(03)00069-7.

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15

Johnston, Katherine S., Bruce Jamieson, and Alan Jones. "Estimating extreme avalanche runout for the Columbia Mountains and Fernie area Rocky Mountains of British Columbia, Canada." Canadian Geotechnical Journal 49, no. 11 (November 2012): 1309–18. http://dx.doi.org/10.1139/t2012-079.

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Extreme snow avalanche runout is typically estimated using a combination of historical and vegetation records as well as statistical and dynamic models. The two classes of statistical models (α–β and runout ratio) are based on estimating runout distance past the β-point, which is typically defined as the point where the avalanche slope incline first decreases to 10°. The parameters for these models vary from mountain range to mountain range. In Canada, α–β and runout ratio parameters have been published for the combined Rocky and Purcell Mountains and for the British Columbia Coast Mountains. Despite active development, no suitable tall avalanche path model parameters have been published for the Columbia Mountains or for the Lizard Range area around Fernie, B.C. Using a dataset of 65 avalanche paths, statistical model parameters have been derived for these regions.

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16

McClung, D. M. "Characteristics of terrain, snow supply and forest cover for avalanche initiation caused by logging." Annals of Glaciology 32 (2001): 223–29. http://dx.doi.org/10.3189/172756401781819391.

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AbstractThis paper contains statistical analyses of parameters to characterize starting zones of destructive avalanches which have resulted from clear-cut logging in British Columbia, Canada. Data from 76 avalanche sites in the Coast Mountains (western British Columbia) and the Columbia Mountains (eastern British Columbia) are analyzed. The parameters include a selection which characterize snow supply (related to potential avalanche frequency), avalanche magnitude and those which are known to affect avalanche formation including terrain features, vegetation density, vegetation height and ground surface roughness. The results provide the data framework for possibly preventing future disasters by altering logging plans.

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17

Evans, S. G., John J. Clague, G. J. Woodsworth, and O. Hungr. "The Pandemonium Creek rock avalanche, British Columbia." Canadian Geotechnical Journal 26, no. 3 (August 1, 1989): 427–46. http://dx.doi.org/10.1139/t89-056.

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In 1959, a rock spur became detached from the headwall of a cirque near Pandemonium Creek in the southern Coast Mountains of British Columbia. Approximately 5 × 106 m3 of blocky, gneissic quartz diorite debris travelled 9.0 km along a highly irregular path, descending a vertical distance of 2 km to the valley of South Atnarko River. The high mobility of the rock avalanche is manifested by superelevation in valley bends, two run-ups, and two right-angle changes in flow direction. This mobility is due, in part, to (1) peculiarities in the path of the landslide (lateral moraines, for example, funnelled and accelerated the debris) and (2) travel over a glacier below the detachment zone. Although most of the debris came to rest on the upper part of a fan at the mouth of Pandemonium Creek, one lobe traversed the fan and entered Knot Lakes, where it generated displacement waves that destroyed trees along the shore.Run-up and superelevation data indicate that the debris was moving between 81 and 100 m/s as it entered the run-up zone at Pandemonium Creek and 21–38 m/s in Pandemonium valley to the east. These velocities were analysed by applying the dynamic model of H.J. Körner (Rock Mechanics, 1976, 8: 225–256) to the path of the landslide. The analysis suggests that the rock avalanche had two phases: a very rapid initial phase from detachment to the beginning of the run-up, and, following sudden energy losses at the run-up, a second phase involving much lower velocities.The Pandemonium Creek landslide is similar in many respects to much larger, highly mobile rock avalanches in other parts of the world, for example, Huascarán (Peru) and Little Tahoma Peak (Washington, U.S.A.). Although much less common than rockfalls and debris flows, rock avalanches are capable of far greater damage. This is a consequence of their size and the fact that they travel great distances at high velocities. The potential exists for other highly mobile landslides of the Pandemonium Creek type in the mountains of western Canada, highlighting the need for caution in the future development of this region. Key words: rock avalanche, dynamic analysis, mobile landslides, evaluation, run-up, superelevation, mountains.

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18

Rominger, Eric M., and John L. Oldemeyer. "Early-Winter Habitat of Woodland Caribou, Selkirk Mountains, British Columbia." Journal of Wildlife Management 53, no. 1 (January 1989): 238. http://dx.doi.org/10.2307/3801341.

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19

Mood, Bryan J., and Dan J. Smith. "Holocene glacier activity in the British Columbia Coast Mountains, Canada." Quaternary Science Reviews 128 (November 2015): 14–36. http://dx.doi.org/10.1016/j.quascirev.2015.09.002.

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20

Menounos, Brian, Johannes Koch, Gerald Osborn, John J. Clague, and David Mazzucchi. "Early Holocene glacier advance, southern Coast Mountains, British Columbia, Canada." Quaternary Science Reviews 23, no. 14-15 (July 2004): 1543–50. http://dx.doi.org/10.1016/j.quascirev.2003.12.023.

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21

Root, Kevin G. "Extensional duplex in the Purcell Mountains of southeastern British Columbia." Geology 18, no. 5 (1990): 419. http://dx.doi.org/10.1130/0091-7613(1990)018<0419:editpm>2.3.co;2.

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22

Terry, E., B. McLellan, G. Watts, and J. Flaa. "Early Winter Habitat Use by Mountain Caribou in the North Cariboo and Columbia Mountains, British Columbia." Rangifer 16, no. 4 (January 1, 1996): 133. http://dx.doi.org/10.7557/2.16.4.1229.

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Winter habitat use was compared between two mountain caribou (Rangifer tarandus caribou) populations in British Columbia. Regional differences were apparent during November and December. Radio-collared caribou inhabiting the gentle plateaus of the northern Cariboo Mountains, near Prince George, B.C. primarily used mid-elevation balsam-spruce stands on moderate slopes (<30%). In contrast, radio-collared caribou in the North Columbia Mountains, near Revelstoke, B.C. used low elevation hemlock-cedar stands and relatively steeper slopes (>30%). To adequately address habitat requirements of caribou, forest management plans should incorporate varying regional and seasonal habitat use patterns. Hypotheses on observed differences in habitat use are discussed.

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23

O'Hanley, David S., Eva S. Schandl, and Frederick J. Wicks. "The origin of rodingites from Cassiar, British Columbia, and their use to estimate T and P(H2O) during serpentinization." Geochimica et Cosmochimica Acta 56, no. 1 (January 1992): 97–108. http://dx.doi.org/10.1016/0016-7037(92)90119-4.

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24

Driver, L. A., R. A. Creaser, T. Chacko, and P. Erdmer. "Petrogenesis of the Cretaceous Cassiar batholith, Yukon-British Columbia, Canada: Implications for magmatism in the North American Cordilleran Interior." Geological Society of America Bulletin 112, no. 7 (July 1, 2000): 1119–33. http://dx.doi.org/10.1130/0016-7606(2000)112<1119:potccb>2.0.co;2.

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25

Souch, Catherine. "New radiocarbon dates for early deglaciation from the southeastern Coast Mountains of British Columbia." Canadian Journal of Earth Sciences 26, no. 10 (October 1, 1989): 2169–71. http://dx.doi.org/10.1139/e89-182.

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Basal dates obtained on organic material from postglacial lacustrine sediments from four lakes in the Kwoiek Creek watershed, southern Coast Mountains of British Columbia, provide minimum dates of deglaciation. The dates obtained (12 255 ± 770, 11 485 ± 185, 10 385 ± 595, and 9640 ± 380 BP), at elevations 835–1120 m, suggest that extensive areas of the mountains of southern British Columbia were ice free prior to 11 500 years ago. This has implications for models of the regional deglaciation of the southern portion of the province.

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26

Seip, D. R., and D. B. Cichowski. "Population Ecology of Caribou in British Columbia." Rangifer 16, no. 4 (January 1, 1996): 73. http://dx.doi.org/10.7557/2.16.4.1223.

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The abundance and geographic range of woodland caribou (Rangifer tarandus caribou) decreased in many areas of British Columbia during the 1900's. Recent studies have found that predation during the summer is the major cause of mortality and current population declines. Increased moose {Alecs alces) populations may be related to past and current caribou declines by sustaining greater numbers of wolves (Canis lupus). Mortality rates were greater in areas where caribou calved in forested habitats, in close proximity to predators and moose. Caribou populations which had calving sites in alpine areas, islands, and rugged mountains experienced lower mortality and were generally stable or increasing. A predator-induced population decline in one area appeared to stabilize at low caribou densities, suggesting that the wolf predation rate may be density dependent.

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27

Pell, J., and P. S. Simony. "New correlations of Hadrynian strata, south-central British Columbia." Canadian Journal of Earth Sciences 24, no. 2 (February 1, 1987): 302–13. http://dx.doi.org/10.1139/e87-032.

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The Hadrynian (Late Proterozoic) Kaza Group is 3800 m thick in the southern Cariboo Mountains of south-central British Columbia, and it consists of a lower division of pelite and psammite (700 m), a middle division of granule conglomerate with thick pelite intervals and some quartzite and carbonate (1400 m), and an upper division of granule conglomerate with little pelite (1700 m). Contacts with both the overlying Isaac Formation of the Cariboo Group and with underlying marble, semipelite, and amphibolite are gradational. The underlying strata can be traced southeastward into the middle marble and the semipelite–amphibolite division of the Hadrynian Horsethief Creek Group. The upper clastic division that caps the Horsethief Creek Group in the Selkirk Mountains is a southeastward-thinning equivalent of the Kaza Group.Two southeastward-tapering wedges of granule conglomerate, pelite, and carbonate constitute the bulk of the Hadrynian Windermere Supergroup of southern British Columbia. The lower wedge is represented by the Horsethief Creek Group, exclusive of its upper clastic division. The upper wedge is represented by the upper clastic division, the Kaza Group, the overlying Cariboo Group, and the middle and upper Miette Group. The two wedges indicate two pulses of crustal thinning and stretching during Hadrynian rifting of western North America.

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28

McMechan, M. E. "Vreeland Diamictites - Neoproterozoic glaciogenic slope deposits, Rocky Mountains, northeast British Columbia." Bulletin of Canadian Petroleum Geology 48, no. 3 (September 1, 2000): 246–61. http://dx.doi.org/10.2113/48.3.246.

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29

Hoffman, P. F. "Vreeland Diamictites - Neoproterozoic glaciogenic slope deposits, Rocky Mountains, northeast British Columbia." Bulletin of Canadian Petroleum Geology 48, no. 4 (December 1, 2000): 360–63. http://dx.doi.org/10.2113/48.4.360.

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30

Beedle, M. J., B. Menounos, and R. Wheate. "Glacier change in the Cariboo Mountains, British Columbia, Canada (1952–2005)." Cryosphere 9, no. 1 (January 7, 2015): 65–80. http://dx.doi.org/10.5194/tc-9-65-2015.

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Abstract. We applied photogrammetric methods with aerial photography from 11 different years between 1946 and 2005 to assess changes in area and volume of 33 glaciers in the Cariboo Mountains of British Columbia for the latter half of the 20th century. These are used to identify changes in extent and elevation primarily for the periods 1952–1985, 1985–2005, and 1952–2005. All glaciers receded during the period 1952–2005; area retreat averaged −0.19 ± 0.05 % a−1. From 1952 to 1985, nine glaciers advanced; following 1985, retreat rates accelerated to −0.41 ± 0.12% a−1. Thinning rates of a subset of seven glaciers likewise accelerated, from −0.14 ± 0.04 m w.e. a−1 (1952–1985) to −0.50 ± 0.07 m w.e. a−1 for the period 1985–2005. Temperatures increased from the earlier to the latter period for the ablation (+0.38 °C) and accumulation (+0.87 °C) seasons, and average precipitation decreased, particularly in the accumulation season (−32 mm, −3.2%). Our comparison of surface area change with glacier morphometry corroborates previous studies that show primary relations between extent change and surface area. We also find that the strength and sign of these relations varied for different epochs. Our results also indicate that the 1985 glacier extent for the study area reported previously by other studies may be slightly overestimated due to errant mapping of late-lying snow cover.

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31

Beedle, M. J., B. Menounos, and R. Wheate. "Glacier change in the Cariboo Mountains, British Columbia, Canada (1952–2005)." Cryosphere Discussions 8, no. 3 (June 25, 2014): 3367–411. http://dx.doi.org/10.5194/tcd-8-3367-2014.

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Abstract. We calculated dimensional change for 33 glaciers in the Cariboo Mountains of British Columbia for the latter half of the twentieth century. All glaciers receded during the period 1952–2005; area retreat averaged −0.19 ± 0.05% a−1. From 1952 to 1985, nine glaciers advanced. Following 1985, retreat rates accelerated to −0.41 ± 0.12% a−1. Thinning rates likewise accelerated, from −0.14 ± 0.04 m w.e. a−1 (1952–1985) to −0.50 ± 0.07 m w.e. a−1 for the period 1985–2005. Temperatures increased from the earlier to the latter period for the ablation (+0.38 °C) and accumulation (+0.87 °C) seasons, and average precipitation decreased, particularly in the accumulation season (−32 \\unit{mm}, −3.2%). Our comparison of surface area change with glacier morphometry corroborates previous studies that show primary relations between extent change and surface area. We also find, however, that the strength and sign of these relations varied for different epochs.

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32

Johnson, Peter G. "Holocene Paleohydrology of the St. Elias Mountains, British Columbia and Yukon." Géographie physique et Quaternaire 40, no. 1 (December 4, 2007): 47–53. http://dx.doi.org/10.7202/032622ar.

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ABSTRACT The evolution of the Holocene paraglacial environment of the St. Elias Mountains has been dominated by hydrological variations which modify the direct glacial depositional environment and trigger instabilities in valley side glacial and talus deposits. Data from the Kaskawulsh Glacier demonstrate how discharge and sediment transport regimes vary through the season, as sediment is flushed out of the system, and a marginal to subglacial drainage change of the Grizzly Creek Glacier illustrates the effects of extraordinary events in transporting large volumes of sediment. A multiple glacier fluctuation model applied to the region produces rapid temporal changes in discharge and sediment regimes throughout the Holocene. The effect of these variations is enhanced by the occurrence of surges of many of the glaciers of the St. Elias Mountains and by sequences of glacier dammed lake formation and drainage in the region.

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33

Rusmore, M. E., G. J. Woodsworth, and G. E. Gehrels. "Two-stage exhumation of midcrustal arc rocks, Coast Mountains, British Columbia." Tectonics 24, no. 5 (October 2005): n/a. http://dx.doi.org/10.1029/2004tc001750.

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34

Allen, Sandra M., and Dan J. Smith. "Late Holocene glacial activity of Bridge Glacier, British Columbia Coast Mountains." Canadian Journal of Earth Sciences 44, no. 12 (December 1, 2007): 1753–73. http://dx.doi.org/10.1139/e07-059.

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Bridge Glacier is a prominent eastward-flowing valley glacier located on the east side of the Pacific Ranges within the southern British Columbia Coast Mountains. The terminus of Bridge Glacier has retreated at rates up to 125 m/year over the last 50 years and currently calves into proglacial Bridge Lake. Field investigations of the recently deglaciated terrain and moraines led to the discovery of detrital boles and glacially sheared stumps. Dendroglaciological analyses of this subfossil wood produced five radiocarbon-controlled floating tree-ring chronologies. The relative age and stratigraphic location of these samples revealed that Bridge Glacier experienced at least four periods of significant advance during the late Holocene: a Tiedemann-aged advance ca. 3000 14C years BP, an unattributed advance ca. 1900 14C years BP, a first millennium advance ca. 1500 14C years BP, and a Little Ice Age advance beginning ca. 700 14C years BP. Lichenometric investigations at eight terminal and lateral moraine complexes identified early Little Ice Age moraine stabilization during the late 13th to early 14th centuries, with subsequent ice-front oscillations ending in the middle 15th, early 16th, middle to late 17th, early 18th, middle to late 19th, and early 20th centuries. These investigations build upon previous research and compliment recent geobotanical evidence emerging from other glaciers in this region that describe multiple late Holocene glacier advances. The discovery of a glacially sheared whitebark pine stump dating to 1500 ± 50 14C years BP provides irrevocable proof for an advance of Bridge Glacier during a time when glaciers throughout Pacific North America were also expanding.

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35

Hofmann, H. J., E. W. Mountjoy, and M. W. Teitz. "Ediacaran fossils from the Miette Group, Rocky Mountains, British Columbia, Canada." Geology 13, no. 11 (1985): 819. http://dx.doi.org/10.1130/0091-7613(1985)13<819:efftmg>2.0.co;2.

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36

Darack, Ed. "Weatherscapes: Coast Mountains of British Columbia – Wilderness of Sky and Ice." Weatherwise 70, no. 5 (September 3, 2017): 8–9. http://dx.doi.org/10.1080/00431672.2017.1346428.

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37

Day, S. J., B. E. Broster, and A. J. Sinclair. "Sulphide erratics applied to subglacial exploration: St. Elias Mountains, British Columbia." Canadian Journal of Earth Sciences 24, no. 4 (April 1, 1987): 723–30. http://dx.doi.org/10.1139/e87-070.

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Petrographic and geochemical data from glacial erratics provide evidence for a hidden subglacial source when compared with data from the only known sulphide deposit outcropping locally. These results are found to be in agreement with geological and glaciological studies conducted as part of a reconnaissance exploration program. It is suggested that the integrated approach described here is an inexpensive and rapid exploration method that can determine the likelihood of additional sub-glacial occurrences in areas of known deposits.

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38

Montgomery, John R., and John V. Ross. "A note on the Quesnel Lake Gneiss, Caribou Mountains, British Columbia." Canadian Journal of Earth Sciences 26, no. 7 (July 1, 1989): 1503–8. http://dx.doi.org/10.1139/e89-128.

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The Quesnel Lake Gneiss is one of several large bodies of gneiss emplaced into the westernmost exposure of the Hadrynian to Paleozoic(?) metasedimentary rocks of the Snowshoe Group in the Omineca Belt, central British Columbia. The gneiss has a deformational history comparable to that of its enveloping rocks, and isotope studies indicate that its age of emplacement is Late Devonian to Early Mississippian and that its age of synkinematic metamorphism is mid-Jurassic. From petrochemical analyses and structural studies, we interpret the gneiss as being a late Paleozoic igneous intrusion into the probable western margin of the North American craton.

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39

Bovis, Michael J. "Rock-slope deformation at Affliction Creek, southern Coast Mountains, British Columbia." Canadian Journal of Earth Sciences 27, no. 2 (February 1, 1990): 243–54. http://dx.doi.org/10.1139/e90-024.

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A 7 year record of rock-slope deformation is reported from Affliction Creek, in the southern Coast Mountains of British Columbia. An estimated 3 × 107 m3 of monzonite basement and overlying Garibaldi-aged volcanic material is involved in a slow gravitational movement. Ground-motion vectors suggest that movement has occurred along a deep-seated shear zone and was accompanied by a downslope extension of the moving mass. Near-surface flexural toppling, producing antislope scarps, has taken place where tension cracks crop out on steep slopes or wherever rock faces with strong planar jointing are glacially undercut. Structural data indicate the feasibility of both sliding and toppling at this site.The stratigraphic evidence indicates that most of the tension cracks, grabens, and antislope scarps constituting the slope-movement complex are less than 4300 years old and that many of these landforms may have developed quite recently, as a result of rock-slope debuttressing during the retreat of Affliction Glacier from its late- Neoglacial maximum. Significant variations in the rate of instrumented movements over the 7 year period are not readily accounted for by variations in the level of seismic activity and may be driven by groundwater fluctuations.

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40

Desloges, J. R., and J. M. Ryder. "Neoglacial history of the Coast Mountains near Bella Coola, British Columbia." Canadian Journal of Earth Sciences 27, no. 2 (February 1, 1990): 281–90. http://dx.doi.org/10.1139/e90-027.

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The maximum Holocene extent of glaciers in the study area is marked by late Neoglacial (Little Ice Age) terminal moraines. Moraine stratigraphy and 14C dates from a small number of sites suggest that glacier advance, almost as extensive as that of the late Neoglacial, occurred about 2500 14C years BP, and that late Neoglacial advance began well before 770 14C years BP (or the thirteenth century A.D.); glacier termini then stood close to the position of the climax moraines for several centuries. Dates of stabilization of end moraines at 16 glaciers were determined by dendrochronology, with tree-ring counts corrected for sampling errors and ecesis. Most terminal moraines date from 1860 to 1900. Many recessional moraines were formed between 1900 and 1940, coincident with a regionally documented phase of cooler and wetter climate. The proposed chronology is similar to results from elsewhere in the Canadian Cordillera.

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41

Friedman, R. M., J. W. H. Monger, and H. W. Tipper. "Age of the Bowen Island Group, southwestern Coast Mountains, British Columbia." Canadian Journal of Earth Sciences 27, no. 11 (November 1, 1990): 1456–61. http://dx.doi.org/10.1139/e90-154.

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A new U–Pb date of [Formula: see text] for foliated felsic metavolcanic rocks of the Bowen Island Group, from Mount Elphinstone in the southwesternmost Coast Mountains of British Columbia, indicates that there the age of this hitherto undated unit is early Middle Jurassic. These rocks grade along strike to the north-northwest into a more sedimentary facies, which north of Jervis Inlet contains a probable Sinemurian (Lower Jurassic) ammonite. The Bowen Island Group thus appears to include Lower and Middle Jurassic rocks and to be coeval in part with volcanic rocks of the Bonanza Formation on Vancouver Island to the west and the Harrison Lake Formation within the central Coast Mountains 75 km to the east.

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42

Déry, Stephen J., Andrew Clifton, Shane MacLeod, and Matthew J. Beedle. "Blowing Snow Fluxes in the Cariboo Mountains of British Columbia, Canada." Arctic, Antarctic, and Alpine Research 42, no. 2 (May 2010): 188–97. http://dx.doi.org/10.1657/1938-4246-42.2.188.

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43

Kathman, R. Deedee. "Eutardigrada from Vancouver Island, British Columbia, Canada, including a description of Platicrista cheleusis n.sp." Canadian Journal of Zoology 68, no. 9 (September 1, 1990): 1880–95. http://dx.doi.org/10.1139/z90-268.

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Thirty-one species of eutardigrades were collected on five mountains on Vancouver Island, British Columbia, during July 1986 and July 1987. Three of the species found were new to science, including 1 species, Platicrista cheleusis n.sp., described herein and 2 species described elsewhere, and 21 others are new to British Columbia; 13 of these are also new to Canada.

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44

Church, Michael, Rolf Kellerhals, and Terry J. Day. "Regional clastic sediment yield in British Columbia." Canadian Journal of Earth Sciences 26, no. 1 (January 1, 1989): 31–45. http://dx.doi.org/10.1139/e89-004.

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The data archive of the Water Survey of Canada, supplemented by data of the British Columbia Hydro and Power Authority, is used to investigate the areal pattern of fluvial sediment yield in British Columbia. The data represent suspended-sediment loads at 63 stations derived from observations within the period 1966–1985. In most of the province there is a single annual peak in sediment transport in spring, corresponding to the dominant snowmelt freshet. However, on the coast winter rainfall induces the sediment peak, and in the Coast and Cascade mountains there is a transitional regime with two peaks. From 65 to 90% of annual sediment yield occurs in the spring three months. Sediment yield per unit area (specific sediment yield) increases with drainage area at all scales from 10 up to 30 000 km2. The pattern persists seasonally throughout the year. This contradicts the conventional model in which sediment yield declines downstream because of deposition along channels of a portion of the load derived from erosion of the land surface. In British Columbia much of the sediment derives from erosion of Quaternary materials along stream banks and valley sides. Rivers draining glaciers and lakes behave distinctively. The observed pattern of sediment yield complicates prediction of drainage-basin sediment yield.

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45

Rusmore, Margaret E., Scott W. Bogue, Karen Dodson, Kenneth A. Farley, and Glenn J. Woodsworth. "Deformation of continental crust along a transform boundary, Coast Mountains, British Columbia." Tectonics 29, no. 4 (July 17, 2010): n/a. http://dx.doi.org/10.1029/2009tc002502.

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46

Friele, Pierre A., and John J. Clague. "Younger Dryas readvance in Squamish river valley, southern Coast mountains, British Columbia." Quaternary Science Reviews 21, no. 18-19 (October 2002): 1925–33. http://dx.doi.org/10.1016/s0277-3791(02)00081-1.

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47

St-Hilaire, Vikki M., and Dan J. Smith. "Holocene glacier history of Frank Mackie Glacier, northern British Columbia Coast Mountains." Canadian Journal of Earth Sciences 54, no. 1 (January 2017): 76–87. http://dx.doi.org/10.1139/cjes-2015-0236.

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Frank Mackie Glacier repeatedly advanced across the Bowser River valley in northwestern British Columbia to impound Tide Lake during the Holocene. The most recent infilling of Tide Lake was associated with a late Little Ice Age glacier advance and ended around 1930 when the lake catastrophically drained. Over the last century Frank Mackie Glacier has retreated and down wasted to reveal multiple glaciogenic sedimentary units within the proximal faces of prominent lateral moraines. The units are separated by buried in-situ tree stumps and laterally contiguous wood mats deposited on paleosols. Dendroglaciological and radiocarbon dating of these wood remains show that Frank Mackie Glacier expanded into standing forests at 3710–3300, 2700–2200, 1700–1290, 900–500, and 250–100 cal. years BP. These advances coincide closely in time with the previously established Tide Lake glacier dam chronology and with the Holocene history of other glaciers in the Bowser River watershed. The findings emphasize the likelihood that most glaciers within northwestern British Columbia underwent substantial size and mass balance changes over the last 4000 years, and often spent hundreds of years in advanced positions before retreating.

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48

Ryder, J. M. "Neoglacial history of the Stikine–Iskut area, northern Coast Mountains, British Columbia." Canadian Journal of Earth Sciences 24, no. 7 (July 1, 1987): 1294–301. http://dx.doi.org/10.1139/e87-125.

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Information about Neoglacial features was obtained from aerial photograph interpretation, observations during low-level flights, ground checking, and historical records. Terminal moraines at Great, Flood, and Mud glaciers date from the late seventeenth to early eighteenth centuries, and recessional moraines at these glaciers and terminal moraines at glaciers farther east date from the late nineteenth to early twentieth centuries. These late Neoglacial terminal moraines appear, in general, to mark the greatest post-Pleistocene extent of the glaciers. Radiocarbon dates from overridden trees and soil indicate that 500–600 14C years BP glaciers were considerably more extensive than they are at present and were advancing. Preservation of a 3800 14C year old caribou antler in a snowbank that is now rapidly shrinking suggests that climate has been relatively cool and moist for the past four millennia.

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49

Pearson, David M., Douglas R. MacLeod, Mihai N. Ducea, George E. Gehrels, and P. Jonathan Patchett. "Sediment underthrusting within a continental magmatic arc: Coast Mountains batholith, British Columbia." Tectonics 36, no. 10 (October 2017): 2022–43. http://dx.doi.org/10.1002/2017tc004594.

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50

Clague, John J., R. W. Mathewes, W. M. Buhay, and T. W. D. Edwards. "Early Holocene climate at Castle Peak, southern Coast Mountains, British Columbia, Canada." Palaeogeography, Palaeoclimatology, Palaeoecology 95, no. 1-2 (August 1992): 153–67. http://dx.doi.org/10.1016/0031-0182(92)90170-a.

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