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« Two Middle Holocene Marker Beds in Vertically Accreted Floodplain Deposits, Lower Fraser River, British Columbia »

Harry F. L. Williams et Michael C. Roberts Géographie physique et Quaternaire, vol. 44, n° 1, 1990, p. 27-32.

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Document téléchargé le 12 février 2017 05:35 Géographie physique et Quaternaire, 1990, vol. 44, n° 1, p. 27-32, 5 fig., 1 tabl.

TWO MIDDLE HOLOCENE MARKER BEDS IN VERTICALLY ACCRETED FLOODPLAIN DEPOSITS, LOWER FRASER RIVER, BRITISH COLUMBIA

Harry F. L. WILLIAMS and Michael C. ROBERTS, Department of Geography and Anthropology, University of North Texas, Denton, Texas 76203, U.S.A., and Department of Geography and Institute for Quaternary Research, Simon Fraser University, Burnaby, British Columbia V5A 1S6.

ABSTRACT Drill cores obtained from the RÉSUMÉ Deux lits repères de l'Holocène ZUSAMMENFASSUNG Zwei Betten, die eastern Fraser Delta and adjoining Fraser moyen dans les dépôts de crue à croissance als Anhaltspunkt dienen, in vertikal angela- River floodplain reveal two middle Holocene verticale du Fraser inférieur, Colombie- gerten Hochflutablagerungen aus dem mit- marker beds—a peat with an age of about Britannique. Des carottes recueillies dans la tleren Holozân, unterer Fraser-Fluss, British 6000 '4C yr BP and a tephra bed, identified partie est du delta du Fraser et de la plaine Columbia. Bohrkerne von dem ôstlichen as Mazama (6800 yr BP). These marker beds, d'inondation adjacente montrent deux lits re­ Fraser-Delta und der angrenzenden Hoch- 4 in conjunction with ' C dates from the flood- pères datant du milieu de l'Holocène, un lit flutebene lassen zwei Betten aus dem mit- plain sediments, indicate that the Fraser River de tourbe datant d'à peu près 6000 BP et un tleren Holozân erkennen, die als Anhalt floodplain aggraded in response to a rise in lit de tephra, correspondant à l'éruption du dienen: ein Torfbett das auf etwa 6000 "1C sea-level, between about 8000 and 2250 yr mont Mazama (6800 BP). Ces lits repères, Jahre v.u.Z. datiert wird und ein Tephra-Bett, BP, and that aggradation kept pace with sea- ainsi que les datations au radiocarbone ob­ das aus der Zeit des Ausbruchs des Maza- level rise. The aggradational deposits form tenues dans les sédiments de crue, montrent mabergs stammt (6800 Jahre v.u.Z.). Die als a sediment wedge consisting mainly of que la plaine d'inondation du Fraser a pro­ Anhaltspunkt dienenden Betten weisen zu- gressé en réponse à une hausse du niveau organic-rich silts and fine sands of overbank sammen mit den von den Hochflutsedimenten origin. The wedge extends at least 20 km into marin survenue entre environ 8000 et 2250 BP ,4 gewonnenen C-Daten darauf hin, dass die the lower Fraser River Valley. Preservation et que !'aggradation suivait la hausse du ni­ Hochflut des Fraser-Flusses als Reaktion auf of the marker beds indicates considerable veau marin. L'accumulation de sédiments, eine Anhebung des Meeresspiegels zwischen channel stability in the lower reaches of the de forme triangulaire, est composée princi­ etwa 8000 und 2250 Jahren v.u.Z. zugen- Fraser River over about the last 7000 years. palement de limons riches en matière or­ ganique et de sables fins d'origine alluviale. ommen hat. und dass diese Zunahme der Le triangle s'étend jusqu'à au moins 20 km Hebung des Meeresspiegels entsprach. Die dans la vallée inférieure du Fraser. La Akkumulationssedimente bilden einen Se- conservation des lits repères démontre la dimentkeil, der vor allem aus organisch rei- grande stabilité des biefs du Fraser inférieur chem Schlamm und feinem Sand alluvialer depuis environ 7000 ans. Herkunft besteht. Der Keil erstreckt sich min- destens 20 km in das TaI des unteren Fraser. Die Erhaltung der als Anhaltspunkte dienen­ den Betten beweist eine beachtliche Kanal- stabilitât in den unteren Stillen des Fraser wâhrend ungefàhr 7000 Jahren.

Manuscrit reçu le 5 mai 1989; manuscrit révisé accepté le 30 octobre 1989 28 H. F. L. WILLIAMS and M. C. ROBERTS

INTRODUCTION Delta at New Westminster, where the river emerges into the lowland of the Strait of Georgia through a narrow gap in the The Fraser River Delta (Fig. 1) has been growing into the Pleistocene uplands (Fig. 1). Strait of Georgia for about the last 9000 years (Williams, 1988). An investigation of the evolution of the delta has dem­ The floodplain of the lower Fraser River occupies a former onstrated that it aggraded in response to a 13 m rise in relative arm of the sea, which presumably was infilled by Fraser River sea-level between about 8000 and 2250 yr BP. Vertical ac­ sediments between about 11 000 to 9000 yr BP, when the cretion on the delta kept pace with rising sea-level as the river established its present course following déglaciation delta continued to prograde into the Strait (Williams and (Armstrong, 1981 ; Clague ef a/., 1983). Roberts, 1989). The river below Hope is divided according to planform into Extension of subsurface investigations from the delta into a straight reach, a wandering gravel-bed reach (Morningstar, the adjoining western Fraser River floodplain has revealed 1987). and a meandering reach (Fig. 1). The wandering gravel- two widespread marker beds within the aggradational deposits. bed reach is characterized by multiple channels separated The upper marker bed is a hitherto undiscovered peat layer by large vegetated islands, large width to depth ratios and at a mean depth of about 4.5 m; the lower marker bed is a gravelly bed material. The meandering reach has, for the Mazama tephra layer at a mean depth of about 7.1 m, pre­ most part, a single sinuous channel containing a few large, viously recognized in a number of locations in the area well-vegetated islands, smaller width to depth ratios and sandy (Blunden, 1973, 1975; Clague et al., 1983). These marker bed material (McLean and Church, 1986). beds provide valuable chronologic control for paleogeomorphic reconstructions in the lower Fraser River Valley. The objectives LATE QUATERNARY SEA-LEVEL CHANGES of this paper are: 1 ) to describe the nature and presently During and immediately following retreat of the Late Wis- known extent of the marker beds; and, 2) to assess the sig­ consinan Cordilleran Ice Sheet about 13 000 yr BP, the sea nificance of the marker beds for paleogeomorphic reconstruc­ occupied the Fraser Lowland up to an elevation of at least tions in lower Fraser River Valley. 200 m above present sea-level (Armstrong, 1981). Isostatic rebound proceeded rapidly following removal of the ice load SETTING (Fig. 2). Raised glacio-deltaic deposits in the Fraser Lowland suggest that relative sea-level fell to about 40 m elevation by GEOMORPHOLOGY around 11 500 yr BP and reached its present level between Lower Fraser River Valley extends from Hope, at the 11 000 and 10 000 yr BP (Clague, 1981 ). Emergence of the downstream end of Fraser canyon, to the apex of the Fraser Fraser Lowland continued, causing the sea to drop about

FIGURE 1. Location map of Fraser Delta and lower Fraser River Localisation du delta du Fraser et de la vallée inférieure du Fraser Valley, showing characteristic channel cross-sections in the wandering et coupes caractéristiques dans les biefs à méandres et à lits de gravel-bed and meandering reaches. gravier divagants.

Géographie physique ef Quaternaire. 44(1). 1990 TWO MIDDLE HOLOCENE MARKER BEDS 29

overbank sedimentation in a relatively low-energy, vegetated, floodplain environment on the basis of their fine grain size and abundant incorporated organic matter. These deposits contain freshwater pollen and spores, including arrowhead (Sagittaria sp.), horsetail (Equisetum sp.), skunk cabbage (Lysichiton amehcanum) and buckbean (Menyanthes trifoliata) (Williams and Roberts, 1989). The peat and tephra marker beds are found within these floodplain deposits, and are clearly traceable from the delta into the adjoining floodplain of the lower Fraser River (Fig. 3).

1110 9876 54 3 2 10 3 PEAT BED RADIOCARBON AGE (x 10 YEARS BP) FIGURE 2. Postglacial sea-level curve for Fraser Lowland (from Clagueef a/., 1982). The peat bed, averaging 250-300 mm thick, in almost all Courbe du niveau marin postglaciaire des basses terres du Fraser cases grades into the enclosing floodplain deposits; the one (de Clague et al.. 1982) exception is site D68 (Fig. 3), where the top of the peat is marked by a sharp contact overlain by a 10 cm thick bed of 13 m below its present level (Clague et al., 1982; Williams fine sand presumably of flood origin. Palynological analysis and Roberts, 1989). of the peat bed from the delta has shown that it represents The early Holocene low stand of sea-level, resulting from the initial stages of a raised peat bog. The pollen spectrum isostatic rebound and possible forebulge migration (Clague, is dominated by shrubs of the Rosaceae family and has rel­ 1983), was followed by a rise in relative sea-level until about atively low arboreal and herbaceous pollen components. These 2250 yr BP when it attained its present level (Williams and findings suggest that the site became sufficiently elevated Roberts, 1989). above high tide level to permit shrub vegetation (probably Spiraea douglasii [hardhack]) to dominate, and to reduce the METHODS input of flood-derived arboreal pollen (Hebda, 1977; Williams, 1988). DRILLING Radiocarbon age determinations on samples of the peat A drilling programme was initiated on the Fraser Delta in bed from three widely spaced locations (sites D52, D69 and the summer of 1984 and was extended upstream into the D71—Fig. 3) were obtained in order to confirm that the peat Fraser River floodplain during 1986. Core was retrieved using bed does represent organic accumulations on a continuous, a Concore C-68 drill rig (split tube samples) and a vibracorer coeval paleosurface. The resulting radiocarbon ages are re­ (Smith, 1984). Field logging of cores included a visual as­ markably close: 6025 ± 105 (S-2872), 5840 ± 145(S-2866) sessment of particle size and sorting, sedimentary structures and 5990 ± 155 (S-2867) yr BP, from sites up to 20 km apart and organic matter contents. The two marker beds were iden­ (Table I). These dates suggest that a hitherto unknown stillstand tified in core. Samples were obtained from cores for the lab­ of sea-level at approximately 6000 yr BP was of sufficient oratory determination of texture, radiocarbon dating, and duration (presumably several hundred years) to allow extensive micropaleontological studies (Williams, 1988). peat deposits to develop on the surface of the Fraser Delta and adjoining Fraser River floodplain. An average rate of peat NATURE AND STRATIGRAPHY OF accumulation of about 0.7 mm/yr has been reported from THE MARKER BEDS Burns Bog on the Fraser Delta (Fig. 1) (Hebda, 1977); thus STRATIGRAPHY the buried peat layer is estimated to have formed in about 400 years. This implies a stillstand in sea-level rise between A stratigraphie section was constructed on the basis of approximately 6200 and 5800 yr BP. lithofacies sequences encountered in cores drilled along a transect from eastern Fraser Delta to western Fraser River The areal extent of this stillstand is presently unknown, floodplain (Fig. 3). On eastern Fraser Delta, the generalized but evidence of a stillstand at ca. 6000 yr BP has been found sequence of lithofacies comprises a basal layer of clean, well in a core from Puget Lowland, Washington (Eronen et al., sorted, fine to medium sand, deposited in the lower tidal 1987), approximately 160 km south of the Fraser Lowland, sandflat environment; interbedded silts and fine sands of mid- suggesting that it may have been at least regional in extent. tidal origin; organic-rich tidal marsh silt; organic-rich floodplain TEPHRA BED silt; and supratidal delta-top peat (Williams and Roberts, 1989). The complete lithofacies sequence is illustrated by core D23 The tephra bed, 10-20 mm thick, is bounded by sharp (Fig. 3). contacts with both the underlying and overlying sediments (Fig. 4). The tephra has a gritty texture and is clearly distin­ The floodplain deposits on the delta grade laterally into guishable in core by its white/pale yellow colour, which contrasts similar sediments underlying the Fraser River floodplain sharply with the greyish brown colour of the enclosing organic- (compare, for example, core D29 and core TH85-14, Fig. 3). rich silts. These sediments, consisting predominantly of horizontally bedded organic-rich silt and interbedded silts and fine sands The radiocarbon dates obtained in this study provide evi­ (see core TH85-14, Fig. 3), are interpreted as representing dence that the tephra layer encountered in many drill cores

Géographie physique et Quaternaire, 44(1), 1990 30 H. F. L. WILLIAMS and M. C. ROBERTS

FIGURE 3. Lithostratigraphic section, from eastern Fraser Delta Coupes lithostratigraphiques, de la partie est du delta du Fraser to western Fraser River floodplain, showing peat and tephra marker jusqu'à la partie ouest de la plaine d'inondation du Fraser, qui beds enclosed by floodplain deposits. montrent les lits repères de tourbe et de tephra contenus entre les dépôts de crue.

TABLE I Radiocarbon Dates

Laboratory Age Core Location Material Elev. (m) No. ("1C years BP) No. Lat. N Long. W. bmsl*

GSC-4194 4410 ± 70 D23 49°10.5' 122°58.4' Peat 1.19 GSC-4238 5500 ± 70 D23 49°10.5' 122°58.4' Organic detritus 3.55 S-2866 5840 ± 145 D69 49°14.3' 122°48.6' Peat 1.8 S-2867 5990 ± 155 D71 49°12.7' 122°41.3' Peat 0.3 S-2872 6025 ± 105 D52 49°10.5' 122°57.7' Peat 3.77 SFU-308 7400 ± 160 FL4 49°09.30' 122°35.15' Wood 3.1 GSC-4255 7960 ± 140 D23 49°10.5' 122°58.4' Organic detritus 11.71

Below mean sea level. is Mazama (ca. 6800 yr BP, Bacon, 1983), confirming previous British Columbia on the basis of its zirconium concentration identifications (Blunden. 1973, 1975; Clagueef a/., 1983). In (Williams and D'Auria, in prep.). seven drill cores (D23, D52, D69, D71, D72, D73 and D74), the tephra bed is found stratigraphically below the buried peat PALEOGEOMORPHIC IMPLICATIONS OF THE marker horizon dated at ca. 6000 yr BP. The identification of MARKER BEDS the tephra bed as Mazama was also made independently on the basis of its trace element composition, using x-ray energy The marker beds represent extensive subaerial surfaces spectroscopy (Cormie et ai, 1981 ). It was found that Mazama of the Fraser River floodplain at two stages of its Holocene could be distinguished from other Holocene tephras in southern evolution; therefore, they play a valuable role in paleogeo-

Géographie physique el Quaternaire. 44(1). 1990 TWO MIDDLE HOLOCENE MARKER BEDS 31

90 100

FIGURE 4. Tephra marker bed (depth 7.4 m) in core D52 enclosed FIGURE 5. Longitudinal profile of the Fraser River floodplain surface, by horizontally bedded organic-rich showing the break in slope between meandering and wandering silt. gravel-bed reaches. Lit repère de tephra (profondeur de Profil longitudinal de la surface de la plaine d'inondation du Fraser, 7,4 m) dans la carotte D52, entouré montrant la rupture de pente entre le bief à méandres et le bief à de limon à lits horizontaux riches lits graveleux en méandre. en matière organique.

morphic reconstruction of lower Fraser Valley. The marker The deposits enclosing the marker beds form, therefore, beds provide insights into: a) floodplain aggradation; b) lateral a sediment wedge that thins up-valley. The marker beds define stability of the river channel; c) grade adjustments of the river two paleosurfaces within this wedge, extending from the Fraser in response to base-level changes. River floodplain onto the surface of the delta.

FLOODPLAIN AGGRADATION LATERAL STABILITY OF THE RIVER CHANNEL

The marker beds can be traced from the Fraser Delta Preservation of the peat and tephra marker beds in the eastwards into the floodplain (Fig. 3). The stratigraphie con­ lower Fraser River floodplain (Fig. 3) is clear evidence that tinuity of the marker beds shows that the floodplain and the lateral channel migration has been quite limited over the last delta aggraded in concert. Rising base level caused accelerated ca. 7000 years. On the basis of the drill core data (Fig. 3). aggradation of both the delta and the floodplain, such that the floodplain deposits underlying the lower reaches of the the rate of sediment accumulation kept pace with the rate of river to a depth of at least 8 m consist mainly of overbank sea-level rise (Williams and Roberts, 1989). Terrestrial con­ deposits, rather than laterally-accreted, in-channel sediments. ditions were thus perpetuated, giving rise to the thick floodplain This is in marked contrast to the wandering gravel-bed reach, unit on both the delta and floodplain (Fig. 3). where, apart from a shallow veneer of overbank deposits, the On the eastern delta, the base of the aggradational deposits floodplain sediments have resulted chiefly from channel mi­ enclosing the marker beds coincides with the base of the gration and island accretion (McLean and Mannerstrom, 1985; thick floodplain unit, radiocarbon dated at 7960 ± 140 yr BP Momingstar, 1987). (GSC-4255; core D23—Fig. 3). This floodplain unit extends RIVER GRADIENT AND BASE-LEVEL CHANGES some 14 m below the delta surface, indicating aggradation of 14 m in approximately the last 7960 years—an average The growth of the sediment wedge resulted in a considerable sedimentation rate of about 1.8 mm/yr. reduction in slope of the lower Fraser River. A longitudinal Clague et al. (1983) obtained a core from the floodplain profile of the Fraser Valley floodplain, based on benchmarks some 18 km up-valley from the delta apex (in the vicinity of on topographic maps (Fig. 5), shows the average gradient of core D72, Fig. 3). A peat layer in this core, from 11.5 m below the lower reaches of the river to be 0.00008. The slope of the surface, yielded a radiocarbon age of 7710 ± 80 yr BP the older floodplain surface, underlying the aggradational de­ (GSC-3099), indicating 11.5 m of aggradation and an average posits (approximated by the estimated position of the ca. sedimentation rate of about 1.5 mm/yr. 7400 yr BP paleosurface in Fig. 3) is 0.0002, indicating a reduction in gradient of over 50%. A core from the floodplain near Fort Langley (about 38 km up-valley; FL-4, Fig. 3), contained a piece of wood at a depth A distinct break in slope of the floodplain surface is shown of about 3.1 m bsl., which was radiocarbon dated at 7400 in the vicinity of Hatzic Lake, at the wandering gravel-bed ± 160 yr BP (SFU-308). The surface of the floodplain here meandering transition (Fig. 5). This raises the possibility that is about 2.6 m asl., indicating a depth of aggradation over the up-valley limit of the sediment wedge is marked by this the last ca. 7400 years of no more than about 5.7 m, and an break in slope, as has been found in previous studies of average sedimentation rate of about 0.8 mm/yr. These findings floodplain aggradation (Mackin, 1948; Leopold and Bull. 1979); suggest that there is a progressive up-valley decrease in the and, that the transition from wandering gravel-bed to mean­ thickness of the aggradational deposits. dering fluvial styles is related to the imposition of a reduced

Géographie physique el Quaternaire. 44(1), 1990 32 H. F. L. WILLIAMS and M. C, ROBERTS

river gradient in the lower reaches of the river. However, in 1975. Urban geology of Richmond, British Columbia—inter­ the absence of further data it is not yet possible to distinguish preting a delta landscape. University of British Columbia, De­ the effects of the downstream base-level rise from upstream partment of Geological Sciences, Adventures in Earth Science Series, No. 15, 35 p. controls on floodplain morphology, such as the propagation of the large gravel fan underlying the wandering gravel-bed Clague, J. J.. 1981. Late Quaternary geology and geochronology of reach. Such interpretations must therefore remain only British Columbia. Part 2 : summary and discussion of radiocarbon- speculative. dated Quaternary history. Geological Survey of Canada, Paper 81-35.41 p. CONCLUSIONS 1983. Glacio-isostatic effects of the Cordilleran Ice Sheet, British Columbia, Canada, p. 321-343. In D. E. Smith and A. G. This study has shown that the lower Fraser River floodplain Dawson, eds., Shorelines and lsostasy. Academic Press. aggraded in response to a middle Holocene sea-level rise. Peat and tephra marker beds represent two extensive pa- Clague, J. J., Harper, J. R., Hebda, R. J. and Howes. D. E., 1982. leosurfaces within the aggradational deposits. Continuity of Late Quaternary sea levels and crustal movements, coastal British the marker beds from the delta into the adjoining floodplain Columbia. Canadian Journal of Earth Sciences, 19: 597-618. demonstrates that the floodplain aggraded in concert with the Clague, J. J., Luternauer, J. L. and Hebda, R. J., 1983. Sedimentary delta, and that the rate of sedimentation in both areas kept environments and post-glacial history of the Fraser River delta pace with sea-level rise. and lower Fraser Valley, British Columbia. Canadian Journal of Earth Sciences 20: 1314-1326. The resulting aggradational deposits form a sediment wedge Cormie, A. B.. Nelson, D. E. and Huntley, D. J., 1981. X-ray fluores­ which extends at least 20 km upvalley. Lithologie and paly­ cence analysis as a rapid method of identifying tephras discovered nologie evidence shows that the deposits consist mainly of in archaeological sites. In S. Self and S. J. Sparks, eds.. Tephra organic-rich silt and sand of overbank origin, and that they Studies. D. Reidel, Dordrecht, Holland. lack in-channel sediments associated with lateral channel- Eronen. M., Kankainen, T. and Tsukada, M., 1987. Late Holocene migration. Preservation of the marker beds, at least in the sea-level record in a core from the Puget Lowland. Washington. lower 20 km of the floodplain, demonstrates that the deposits Quaternary Research. 27: 147-159. have not been fluvially reworked, and suggests channel stability over this distance during the last 7000 years. Hebda, R. J., 1977.Thepaleoecologyof a raised bog and associated deltaic sediments of the Fraser River delta. Ph.D. Thesis. University Further drilling of the floodplain is required to establish the of British Columbia, Vancouver, B.C.. 202 p. extent of the sediment wedge and to explore further the relations Leopold. L. B. and Bull, W. B., 1979. Base level, aggradation, and between growth of the deposits and the morphologic and grade. Proceedings of the American Philosophical Society 123: depositional response of Fraser River. No. 3. 168-202. Mackin, J. H.. 1948. Concept of the graded river. Geological Society ACKNOWLEDGEMENTS of America Bulletin. 59: 463-512. We extend thanks to our field assistants and drill crew McLean, D. G. and Church, M. A., 1986. A re-examination of sediment volunteers—Greg Gjerdalen, Nick Kiniski, John White, Nancy transport observations in the lower Fraser River. University of Hon', Harry JoI, Bill Ophoff, Butch Morningstar, Valerie British Columbia, Department of Geography, Fraser River Project Cameron, Cliff Roberts and Kathy Mittag. Bruce Cameron, Progress Report No. 4. 52 p. Richard Hebda and Geoff Quickfall are thanked for their help McLean, D. G. and Mannerstrom, M., 1985. History of channel inst­ with the micropaleontological studies. June Ryder, Ian Brookes ability: lower Fraser River, Hope to Mission. University of British and an anonymous reviewer are thanked for their valuable Columbia, Dept. of Geography, Fraser River Project Progress reviews of an earlier draft of this paper. The study was funded Report No. 2, 18 p + map. by an Energy, Mines and Resources research grant awarded Morningstar, O. R.. 1987. Floodplain construction and deposition in to M. C. Roberts and a Geological Society of America dis­ a wandering reach of the Fraser River. Chilliwack, B, C. M.Sc. sertation grant awarded to H. F. L. Williams. Thesis, Simon Fraser University, Burnaby. Smith, D. G., 1984. Vibracoring fluvial and deltaic sediments: tips on REFERENCES improving penetration and recovery. Journal of Sedimentary Pe­ trology, 54: 660-663. Armstrong, J. E., 1981. Post-Vashon Wisconsin Glaciation, Fraser Lowland, British Columbia, Canada. Geological Survey of Canada, Williams, H. F. L.. 1988. Sea-level change and delta growth: Fraser Bulletin 322. 34 p. Delta, British Columbia. Ph.D. Thesis, Department of Geography, Simon Fraser University. Burnaby. 256 p. Bacon, C. R., 1983. Eruptive history of Mount Mazama and Crater Lake caldera, Cascade Range, U.S.A. Journal Of Volcanology Williams, H. F. L. and D'Auria J. (in preparation). A Mazama tephra and Geothermal Research, 18: 57-115. marker bed in lower Fraser Valley, British Columbia.

Blunden, R. H., 1973. Urban geology of Richmond, British Columbia. Williams, H. F. L. and Roberts. M. C11989. Holocene sea-level change University of British Columbia, Department of Geological Sciences, and delta growth : Fraser River delta, British Columbia. Canadian Report No. 15, 13 p. Journal of Earth Sciences. 26: 1657-1666.

Géographie physique et Quaternaire. 44(1). 1990