UBC Theses and Dissertations

UBC Theses Logo

UBC Theses and Dissertations

Marine geology of upper Jervis Inlet MacDonald, Robert Drummond 1970

You don't seem to have a PDF reader installed, try download the pdf

Item Metadata


UBC_1970_A7 M33.pdf [ 26.33MB ]
JSON: 1.0053136.json
JSON-LD: 1.0053136+ld.json
RDF/XML (Pretty): 1.0053136.xml
RDF/JSON: 1.0053136+rdf.json
Turtle: 1.0053136+rdf-turtle.txt
N-Triples: 1.0053136+rdf-ntriples.txt
Original Record: 1.0053136 +original-record.json
Full Text

Full Text

MARINE GEOLOGY OF UPPER JERVIS INLET by ROBERT DRUMMOND MACDONALD B.A.Sc. University of British Columbia 1965 A THESIS SUBMITTED IN PARTIAL FULFILMENT OF THE REQUIREMENTS FOR THE DEGREE OF MASTER OF APPLIED SCIENCE in the Department of Geology We accept this thesis as conforming to the required standard THE UNIVERSITY OF April BRITISH COLUMBIA 1970 In presenting this thesis in partial fulfilment of the requirements for an advanced degree at the University of British Columbia, I agree that the Library shall make it freely available for reference and study. I further agree tha permission for extensive copying of this thesis for scholarly purposes may be granted by the Head of my Department or by his representatives. It is understood that copying or publication of this thesis for financial gain shall not be allowed without my written permission. Depa rtment The University of British Columbia Vancouver 8, Canada Date ABSTRACT Manganese-iron oxide concretions are presently forming on Patrick Sill in upper Jervis Inlet. The marine geology of Patrick Sill and the adjoining basins (Queen's Reach and Princess Royal Reach) was studied to define the environment in which the con cretions form. The river at the inlet head is the principal source of sediment to the upper basin. The average grain size of surficial bottom sediments within this basin decreases uniformly with distance from the source. Patrick Sill separates the upper from the lower basin. The sediment distribution pattern within the lower basin differs markedly from the upper basin as there is no dominant source of material but rather many localized sources. Abundant shallow marine faunal remains recovered in deep water sediment samples indicate that sediments deposited as deltas off river and stream mouths periodically slump to the basin floors. Geologic and optical turbidity information for the upper basin can best be explained by slump ing from the delta at the inlet head with the initiation of turbidity or density currents. Patrick Sill appears to create a downstream barrier to this flow. The mineralogy of the bottom sediments indicates derivation from a granitic terrain. If this is so, the sediments presently being deposited in both basins are reworked glacial materials initially derived by glacial action outside the present watershed. Upper Jervis Inlet is mapped as lying within a roof pendant of pre-batholithic rocks, principally slates. Patrick Sill is thought to be a bedrock feature mantled with Pleistocene glacial material. The accumulation rate of recent sediments on the sill is low especially in the V-notch or medial depression. The manganese-iron oxide concretions are forming within the depression and apparently nowhere else in the study area. Also forming within the depression are crusts of iron oxide and what are tentatively identified as glauconite-montmorillonoid pellets. The concretions are thought to form by precipitation of manganese-iron oxides on pebbles and cobbles lying at the sediment water interface. The oxide materials are mobile in the reducing environment of the underlying clayey-sand sediment but precipitate on contact with the iii oxygenating environment of the Jurficial sediments. The iron crusts are thought to be forming on exten sive rocky surfaces above the sediment water inter face. The overall appearance and evidence of rapid formation of the crusts suggests they formed from a gel in sea water. Reserves of manganese-iron concretions on Patrick Sill were estimated to be 117 metric tons. Other deposits of concretions have recently bean found in other inlets and in the Strait of Georgia but, to date, the extent of these has not been determined. iv Table of Contents Abstract Page i Chapter 1 Introduction i I History and Purpose of the Study II Location and Physical Setting III Previous Work IV Field Work and Acknowledgments Chapter 2 Geologic History and Regional Geology 9 I Geologic History of Southwestern British Columbia II Origin of Fjords III Regional Geology Chapter 3 Methods of Study 19 I Field Methods 1. Positioning 2. Sample Collection 3„ Photography 4„ Echo Sounding and Continuous Seismic Profiling II Laboratory Methods 1. Grain Size Distribution in Sediments 2„ Mineralogy of Sediments 3„ Gravity Core Analyses 4= Composition, Structure and Abundance of Manganese-Iron Concretions V Page Chapter 4 Oceanography 31 I Bathymetry II Temperature and Salinity III Oxygen Content and Circulation IV Tides V Optical Turbidity Chapter 5 Basin Structure and Sediment Thickness 41 Chapter 6 Sediments 48 I Colour II Total Carbon Content III Free Iron Content IV Particle Morphology V Mineralogy 1„ Granule and Larger Size Material 2. Sand Size Material 3. Clay Size Material VI Grain Size Distribution VII Characteristics with Depth Chapter 7 Sedimentation in Jervis Inlet -\12 Chapter 8 Authigenic Minerals 116 I Manganese Concretions 1. Source Area 2, Age and Growth Rates 3„ Structure 4„ Chemical Composition 5. Mineralogy 6. Formation of Concretions 7. Abundance and Value II Iron Crusts III Glauconite-Montmorillonoid Pellets IV Discussion V Exploration List of Tables Time Stratigraphic Units for Pleistocene of Southwestern B.C. Table of Map Units Mineral Abundances in Fine Sand Fraction jjDOlj Peaks (in Angstroms) of Minerals in Clay Size Fraction Relative Abundances of Clay Mineral Species Chemical Analysis of Jervis Inlet Concretions Comparison of Elemental Analyses of Manganese Concretions v i i List of Figures Pag Figure 1 Location Map-showing upper Jervis 2 Inlet study area 2 Middle and upper Jervis Inlet - 16 showing geology and drainage pattern 3 Sample Station Locations -(in pocket) 4 Sampling Equipment 20 a) Petterssen grab sampler b) Underwater camera c) Phleger corer 5 Procedure for Sample Analysis 26 6 Bathymetry of upper Jervis Inlet -( in pocket) 7 Transverse Sections of upper 33 Jervis Inlet 8 Average Vertical Profile of Tempera- 34 ture and Salinity - Jervis Inlet 9 Water Circulation as Indicated by 37 Longitudinal Profiles 10 Optical Turbidity along Jervis Inlet 39 11 Continuous Seismic Profile along 43 upper Jervis Inlet 12 Classification of Jervis Inlet 49 Sediments 13 Grain Size Distribution along Axis 51 of upper Jervis Inlet 14 Total Carbon Content of Sediments (In pocket) 15 Clay Size Particle and Total Carbon 54 Content Along Axis of Upper Jervis Inlet 16 Iron Extracted During Sample 59 Preparation for X-ray Analysis. viii Page Figure 17 Microphotographs of Sand Grains 62 a) Station J-101 b) Station J-101 c) Station J-110 18 Microphotographs of Sand Grains 63 a),b) Station J-126 c),d) Station J-19-67 19 Mineral Distribution along Axis of 74 upper Jervis Inlet 20 Sediment Type Distribution (in pocket) 21 Clay Size Particle Distribution (in pocket) 22 Mean and Standard Deviation of 87 Grain Size along Axis of upper Jervis Inlet 23 Kurtosis a nd Skewness Parameters 88 along Axis of upper Jervis Inlet 24 Longitudinal Profile of Queen's 90 Reach - Cumulative and Frequency Curves 25 Transverse Profiles of Queen's 92 Reacth - Cumulative and Frequency Curves 26 Bottom Photographs - Station J-126 93 27 Bottom Photographs - Station J-126 94 28 Longitudinal Profile of lower 96 Queen's Reach and upper Princess Royal Reach - Cumulative and Frequency Curves 29 Bottom Photographs - Station J-19-67 98 30 Bottom Photographs - Station J-19-67 99 ix Page Figure 31 Transverse Profile of Queen's 101 Reach (over Patrick Sill) -Cumulative and Frequency Curves 32 Longitudinal Profile of Princess 103 Royal Reach - Cumulative and Frequency Curves 33 Transverse Profile of Princess 104 Royal Reach - Cumulative and Frequency Curves 34 Bottom Photographs •- Station J-160 106 35 Bottom Photographs - Station J-160 107 36 Gravity Cores from Jervis Inlet 109 37 Bathymetry of Patrick Sill (in pocket) 38 Bottom Photographs - Station J-19-67 118 Concretion Locality 39 Bottom Photographs - Station J-19-67 119 Concretion Locality 40 Examples of Concretions .122 a) Side View of Discoidal Variety b) Siliceous Sponge on Spheroidal Variety c) Coalescence of two Spheroidal Concretions 41 Cross Sections of Manganese 124 Concretions 42 Cross Sections of Manganese 125 Concretions 43 Manganese Concretions 135 a) Recovery in Petterssen Grab Sampler b) Density of Occurrence c) Largest Specimen Recovered 44 Iron Crusts from Patrick Sill 138 1 CHAPTER 1 INTRODUCTION 1- History and Purpose of the Study Little work has been done on the marine geology of British Columbia inlets. Sediment studies have been made in Bute Inlet (Toombs .1956), Saanich Inlet (Gucleur and Gross 1964), and Howe Sound (Murray and Ricker—unpublished report)„ A sedimentologic survey of Jervis Inlet was undertaken in May, 1966 ^I.O.U.B.C. Cruise 66/12) to obtain information for comparison with sediment data from Howe Sound. Systematic sampling of upper Jervis Inlet revealed a localized deposit of manganese-iron concretions, or nodules, on a sub marine sill (Patrick Sill). Thereupon, a more intensive study of Patrick Sill and adjacent basins of upper Jervis Inlet was conducted. Chemical studies of the concretions, the inter stitial water of the sediments, and the water column are being made by Dr. E. V. Grill of the Institute of Oceanography at the University of British Columbia. A study of all the oceanographic aspects of the upper Jervis Inlet system may lead to a better understanding of the formation of manganese con cretions in shallow coastal waters. 3 IT.„ Location and Physical Setting Jervis Inlet is located in the northwesterly trending Pacific Range of the Coast Mountains. The mouth of the inlet lies approximately 46 nautical miles (85 kilometers) west-northwest of Vancouver, British Columbia, on the eastern margin of the Strait of Georgia. The inlet is 48 nautical miles (89 kilometers) long and the width averages 1.7 (3.2 kilometers) and seldom exceeds 2.5 nautical miles (4.6 kilometers). The study area (Figure 1) encompasses the northern or upper part of the inlet which is divided into two legs or reaches by a right-angle change in strike of the axis. Queen's Reach is uppermost and has a north-westerly trend while Princess Royal Reach trends to the north-east. Princess Louisa Inlet, which opens into Queen 's Reach, was not included in the study. Patrick Sill lies perpendicular to the axis of Queen's Reach at the point where Queen's Reach turns into Princess Royal Reach. The manganese concretions occur on the southern flank of Patrick Sill at 50°06.2' north latitude and 123°47.8' west longitude. 4 Access to the area is by boat or aircraft only. Jervis Inlet is a glacially modified Pliocene river valley which was invaded by the sea with the waning of the Pleistocene ice sheet. The mountains surrounding the inlet tower to 6,000 to 8,000 feet (1800 to 2200 meters) above sea level. Steep moun tain sides dip at angles averaging 30° to 35° to the water's edge and disappear with no change of slope. Deep striations on rock surfaces, mountain sides too steep and polished to trap soil to support vegetation, and hanging valleys all indicate extensive glaciation. The watershed area of upper Jervis Inlet is small, and many of the streams are intermittent. Queen's Reach and Princess Royal Reach have water shed areas of 27 3 and 157 square miles (855 and 523 square kilometers) respectively. Unlike the majority of long inlets, the run-off into Jervis follows the coastal rainfall pattern closely, i.e. above average in the spring and winter months and below average during July through September. This is due to the absence of large, permanent snow-fields within the watershed to store precipitation. 5 The mean annual fresh water discharge into Jervis Inlet is 236 cubic yards (180 cubic meters) per second. Howe Sound, which has a length of 23 nautical miles (42 kilometers), receives a mean annual discharge of 630 cubic yards (480 cubic meters) per second. (Trites 1955). The average rainfall for southern inlets is estimated to be 60 to 100 inches (150 to 250 centimeters) annually at lower elevations (B.C. Atlas of Resources,1956). However, with altitude, the amount of precipitation can increase to 100 to 150 inches (250 to 380 centimeters) annually, especially towards the heads of the inlets. The inlets funnel moist Pacific air inland until, at the head, this air is forced to rise abruptly. About 10 to 15 per cent of precipi tation falls as snow. The mean monthly temperature at the heads of fjords along the west coast ranges from 20° to 25°F (-7°to -4°C) in January, to 38° to 62°F (3°to 17°C) in July. On a daily basis, the mean maximum temperature is 70° to 75°F (21° to 24°C). The average minimum temperature and the number of frost-free days increase from the heads to the mouths of the inlets (3„C.Atlas of Resources, 1956). 6 With some exceptions, the mountain slopes are covered with vegetation to an elevation of approxi mately 4600 feet (1400 meters). This elevation does not represent the true tree line, but reflects a general lack of soil at higher elevations. The lower, vegetated areas are classified as Coast Forest biotic region. Characteristic are extensive stands of sitka spruce, red and yellow cedar, fir, western and mountain hemlock, and western white pine. These stands of timber support many small logging operations along the length of the inlet. Typical of the Coast Forest region is a dense underbrush of maple, alder, ferns, salal, devil's club, huckleberry, salmonberry and thimbleberry. With increase in elevation, the Coast Forest gives way to the Subalpine Forest biotic region. Alpine varieties of spruce, fir, and pine in open stands and a matting of blueberry and heather typify this region. III. Previous Work Prior sedimentologic work in Jervis Inlet has been done only on a reconnaissance basis as part of an overall study of the B„ C. coastline (Pickard, 1956), and the continental shelf (Cockbain 1963). More detailed geologic studies have been made in 7 Bute Inlet (Toombs 1956), Saanich Inlet (Gucleur and Gross 1964) and Howe Sound (Murray and Ricker -unpublished)„ The surficial geology of the upper Jervis Inlet area was mapped on a reconnaissance basis by LeRoy (1908). Since then no further work has been published for this area. Bacon (1957) des cribed the geology of the lower Jervis Inlet area. The coast mapping project of the Geological Survey of Canada, which is presently underway, will give the first unified map of the geology of Jervis Inlet. The physical oceanography of Jervis Inlet has been studied by many workers. Pickard (1961) described and classified the inlets of the B.C. coast and presented observations of optical tur bidity (Pickard and Giovando 1960). Lazier (1963) studied Jervis Inlet as an example of a deep silled inlet and described a circulation of unknown period. IV. Field Work and Acknowledgments Field work was carried out from the vessels C.S.S.Ehkoli and C.S.S.Vector of the Department of Energy, Mines and Resources of the Federal Govern ment. The assistance of the officers and crew of 8 these vessels was invaluable. Detailed bathymetric charts (field sheets) of the study area were generously supplied by the Canadian Hydrographic Service. Financial support was gratefully received from the Dean's Research Fund of the University of British Columbia, National Research Council of Canada, Geological Survey of Canada (Contract EMR-63-IU), Special Projects Division of Eear Creek Mining Company and the International Nickel Company of Canada. Dr. J. W. Murray of the Department of Geology at the University of British Columbia was the supervisor of this work. CHAPTER 2 y GEOLOGIC HISTORY AND REGIONAL GEOLOGY Io Geologic History of Southwestern B.C. Early Jurassic marked the beginning of tectonic events which were to ultimately form the Insular and Coast Mountain region. This orogenic episode, which was to continue in stages to mid-Tertiary time,involved a late Paleozoic eugeosynclinal-like succession -®f sedi mentary and submarine volcanic rocks. Intense folding, metamorphism and uplift were accompanied by volcanism and the development of large plutonic masses. Success ive stages of tectonism followed by erosion removed much of the rock cover from the batholithic cores. The derived sediments were deposited in flanking basins under marine and brackish conditions. The resulting land surface was a peneplain of low relief and average elevation of 900 to 1200 feet (270 to 370 meters)be.low the present average. (Holland, 1964). Differential uplift of this ercaion su-r-Jacc. occurred during early Tertiary with greatest movement along two main axes of intrusion. Separating these axes, now the Insular and Coast Mountains, was a trough now corresponding to the Strait of Georgia. Sediments dervied from further erosion of rejuvenated areas were deposited in this Coastal Trough along with lavas and fragmental prod ucts of regional volcanism. Erosion continued through the middle Pliocene and further unroofed the granitic 10 cores of the uplifted areas. The land surface was reduced to one of low to moderate relief, co extensive with a similar surface with a relief of 1500 to 2000 feet (460 to 610 meters) in Central British Columbia. (Holland, 1964). Late Pliocene time marked the advent of renewed differential uplift along the previously active axes resulting in rejuvenation of the erosive power of all the streams. A transverse upwarping divided the coastal trough into the Hecate Depression to the north, and the Georgia Depression to the south. The late Tertiary erosion surface was deeply dissected and partially to almost completely destroyed. The present topography is essentially that of the late Pliocene, considerably modified by Pleistocene glaciations. During Pleistocene time, southwestern B.C. was extensively glaciated by cirque, valley, and contin ental glaciers. Like the tectonic history of the area, the glacial history is very complex. Studies indicate at least two major Cordilleran ice sheet glaciations separated by an interglacial stage. Some peripheral areas may have been subject to three or more major ice advances. The sequence of major Plei stocene events in southwestern B„C. is given below. Table I. Time Stratigraphic Units for Pleistocene of Southwestern B.C. ., (after Armstrong et al, 1965) 1) Salmon Springs Glaciation ^> 37,000 years B.P. 11 Olympia Interglaciation <24, 500 y 15,000 37,-000 years B.P. During this period, ice was absent from the lowlands of southwestern B.C. This glaciation is probably the regional equivalent of the Wisconsin Glaciation of the mid-western United States. a) Evans Creek Stade 17,000 - 25,000 years B: By definition, during this period, large alpine glaciers formed and reached their maximum extent. In British Columbia, expansion of the glaciers apparently resulted in ice-sheet formation. b) Vashon Stade 13,000 - <21,000 By definition, the Vashon is the last major climatic episode during which drift was deposited by continental ice origina ting in British Columbia, and occupying the lowlands of southwestern B.C. and northwestern Washington. c) Everson Interstade 11,000 - 13,500 years B This period began with the invasion of the lowlands by the sea, and ended with either the advance of the Surnas ice sheet or, the withdrawal of the sea and the dis appearance of the floating ice. d) Surnas Stade 9,500 - 11,000 years B.P A climatic episode during final stages of emergence of the Fraser Lowland when a valley glacier occupied the eastern part of the lowland. This glacier may have been only a local advance of the Cordilleran ice sheet. Fraser Glaciation approx. 9, 500 -)>15,000 \25, 000 years B.P. 1-2 The valley glaciers widened and deepened trunk valleys to a U-shaped cross-section leaving truncated spurs, hanging valleys and scoured rock surfaces. A result, perhaps not immediately evident, was the over-deepening of many of the valleys. For example, the maximum depth in Jervis Inlet is 385 fathoms (7 05 meters) and occurs about 10 nautical miles (18 kilometers) from the mouth, just north of Nelson Island. This depth exceeds by 178 fathoms (326 meters), the maximum depth in the Strait of Georgia. The valley glaciers which flowed into the Strait of Georgia coalesced and flowed south and southeast down the Strait then southwest to west across the end of Vancouver Island. The ice sheet which accumulated during the Vashon attained an estimated thickness of from 5,000 to 8,000 feet (1500 to 2400 meters). The weight of the ice sheet depressed the land surface with respect to sea level. The net effect on the crust of unloading, due to the waning of the ice sheet, was the emergence of the land surface. The height of emergence, as measured from raised beach deposits, in the vicinity of the mouth of Jervis Inlet was 424 feet (129 meters) at Texada Island 13 and 500 feet (152 meters) at Campbell River. (Holland,1964). With the retreat of the Cordill-eran ice sheet, the heavily scoured and probably nearly sediment-free inlets became depositional basins for glacial and glaciomarine sediments. II. Original of Fjords The structural pattern of the B. C. coastline has two components—one dominant and forming a crudely rectangular network in the north-west and north-east directions, and the other subordinate in the north and east directions(Peacock 1935). The former is concordant with the north-westward trending grain of the coastline and is thought to have originated from Jurassic tectonism. The sub ordinate trend is thought to have resulted from early Tertiary tectonism (Peacock 1935). A majority of the inlets have abrupt high angle changes in strike of their axes-a feature explainable by structurally controlled fluvial erosion. Rejuvenation of the earlier Pliocene erosion surface during the late Pliocene created a deeply dissected and immature topography before Pleistocene glaciations. Thus fjords are the drowned lower parts of immature valleys developed by fluvial erosion and modified by intense glacial 14 action (Peacock, 1935). Characteristic of fjords is extensive over-deepening and general presence of one or more thresholds or sills along their length. Over-deepening is apparently related to glacial erosion but the origin of the sills is debatable. Some sills are resistant granitic rock which for part of their length rise above sea level as islands or extend the shoreline to create a narrows. Sills formed intermediate along the length of many inlets are thought to represent terminal moraines deposited at points of furthest advance of valley glaciers. Ill. Regional Geology The reconnaissance map of upper Jervis Inlet by LeRoy (1908) shows Queen's Reach and Princess Royal Reach to be incised in a roof pendant of pre-Coast intrusive rocks. LeRoy stated these rocks were Paleozoic but James (1929) considers them early Mesozoic. LeRoy recognized two pre-Coast intrusive rock units consisting of a secruence of igneous rocks which he correlated with similar rocks on Texada Island (the Texada Group) and a series of sedimentary rocks correlated with rocks at Britannia Beach (the Britannia Group). LeRoy found the Britannia Group rocks ,to be by far the most abundant in the upper Jervis Inlet area. The Texada Group outcrops near sea level in a narrow band along the north-east shore of Queen's Reach between Malibu Rapids and the head of Jervis Inlet. James' (1929) work on the Britannia Beach area shows a sequence of volcanics and sediments which he correlated with LeRoy's Britannia Group. Bacon (1957) combined the Texada and Britannia Groups of LeRoy with two other rock units and used the term Jervis Group to include all rocks of pre-batholithic age. LEGEND JURASSIC OR LATER •Coast Rangs bathclith/' (mainly qucrtz diorita) nQuartz fold porphyry AGE UNKNOWN Cl Basalt, ondesite and J associated pyroclasticV •Argillite. conglomerate^* grsywacke, sandstono • Attitude of bedding, faults * inclined x vertical ^ fault with dip ' ... Boundaries geological ^x„./ watershed FIG. 2 MIDDLE AND UPPER JERVIS INLET SHOWING GEOLOGY AND DRAINAGE PATTERN GEOLOGY AFTER BACON (1957) AND LEROY (1908) : MMM vet*, i 17 Table 2 Age Table of Map Units (after Bacon,1957) Map Unit Description 8 mainly coarse grained hornblende granodiorite Jurassic Coast 7 medium grained biotite granodiorite or later Intru sions 6 main batholithic mass; quartz diorite.granodiorite 5 quartz feldspar porphyry Intrusive Contact Age Un known Jervis Group basalt, andesite and asso ciated py.roclastics, minor limestone, dolomitic lime stone, chert, argillite mainly conglomerate., , grey-wacke, sandstone, argillite, greenstone metavolcanic rocks, meta-sedimentary rocks, metadiabase Gneiss Discrepancies exist where the pertinent areas of geologic maps by Bacon (lower Jervis Inlet) and LeRoy (upper Jervis Inlet) overlap. However, a tentative map of the geology of middle and upper Jervis Inlet was compiled (Figure 2) using Bacon's nomenclatureo Judging from rock specimen descri tions given by both authors, LeRoy1s Texada and Britannia Groups are approximately equivalent to Bacon's map units 4 and 3 respectively. Figure 4 1/6 square meter Petterssen grab sampler ready to be lowered b Edgerton, Germeshausen and Grier underwater camera assem bly. Not visible in picture is the compass and vane which is suspended beneath the camera„ c Rigging a Phleger corer just prior to lowering. The trian gular-shaped part with arm is a bottom contact crip. 19 CHAPTER 3 METHODS OF STUDY I. Field Methods 1) Positioning The sample localities were chosen beforehand and plotted on a large-scale chart of the area. Position ing was done by combined use of echo sounder and Decca radar. Since the inlet is narrow and very steep-sided in most instances, radar was used to good advantage. However, when more accurate positions were desired so that a station could be reoccupied, the position was taken by sextant, Sampling station locations are show in Figure 3 (in pocket), 2) Sample Collection Samples of surficial sediments were collected by use of a Potterssen grab sampler (Figure 4a) which sampled an area of 5.9 square feet (1/6 square meter) . The ^4wkwardness of this sampler, due to its weight, was more than compensated for by its relia bility, especially when sampling the deep basins or precipitous sides of the inlet. The usually gela tinous block of sediment recovered was broken open and the laboratory sample was taken from the relatively undisturbed interior. This sample was placed in a one-quart plastic container and sealed with plastic 21 electrical tape. The remainder of the sampler con tents was discarded. However, if the sample contained coarse sand or greater-sized material, the remainder of the sample was seived with a 10 mesh (2 mm) seive and the +10 mesh material was also collected. Gravity cores were taken along the axes of the basins using a 1%" (3.2 cm) diameter Phleger corer (Figure 4c) and a 2 3/8" (6 cm) diameter gravity corer. In both instances the sample was retained within a clear plastic barrel liner which was removed from the corer, capped and used for sample storage. Experience showed it was advantageous to use both corers in the free-'fall mode rather than with a bottom contact tripping device. The corer was lowered until the meter block indicated the cutting edge was about 12 feet (4 m.) above the bottom. The winch was then stopped, taken out of gear and allowed to"free-wheel". Adequate penetration was achieved using a minimum number of weights. 3) Photography Underwater photographs were taken at selected stations using an Edgerton, Germeshausen and Grier photographic assembly (Figure 4b). This consists of an automatically timed 35 mm. camera and a 110 joule strobe flash housed in identical but separate stainless 22 steel pressure resistant cylinders. Both cylinders are mounted on a frame - the camera in the vertical plane and the strobe flash angled so the intersec tion of the axes to the two units occurs at the focal point of the camera. Once started, the unit takes one picture every 12 seconds until the battery is drained, the film is consumed, or the unit is raised to the surface and stopped by disconnection of the synchronizing or power lead. Generally, 100 foot rolls of Kodak Plus-X film with an ASA rating of 125 were used. With the camera focused at 6 feet (1.8 meters), the optimum diaphragm opening was found to be f8 - fll. A compass was hung from the frame in the camera field. The compass needle is usually visible in the photograph (sometimes special processing is required). The compass assembly includes a 10 inch (25 cm) vane, which, by propor tioning, can be used to determine scale as well as to indicate current direction. At the time the photographic stations in Jervis Inlet were occupied, the assembly was positioned at the correct distance off the bottom by trial and error. The assembly was followed by echo-sounder until near the bottom. 23 When 3 to 6 fathoms off bottom, the rate of lowering was decreased until the bottom was touched by the legs of the frame. This touchdown could be detected at the winch. The assembly was then raised to the desired height off the bottom. This procedure was repeated every 5 to 10 minutes while on station. Useable pictures were obtained but the success ratio was only about one frame in twelve and sometimes one in twenty depending on the depth of operation. Subsequently, a bottom-finding pinger has been included in the assembly. An omnidirectional trans ducer pings at a set rate thus allowing the distance from the assembly to the bottom to be measured from the difference in arrival times between the direct pulse and the reflection of the pulse from the bottom. The use of this pinger on other projects resulted in an increase of the success ratio to one frame in five or sor.etimes loos b^Wef. The films were processed commercially after the cruise returned. Lack of space, time and necessary equipment aboard ship precluded on-the-spot process ing, which however, would have been advantageous. 24 4) Echo Sounding and Continuous  Seismic Profiling The foathymetric map of Jervis Inlet (Figure 6 - in pocket) was drawn from the Canadian Hydro-graphic Service Field Sheet No. 2228-L entitled "Jervis Inlet — Northern Portion". However, a more detailed survey was made of the manganese concretion locality. Five lines were run transverse to the axes of the inlet over Patrick Sill. These were tied in by four lines run consecutively on a rectangular pattern. A 38 KHz Kelvin-Hughes sounder gave good records, even though the subsurface topography was steep. Positions were plotted every two minutes by Decca radar. This data was corrected and aombined with data from the Field Sheet in order to compile a large-scale bathymetric map of Patrick Sill (Figure 37 - in pocket). During I.O.U.B.C. Cruise 66/1, a continuous seismic profile was made from the head to the mouth of Jervis Inlet (Tiffin and Murray, 1966). The 5000 joule seismic profiling equipment consisted of Edgerton, Germeshausen, and Grier power supply, capacitor banks, and trigger, coupled to a "spark-array" transducer. Echos were picked up by hydro phone, amplified, filtered, and then recorded by an Alden wet-paper Precision Graphic Recorder. 25 II. Laboratory Methods 1) Grain Size Distribution in Sediments The procedure for processing a sample is illus trated in Figure 5. Each sample was kept frozen until analyzed. To begin, the sample was first thawed and then homogenized by stirring. Three sub-samples were taken by means of a 5/8 inch (16 mm) inside diameter glass tube with a tapered cutting edge. The sub-sample was extracted by rotating the tube and applying a slight vacuum by mouth to the free end. As the tube was pushed into the sediment, the level of the sediment within the tube was kept the same as that surrounding. In this way, any biasing of grain size parameters etc. by sub-sampling techniques was hopefully minimized. The sub-samples for clay mineral analysis and total carbon content were air-dried. Carbon analyses were made using a Leco induction furnace and CO2 absorption system. Grain size analyses were made by dry sieving for the y 63/u material and by hydrometer for the <(63^u material. Before sieving, the )> 63/u material was given successive treatments with hydrogen peroxide in order to dissolve organic components. This step was included as the concentration of organics was sufficient to prevent disaggregation 26 CLAY MINERAL SAMPLE ANALYSIS ' -a—' ( X-RAY DIFFRACTION ) WASH WITH" DISTILLED H90 MOISTURE CONTENT TOTAL CARBON CONTENT (LECO) CENTRIFUGE SUPERNATANT SALT — EVAPORATE LIQUID CONTENT .SEDIMENT - WET SIEVE WITH DISPERSANT + 62^ FRACTION 62/* FRACTION. WASH WITH H20 AND DRY DISSOLVE ORGANICS (HgOg) DRY SIEVE (\/Z 0 INTERVAL) + 62,*. FRACTIONS STORE -f 125^ 1 - 62^ FRACTION FRACTIONS -125 4-62/.'- FRACTIONS r BROMOFORM, SEPARATION LIGHTS HEAVIES t t Is*, rxr> «a «a» e=» «=» c=» .SPLIT FOR GRAIN STIR AND MAKE UP TO IOOO ml. ! HYDROMETER ANALYSIS PIPETTE FOR Tt) MOUNTS 27 especially if the sediment was dried. Grains with a diameter of <^ 63derived from seiving the coarse fraction were added to the sedimentation cylinders before the hydrometer analyses were made. Hydrometer analyses were conducted according to ASTM specification (ASTM D422-61T) using a 152H hydrometer. The initial weight of the sub-sample for grain size analysis was estimated so the<^63/u material would weigh from 10 to 15 grams. Prelimin ary analysis indicated this weight of material in suspension gave optimum results. All hydrometer analyses were done at 84°F (30°C) because room temperature was not likely to exceed this tempera ture. The constant temperature bath used maintained the set temperature as long as this was above ambient. However, the bath had no direct means of cooling if ambient exceeded set temperature. Initially, the tines at which hydrometer read ings should be made to derive a weight distribution in even 0 values (i.e. 4.50, 50, 60, etc. where 0 = -log2 grain diameter in mm.) were taken from a chart calculated for the settling velocities of quartz spheres. However, these times did not give the weight distribution in even 0 values for the material- being 28 analysed. Through a series of successive approxi mations, appropriate reading times were calculated. The total weight of sediment in the -63/u fraction (tj2f weight) was difficult to determine by hydrometer. Thus when a hydrometer analysis was complete, the sediment was stirred back into suspen sion, and the tj# weight was determined by immediately pipetting off 50 ml of suspension. 2) Mineralogy of Sediments Mineral analyses were carried out on select samples taken from the axes of the basins. The 63/u to 88/u and the 88/u to 125/u seive samples were combined and then a heavy mineral separation was made using bromoform. Thin sections were made of both the light and heavy fractions and the mineralogy was determined petrographically by point-counting. The clay mineral analyses were conducted on separate sub-samples of the main sample. The size fractions were separated according to the procedure described by Kittrick and Hope (1963). X-ray diffraction analyses were carried out on the 20 - 5/u, 5 - 2/u, and 2yu fractions. The \2^u fraction was given a series of treatments to aid in 29 identification of the clay minerals present. These were K saturation, K saturation heating to 300°C, K saturation heating to 500°C, Mg saturation and Mg and glycerol saturation, The iron extracted in preparation of the clays for X-ray analysis was determined by atomic absorption spectrophotometer. 3) Gravity Core Analyses The large diameter gravity cores were split by using a circular saw to cut the core barrel and a piece of thin piano wire to cut the sediment. Structures in the sediments were revealed by running a stream of water down the cut face. No analyses were carried out on the sediments due to time limitations. The cores were sealed in con tainers for future reference. 4) Composition, Structure and Abundance  of Manganese-Iron Concretions The elemental composition of the manganese concretions was determined by Dr. E. V. Grill of the Institute of Oceanography at the University of British Columbia (Grill, Murray and Macdonald 1968). The Special Projects Division of Bear Creek Mining Company Ltd. and the B.C. Department of Mines carried out independent analyses. The mineralogy of the concretions was determined by X-ray diffraction. 30 Polished sections of the concretions were made for reflected light studies and photographic purposes. To make the sections, the concretions were first impregnated due to their very friable nature. Impregnation was carried out in a vacuum dessicator using Castolite resin. The proportions of resin to thinner to hardener used were in the ratio of 24 mis. to 8 mis. to 3 drops. A curing time of 24 hours in an oven at 80°C was used. The entire concretion was impregnated and then cut. A second impregnation was necessary before the cut surface could be polished satisfactorily. The final polishing was done on a diamond lap. The estimate of the weight of dried manganese concretionary material per unit area was made from a typical 1/6 meter2 (1.8 feet2) Petterssen grab sample. The concretions recovered were dried and oxide materials were broken away from the nucleat ing rock fragments and weighed. 31 CHAPTER 4 OCEANOGRAPHY I. Bathymetry The study area encompasses two basins separa ted by a sill. The upper or more northerly basin coincides with Queen's Reach, while the lower coin cides with the upper two-thirds of Princess Royal Reach. The bathymetric map is presented in Figure 6 (in pocket). The sill depth of the upper basin is 160 fathoms (290 meters), while that of the lower is 220 fathoms (400 meters). The maximum depths are 190 and 290 fathoms (348 and 530 meters) res pectively. The slope along the basin axis at the head of the inlet measures 1°50', but rapidly increases to 10°36'. Beyond Station J-102, the slope slowly decreases to an average of 0°14' for the remainder of the length of the upper basin. The slope of the bottom of the second basin is approximately 0°021. The south-facing flank of Patrick Sill dips at 18°30' on the axial line but the angle increases towards the inlet sides. Transverse sections (Figure 7) illustrate the modified catenary or U-shaped cross-section which is typical of glacially-scoured valleys. 32 In the upper basin, the 160 fathom (293 meter) contour marks the approximate break in slope between the sides and bottom of the inlet. In the lower basin, the break in slope occurs at 280 fathoms (513 meters). The slope of the inlet sides ranges from 10° to 47° and probably averages about 35°. Echo and wire soundings at Station J-160 indicate a very steep slope. The echo-sounder recorded a depth of 200 fathoms (366 meters), while a wire sounding gave a depth of 292 fathoms (534 meters). Pickard (1961) noted from transverse sections that a flat bottom was characteristic of the upper basin and was most pronounced just inside the sill at the deepest portion of the basin. From this and other data (i.e. optical turbidity), Pickard postulated the existence of turbidity currents within the upper basin. Also noticeable on the sections is the transverse asymmetry of the inlet at sea level and below. The bathymetric map of Upper Jervis Inlet shows several banks within the upper basin, while none appear within the lower basin. These features are found along the margins of the inlet. Also noticeable is the biconcave or venturi shape of 55 Vertical Scale » Horizontal Scolo Nautical Miloo FIG. 7 TRANSVERSE SECTIONS Patrick Sill. Pi section transverse to the basin axis through Patrick Sill reveals a distinct medial depression or "V" notch. The origin of these features will be discussed later. II. Temperature and Salinity (after Lazier, 1963) The average vertical profiles of temperature and salinity for Jervis Inlet in March 1962 are given in Figure 8. These represent more or less stable conditions during the year Lazier studied the inlet circulation (March 1962 - March 1963). Temperature °C Salinity %o a co o E 100-Figure 8 Average Vertical Profiles of Temperature and Salinity for Jervis inlet during March i962 After Lazier, IS63 35 The average salinity-depth profile indicates that over most of the inlet there is a lack of a homogeneous surface layer of low salinity and thus there is no distinct halocline. The salinity increases from the surface to depth with a decreas ing rate. Surface water salinity reaches 50% of the deep-water salinity at a depth of about one fathom, and 90% of the deep-water salinity within a depth of between 4 to 11 fathoms„(Pickard 1961). The average temperature-depth profile resembles the salinity-depth profile. However, as the mean daily temperature increases with the advent of summer, the surface waters warm considerably resulting in the formation of a temperature minimum at about 15 fathoms. This minimum remains in evidence until October. At this time the decreasing surface temperature results in a temperature maximum at about the 15 fathom depth. III. Oxygen Content and Circulation (after Lazier 1963) Jervis Inlet is classed as a deep-silled inlet in that the sill at the mouth is of sufficient depth so that tidal waters may enter and leave without unduly modifying the vertical stratifica tion of the resident inlet waters. Flows may occur 36 in both directions simultaneously. Since the surface runoff into Jervis Inlet is small, the estuarine circulation is generally weak. Changes in metcorlogical and oceanographical con ditions in the area will produce flows which will dominate the estuarine circulation. Oxygen profiles display most distinctly the circulation within the inlet.(Fig.9) Lazier des cribed a mid-depth oscillatory flow of unknown period which occurred during the winter of 1963-63. A possible mechanism for this flow is described by Lazier as follows: "It was proposed that strong southwesterly winds in the autumn, particularly those associated with Typhoon Frieda, caused the water level within Jervis Inlet to rise. To compensate for the increase in water volume, a mid-depth outflow was created. This outflow produced a horizontal pressure gradient that tended to reverse the direction of the flow. When the flow reversed, the water level in the inlet again became greater, and the surface outflow increased. A negative correlation between the direction of the mid-depth flow and the depth of the surface layer was noted. The low oxygen content in the water at mid-depths near the head of Jervis Inlet was attribu ted to weak estuarine circulation ;which results in slow removal of water near the head." FIGURE 9 WATER CIRCULATION AS AFTER LAZIER, 1963 INDICATED BY LONGITUDINAL OXYGEN PROFILES IV. Tides The British Columbia coast is subject to semi diurnal tides which have marked irregularities between the heights of successive low waters. The time of either high or low water at the heads of the inlets is not more than ten minutes later than at the mouth. The range at the head is from 1 to 1 per cent greater than at the mouth (Pickard,1961). Current directions were calculated for the man ganese locality (Station J-19-67) by use of the compass which hangs in the field of view of the underwater camera. The directions indicated coin cide with the direction of the surface tidal flow i.e. northwest on a flood tide and southwest on an ebb tide. Measurements were made when the compass was 1 to 2 feet from the bottom. V. Optical Turbidity (after Pickard and Giovando, 1960) Figure 10 illustrates measurements of optical turbidity made in Jervis Inlet on two occasions -February 1958 and June 1958. A light-scattering method of measurement was used and values of optical turbidity represent fractional reduction in light intensity per meter length due to scattering. Data indicates that the majority of suspended material was minerogenic, 59 JUNE 1958 FIG. 10 OPTICAL TURBIDITY ALONG JERVIS INLET 40 relatively transparent, and optically anisotropic. Also indicated was the presence of white opaque particles or transparent material with multiple internal reflecting surfaces. In the surface water samples collected in June, the diameters of the suspended particles ranged from 0.7 5 to 49/u with a geometric mean of 16.7 ± 1.5/u. Inorganic materials accounted for 99 per cent of the total. Samples collected in February contained particles with diameters ranging from 0.5 to 15/u having a geometric mean of 7.3 + 1.5/u. In these, inorganic materials accounted for 90 per cent of the total. Pickard suggests, as a bold estimate, a sedimen tation rate of 35 cm. per 1000 years. Current measurements made in Knight Inlet (Pickard and Rodgers, 1959) show that at a distance of 27 fathoms above the bottom in 190 fathoms of water, there exists a current of tidal period of a few centimeters per second. Thus the increase in turbidity in the bottom waters of Queen's Reach, as illustrated in Figure 10, may be due to a similar current reaching the bottom sediments. As an alter native, Pickard postulates the existence of turbidity currents. 41 CHAPTER 5 BASIN STRUCTURE AND SEDIMENT THICKNESS Figure 11 is a tracing from a continuous seis mic profile made by Dr. J. W. Murray and Dr. D. L. Tiffin of the Institute of Oceanography, University of British Columbia. The course along -which the profile was taken appears at the lower left hand corner of the figure, and also on Figure 3 (in pocket) with positions of sample stations. The "Spark-array" transducer produces an acoustic pulse by means of an instantaneous arc discharge underwater. The arc creates a plasma bubble, which rapidly expands and then collapses. The outgoing wave form consists of several peaks, and therefore, on the seismic record,a reflecting layer will appear as a closely spaced series of lines rather than one. Return or reflected energy is filtered and only that with a frequency in the 40 to 200 Hzrange is recorded. Use of low frequen cies results in good penetration but poor definition. Tiffin (oral comm,1969) estimates that a horizontal layer must have a minimum thickness of about 5 fathoms (9 meters) before it can be detected. On a slope this minimum thickness increases. 42 The slow firing rate of the transducer (one or more seconds per pulse depending on depth and energy/pulse) results in a record on which the vertical scale is greatly exaggerated and apparent angles are much steeper. The vertical scale on the recorder is calibrated with respect to the speed of sound in sea water (about 4800 feet/second). However, the speed of sound in Recent and Pleisto cene sediments varies from about 4800 to 7800 feet/ second. (Dobrin, 1960). Therefore sediment thick ness taken from a seismi.c record must be multiplied by the ratio of the speed of sound in the material/ 4800 f°r correction. The record presented in Figure 11 may be confus ing because many underwater peaks are evident. How ever, since the course followed was a zig-zag pattern, many of the apparent peaks result from approach to and turning away from the shoreline. Also, as the ship's speed was not constant, the horizontal scale is variable. Noticeable in Figure 11 is the relatively uniform sediment thickness in the basins. With the exceptions of the very thick accumulation off Malibu Rapids, sediment thickness in the upper 44 basin averages about 480 feet or 146 meters (assum ing an average speed of sound to be 7000 feet/second). The thicknesses range from 480 feet (146 meters) for section B-C to 67 2 feet (205 meters) for section F-G and 336 feet (102 meters) for section G-H. The increase in thickness in section F-G is probably due to addition of material from the delta at MalibUo In the lower basin the average sediment thickness is 720 feet (220 meters). Reflecting horizons within the sediments are thought to represent bedding planes. On the slope at the head of the inlet the more recent beds dip gently to the southeast (i.e.down the inlet). These beds appear to overlie flat-lying basal sediments, apparent in section B - C of Figure 11. Unfortun ately, only the base of the slope was covered by the seismic line and therefore the extent of the unconformity is not known. If the unconformity is traceable to the inlet head, perhaps it represents the overlapping of recent sediments deposited by slumping on sediments deposited during shelf ice conditions. Determination of sediment thickness on slopes such as the inlet walls and the sill cannot be made 45 because of record distortion inherent in the use of a low frequency and wide beam angle transducer. However, the action of the grab sampler as detected by hand on the winch cable and the damage done to the grab while sampling the inlet walls and V-notch of the sill, indicate that the sediment cover is often thin and sometimes lacking. Also, one of the underwater photographs (Figure 29a) taken in the concretion locality shows what is likely bedrock but possibly a large glacial erratic. Iron crusts (Figure 44) and sponges recovered from this locality appear to have been broken off rock faces. Although little or nothing can be determined about actual sediment thicknesses which have accumulated on slopes, or in the V-notch, some doubt is cast on the terminal moraine origin of sills. Patrick Sill and other similar sills have usually been regarded as terminal moraines origina ting from ice advance during the Sumas Stade. The concavo-convex shape of some sills (ecg.the inner sill of Howe Sound) tend to support this explanation. However, little is known about the extent of Sumas Stade glaciation except for the advance in the Sumas area of the Fraser Valley. Evidence suggests Patrick Sill is not a terminal moraine but a bedrock feature 46 covered,for the most part, by a sediment veneer of varying thickness. Several exposed sills are bed rock features and their position with respect to former ice flow channels offers a possible explana tion for thej.r formation. Major sills are generally located at points where valleys which confined the ice suddenly widen or, in the valleys of smaller glaciers where these met trunk glaciers at or near right angles. The sill creating Malibu Rapids is an example of the latter. At this point a smaller glacier would have coalesced with a much larger ice mass moving at right angles. At the point where coalescence of the ice masses occurred, the downward erosive capab ility of the smaller would likely be decreased resulting in a sill. The sill at Malibu is a bedrock feature and biconcave in plan. view. Possibly glacial action only sculptured the sill and the basic control is structural. Intense shearing at the point of coalescence of the ice masses would also mean that as the ice masses began to waste, these areas would melt the most rapidly due to the greater surface areas exposed by fracture surfaces. In this way,depending 47 on sea level, the biconcave plan and especially the V-notch of sills may be accentuated as these areas •would form sinks for the initially derived glacial debris. As wasting of the ice masses progressed, more and more of the released sediments would be deposited over the basin as a whole. The bathyraetric map of the study area (Figure 6) shows the presence of bank or ridge-like features along the sides of the upper basin. These features are not present in the lower basin. Even though seismic records are poor because of the slope involved, they indicate that the banks, like the sill, are bedrock features-possibly glacially sculp tured granitic plugs within the roof pendant of shale. Several such plugs are known to exist along the shore of the upper basin as the contacts have been explored for economic minerals. CHAPTER 6 SEDIMENTS A sample recovered with a Petterssen grab sampler represents at least the top 20 to 30 centi meters of sediment, assuming the material has the consistency of a typical marine silty clay. If Pickard's estimate of 35 cm/1000 years for the sedimentation rate in Jervis Inlet is assumed correct, a grab sample could conceivably represent a section with an age span of about 550 to 850 year While this is only an example, it does illustrate that parameters derived from laboratory analysis of sediment collected by grab sampler represent only a crude average taken over an indeterminable number of years. Interpretation based on these parameters should be made with this in mind. The surficiai sediments were classified textur-ally according to a scheme proposed by Shepard (1954). Basically, the sediments consist of equal parts of silt and clay-sized particles (Figure 12) with the amount of sand and gravel varying from 0.5 to 85 per cent. This characteristic is also noticeable in data presented by Cockbain (Cockbain 1963) for Vancouver Island inlets. Cockbain's data A/AA'AA/AAAA \A.- \'\.'}j,\/\>\'"\'\ CLASSIFICATION OF JERVIS SEDIMENTS ACCORDING TO SIZE DISTRIBUTE Depth lass than 100 fathoms Dspth greater than 100 fathoms GRAVi end SAND AVO\A?\/\A/V\^ A~A Vi\~A/•./\'\X-V"A••• v\AA£r"/VVvVV\T)vUVYlViAAAA7y\A/Wv\ /\/w\~\A~A ATT Q/</?'A'"A. A^A A A AA A A AAMa? A AA/\ A, \ AA A/w\/ V V V A A <\ A A/.AAA . V/(T> \ A VYSI \/y\/\AA/\A/\/v\A/\/\Ayy>/\/v\A/-.AA/\/\ A>t \ \A. y\ -v./* ~/^'y\'AVy\/\/V\/\/\/\/yi>/\^/\A/\MO'\Ao/VV A'TOWi '»/ AfoV*AAy\;\AA?V»'VV\^AAA^ v^^'AAJV^ v\//V\n/\/V° J A/VVAAAAAAAAAAV^ "A V-A7\7X->yV/rA/yV V\A?AAA7Y_;-AAA /wN/\A/V\AAAAAA7\A/W CLA' 50 for mainland inlets, plotted in the same manner, indicates a slight skewness towards clay-sized particles, with the average abundance of sand and gravel less than for Jervis Inlet. This difference may be a result of differences in sampling pattern and/or the below average sedimentation rate in Jervis Inlet. Figure 13, showing sediment grain size distri bution along the axis of upper Jervis Inlet is presented as a reference to the discussion of total carbon content, free iron content and mineralogy of the sediments. In each of the figures similar to Figure 13 the data being presented is superimposed on the bottom profile taken along the inlet axis. I. Colour The colour of the wet sediments is characteris tic of the coastal marine province and varies from a greyish olive (10Y4/2) to an olive grey (5Y3/2). The sediments of the upper basin tend to be more lightly coloured (i.e. greyish olive) while those in the lower tend towards the darker olive grey colour. Samples collected along the axes of the lower basin from Station J-146 southward contained varve-like laminations of olive grey alternating 52 with black material. These were the only samples within the lower basin to contain distinct concen trations of H2S. Samples from the upper basin which contained noticeable concentrations of H2S were collected nearshore in relatively shallow waters (Station J-101, J-102, and J-128). Cores taken by Dr. E. V. Grill indicate the presence of a thin (approx. 0.5.to 1.5 cm) and very fluid, dark yellow-brown to red-brown oxidized layer which forms at the sediment-water interface over most of the study area. This oxidized layer is not noticeable in the grab samples except in those collected over the concretion locality. In this area, this layer thickens to several centimeters and includes within its depth a layer of coarse sand to cobble-sized material. The olive-green colour of the wet sediments is thought to be due primarily to the organic content (Pantin, 1969). Reduced iron may add to the overall colour effect. Figure 16 illustrates the amount of iron extracted in preparation of samples for clay mineral analysis, and Figure 15 illustrates the total carbon content in these samples. Examination of these figures reveals a closer correlation between 53 total carbon content than extractable iron content with the darker colour of the sediments of the lower basin. When the samples are dried at toom temperature, the colour becomes light grey to light green-grey. II. Total Carbon Content The total carbon content was determined for each of the surficial samples collected. Figure 14 (in pocket) shows the distribution of carbon content over the entire study area. Figure 15 shows the carbon content in comparison with the weight of clay size particles along a longitudinal profile. In order to convert a total carbon percentage into an organic matter percentage Trask recommends a multiplication factor of 1.8 (Trask, 1938). Figure 15 shows the total carbon content to vary approximately as the weight of clay-size particles. This correlation is likely due to environmental energy factors. The organic material has a density near that of sea water with the majority of partic= les having an effective diameter in the silt size range. The result will be a very low settling velocity. Therefore, the maximum accumulation of organic debris will occur in the environment of 55 minimal energy as will the finest of mineral particles. The trend in the total carbon content ia a gradual increase with increase in distance from the head of the inlet. This trend is inter rupted in the area of the V-notch of Patrick Sill as the notch represents a much higher energy environment than its surroundings. There are several possible explanations for the observed trend. Much of the organic debris is thought to originate from phytoplankton. Thus, a lower productivity of the surface waters over the upper basin would give the observed carbon distribution pattern. However, another and perhaps more plaus ible reason could be differing factors of dilution of the organic debris by sediment being added and deposited contemporaneously. Grain-size analyses and optical turbidity data indicate that the river at the head of the inlet is the prime source of sediment for upper Jervis Inlet. Most of the sediment is deposited in the upper basin, thus diluting the organic debris more in the upper than in the lower basin. The greater water depth through which the organic debris must settle in the lower 56 basin apparently has little effect on the amount oxidized before being deposited on the basin floor. The difference in total carbon distribution between the upper and lower basins is best illus trated in Figure 14 (in pocket). Most noticeable is the relatively constant distribution in the upper basin versus the zonal distribution in the lower basin. Over a large part of the upper basin, the total carbon content is in the 2-3% range with exception of certain nearshore areas and the slope at the head of the inlet. Dilution and possibly lower productivity probably account for the low values at the head of the inlet. The localized, nearshore areas of higher carbon content coincide closely with log-booming grounds or streams which drain areas presently being logged. Considerable amounts of similar coarse organic debris are added from Princess Louisa Inlet to the delta on the Jervis Inlet side of Malibu Rapids. The lower basin can be divided into three apparently distinct zones on the basis of carbon content. The nearshore zone has a low total carbon content ( <C 2%) and is coextensive with the steep walls. The intermediate zone, with an average 57 carbon content of 2 - 3%, coincides with the break in slope between the walls and floor, while the deep zone, with a carbon content of 3 - 4% coincides with the basin floor. The higher values for samples collected within the bay along the southeast shore may be due to local addition of organic material by streams and/or increased produc tivity of the more sheltered surface waters. III. Free Iron Content In the preparation of a sample for X-ray diffraction analysis, it is necessary to remove free iron, the presence of which could cause fluor escence with resultant loss of sensitivity. The first stage of sample treatment was the dissolution of carbonate minerals by addition of pH5 Sf sodium acetate (NaOAc). Organic materials were then des troyed by the addition of hydrogen peroxide (H202)„ Free iron was extracted by adding sodium dithionite to the heated sample to which a citrate buffer had been added, stirring every two to three minutes for a total of fifteen minutes. The supernatant liquid, as separated by centrifuge, was diluted to 1000 ml. and analyzed for iron by atomic absorption. However, the supernatant liquid derived from the organic 58 oxidation step was often coloured ranging from light greenish to distinct red-brown indicating the presence of iron. These solutions were saved and analyzed similarly to those from the sodium dithionite treatment. The results of the analyses are plotted in Figure 15 which shows the total free iron as a sum of that extracted by the two treat ments. This procedure results in removal of only the adsorbed iron and will not destroy well cry stallized iron compounds nor extract iron from interlayer positions that it may occupy in certain minerals such as chlorite. The concentration of the iron extracted by sodium dithionite is relatively constant with dis tance from the head of the inlet, averaging about 0.35% (3500 ppm). The state of this iron in the sediments is probably as poorly crystalline particu late iron oxides and as iron adsorbed to clay minerals. A ratio of iron extracted by sodium dithionite to percentage of clay-size particles (all the samples had the same initial weight) indicates a pronounced decreasing trend from the head of the inlet. Work done by Dr. E. V. Grill on metal content of sea waters from upper Jervis Nautical Miles 18 16 .14 12 10 . 8 6 . . 4 ... 2 0 FIG. IS IRON EXTRACTED DURING SAMPLE PREPARATION FOR X-RAY ANALYSIS Inlet shows the source of particulate iron to be the river at the inlet head. Isopleths of suspen ded iron oxide content are approximately vertical with decreasing gradient from the source. Since the ratio curve tends to approach a base level, an explanation for the shape of the curve might be dilution of particulate iron with distance from the source, while iron adsorbed by clay-size particles (of which approximately 70% are clay minerals and micas) remains constant. The chemical state of the iron within the sediment extractable by hydrogen peroxide is not known. Possibly it was associated with the organic material. Comparison of Figure 16 and Figure 15 indicates a correlation between iron extracted by peroxide and total carbon content. The area with sediments containing minimal extractable iron corresponds to the manganese-iron concretion locality on Patrick Sill. The total carbon content and the percentage of clay-sized particles is also at a minimum because of the higher energy of the environment. Iron crusts recovered from the locality indicate iron is being precipitated on exposed rock surfaces. These crusts will be described later with the manganese concretions. 61 IV. Particle Morphology Granule-sized and larger fragments, when present, showed a wide range in degree of roundness, varying from angular to sub-rounded. Evidences of a glacial origin, such as scour marks and faceting, were not confirmed on any of the samples examined. Distinct faces on some rock fragments appeared to represent jointing. Mineral grains from the 500 - 300/u(1.0 - 1.50) and 88 - 63/u (3.5 - 40) fractions were examined by binocular microscope to determine the general shape and roundness and, if possible, any trends. Figures 17 and 18 are photomicrographs of the fractions examined for samples J-101, J-110, J-126 and J-19-67. Photograph J-126A shows a fragment of a sponge spicule and photograph J-19-67-B shows rounded and partially dessicated fragments which are thought to be glauconite-montmorillonoid pellets. The shape of many grains often reflected their granitic origin. Quartz was generally equidimen-sional as in the assumed parent rocks. Some of the grains were elongate and very angular and probably Figure 17 a Station J-101 (approx.11OX) Photomicrograph of mineral grains from very fine sand fraction (63 to 88yv.) b Station J-101 (approx„60X) Photomicrograph of mineral grains from medium sand fraction (350 to 500/u) c Station J-110 (approx,110X) Photomicrograph of mineral grains from very fine sand fraction (63 to 88/u) Figure 18 a Station J-126 (approx.110 X)Photo micrograph of mineral grains from very fine send fraction (63 to 88/u). The long prismatic fragment is a portion of a spicule from a silic eous sponge. b Station J-126 (approx. 60 X) Photomicrograph of mineral grains from medium sand fraction (350 to 500/u). Note angularity and apparent concoidal fracturing of quartz grains. c Station J-19-67 (approx.110 X) Photomicrograph of mineral grains from a very fine sand fraction (63 to 88/u) d Station J-19-67 (approx.60 X) Photomicrograph of mineral grains from medium sand frac tion (350 to 500/u). Note rounded, partially dessicated pellets in lower half of photo graph. These are tentatively identified as glauconite-montmorillonoid pellets. 63 FIGURE 18 64 were formed by shattering under high stress. Plagioclase and hornblende grains ranged from approximately equidimensional to elongate or lath like. External evidence of alteration was not common. Generally, the mineral grains were angular indicating erosion by physical processes followed shortly by deposition with little or no re-working. Along the axis of the basins, however, subangular to subrounded grains were found at the inlet head and on the nodule locality. A transverse section, just above Princess Louisa Inlet indicated the central basin sediments to be better rounded than the slope sediments. A similar section along the crest of the sill indicated the opposite in that angularity increased with depth. A third trans verse section, this one across the lower basin, indicated more rounding with depth. If rounding of mineral grains is occurring approximately in situ, the areas with greatest current action are the head of the inlet and the nodule locality. 65 V. MINERALOGY 1. Granule and Larger Size Material ( y 2.0 mm) Thin sections were cut from cobble-sized frag ments of each of the major rock types present in the sediments. Identification of minerals while they were still members of a rock-forming assemblage was much easier than when they were discrete grains in grain mounts. Rocks of approximately quartz dioritic to quartz monzonitic composition accounted for 65 - 7 5% of the granule-sized and larger material recovered in grab samples. Granite and minor pegmatite accounted for 5 - 15%, volcanics (usually basaltic) for 5 - 20%, and slates with occasional hornfels and amphibolite fragments for 0-5%. Hand specimens generally appeared fresh and revealed little evidence of alteration in the present marine environment. Where surface alteration was apparent, the mafic minerals had been most noticeably affected. Whether this alteration occurred in the marine environment is not known. A surface coloura tion, variable from light green to dark red-brown was particularly noticeable on leucocratic rocks.Polished sectioned revealed that this stain occurred as a rind 66 and extended to depths from 1 to 5 mm. The state of alteration within the stained area was no more advanced than without. The red-brown stains may have been due to absorbed iron oxides, whereas the green stains were possibly of organ.i.c origin. Thin sec tion study indicated the state of alteration of a mineral within a fragment bore little or no relation to distance from the fragment's surface. In a typical quartz diorite cobble, sodic plagioclase (Abgo-70) accounted for about 60% of the rock. The plagioclase was generally subhedral to anhedral and often complexly twinned, although in foliated rocks, twinning was much less noticeable. A majority of grains showed little or no alteration. Quartz formed about 10% of the rock and was usually anhedral and intergranular. Extinction patterns were often wavy or undulatory. Biotite was the prin cipal mafic mineral. The lathes were usually inter-tranular and sometimes bent, Pleochroism was masked by the green or sometimes yellow-green colour. Micas (in places) showed signs of alteration along contacts with other minerals. Potassium feldspar occurred in minor quantities. Unlike plagioclase, these grains 67 usually showed some signs of alteration. Also present were hornblende, sphene, zircon, and magnetite. In some speciments, hornblende was the principal mafic mineral. Typically the grains were subhedral. Pleo-chroism varied from yellow-green to blue-green^ In the more acidic quartz monzonite cobbles quartz occupied about 45% of the section, K-feldspar 25%, plagioclase 25% and mafics and opaques 5%. The constituent minerals displayed the same spatial rela tions. In the samples examined, alteration of feld spar species was equal and most pronounced in the cores of the crystals. The average composition of the granites was 30 - 35% quartz, 55 - 60% K-feldspar, and 5 - 10% plagioclase. The K-feldspar was often considerably altered. The volcanic rocks were basaltic. A specimen of porphyritic basalt contained phenocrysts of plagioclase (Anyg) an<3 pyroxene with minor amounts of olivine, biotite, magnetite, and hematite. The groundmass was dark brown to black. In hand specimen the rock appeared altered but thin section examina tion did not verify this. 68 i i Hornfels fragments were black, fine-grained, schistose and often porous. The cavities were lined with limonite and in places contained pyrite. Plagio clase feldspar and/or quartz made up 55% of the rock, hornblende 40%, and opaques 5%. Minor quantities of biotite and epidote were present. Hornblende crystals were arranged in parallel to sub-parallel alignment. There was little alteration of essential minerals. The hand specimens of amphibolite were fine grained, slightly foliated, and dark green in colour. Hornblen de comprised about 70%, plagioclase 25%, and quartz 5% of the rock. Alteration was relatively minor. 2. Sand Size Material (0.063 - 2.0 mm) Within the sand size and coarser fractions, the mineralogy was determined for only the fine sands of diameter range 62/u to 125/u (40 to 30). The individual grains within this fraction were essentially monomineralic. However, the majority of grains of the heavier, mafic minerals were in this size range and therefore, the calculated average composition will be skewed towards the mafic minerals. The mineralogy of 16 samples, all collected along the basin axes, was determined. Mineral content 69 of the sediments along transverse profiles was not investigated. The mineral percentages (by point count) are given in Table 3. Crystallographic pro perties and degrees of weathering were not tabulated. The following is a list of minerals identified petrographically in thin-sectioned grain mounts. Essential Accessory and Trace Quartz 'Epidote K-feldspars PyroxenPlagioclase feldspars Magnetite Chlorite ApatitBiotite Sphene Amphibole (principally Garnet hornblende) Tourmaline Zircon Sta. No. Quartz K Feldspar Plag. Indet. Mic Chlor as .Blot Amph 101 20.0 4. 5 35.5 7.9 2.9 0.9 15.9 102 23.8 4. 4 31.9 13.1 8.0 3.0 12.5 103 27.0 10. 4 29.0 7.5 7.1 2.2 7.4 104 32.6 9. 8 21.4 8.5 2.5 4.1 10.5 105 27.7 7. 2 21.5 8.5 13.1 4.3 12.2 108 19.3 2. 6 15.5 6.4 2.1 4.1 28.9 109 21.1 5. 1 42.1 8.9 9.1 4.8 8.2 110 24.8 8. 0 34.8 9.6 - „ -118 18.9 8. 0 50.0 3.3 8.2 1.2 6.0 19-67 22.6 5. 7 41.5 9.3 9.9 2.2 5.0 126 23.8 6. 7 49.5 4.3 4.4 4.9 4.1 132 29.8 3. 6 46.1 1.6 2.5 10.4 3.1 138 20.8 7. 44.2 5.7 3.3 8.2 5.7 147 18.7 5. 5 4.1.6 2.5 13.4 13.4 2.3 155 23.5 12. 6 40.3 6.3 8.9 3.5 3.2 Table 3 Mineral Abundances in Fi ne 3 ai Pyroxene Epidote Magnetite Apatite Unident. Clino. Ortho & Misc. 0.8 0.5 6.6 1.3 3.0 1.0 0.5 3.1 0.1 0.1 3.1 0.5 0.3 2.9 0.4 - 5.2 0.5 0.1 3.0 0.3 0.6 4.4 0.1 ~ 3.7 1.0 0.1 1.9 0.8 2.0 12.7 1.2 0.4 4.9 1.8 0.3 1.7 1.1 0.2 1.0 0.2 1.0 0.3 0.7 - 2.1 0.1 0.2 1.0 0.7 - 1.9 0.2 0.4 0.3 0.3 0.1 1.0 - 0.3 0.5 0.2 - 1.0 - 0.4 1.7 0.3 - 2.6 _ 0.1 0.6 0.1 -- 2.0 - 0.2 0.3 0.2 - 0.9 Fracti on (by percent) o 71 From 4% to 15% of the mineral grains counted were unidentifiable. Of these, about 7 5% appeared to be feldspars but were altered to such an extent that identification was uncertain. Rock fragments were included as unknown minerals. However, the occurrence of these, in this fraction, was minor. An average composition of the fine sand fraction of the recent sediments would be: Plagioclase 37% Biotite 5% Quartz 24% Epidote 3% Amphibole 8% Pyroxene 1% K-feldspar 7% Unidentifi- 9% Chlorite 6% able rock fragments and opaques There was a marked similarity of physical and optical properties of minerals between the fine sand fraction and the cobble fraction. Most of the coarse surficial sediments are thought to have been derived from Coast Range batholithic rocks, as this is the only available source of granitic rock. Roddick (1965) discussed the Coast Range batho-lith of the Vancouver North, Coquitlam and Pitt Lake map areas and gave an average composition of the granitic rocks. The average was an h-quartz diorite (where h denotes hornblende is more abundant than biotite) and had the following composition; 72 Plagioclase 56% K-feldspar 1% Quartz 30% Sericite 1% Hornblende 7% Opaques 0.5% Biotite 5% Chlorite 0=5% Roddick's average composition does not correlate with that of the marine sediment fraction examined. However, since the mafic minerals tended to be con centrated within this fraction, discrepancies would be expected. As the geology of the study area is unmapped, except on a reconnaissance basis, the mineralogy of rocks from possible sediment source areas is not known. Perhaps the granitic rocks of the sediment source area tend to be more acidic than in the area .studied by Roddick. The occurrence of minerals such as chlorite (6%) , epidote (3%) and pyroxenes (1%) in these percentages is probably an expression of the presence of pre-batholithic rocks which are mapped as outcropping over most of the watershed of upper Jervis Inlet. The igneous rocks of the Texada Group, as described by LeRoy (1908), are extensively altered and often large percentages of the minerals are secondary with calcite, chlorite and epidote being the most common. 73 Since the sediment samples collected for miner-alogic analysis were likely recently deposited, one would expect the influence of the surrounding out cropping rock to be more pronounced. However, if the pre-batholithic material in which the upper part of the inlet is incised is primarily slate, then the diameter of eroded particles may be smaller than the range examined. Another possibility is that the extent of the roof pendant of pre-batholithic material may not be nearly as great as presently mapped. However, assuming the gross geology, as mapped to date, to be reasonably correct, the source of sand size and larger material being deposited in the inlet must be relict Pelistocene deposits undergoing reworking in both terrestrial and marine environments. The presence of sills prevents loss of all but the very finest of material carried into the inlet. Several trends were noted within mineral groups.(Figure 19). Biotite, which gradually increases in abundance from the head of the inlet, was usually a dark green colour. However, over the sill, a red-brown variety predominates. Whether this effect is goochemic-a-l or an expression of present and/or past sedimentation patterns is not 75 known. From the head of the inlet to Station J-118, hornblende was the only amphibole present. However, from J-118 to the end of the study area, tremolite-actinolite was also found, although never with the same abundance as hornblende. Even.though sediment is being added to the inlet elsewhere than at the head, the relatively uniform sediment mineralogy from Station J-110 down the inlet indicates most sediment sources have a similar mineralogic composition. The exception to the approximately uniform trend in mineralogy occurs at the head of the inlet between Stations J-101 and J-110. Here it appears that slumping plays a major role in sediment distri bution. The break in slope occurring at J-108 corresponds with a marked increase in heavy minerals and a decrease in micaceous minerals. 3) Clay Size Material Mineralogic analyses of clay size particles were made for each of the samples for which the mineralogy of the sand and cobble fraction was deter mined. Table 5 gives the results of these analyses. Interpretation of abundances from diffractograms was made with reference to three sample interpretations 76 made by Dr. L. M. Lavkulich (Department of Soil Sciences, University of British Columbia.) The following scale of abundance was used: 5 Dominant 65 - 100% 4 Major 35 - 65% 3 Minor 10 - 35% • 2 Trace 0 - 10% 1 ^7one Clay mineral identification was based on X-ray diffraction data only. The relative amounts of Fe, Mg, and Al .in the chlorites was based on diffraction patterns given by Weaver (1958). Some peaks which appeared on the diffractograms could not be identi fied, but the magnitude of these indicated trace abundances. A list (Table 4) of the recognized mineral species and their |poij peaks (in Angstroms) according to treatment appears on the following page. MINERAL K K 300°C K 500°C Mg Mg & Glycerol Chlorite 14 14.2 14.2 14.2 14.2 11lite 10 10 10 10 10 Vermiculite 10-13 10 10 14-15 14 Montmo ri11on it e 12-14 10 10 12.8-14 17-18 Iliite-montmorillonite 10-14 10 10 10-14 10-18 111ice -vermiculite 10-13 10 10 10-15 10-14 111ite-chlorite 10-14 10-14 10-14 10--14 10-14 Plagioclase 3.18 3.18 3.18 3.18 3.18 Quartz 3.3 3.3 3.3 3.3 3.3 Amphibole (hornblende) 8.40 8.40 8.40 8.40 8.40 K-feldspar 3.24 3.24 3.24 3.24 3.24 Table 4 !00l| Peaks (in Angstroms) of Minerals in Clay Size Fraction 78 Plagioclase feldspar, quartz and amphibole (principally hornblende) were present in nearly constant proportions for the length of the inlet. K-feldspar occurred as a trace mineral in con siderably lesser quantities than plagioclase and quartz. As with some of the minerals in the coarser fractions, K-feldspar content increases significantly at Station J-118 where the influ ence of Princess Louisa Inlet would be expected. Several interesting trends were noted in the clay mineral abundances. There is insuffic ient information to determine whether or not the observed trends are geochemically significant. Many investigators (Grim, 1968) have concluded that variations in settling rates of clay mineral species are adequate to explain variations in abundances in situations like upper Jervis Inlet where there is a dominant sediment source. With increase in salinity the settling velocity of illj.te and kaolinite has been found to increase rapidly while that of the smectites (e.g. mont-morillonite) is little affected. The most noticeable trend is the disappear ance of montmorillonite and illite-montmorillonite 79 intergrade by Station J-103, i.e. shortly after the material enters the marine environment. With the disappearance of these species, vermiculite and an illite-vermiculite intergrade appear. The illite-vermiculite intergrade occurs with an approximately constant abundance for the remaining length of the study area. Vermiculite gradually increases in abundance until, on the sill, it becomes the dominant clay mineral. For the remain ing samples analyzed, vermiculite remains one of the dominant or near^dominant types. The overall trend is thus an increase in vermiculite with distance from the head of the inlet with the increase being accentuated on the sill. The only other type trend noted was the appearance of an illite-chlorite intergrade at Station J-118. This intergrade occurs in most samples taken farther down the inlet, but only in trace amounts. The two dominant clay minerals are Fe and Fe-Mg chlorite and illite. There is no noticeable trend in abundance of these. Montmorillonite is a dominant clay mineral in sediments collected from the inlet head. Therefore, if differential settling of the clay mineral 80 species is occurring, it is likely to be doing so on a smaller scale than on which upper Jervis Inlet was sampled. The apparent rapid disappear ance of montmorillonite and illite-montmorillon-ite intergrcide with deposition in the saline inlet environment suggests that potassium and magnesium are being absorbed from sea water by the montmorillonite. Absorption of these ele ments collapses the montmorillonite structure resulting in the formation of illite and chlorite. 81 TABLE 5 RELATIVE ABUNDANCES OF CLAY MINERAL SPECIES J-101 Illite 3-4 Fe chlorite 3-4 Illite-montmor. 3-4 Montmorillonite 3 Amphibole 2 Plagioclase 2 Quartz 2 J-103 Fe Chlorite 3-4 Illite 3-Vermiculite 3 Illite-vermic. 3 Plagioclase 2-3 Quartz 2-Amphibole 2 J-105 Fe chlorite 3-4 Illite 3-Vermiculite 3-4 Illite-vermic. 3 Plagioclase 2 Quartz 2 Amphibole 2 J-109 Mg-Fe chlorite 4 Illite 3-4 Vermiculite 3 Illite-vermic. 3 Plagioclase 2 Quartz 2 Amphibole 2 Illite-chlorite 2 J-118 Mg-Fe chlorite 3-4 Illite 3-Vermiculite 3-4 Illite-vermic. 3 Plagioclase 2 Quartz 2 Amphibole 2 Illite-chlorite 2 J-102 Fe chlorite 4 Illite-montmor. 3 Illite 3 Montmorillonite 3 Plagioclase 2 AmphiboleQuartz 2 J-104 Mg-Fe chlorite 4 Illite 3-4 Vermiculite 3 Vermic.-illite 3 Plagioclase 2 Quartz 2 Amphibole 2 J-108 Fe chlorite 4 Illite 3-4 Vermiculite 3 Illite-vermic. 3 Plagioclase 2 Quartz 2 Amphibole 2 J-110 Mg-Fe chlorite 3-4 Vermiculite 3-4 Illite-vermic. 3-4 Illite 3 Plagioclase 2 Quartz 2 Amphibole 2 J-123 Mg-Fe chlorite 4 Illite 3-4 Vermiculite 3-4 Illite-vermic. 2-3 Illite-chlorite 2 Quartz 2 Plagioclase 2 Amphibole82 TABLE 5 (contd.) J-147 Vermiculite 4 J- 19-67 Vermiculite 3-4 Mg Fe chlorite 3 Fe chlorite 3-•4 Illite 3 Illite 3 Illite-vermic„ 3 Illite-vermic B 2-3 Quartz 2 Quartz 2 Illite«chlorite 2 Plagioclase 2 Plagioclase 2 Amphibole 2 Amphibole' 2 Illite-chlorite 2 Fe chlorite 4 J-•138 Fe chlorite 3-•4 Vermiculite 3--4 Illite 3-•4 Illite 3 Vermiculite 3 Illite-vermic. 2--3 Illite-vermic„ 2-•3 Quartz 2 Illite-chlorite 2 Plagioclase 2 Quartz 2 Amphibole 2 Plagioclase 2 Illite-chlorite 2 Amphibole 2 Vermiculite 4 J-•155 Fe chlorite 3-•4 Mg Fe chlorite 3--4 Illite 3-•4 Illite 3--4 Vermiculite 3-•4 Illite-vermic. 2--3 Illite-vermic. 2-•3 Plagioclase 2 Quartz 2 Quartz 2 Plagioclase 2 Amphibole 2 Amphibole 2 Illite-chlorite 2 Illite-chlorite 2 83 VI. GRAIN SIZE DISTRIBUTION The grain size distribution and corresponding parameters were calculated with a computer program developed by Dr. A. J. Sinclair of the Department of Geology, University of British Columbia. Calculations were based on a cumulative curve plotted with arith metic ordinates and developed by joining successive data points with straight lines. A minimum grain size was needed in the program and was arbitrarily set at 0.06/U ( 14 0 ) The following is a list of parameters calculated for each sample. Mean Arithmetic Graphic (Folk) Graphic (Inman) Standard Deviation Arithmetic Graphic (Folk) Graphic (Inman) Inclusive Graphic Phi Quartile Sorting Coefficient(Trask) Skewness Moment Phi Quartile Graphic Inclusive Graphic Kurtosis Moment Graphic Transformed Graphic Parameters used for interpretation in this study 84 were the graphic mean (Folk), graphic standard deviation (Folk), inclusive graphic skewness, and graphic kurtosis. These parameters were the more efficient with respect to the average grain size distribution of the sediment analyzed and the labora tory methods used. The majority of the sediment in upper Jervis Inlet contains abundant material in the silt and clay size fractions. Hydrometer analyses were taken as far as 0.98/u (10 0) with the result that a considerable percentage of the material (up to 34%) was not directly analyzed, i.e., was of diameter less than 0.98/u. The usefulness of grain size parameters in such an environment is therefore suspect. However, certain trends did show up in longitudinal profiles. The graphic mean as proposed by Folk reflects the average particle diameter of a sediment. Since the 0 diameter is defined as -log2 (particle diameter in millimeters) a trend showing an increase in 0 value would indicate a decrease in particle size. This parameter is calculated from the follow ing equations Folk and Ward (1957) Mg= 016 + 050 + 084 where 016, 050 and 084 are the 0 values taken from 85 a cumulative curve for the appropriate percentiles. However, the graphic mean gives no indication of the range of the grain size diameters and for interpre tive purposes the inclusive graphic standard devia tion must be considered simultaneously. The equation of this parameter, which gives the "sorting" or dis persion of the population ist Folk and Ward (1957) Oi = (084-016) - (095-05) 4 6.6 The inclusive graphic skewness and the graphic kurtosis should also be considered as a pair. The equations of these parameters are: Folk and Ward (1957) Skewness S,,= 084-016+2050 + 095-05-2050 2(084-016) 2(095-05) Kurtosis K_ = 095 - 05 2.44(07 5-02 5) Skewness and kurtosis are measures of non-normality of a distribution. The degree of asymmetry is measured by the skewness parameter. A negative value indicates a distribution curve asymmetric to the left (i.e. excess of coarse material), while a positive value indicates asymmetry to the right, (i.e. excess of fine material). A skewness value is a pure number and the absolute limits are -1.00 and +1.00. 86 Kurtosis is a measure of peakedness of a curve, and is a ratio between sorting in the tails and sorting in the central portion. Low values for kurtosis (i.e. 0.9) indicate better sorting in the tails than central portion. A distribution with low kurtosis is often bimodal. As with skewness, a kurtosis value is a pure number. The absolute limits of the measure a +0.41 and infinity, but most samples fall in the 0.60 to 5.0 range (Folk 1961). Figure 20 (in pocket) shows the distribution of sediments according to grain size based on Shepard's (1954) classification. Figure 21 (in pocket) shows the clay size particle distribution in upper Jervis Inlet and Figures 22 and 23 are longitudinal pro files of grain size distribution parameters. Frequency curves plotted from the grain size analyses indicate that the surficial sediments in upper Jervis Inlet can generally be divided into two dominant modes. The coarse mode usually falls in the 250 to 63/u (20 to 40) range, while the finer mode in the 16 to 4^u (60 to 80) range. These ranges represent the fine to very fine sands and Gutico! Miles i3 • ct ion 4-o Q 3-O or < a 2-1 8-\ < UJ4-165 152 147" 146 145' 144 I 138 !9L67I32 I 126 I25'i24 \iz MEAN STANDARD DEVIATION -260 -280 -300 -320 -340 FIGURE 22 MEAN AND STANDARD DEVIATION OF GRAIN SIZE . OF SURFICIAL SEDIMENTS ALONG AXiS ^ OF UPPER JERVIS INLET FIGURE 2 3 KURTOSIS AND SKEWNESS PARAMETERS OF SURFICIAL SEDIMENTS' ALONG AXIS OF UPPER JERVIS INLET § 39 and medium silts to clays respectively. The para meters presented in Figures 22 and 23 can be inter-, preted in terms of varying proportions of these two modes. Most noticeable on the map showing sediment type distribution was the uniform decrease in average particle diameter with distance from the head of the inlet within the upper basin. The cumulative . curves and histograms, in Figure 24 also illustrated this. The particle size distribution of sample J-lll represented an approximate average for the upper basin (0.9% sand, 51.9% silt, 47.2% clay). For the sediment collecting on the floor of the upper basin, the graphic mean (in jZf values)increased while the inclusive graphic standard deviation re mained approximately constant. Overall, kurtosis followed a slowly decreasing trend, and skewness an approximately constant trend. The principal source of sediment within the upper basin would therefore be interpreted as being the river and river delta at the inlet head. However, an appreciable amount of material is being added from Princess Louisa Inlet and the deltaic deposit formed along the shore FIGURE 24 LONGITUDINAL PROFILE . OF QUEENS REACH - CUMULATIVE AND FREQUENCY CURVES OF SURFICIAL SEDIMENTS 91 of Jervis Inlet at the point where the two inlets are connected (Malibu Rapids). Figures 22 and 23 indicate that addition of fine sand and silt is occurring in the vicinity of Station J-117. The mineralogy of the material being added closely resembled that of the sediment originating from the inlet head, probably indicating a common glacial origin. On an ebb tide, a vigorous tidal current (maximum velocity 10-12 knots, where 10 knots is equivalent to 520 cm/sec.) flows from Princess Louisa Inlet into Jervis Inlet. This tidal jet, at the point of maximum velocity, would be sufficient to carry cobble or boulder-sized material. Even though the velocity would attenuate rapidly once the water spread into Jervis Inlet, considerable reworking of the deltaic sediments would likely occur. The finer sands and smaller material would be deposited as foreset beds or carried in suspen sion by the weak estuarine circulation and deposited elsewhere. Subsequent slumping of the delta would carry the fine sands to the depths of the basins. Figure. 25 presents the cumulative and frequency curves for a transverse section of Queen's Reach at a point above Malibu Rapids. The abundance of the Nautical Miles FIGURE 25 TRANSVERSE PROFILE OF QUEENS REACH - CUMULATIVE AND FREQUENCY CURVES OF SURFICIAL SEDIMENTS Bottom Photographs The scale of the photographs depends on the camera to sea floor distance. Where present, the compass assembly can be used as a scale indicator. The diameter of the compass dome is 3 in. (7.55 cm.) and the length of the vane is 10 in. (25 cm.) On an average, the photographs cover an area of about 3 feet by 4 feet (approx. 1 m. x 1.3 m). Figure 26 a Note hummocky microtopography. Whether this is due to the presence of animals or to deposition^ processes is not known. b Note shadow of compass. This different aspect of the micro-topography is likely due to difference in camera angle. Figure.27 a Note the skate partially concealed in the bottom sedi ments. Hummocky microtopo graphy still prominent. b All photographs approx. 1/8 true scale 33 95 coarse mode decreases with depth, while that of the finer mode increases. Figures 26 and 27 are bottom photographs teken at Station J-126. These were taken at a depth of 130 fathoms (350 meters) which is the maximum depth in the upper basin. Each photograph covers an area measuring about 3 by 4 feet, (1 by 1.3 meters). The microtopography appears hummocky. The origin of these hummocks is not known, but animals obviously have some effect as shown by Figure 27a in which a skate had just partially buried itself in the sedi ment. However, photographs taken in an area where slumping is almost certainly occurring (Figures 34 and 35) show a similar topography. Thus,slumping is also a possible explanation for the topography pictured. Photographs of better quality, covering a larger area and preferably as stereo pairs would be very advantageous to such .interpretation. Perhaps the most interesting area, even from a sedimentologic point of view, is Patrick Sills The medial depression or V-notch and the flanks of the sill in line with the notch are apparently areas of sediment reworking. Figure 28 illustrates how the sediment characteristics change in passing from the upper to the lower basin over Patrick Sill. The FIGURE 28 LONGITUDINAL PROFILE OF LOWER QUEENS REACH AND UPPER PRINCESS ROYAL REACH CUMULATIVE AND FREQUENCY CURVES OF SURFICIAL SEDIMENTS 97 sediments collected above and below the sill (Stations J-125 and J-146 respectively) are very similar. The. concretion locality (Station J-19-67) sediments have a mean diameter of 63/u (40) with a high standard deviation. Skewness is high and kurtosis is low. Apparently a current is winnow ing the sediment, leaving a lag deposit of material with a dominant mode in the 250 to 125/u (20 to 30) range. This sediment is noticeably coarser than any other collected in the study area from depths greater than 100 fathoms (183 meters). The photo graphs in Figures 29 and 30 were taken near the nodule locality. The rock out-cropping in Figure 29a may be a glacially rafted boulder, but appears to be bedrock. The current direction would be per pendicular to the plane in which the gorgonian coral is growing. Figures 29b and 30a show the lag deposit and Figure 30b a more typical bottom sediment, near but not in the medial depression, indicating the maximum intensity of the current is confined to the medial depression. Sediments collected on the sill flanks at Station J-131 and J-143 were similar in grain size Figure 29 a Bedrock or large boulder in vicinity of concretion local ity. Low rates of sediment deposition in this area allow animal growth. Plane of gor-gonian coral in background is normal to current direction, (approx. 1/8 X) b Lag deposit in area of con cretion locality. Note abund ance of squat lobsters, (approx. 1/8 X) i Photograph taken on slope of medial depression. A low sedimentation rate is indicated by the presence of siliceous sponges etc. (approx. 1/8 1Q Photograph taken on slope of medial depression to the east of the concretion locality. A low sedimenta tion rate is indicated as well as minor influence of bottom currents (approx.1/8X) 100 distribution. If thr= origin of the dominant mode in the 250 to 125^/u (20 to 30) range were the crest of the sill, a current velocity of at least 25 cm/ sec. must flow in the medial depression. Slumping may carry the material derived from the sill to the flanks as the current velocity within the medial depression probably would not be maintained over the flanks. The two-way action of the current through the depression indicated by sediment parameters and size distribution curves, suggests a tidal origin. However, current action in the south easterly direc tion apparently is more pronounced. Cumulative and frequency curves plotted for sediments collected on the sill along a line trans verse to the medial depression are presented in Figure 31. Most noticeable is the very poor sorting, especially for samples collected on either side of the medial depression. The deeper the sample station, the more dominant is the coarse fraction. This trend is the reverse of that pictured in Figure 25. The very poor sorting and wide range of grain sizes indicates that the surficial sediments of the sill are probably of a glacial origin and, with exception /OJ 29i FIGURE 31 TRANSVERSE SECTION OF QUEENS REACH (OVER PATRICK SILL) CUMULATIVE AND FREQUENCY CURVES OF SURFICIAL SEDIMENTS .102 of those, sediments in the medial depression, have been little affected since initial deposition in Pleistocene times The distribution characteristics of sediments collected along the axis of Princess Royal Reach (lower basin) are presented in Figure 32. The two dominant sediment modes apparent on a similar longi tudinal profile for the upper basin (Figure 24) are apparent in sediments from the lower basin. However, the material collecting in the lower basin is orig inating from many sources, each with a localized effect, whereas that in the upper basin comes from one dominant source. This is even more apparent in Figure 20 (in pocket). Evidence of slumping was obtained from Station J-160. Figure 33 presents cumulative and frequency curves for a section approximately transverse to the axis of Princess Royal Reach. Depth recordings made while attempting to collect a sample on Station J-160 indicate that the south wall of Princess Royal Reach is much steeper than shown on the Hydrographic Service charts. The sediment sample collected on Station J-160 at a depth of 285 fms.(522 meters) contained abundant shallow and mid-depth faunal FIGURE 32 LONGITUDINAL PROFILE OF PRINCESS ROYAL REACH CUMULATIVE AND FREQUENCY CURVES OF SURFICIAL SEDIMENTS FIGURE 33 TRANSVERSE PROFILE OF PRINCESS ROYAL REACH CUMULATIVE AND FREQUENCY CURVES OF SURFICIAL SEDIMENTS 105 remains. Identified as contributors to the shell debris were blue mussels (Mytilus edulls), brachio-pods (Laqueus californicus vancouverensis), pele-cypods (Thyasira cygnus and an unidentified pectin) , scaphopods (Cadulus tolmei) and numerous solitary corals (Balanophyllia elegans and Caryophyllia  alaskensis). Also included in the organic debris were numerous wood fragments. One of the photo graphs taken showed a partially decomposed tree trunk embedded in the sediments Figures 34 and 35 are bottom photographs taken on Station J-160. The hummocky topography resembles that appearing in Figures 26 and 27 taken on Station J-126. Sediment collected at Station J-162 was pre dominantly medium to fine sand, likely deposited as a delta by the large stream flowing into the inlet nearby (Figure 33). Sample J-161 was collected further offshore from J-162 at the top of the steep slope leading to the basin floor. Sediments collected from J-161 resemble those deposited further inshore (J-162) but with a less pronounced medium to fine sand mode and a greater abundance of silt size material. However, the sediment collected at Station J-160 near the bottom of the slope Figures 34, 35 Photographs taken in area where abundant shallow water faunal remains were recovered. The depth this station was 285 fathoms (522 meters).Note disordered, humrnocky topo graphy. All photographs approx. 1/8 X true scale. /0<2 a FIGURE 34 BOTTOM PHOTOGRAPHS - STA J -160 b 1 only vaguely resembles that of Station J-161„ As Station J-162 is located near the south foot of the sill, perhaps the sediment accumulating there has more than one source. The pronounced double mode in the silt-clay region of particle size distribution also occurs in the sc>diment collected further down the inlet at Station J-145 (Figure 32). VII. Characteristics with Depth Four gravity cores, taken at sites shown in Figure 36, were split as previously described and logged visually. Generally the cores appear feature less. The average colour of the three cores taken in the upper basin matches that of the surficial sedi ments and was best described as grayish olive(10Y4/2) The core taken from the lower basin was a noticeably darker olive gray (5Y3/2). The majority of struc tures shown in Figure 36 appear as slight changes in hue which were most visible just after the core had been split and the surface smear washed away. The average grain size of the core material resembles that of the corresponding surficial sediments, i.e. the three collected in the lower part of the upper basin are silty clays, whereas the core material from the lower basin is a clayey silt with minor fine sand In. Cm. --20 12---40 24--60 -80 38-- — -- -100 48--120 - -- -140 I • GO--160 _ LEGEND Q O / i i / i ' / i / / / / ' / / ? I 2\ ^—i FIG. 36 UPPER Q Gastropod ff Scaphopod Q Pelecypod Organic fragments (wood etc) . GRAVITY CORES FROM -JERVIS INLET. ^2 Dark green gray clay Sand lens Sand grains Void (due to dessication) Minor structures 110 The core taken at Station J-123 contained three distinct, but thin, layers of fine sand and a two-foot layer of a green-gray clay. The core taken at J-126 contained a single thin sand layer and a much thinner layer of green-gray clay. This clay repres ented the only lithology that may be useful as a reference horizon. The sand layers appeared to represent discontinuous lenses. The competency under stress of the green-gray clay is much less than that of the more typical gray-olive to olive-gray sediment. Thus the material may be quite mobile as the sediment column compacts. This may explain the thick section in core J-123 but minor occurrence in core J-126 and absence in core J-110. Small diameter (Phleger) cores taken by Dr. E. V. Grill on and in the vicinity of the concretion locality on Patrick Sill contained green-gray clay starting at depths of 12 to 24 inches (30 to 60 centimeters). If large areas of the surficial sediments on the sill are underlain by this clay it would likely promote decollement and slumping into the basins on either side. Wood fragments were the most abundant coarse material. These were not evenly distributed throughout Ill the core, but tended to be abundant in particular horizons. Generally the fragments occurred with their long axis parallel or sub-parallel to the bedding indicating a non-turbulent deposition. However, in some layers within the cores, the frag ments were randomly oriented indicating a turbulent deposition as in a slump (e.g. core J-123 4'00" to 4'02")„ A few shells and shell fragments were visible in the cores. Recognizable were gastropod, scaphopod, and pelecypod shells. The latter two belonged to the same species recovered in the surficial sediment samples (i.e. Cadulus tolmei and Thyasira cygnus respectively). Possibly more, information could have been derived from longer cores. The collection of these would present no problem if the sediment mechanical characteristics at greater depths do not change markedly from those of the cores already taken. 112 CHAPTER 7 SEDIMENTATION IN JERVIS INLET Studies in the Fraser Valley by Armstrong and Brown (1965) revealed that much of the late Pleisto cene sediments are fossiliferous stony, silty clays. The stony clays are mixtures of varying proportions of marine drift and normal marine clays. Basal sediments are marine drift but these decrease in abundance upwards and are replaced by normal marine clays. This transition occurred with the waning of the continental ice sheet. Marine drift was carried by and deposited from shelf, berg and sea ice. As the ice disappeared, rivers became the principal method of transport. The river-borne materials were deposited as normal marine clays. The totaJ. depth of sediments within the basins studied was determined from seismic profiles, but the sedimentation rate cannot be calculated because of its time dependence. The average rate for the entire inlet of 14 inches (35 centimeters) per 1000 years estimated by Pickard (I960) for present sedi ment accumulation is still the most valid available. As Pickard mentions, this rate is likely higher within the upper reaches of the inlet where most of 113 the sediment is added to the system. Material added by slumping from the inlet sides would increase this estimated rate. The green-gray clay was an anomalous lithology within the cores. The depths of this clay may be misleading because the incompetent, nature of the material may allow horizontal and vertical movement as the total sediment column compacts. The green-gray clay was found within typical olive-gray marine sediments. Cores taken elsewhere along the continental shelf (e.g. Barclay Sound and Queen Charlotte Sound) also pene trate a horizon of green-gray clay. The significance of this clay is not known but in view of its appar ently widespread distribution further study may prove rewarding. Sediment is being transported to the basin floors by several mechanisms. These include settling through the water column of fine-grained fluviatile material and periodic slumping of coarser grained material from the steep inlet walls with the possible initiation of turbidity currents. The optical turbidity data presented by Pickard indicates that a major percentage (up to about 50%) of suspendable mater ial added to the inlet waters from the river at the head is carried down the inlet within the low salinity surface waters. There is however, a marked increase in turbidity on the bottom waters of the upper basin. In explanation Pickard suggested bottom currents or turbidity currents. Slumping almost certainly occurs from the steep inlet walls which have an average slope of about 35°. The abundance of shallow water faunal remains at the base of a steep submarine cliff in the lower basin (Princess Royal Reach) attests to this. Other active areas are the large deltaic deposit off Malibu Rapids, which is swept by the tidal jet through the narrows, and perhaps all the smaller deltas which likely became unstable during periods of rapid sediment accumulation. Slumping is also thought to occur at the inlet head and perhaps on the south facing flank of Patrick Sill where long unbroken slopes may result in the formation of turbidity currents. Gravity cores collected within the upper basin were examined only visually and revealed no distinc tive graded bedding. Future examination by X-ray or by thin-section may give more information. The lack of orientation of elongate organic fragments within certain horizons in the cores suggests deposition under turbulent conditions. 115 Sand lenses within the cores taken from the upper basin likely represent the influence of slumping from the nearby inlet walls rather than from the inlet head. Bottom photographs taken in the upper basin show a hummocky non-oriented topography. These support Pickard's conclusion that bottom currents are probably not the cause of the turbidity pattern described. If bottom currents were sufficiently strong to stir up the sediments, bed forms with a distinct orientation should have been visible in the photographs. There is a marked difference in grain size distribution between the upper and lower basins. Patrick Sill forms a boundary between these basins. To explain the depositional patterns, one must postu late either that the sill arrests the dominant de positional mechanism influencing the upper basin,or that the streams flowing into the lower basin have a much greater effect than those which flow into the upper basin. The relief of the sill is not sufficient to act as such an effective barrier if the majority of sediment is being added to the upper basin by the settling of particles through the water column. However, the sill is high enough that it would likely bar the passage of a density or turbidity current. 1.1 CHAPTER 8 AUTHXGENIC MINERALS I. MANGANESE CONCRETIONS 1) Source Area Manganese concretions occur in the medial depression or V-notch on the south-facing slope of Patrick Sill. (Figure 37 - in pocket). Depth of the locality is between 17 5 and 190 fathoms and the areal extent is estimated to bo 36,000 square yards (30,000 square meters). As mentioned, the sill is thought to be a bedrock feature mantled by post-Pleistocene sediments of varying thickness. There is little possibility these sediments pre-date the last major glacial advance in view of the estimated thickness of the ice sheet which passed over the area. The sediments collected with the concretions were generally similar to those collected elsewhere within the area studied. However, some sediment sam-. pies recovered from the concretion locality indicated the presence of a flocculant red-brown surface layer, one to several centimeters in thickness. The sedi ment within this layer often had a predominant coarse grained component which is thought to represent a 117 lag deposit. If the abundant fine sand noted at Station J-143 came from the concretion area, then the current within the V-notch must attain veloci ties of about 25 centimeters/second in order to move the sand. Underwater television observations of the locality substantiated the existence of a bottom current of approximately the velocity calcu lated. Bottom photographs taken on the sill show what appears to be a lag deposit associated with the concretions. Lag deposits are not evident in photo graphs taken near, but not on the concretion locality. Apparently, the strongest currents in the area occur where the concretions are forming. Sedimentation rates here should be correspondingly low. The total extractable iron and total carbon contents of the sediments recovered with the concretions were anomalously low. The low carbon content would reflect the sweeping away of the light organic material by the currsnt. Figures 38 and 39 are photographs of the concretion locality. 2) Age and Growth Rates The maximum age of the concretions would be determined by the time of ice retreat after the last major advance during the Pleistocene. This is Figures 38, 39 Photographs taken on the concretion locality. The rounded, exposed to par tially buried masses are manganese concretions. Note general coarse texture of surficial sediments. All photographs approx. 1/8 X true scale. ue a FIGURE 38 BOTTOM PHOTOGRAPHS-CONCRETION LOCALITi 12 estimated to be about 12,000 B„P.(Armstrong et al)„ Evidence that the concretions formed in situ is provided by the recovery of siliceous sponges having a thick manganese-iron oxide coating. The discoid shape and friable nature of the concretions precludes transport. The maximum thickness of oxide material measured on any one concretion was 1.4 inches (35 millimeters) The accumulation rate of oxide material is highest in the horizontal plane. Assuming the age of the concretions to be .12,000 years, the apparent growth rate would be .in the neighbourhood of 3 millimeters/ 1000 years or less. This value is somewhat lower than the general accumulation rate of 10 to 1000 millimeters/1000 years suggested by Manheim (1965) for shallow marine concretions. However, Manheim noted that concretion development in nearshore environments may be very irregular with wide varia tions over small areas. The porous nature and wide variation in lamination thickness of Jervis Inlet concretions suggests the deposition rate was erratic, and, when deposition was occurring, much more rapid than the average rate of 3 millimeters/1000 years. 121 3) Structure The concretions occur in two distinct shapes --discoidal and spheroidal. Discoidal masses are usually larger and range up to 6 inches (15 centi meters) in diameter. Rock fragments, mostly granitic, form the nucleus of all specimens examined. The upper surfaces of the concretions are dark red-brown to brown, the under surfaces light yellow-brown. Brach-iopods, serpulid worm tubes, bryozoan plates, silic eous sponges and corals may be attached to the upper surfaces. The discoidal concretions frequently exhibit several interesting features. A side view (Figure 40a) reveals the typical shape of this variety with a rock nucleus surrounded by a skirt of oxide mater ial. The under-surface of the skirt is usually even, and flat or concave downwards in contrast to the upper surface which is often very irregular. Some specimens of discoidal concretions have apparently been rotated about a horizontal axis at one time during their formation. On one side of the nucleus the oxides have accumulated in two lobes or skirts to form a lip-like structure while the opposite side Side view of a large discoidal manganese concretion. The nuclc is a granitic boulder. Major diameter 5,5 inches (l3.1 cm,) Small diameter (1,2 inches or 3 cm) spheroidal concretion with attached siliceous sponge. Coalescence of two discoiete-1 concretions. Major diameter approx, 3 inches (7,5 cm.) I2Z 123 of the nucleus is nearly devoid of oxides. Oxide materials are apparently deposited about a nucleus in a plane parallelling the sediment water interface. The asymmetry in plan view of the oxide skirt of many of the specimens indicates a favoured direction for greatest growth. This orientation is also exhibited, by the oxide crusts which have formed as plateaus on dead siliceous sponges which have toppled. The nuclei of spheroidal concretions are com pletely enclosed by oxides. The difference between spheroidal and discoidal types may be due in part to the size and shape of the nucleus. The generally smaller and more equidimensional nuclei of the spheroidal types perhaps allow these to be rolled about the bottom by currents or animals. Figure 40c shows two spheroidal masses which have coalesced with the formation of a surrounding skirt. Since coalescense, this mass has behaved as a discoidal concretion. Cross sections of concretions are pictured in Figures 41 and 42, The dark laminations correspond to finer-grained material and are generally much thinner than the lighter coloured layers. The lighter coloured laminations include most of the Cross-section of discoidal •manganese concretion (approx. 5.5 X)o The nucleus is an angular fragment of granitic rock „ Corresponds to area outlined in photograph 1 a'. Tcxtural, colour and thickness differ ences between successive layers of oxide materials likely indicate erratic growth rates, (approx. 44 X) Corresponds to area outline in photograph 1 a'. The uncon formity shown may have been the result of tilting of the concretion with subsequent change in preferred growth direction, (approx. 44 X) 12+ Cross-section of middle portion of discoidal concretion •which had nucleus completely enclosed by oxide materials (approx. 4.3 X). Early layers of oxides were preferentially deposited on left side of nucleus as it appears in the photograph. Enlargement from concretion pictured in 'a' showing detrital mineral included in accreted oxide materials. Detrital minerals are gener ally most abundant in the porous,lighter coloured oxide layers (approx. 43 X). FIGURE 42 126 detrital material,, Apparently the darker layers represent periods of slow deposition. In a vertical section the laminations are shown to bo reasonably symmetrical about a horizontal plane. Figure 41c shows the effect of either periods of erosion of oxide materials followed by renewed deposition or of changes in position of the concretion. The latter idea is favoured because unconformities are not evident. Detrital minerals included by oxides are pre dominantly quartz and feldspars. These also dominate in the underlying sediments. 4) Chemical Composition The chemical composition of the concretions was determined by Dr. E. V. Grill of the Institute of Oceanography (Table 6). For purposes of comparison, Table 7 gives the average compositions of deep ocean and Baltic Sea concretions and the composition of shallow water concretions from the Vermilion Sea off Baja California (Manheim 1965 and Mero 1965). Total carbon analyses of Jervis Inlet concre tions indicated a carbon content equal to or slightly less than that of the underlying sediments (which had an average content of 1.26 per cent). 127 Table 6 Chemical Analyses of Jervis Inlet Concretions (Analyses by Dr. E. V. Grill, I.O.U.3.C.) Sample A* B % Soluble 81. 75 81. 09 Fraction Soluble Insoluble Soluble Insoluble Fe203 7.65 3.06 6.55 2.45 FeO - 1.79 .„ 1.23 MnO 51.70 0.10 52.31 0.10 Si02 2.3 64.9 67.1 AI2O3 0.41 15.8 0.71 15.3 Ti02 0.096 0.62 0.035 0.58 P2O5 0.94 0.11 0.72 0.16 Ka20 1.06 2.27 1.05 2.37 K20 1.11 1. 52 1.18 1.51 MgO 3.19 2.24 3.36 1.66 CaO 1.55 3.19 1.56 3.17 BaO 0.27 0. 55 0.36 0.83 M0O3 0.041 0.007 0.049 0.006 V2O5 0.028 - 0.043 -CoO 0.020 - 0.022 -NiO 0.040 - 0.060 -CuO 0.0084 - 0.014 -ZnO 0.0029 - 0.0056 -PbO ND - ND -Te02 0.018 - 0.020 -S03 0.13 - ... -C02 0.56 - -NaCl 1.09 - 1.09 -Active 0 10.12 — 10.09 --110 H20 3.8.1 0.93 8.84 0.94 H 0+110 8.63 2.94 8.29 3.17 Sum 99.82 100.03 96.41 100.58 All analyses are presented as weight percentages on an air dried basis. A dash indicates no analysis and ND means not detected. *Sample A (the unfractionated crust) also contains 0.0012% Cr203,, Table 7 Comparison of Elemental Analyses of Manganese Concretions Jervis Inlet Baltic Sea Average Deep Ocean V.S.78 A B (i©st .average)' Al 1.70 1.83 1.54 8.57 1.90 Ca 1.33 1.33 1.21 1.57 1.16 Co .013 .014 .016 0.28 ..010 Cu .0055 . 0091 . 0048 0.40 .010 Fe 5.01 4.21 22.4 11.7 .86 K .98 1.03 .076 .68 .96 Mg 1.82 1.83 .57 1.38 -Mn 32.72 32.82 14.0 19.0 38.9 No .023 .027 . 013 .038 .022 Na .95 .97 .35 2.08 -Ni .026 .038 .075 .58 .045 p .34 .27 .70 .19 -Pb ND ND . 0038 .10 .025 Ti .096 . 089 . 11 .47 .. 07 Te .012 . 013 - - -Zn .0019 .0036 .008 0.04-0.40 .023 Jervis Inlet A Discoidal type - Grill 1968 B SpheroidaJ l. type Baltic Sea Average - Manheim 1965 Deep Ocean (estimated average) Manheim 1965 V.S. 78 (Vermilian Sea) - Mero 1965 129 Hov;ever, the carbon analyses represent an avercige. over the depth of penetration of the sampler (about 12 inches) and therefore are only an indication. The ratio of manganese to iron (Mn/Fo) has been correlated with depth and used in an attempt to distinguish and classify concretion localities (Mero, 1965). These ratios can be extremely variable with a considerable range sometimes occurring within a single specimen. In general, concretions from neritic and lake environments have a Mn/pG ratio of less than unity. A majority of pelagic nodules have a ratio of greater than unity. Jervis Inlet concre tions have an average Mn/Fe ratio of 5, there being little variation between samples. While this ratio does not follow the norm for shallow water concre tions, it is by no means unique. Some nodules close to the North and South American coasts and near Japan have Mn/Fe ratios ranging from 12 to 50 (Price, 1965). As more analyses are published, the less evident becomes the supposed relationship between depth and Mn/F ratio. The oxidation state of the manganese was cal culated by Grill (Grill, Murray and Macdonald,1968) to be MnO]_o87 for sample A and MnO^ Q6 for sample B, assuming all the active oxygen was associated with higher oxides of manganese. This O/Mn ratio is somewhat higher than the average value for neritic areas (1.55) and lower than that for the pelagic areas (1.9 - 2.0) (Manheim, 1965). Unlike the Mn O /pe ratio, the ratio apparently has a sig nificant covariance with depth (Manheim 1965). However, a considerable overlap of ^/jy[n ratios exists between shallow and deep-water concretions. The minor element content of Jervis Inlet concretions approximates that of other neritic occurrences. Elements of economic concern such as Ni, Cu, Zn, and Co have abundances ranging from 1 to 2 orders of magnitude below the estimated deep ocean average. Lead was not detected while molybdenum occurred with an abundance similar to that of deep sea concretions. The original analyses by Grill (Table 6) were given as oxide percentages of the soluble and insoluble (in a heated solution containing 10 ml of hydrochloric acid and 10 g. of hydroxylamine hydrochloride) fractions. The major 13.1 elements in the insoluble fraction were silicon, aluminum, iron, calcium, magnesium and sodium. These likely formed the detrital silicate minerals which were included within the ferromanganese oxide crusts. The phosphorus content of manganese concretions is thought to be related to their association with stag nant or semi-stagnant sediments (Manheim 1965). Jervis Inlet concretions, which are associated with semi-stagnant sediments, contained approximately 0.3 per cent phosphorus which is considered common for shallow marine forms. Tellurium was detected in the soluble fractions of both the Jervis Inlet samples analyzed. 5) Mineralogy Todorokite was identified as the principal manganese mineral in Jervis Inlet concretions (Grill, Murray and Macdonald 1968). The suggested composition (Straczek, Horen, Ross and Warshaw, 1960) is: (Ca,Na,Mn+2,K) (Mn+4,Mn+2,Mg)6 012 .3H20 Calculation of atomic proportions (the number of atoms per unit cell) of Mn+4, Mn+2, Mg (including Co, Cu), Ca (including Ba, Sr), Na and K for soluble Jervis Inlet material agrees with similar data pres ented for todorokite by other authors.(Grill et al 1968). 132 6) Formation of Concretions The mechanism of formation of manganese concre tions can only be postulated. Many workers (e.g. Manheim, 1965 and Price, 1967) consider the growth of concretions to be due to the precipitation of elements from the interstitial waters of the underlying sedi ments. Metals present in low concentrations in sea water are deposited as oxides or as ions adsorbed on clay and organic particles. Release of these metals to the interstitial waters would occur with sedi ment burial due to the reducing effect of the organic matter. The resulting high concentration of elements in the interstitial waters as well as electrochemical differences between the adjacent reducing and oxidiz ing environments will set up a diffusion potential so causing the upward movement of these elements (Price, 1967). This mechanism could produce a variety of con cretion habits. Manheim (1961) suggests that in areas where the sediment water interface is neutral or reducing, nodules will not form but the trace-element content of the bottom waters will be increased. Conversely, in areas where the surficial sediments are highly oxidized, pea ores may form within the sediment .133 itself (Gripenburg, 1934). The most common habit is the discoid concretion (Kindle, 1932.,Gripenburg, 1934, Manheim,1965). Although the basic mechanisms for the formation of concretions in the shallow water and open ocean environment are believed similar, the concentration of many minor metals such as Cu, Co, Ni, Pb, and Zn tends to be one to several orders of magnitude less in shallow than in the deep ocean varieties. This trend is thought to be due to differing concentra tions and types of organic matter present in the two environments. In neritic and lacustrine conditions, burial of the sediment and reduction in the presence of organic material releases most Mn, Pb, and Zn to the interstitial waters while the loss of Fe, Ni, Co and Cu is smaller and possibly due to retention of these elements in .iron sulphides (Price, 1967). Water soluble organics, amino acids and humic acids within the sediments are also thought to affect metal concentrations of shallow water concretions by modifying the inorganic uptake of minor metals such that Pb, Zn, and Cu are not sorbed by the manganese-iron phases. In the open ocean environ ment the low abundance of organic matter in the .134 sediments would likely minimize the mobility and upward diffusion of manganese and other elements during sediment burial„ 7) Abundance and Value Figure 43a shows manganese-iron concretions as they were recovered in a grab sampler. The bulk of the sample is coarse to fine-grained sediment on which the concretions form. Figure 43b is an approximate average sample recovered from one lower ing of the grab on to the locality. The square out line within which the concretions are pictured represents the area covered by the open jaws of the sampler. The total air dried weight of the concretions pictured was 1.97 pound (.894 kilograms) of which 72.9 per cent or 1.43 pounds (.684 kilograms) was oxide material. Since the area within the open jaws is approximately 0.2 square yards (.17 square meters) the concentration of oxide material, assuming total recovery, vjould be 7.1 pounds/square yard (3.9 kilo grams/square meter). If the area of the deposit is taken to be 36,000 square yards (30,000 square meters) the tonnage of oxides present would be 128 short tons (117 metric tons). This estimate could Petterssen grab sampler on deck with recovered manganese concre tions and sediment substrate. An average density of manganese concretions. Black outline represents area covered by open jaws of Petterssen grab sampler. The area is 1/5 meter ,, Top view of large discoidal concretion. Note the preferred direction for accretion of oxides. (Major diameter is 5.5 in. or 13.1 cm.) a c FIGURE 43 136 be in error by a considerable amount (perhaps + 50 per cent) as the area of the locality is poorly known and only one sample which, from photographs,appeared to represent an average sample, was weighed. While the above method of determining reserves of authigenic oxides on Patrick Sill is accurate within itself, many similar samples will have to be taken in order to estimate reasonably accurately the total tonnage. Perhaps a better method to determine this information would be to combine a small underwater camera and light source with the grab sampler. If the camera was triggered 10 feet or so off the bottom the concentration of concretions within the grab sampler could be extrapolated to the much larger area covered by the photograph. Underwater television was tried as a method to determine concentrations but concretions could not be distinguished from barren boulders with the system available. II. Iron Crusts Maintaining station over the concretion locality was difficult and only about 50 per cent of the attempts to obtain samples were successful. One attempt, which proved to be too far to the west by about 100 to 200 feet resulted in the sampler hitting 137 either bedrock or very large boulders. However, within the grab sampler were ferruginous crusts (Figure 44) which had been broken off the rock surface. The external surfaces of the crusts vary from smooth to irregular. Cross sections reveal a dis tinct layering. The surface or outer layer is rind-like and varies in thickness from about .04 to 0.6 in. (.1 to 15 mm). The colour is red brown to dark brown and black. The material is non-porous and has a vitreous to opaline lustre as if deposited as a gel. On dessication at room tempera ture the thicker portions have cracked forming inter locking polyhedral masses. Deposition of the gel like material must have occurred reasonably rapidly as large bubble-like cavities were formed (Figures 44b, c). The principal mineral forming this outer layer is goethite (FeOOH). The bulk of the material forming the crust is reddish yellow to yellow-brown, fine-grained, loose and very porous. An X-ray powder diffraction pattern indicated the principal minerals to be quartz, feldspar and goethite. This material likely Figure 44 a Iron crust as recovered from rock face near but not on (i.e. within about 100 meters) the concretion locality, (approx. 1.6 X) b,c Bubble-like structure shown by some of the iron crusts recovered from vicinity of concretion locality. Note layering within material of bubble and base and fragments of sponges within bubble. Approx. 1.6 X /38 139 represents sediments which accumulated and were then included in the structure of the crusts by the deposi.tion of the gel-like material . The layering mentioned is due to alternating layers of loose porous and vitreous materials,. The nature of the material which formed the bond with the rock surface is not known. There is no feature of the crust which would give an indication of age. III. "Glauconite-Montmorillonoid" Pellets Murray and Macintosh (1968) described interstrati-fied glauconite-montmorillonoid pellets from Queen Charlotte Sound. Mineralogic and morphologic studies of Jervis Inlet sediments revealed the presence of physically identical pellets (Figure 18d) . pellets were found over a considerable area of the sill as well as in localized areas on the sides of the lower basin. Pellets were not noted in samples collected from the upper basin. No X-ray or chemical analyses have been made of these pellets to date. The pellets are generally spheroidal and light yellow-green to gray-green in colour. In the frac tions examined, the pellets are most abundant in the fine sands (i.e. 88 to 63/u or 3.5 to 4 0) but some .140 samples contained pellets in the 500 to 350/u (1.0 to 1.5 0) range. Both these fractions of sample J-135, which is near but not on the concretion locality, were estimated to be 40% pellets. The finer fraction of sample J-164 was also about 40% pellets. Sediments collected with concretions were, about 15% pellets for the fractions examined . Often recovered with the pellets were sponge spicules and radiolarian tests. IV DISCUSSION The sill environment, especially on and near the medial depression is mineralogically unique within the study area. Why manganese concretions and iron crusts should form there and apparently not elsewhere within upper Jervis Inlet is not known. The area of the medial depression is affected by a bottom current with an approximate velocity of 25 centimeters/second. This current limits the deposition of detritus, both minerogenic and organic, and in some areas is capable of winnowing, with subsequent formation of lag depos its. The surficial sediments of the concretion locality are a dark red-brown colour for a depth of about 1 to 2 centimeters. Below this layer the sedi ments are generally a typical olive-green. The 141 colour of the surficial sediments indicates oxidizing conditions probably due to the constant renewal of overlying waters and the lower organic matter content of the sediments. Iron is being deposited as goethite crusts on exposed rock surfaces within the medial depression of the sill. Apparently simultaneously and in close proximity, manganese concretions are forming around rock fragments resting on sediments. Whereas the source of the goethite is likely a gel formed in the seawater, the concretion-forming manganese is appar ently derived from the substrate. Further studies which might prove interesting would be determination of the concentration of iron on the surface versus the underside of concretions and, although possibly not yet feasible, the determination of groundwater cir culation within the sill. What are thought to be "glauconite-montmorillonoid" pellets are also forming within upper Jervis Inlet, but they are not unique to the sill. Certain samples collected from the wall of the lower basin contained these pellets in considerable quantity, but no pellets were found in the sediments of the upper basin. 142 Whether these pellets form on or beneath the sediment-water interface is not known. The depth zonation noticed by Porrenga (1966) in which goethite occupies the 0 to 50 meter zone and glauconite the 30 to 2000 meter zone is only partly applicable in this area. However, since it is not known if the goethite crusts and pellets are forming presently or what the fluc tuations in sea level have been since Pleistocene time, little can be said. More thorough sampling might necessitate revision of ideas about distribution patterns. V EXPLORATION If, at some time in the future, the mining of con centrations of shallow marine concretions becomes profitable, the question will arise as to how to locate these deposits. At present, the best guide would probably be bathymetry. Favourable conditions appear to be achieved on the crests of banks and sills or on basin margins. All presently known local occurr ences of concretions have been found in the 100 to 200 fathom range. However, the significance of depth is not known. Movement of the overlying waters is needed to maintain a low sediment accumulation rate and oxidizing conditions within the bottom waters and top centimeter or so of the sediments. The occurrence 143 of a stagnant to semi-stagnent basin adjacent to the elevated area is thought to be important (Price 1967). To date, not enough is known about trace element concentrations within sea water and sediment in areas where concretions form to enable one to use such data for exploration. 144 3ibliography Armstrong, J. E. and W„ L. Brown, .1954, Late Wisconsin Marine Drift and Associated Sediments of the Lower Fraser Valley, British Columbia, Canada. Bull. Geol. Soc. Amer., Vol. 65: 349-364 Armstrong, J. E. et al., 1965, Late Pleistocene Stratigraphy and Chronology in Southwestern British Columbia and Northwestern Washington. Bull. Geol. Soc. Amer., Vol.76: 321-330 Bacon, W. R. , .1.957, Geology of Lower Jervis Inlet, B. C. Dept.of Mines and Petroleum Resources Bulletin 39 3. C. Natural Resources Conference, 1956, British Columbia Atlas of Resources Carter, N. M. 1934 Physiography and Oceanography of Some British Columbia Fjords, Proc. Fifth Pacific Sci. Cong. 1933, Vol.1: 721-733 Cockbain, A. E. 1963, Distribution of Sediments on the Continental Shelf off the Southern B. C. Coast, Manuscript Report 15, I.O.U.B.C. Dobrin, M.B., 1960, Introduction to Geophysical Prospecting McGraw-Hill, 446 pp. Folk, R. L. 1961, Petrology of Sedimentary Rocks, The University of Texas, 154 pp. Folk, R. L. 1966, A. Review of Grain Size Parameters, Sedimentology 6: 7 3-93 Folk, R. L. and W.C. Ward, 1957, Brazos River Bar, a Study in the Significance of Grain Size Parameters, J. Sediment. Petrol., 27: 3-27 Grill, E.V., J. W. Murray and R. D. Macdonald 1968, Todorokite in Manganese Nodules from a British Columbia Fjord, Nature, Vol.129,No.552: 358-359 Grim, R. E„, 1968 Clay Mineralogy, McGraw-Hill,596 pp. Gucleur, S.M. and M.G. Gross,1964, Recent Marine Sedi ments in Saanich Inlet, a Stagnant Marine Basin, Limn.and Ocean., Vol.9, No.3: 359-37 5 Holland, S„S., 1964, Landforms of British Columbia, Bo C. Dept.of Mines and Petroleum Resources, Bull. No.48 Kittrick, J.A. and S„W. Hope, 1963, a Procedure for the Particle Size Separation of Soils for X-ray Diffraction Analysis, Soil Science 95s 319-325 Lazier, J.R.N., 1963, Some Aspects of the Oceanographj. Structure in the Jervis Inlet System, M.Sc Thesi University of British Columbia LeRoy, O.E., 1908, Preliminary Report on a Portion of the Main Coast of British Columbia and Adjacent Islands, Geologic Survey of Canada, Report No.996 Publications 1908 Vol. 1 Manheim, F. T., 1965, Manganese-Iron Accumulations in the Shallow Marine Environment, Symposium on Marine Geochemistry, Narragansett Marine Labor atory, University of Rhode Island, Occas. Public. No. 3 - 1965. 217-275 Mero, J. L. 1965, The Mineral Resources of the Sea, Elsevier Publishing Company, 312 pp. Murray, J.W. and E.E.Mackintosh, 1968, Occurrence of Interstratified Glauconite-Montmorillonoid Pellets, Queen Charlotte Sound, British Columbia, Canadian Jour, of Earth Sciences, 5s 243-247 Pantin, H.M. 1969, The Appearance and Origin of Colours in Muddy Marine Sediments Around New Zealand, New Zealand Jour.of Geol. and Geoph., Vol. 12, No.Is 51-56 Peacock, M. A. 1935, Fjord-Land of British Columbia, Bull. Geol. Soc.of Amer.46s 633 Pickard, G. L.,1961, Oceanographic Features of Inlets in the British Columbia Mainland Coast, Jour. Fisheries Research Board of Canada, Vol. 18, No. 6: 907-999 Pickard, G.L. and G.K.Rodgers, 1959, Current Measure ments in Knight Inlet, British Columbia, Jour, of Fisheries Research Board of Canada, 16: 635-678 Pickard, G.L. and L.F. Giovando, 1960, Some Observa tions of Turbidity in British Columbia Inlets, Limn, and Oceanog. 5 (12): 162-170 Porrenga, D.H., 1966, Glauconite and Chamosite as Depth Indicators in the Marine Environment. Marine Geology 5: 495-501 Postma, H., 1967, Sediment Transport and Sedimenta tion in the Estuarine Environment in Estuaries, Amer. Assoc. Adv. of Science Publ. No. 83 :158-180 Price, N.B., 1967, Some Geochemical Observations on Manganese-Iron Oxide Nodules from Different Depth Environments, Marine Geology 5; 511-538 Roddick, J.A, 1965, Vancouver North, Coquitlam and Pitt Lake Map J.reas, British Columbia, G.S.C. Memoir 335 : 376 pp Shepard, P.P., 1954, Nomenclature Based on Sand-Silt-Clay Ratios, Jour. Sedimentary Petrology, Vol. 24: 151-158 Soren, R.K. 1967, Manganese Nodules: Nature and Sig nificance of Internal Structure, Economic Geology, Vol. 62, No.l: Tiffin, D.L. and J.W. Murray, 1966, Mapping Offshore with Continuous Seismic, Oil Week, Nov.7,1966 Toombs, R.B.,1956, Bute Inlet Sediments, Trans.Roy. Soc. Canada, Ser. 111,50: 59-65 Trask, P.D., 1938, Organic Content of Recent Marine Sediments, Recent Marine Sediment -- A Symposium, Dover Publications, 7 36 pp. Trites, R.W„,1965, A Study of the Oceanographic Structure in British Columbia Inlets and Some of the Determining Factors, PhD Thesis, Univer sity of British Columbia, Vancouver, B.C. Weaver, C.E.,1958, Geologic Interpretation of Argilla ceous Sediments, Part 1, Origin and Significance of Clay Minerals in Sedimentary Rocks, Bull.Amer Assoc. Pet. Geol.,Vol.42, No.2: 254-271 JERVIS INLET (Northern Portion) FIGURE 3 SAMPLE LOCATIONS 123° 46 1 LEGEND GRAB SAMPLE SEISMIC PROFILE 123s 42 CAMERA JERVIS INLET (Northern Portion) FIGURE 14 TOTAL CARBON PERCENT 123 58 123,54 •1.87 123° 50' 123° 46 123* 42 ' i \ ! I i!_L JERVIS INLET (Northern Portion) FIGURE 20 SEDIMENT-TYPE DISTRIBUTION 123 58 123° 54 123° 50' 123° 46 123° 42 50*07'00 50° 06 0d 50* 05 00 JERVIS INLET (Northern Portion) FIGURE 21 CLAY PARTICLE PERCENT 123 46 123* 42 


Citation Scheme:


Usage Statistics

Country Views Downloads
Germany 22 21
United States 14 0
China 7 8
United Kingdom 5 2
Canada 3 1
Japan 2 0
City Views Downloads
Unknown 27 21
Shenzhen 6 8
London 5 2
Ashburn 5 0
Mountain View 4 0
Vancouver 2 1
Tokyo 2 0
Houston 1 0
Beijing 1 0

{[{ mDataHeader[type] }]} {[{ month[type] }]} {[{ tData[type] }]}
Download Stats



Customize your widget with the following options, then copy and paste the code below into the HTML of your page to embed this item in your website.
                            <div id="ubcOpenCollectionsWidgetDisplay">
                            <script id="ubcOpenCollectionsWidget"
                            async >
IIIF logo Our image viewer uses the IIIF 2.0 standard. To load this item in other compatible viewers, use this url:


Related Items