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Volcanic facies architecture of the Chilcotin Group basalts at Chasm Provincial Park, British Columbia Farrell, Rebecca-Ellen 2010

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VOLCANIC FACIES ARCHITECTURE OF THE CHILCOTIN GROUP BASALTS AT CHASM PROVINCIAL PARK, BRITISH COLUMBIA  by   Rebecca-Ellen Farrell  B.A., Smith College, 2004    A THESIS SUBMITTED IN PARTIAL FULFILLMENT OF THE REQUIREMENTS FOR THE DEGREE OF    MASTER OF SCIENCE  in   The Faculty of Graduate Studies   (Geological Sciences)    THE UNIVERSITY OF BRITISH COLUMBIA (Vancouver)    August 2010     Rebecca-Ellen Farrell, 2010 ii ABSTRACT The Chilcotin Group basalt (CGB) of south-central British Columbia, Canada defi nes a medium-sized igneous province (ca. 17, 000 km2), characterized by basaltic lavas, volcaniclastic deposits, and paleosols with minor ash deposits. The CGB has previously been mapped only at reconnasissance scale (1:250 000), and most studies concentrated on geochemical and petrological studies; no stratigraphic relationships or volcanological models were attempted. Chasm canyon exposes one of the thickest successions of the CGB. Here, I explicate the volcanic facies architecture at Chasm to reconstruct the emplacement history and volcanism in the Neogene using geological mapping, cross-sections, and graphic logs. Specifi cally, seven discrete facies are recognized. The coherent facies are: i) vesicular/amygdaloidal pahoehoe lobes; ii) columnar-jointed, sheet-like lava; and iii) intact basaltic pillow lava. The clastic facies are: iv) paleosols; v) pillow-fragment breccia; vi) hyaloclastite; and vii) lacustrine sandstone. Facies are grouped into broad facies associations including the subaerial facies and interstratifi ed subaqueous and subaerial facies. The subaqueous facies are a minor component in the canyon stratigraphy.  The geometry of the lavas is indicative of the eruptive style of volcanism at Chasm, which defi nes the volcanic facies architecture. Four architectural elements have been observed: i) tabular-classic (TC), which represents a steady continuous supply of subaerial effusive basaltic lavas; ii) compound-braided (CB), which is typical of a shield volcano where anastomosing, branching fl ow fi elds result; iii) transitional-mixed, a combination of TC- and CB-type suggestive of bimodal emplacement, perhaps sourced from coalesced shield volcanoes and fl ank fi ssures; and iv) foreset-bedded indicative of subaqueous lavas. The exposed rocks record the evolution of CGB volcanism through ten distinct eruptive episodes and intermittent lakes, with periods of quiescence characterized by the paleosol development. Whole-rock Ar-Ar dates were obtained; the duration of volcanism is calculated as 1.28 ± 0.61 m.y. Emplacement is suggestive of shield volcanoes and small fi ssure eruptions with a northerly fl ow direction. iii   Laterally extensive paleosols, classifi ed as Brunisolic soils, were examined closely and display a range of morphological features suggestive of the paleo-environment. Lateral variability amongst paleosols have been mapped over a distance of more than 8 km, including a subqueous to subaerial transition. iv TABLE OF CONTENTS ABSTRACT ..................................................................................................................... ii TABLE OF CONTENTS ............................................................................................... iv LIST OF TABLES .......................................................................................................... vi LIST OF FIGURES ...................................................................................................... vii ACKNOWLEDGEMENTS ........................................................................................... x DEDICATION ............................................................................................................... xii CO-AUTHORSHIP STATEMENT ............................................................................xiii 1    OVERVIEW .............................................................................................................. 1 1.1 – Statement of the Problem ................................................................................ 1 1.2 – Organization of the Thesis .............................................................................. 2 2    REGIONAL GEOLOGY ......................................................................................... 3 2.1 – Previous Work .................................................................................................. 3 2.1.1        Nomenclature of rock types in the CGB ................................... 3 2.1.2        Thickness and styles of volcanism in the CGB ......................... 4 2.1.3        Aerial extent of the CGB ........................................................... 4 2.1.4        Regional mapping ..................................................................... 6 2.1.5        Landslides .................................................................................. 8 2.2 – Detailed Geology at Chasm Provincial Park ............................................... 10 2.2.1        Cache Creek Group ................................................................. 12 2.2.2        Kamloops Group ..................................................................... 12 2.2.3        Deadman River Formation ...................................................... 13 2.2.4        Chilcotin Group basalt ............................................................ 14 3    CHILCOTIN VOLCANIC STRATIGRAPHY .................................................... 15 3.1 – Facies Analysis ................................................................................................ 16 3.1.1        Introduction ............................................................................. 16 3.1.2        Methodology ........................................................................... 17 3.2 – Facies Descriptions ......................................................................................... 23 3.2.1        Coherent facies ........................................................................ 23 3.2.2        Clastic facies ........................................................................... 25 3.2.3        Mineralogy .............................................................................. 27 3.3 – Facies Associations & Interpretations .......................................................... 34 3.3.1        Facies associations .................................................................. 34 3.3.2        Discussion................................................................................40 3.3.3        Geochronology ........................................................................ 40 v4    PALEOSOL CLASSIFICATION .......................................................................... 51 4.1 – Introduction .................................................................................................... 51 4.1.1        Paleosol overview ................................................................... 52 4.2 – Paleosol Profi les at Chasm ............................................................................ 53 4.2.1        Field methods .......................................................................... 54 4.2.2        Horizon defi nition ................................................................... 68 4.2.3        Colour and thickness of horizons ............................................ 68 4.2.4        Horizon boundaries ................................................................. 69 4.2.5        Results ..................................................................................... 76 4.3 – Discussion........................................................................................................ 79 4.3.1        Duration of hiatuses between lava fl ow fl ows ......................... 79 4.3.2        Soil maturity ............................................................................ 82 4.3.3        Paleoclimate ............................................................................ 83 4.3.4        Comparative studies ................................................................ 83 4.3.5        Soil geochemistry .................................................................... 85 4.4 – Future Work ................................................................................................... 88 5    VOLCANIC FACIES ARCHITECTURE ............................................................ 90 5.1 – Introduction .................................................................................................... 90 5.1.1        Methodology ........................................................................... 91 5.1.2        Volcanic facies architecture ................................................... 101 5.1.3        Stratigraphic analysis of Chasm lavas ................................... 104 5.2 – Volcanic Interpretation .................................................................................111 5.2.1        Subaqueous to subaerial succession .......................................111 5.2.2        Lateral mapping of the paleosols .......................................... 113 5.2.3        Locating eruptive centre(s) .................................................... 116 5.2.4        Emplacement model at Chasm canyon ................................. 118 5.3 – Implications for Regional Chilcotin Group ............................................... 123 REFERENCES ............................................................................................................ 125 APPENDICES ............................................................................................................. 135 APPENDIX A- Field Methodology.............................................................................135 APPENDIX B- Ar/Ar Sample Preparation................................................................138 APPENDIX C- Regional Geochronological Data (See Included CD)......................140 APPENDIX D- Structure Data....................................................................................142 APPENDIX E- XRD Results........................................................................................144  vi LIST OF TABLES Table 3.1: Volcanic and sedimentary facies of the Chilcotin Group in the Chasm study area.......................................................................................................................................24 Table 3.2: Facies associations within the Chilcotin Group in the Chasm study area....33 Table 3.3: Chasm magnetic susceptibility data.................................................................39 Table 3.4: Chasm geochronology........................................................................................48 Table 4.1: Paleosol samples from Station 069...................................................................61 Table 4.2: Paleosol samples from Station 070...................................................................62 Table 4.3: Paleosol samples from Station 071...................................................................63 Table 4.4: Micromorphological data..................................................................................67 Table 4.5: Paleosol chemistry..............................................................................................86 Table 5.1: Architectural-type comparison to relevant volcanic provinces....................119 Table C1: Regional geochronology....................................................................................141 Table D1: Chasm structure measurements for map.......................................................143 Table E1: Results of qualitative analysis..........................................................................146 vii LIST OF FIGURES Figure 2.1: Simplifi ed geological map of the southern Interior Plateau region..............5 Figure 2.2: Chasm Provincial Park & vicinity geological map (1:20 000)......................7 Figure 2.3: Photo plate of basement rocks at Chasm Provincial Park............................9 Figure 2.4: Photograph of 3 of the 4 rock formations in the canyon and a schematic vertical section summarizing the stratigraphy.................................................................11 Figure 3.1: Composite graphic log for eastern wall of the Chasm canyon....................19 Figure 3.2: Composite graphic log for the western wall of the Chasm canyon.............20 Figure 3.3: Photo plate of the lacustrine sandstone facies (lsS)......................................28 Figure 3.4: Overview of petrographic observations at Chasm highlighting the younger lavas......................................................................................................................................29 Figure 3.5: Petrographic stratigraphic log for eastern main section..............................30 Figure 3.6: Magnetic susceptibility plots..........................................................................37 Figure 3.7: Histogram of the magnetic susceptibility values for Chasm........................38 Figure 3.8: Representative geochronology plots for Chasm (Plate 1)............................42 Figure 3.9: Representative geochronology plots for Chasm (Plate 2)............................43 Figure 3.10: Representative geochronology plots for Chasm (Plate 3)..........................44 Figure 3.11: Representative geochronology plots for Chasm (Plate 4)..........................45 Figure 3.12: Representative geochronology plots for Chasm (Plate 5)..........................46 Figure 3.13: Representative geochronology plots for Chasm (Plate 6)..........................47 Figure 3.14: Plot of the 40Ar/39Ar ages for Chasm and related CGB outcrops..............50 Figure 4.1: Field photographs of paleosols exposed at Station 068................................55 Figure 4.2: Field photographs of paleosols exposed at Station 069................................56 Figure 4.3: Field photographs of paleosols exposed at Station 070................................57 viii Figure 4.4: Field photographs of paleosols exposed at Station 071................................58 Figure 4.5: Paleosol profi le for Station 069.......................................................................59 Figure 4.6: Paleosol profi le for Station 071.......................................................................60 Figure 4.7: Summarizing the key soil micromorphology ...............................................71 Figure 4.8: Clay coating with fi ne laminations microphotograph..................................72 Figure 4.9: Station 069 micromorphology thin section plate..........................................73 Figure 4.10: Station 070 micromorphology thin section plate........................................74 Figure 4.11: Station 071 micromorphology thin section plate.........................................75 Figure 4.12: Duration of hiatuses between lava fl ows......................................................80 Figure 5.1: Inset map showing lateral extents of the 3 cross section..............................92 Figure 5.2: Lookout photomosaic......................................................................................93 Figure 5.3: Liden photomosaic...........................................................................................94 Figure 5.4: Eastern photomosaic.......................................................................................95 Figure 5.5: Generalized composite Chasm canyon stratigraphic log.............................97 Figure 5.6: Field photographs illustrating volcanic facies architecture.........................98 Figure 5.7: Photomosaic of a section of the western wall of Chasm canyon illustrating the irregular, non-linear geometry of the canyon wall....................................................99 Figure 5.8: Detailed view of interpreted line-diagram of a section of the eastern wall illustrating the stratigraphic complexity of the paleosols..............................................102 Figure 5.9: Paleosol truncates against a local paleo-topographic high formed by pre- existing lobe of lava...........................................................................................................103 Figure 5.10: Schematic diagram illustrating the transition from the intact pillow basalt (ipB) and pillow-fragment breccia (pfB) facies transitioning into the paleosol (P) facies.............................................................................................................................108 ix Figure 5.11: Schematic representation of stratigraphic relationships in a portion of the western canyon wall..........................................................................................................109 Figure 5.12: Field photograph and interpreted line-diagram showing the relationship between paleosol thickness and lava architecture..........................................................114 Figure 5.13: Emplacement model for Chasm canyon....................................................117 Figure E1: X-ray diffractogram of sample 08REF030A02............................................147 Figure E2: X-ray diffractogram of sample 08REF034A01............................................148 Figure E3: X-ray diffractogram of sample 08REF030A01............................................149 Figure E4: X-ray diffractogram of sample RE-CH07-53..............................................150 Figure E5: X-ray diffractogram of sample RE-CH07-58..............................................151 xACKNOWLEDGEMENTS This M.Sc. research was funded by the Targeted Geoscience Initiative- III Project  (TGI- 03), through the Geological Survey of Canada. Field costs were covered by Kelly Russell and the Geological Survey of Canada, courtesy of Bob Anderson. Geoscience BC contributed funding to the regional Chilcotin Project.  Firstly, thanks to my supervisor, Kelly, you were available and eager to discuss science nearly twenty-four hours of the day, I appreciated your knowledge, support and feedback while writing this thesis. I would like to thank my committee members, Bob Anderson, Kirstie Simpson and Jim Mortensen, for their time during many informative research discussions. I am grateful for their assistance and geological mentorship in the fi eld, lab, and involvement in the Chasm map. I want to extend a special thanks to Paul Sanborn, for providing his time and soil science guidance for this thesis. I learned a great deal through the Chasm soil fi eldwork, the Nazko trip, and your mentorship for my micromorphological study at UNBC. In addition, I want to thank the researchers, who were part of the regional Chilcotin project, Graham Andrews, Jackie Dohaney and Sarah Gordee for their collaboration. I want to thank Lucy Porritt for research discussions and her review of earlier drafts of the thesis. I want to thank Stephen Moss for this feedback on two of the chapters. Thank you Carol Wagner, Stephen Williams, Scott Smith, Brett Gilley, Arne Toma for technical and fi eld support. Thank you Jenny Lai for the XRD work. Thank you to my fi eld assistants: Nina Schwartzman, Ryan Emperingham, Agatha Soful, Emiliano Sepulveda, Mandy Tang and Nimmi Dhada. I want to thank the residents of Clinton, Chasm, Dog Creek and Canoe Creek, especially the Hancock family, John Grawhler, Gerhard and Florence Singer, Casa Blanca at 59 Mile, and Skookum Horse.  Thank you to the members of the VPL, past and present- Stephen, Nils, Jenny, Genevieve, Curtis, Jackie, Krista, Betsy, Shelley, and Chanone. So many off-the-cuff research discussions, daily encouragement, and friendship, I thank each of you! xi  Thank you to my family for their constant love and encouragement during my time in Vancouver- Dad, Anne, Hayley, Thomas, Melissa, Gigi and Pop-Pops. I will love each of you for the next 220 million years! I am utterly blessed. And thank you to my friends for all of your support: Sandra, Chanelle, Julie, Emily, Silke, Jenny, Brian, Elspeth, Ines, Bram, Heather, Rosie, Lucy H., Lucy P., Emiliano, Julia, Sasha, Sarah, Erica, Jennifer Telford, Bin Lim, Heli McPhie, Laura Louie, Carolyne Abrams, Lindsay Stewart, Ailsa Le May, Keven Fitzpatrick, Brandon McNamee, Elsbeth Ruder, Emily Ferry, Steph Loetze, Emma Anderson, Ray Daniels, Ari, and the members of the VSSC. xii DEDICATION “If your Nerve, deny you- Go above your Nerve-” Emily Dickinson (P292) xiii CO-AUTHORSHIP STATEMENT This thesis comprises a published geological map, cross-sections, and portions of two Current Research publications make up parts of Chapters 2 and Chapter 3. Figure 2.2 is the published geological map (January, 2010), titled ‘Chasm Provincial Park & Vicinity’ (scale 1:20 000). It holds a joint citation of 1) Geological Survey of Canada: Open File 6230, 2) Geoscience BC, Map 2009-16-1. I am the fi rst author, and Dr. R.G. Anderson, Dr. K.A. Simpson, Dr. G.D.M Andrews, and Dr. J.K. Russell are my co-authors. J. Mortensen reviewed the geochronological calculations. Field assistance (geological mapping, graphic logging, and cross-sections) has been provided by Dr. K.A. Simpson, Dr. G.D.M. Andrews and Dr. J.K. Russell. Figures 5.2, 5.3, and 5.4 cross-sections are in review for publication with the Geological Survey of Canada, as an Open File and Geoscience BC map. The title is ‘Bedrock cross-sections for Chasm Provincial Park.’ I am the fi rst author, and Dr. J.K. Russell and Dr. K.A. Simpson are my co-authors. All authors assisted in the fi eld. I mapped the cross sections, and constructed the fi nal digitized panoramas and interpreted line- diagrams. Dr. J.K. Russell was involved in the fi nal review of the stratigraphic analysis of the Chasm lavas, and assisted in discussing the descriptive model used for the lateral mapping of the paleosols. Portions of Chapter 2 and Chapter 3 have been published in a Geological Survey of Canada Current Research Paper 2008-13. I am fi rst author, and Dr. K.A. Simpson, Dr. G.D.M. Andrews, Dr. J.K. Russell, and Dr. R.G. Anderson are my co-authors. All authors contributed edits during the review process to text and fi gures. A portion of Chapter 3 has been published in a Geological Survey of Canada Current Research Paper 2007-A5. I am fi rst author, and Dr. G.D.M. Andrews, Dr. J.K. Russell, and Dr. R.G Anderson are co-authors. All authors contributed edits during the review process to text and fi gures. 1CHAPTER 1 OVERVIEW 1.1 STATEMENT OF THE PROBLEM  The Chilcotin Group basalt (CGB) covers approximately 17, 000km2 of the Intermontane Belt (Dohaney 2009) of British Columbia, Canada, and extends from Kamloops to Prince George.  Previous work comprises reconnaissance and regional scale mapping and geochemistry (Tipper 1971; Bevier 1981). To date, there has been no descriptive physical volcanology of the CGB.  The primary goal of this study is to provide descriptive or interpretive data on the physical volcanology studies of the CGB. Specifi cally, this study will examine the emplacement events in Chasm canyon, which exposes one of the thickest successions of the CGB. The Chasm canyon is a late-glacial erosional feature exposing a 100 m thickness of the CGB including a series of sub-horizontal to gently dipping basalt lavas.  Distinctive red, orange, or buff paleosols are commonly interstratifi ed with the basalt lavas and are interpreted to represent periods of quiescence between volcanic episodes. This study provides map, stratigraphic and facies details of the basaltic lavas and the paleosols at a variety of scales with the intent of reconstructing the volcanic events responsible for creating the basalt rocks in Chasm Canyon. Stratigraphic logging and analysis of fi eld data helped to identify discrete lithological units, and divided them into separate volcanic facies i.e., units that share characteristic properties of mappable units (e.g., textures, geometry, lithology etc.). Mapping of the canyon walls helped discriminate between lavas, and correlate them from one wall of the canyon to another, thereby providing a spatial and temporal context for the stratigraphy. These data lead to an emplacement model for Chasm Canyon of the CGB consisting of a description and explanation of the facies architecture, and interpretations of the sub-aqueous to emergent succession eruption duration and style, and paleo-landscape in the canyon. 21.2  ORGANIZATION OF THESIS In addition to this introductory chapter, four additional chapters provide the following descriptions, data and interpretation. Chapter 2 provides a systematic description of rock units in Chasm Canyon, expanding on summaries in a Geological Survey of Canada Current Research paper (Farrell et al. 2007).  Data collection in the fi eld and subsequent interpretations of the basement rocks at Chasm are compared to the geological descriptions from previous workers.  Chapter 3 describes the volcanic stratigraphy of the canyon, comprising coherent and clastic rocks that are divisable into separate facies. The Chilcotin Group basalt is characterized using mineraology, magnetic susceptibility, and geochronology.  This data is then correlated to the volcanic facies based on the descriptive physical volcanology of the units. The descriptions and spatial and temporal relationships of these facies allow interpretation of subaerial and subaqueous lava emplacement. Further associations are made based on geometry, morphology and textures of the lavas. Chapter 4 is a fi eld and laboratory study of the paleosols interstratifi ed with the lavas within the canyon walls. Chasm paleosols are described in detail and separated into different horizons using soil profi le logs. Thin section soil micromorphology is used to further characterize the soil.  In Chapters 5, a conceptual model for the emplacement of the basalt exposed in the Chasm Canyon is presented, using lateral mapping of the cliff exposures (Architectural Element Analysis).  Architectural-type comparisons are compared to similarly-sized igneous provinces. The graphic logs (Chapters 2, 3) provide tests of the model and incorporate interpretations of the various textures of the lavas.  3CHAPTER 2 REGIONAL GEOLOGY 2.1  PREVIOUS WORK  The Chilcotin Group basalt (CGB) constitute a volcanic fi eld situated in the Intermontane Belt of south-central British Columbia. The CGB is expressed physiographically as a series of aerially extensive plateaus (e.g., Cariboo, Chilcotin, and Fraser) (Mathews 1991) that are incised by large rivers, and surrounded by higher topography underlain by basement rocks. Chasm canyon is situated on the southern margin of the Fraser Plateau, approximately 20 km north of the town of Clinton and 7 km east of Highway 97. Previous studies of the CGB involved mainly regional-scale mapping or geochemistry studies (e.g., Mathews 1963; Tipper 1978; Bevier 1983; Rouse and Mathews 1986; Matthews 1988; Read 1989; Dostal et al. 1996; Anderson et al. 2001). The CGB are transitional basalts (Bevier 1982; Dohaney 2009), which imply olivine-normative basalts with either hypersthene or nepheline-normative. 2.1.1 Nomenclature of rock types in the CGB  The earliest description of the CGB lavas noted them as ‘fl at-lying basalt lavas’ (Dawson 1879; 1895).  The ‘Chilcotin Basalts’ were named by Tipper (1978) and included the basaltic lavas and the underlying sedimentary units in terms of color, rock type, general mineralogy and common structures such as columnar joints. The ‘Chilcotin Basalts’ were then formally defi ned as a mappable rock unit by Matthews (1988).  The extent is specifi ed as ranging from the Okanagan Highlands to the Nechako Plateau, but does not include the Anahim belt (Bevier, 1979) ‘valley basalts’ (Matthews, 1964).  Matthews (1964) described the basalts as ‘plateau basalt,’ (Farquharson and Stipp, 1969), although previously the name ‘plateau lavas’ had been used (Rice, 1947).  In the Chasm study area, Read (1989b) used the term ‘Chasm Formation,’ to describe the CGB basalts in the canyon. 42.1.2 Thickness and styles of volcanism in the CGB  Recent work has indicated that the thickness of the CGB (Andrews and Russell 2007, 2008; Mihalynuk 2007) and the styles of volcanism (Gordee et al. 2007; Farrell et al. 2007; Farrell et al. 2008) vary signifi cantly.   The CGB is spatially and temporally complex, rather than being a relatively homogeneous sheet, yielding locally unique exposures. Bevier (1982) interpreted that the CGB and the Columbia River Flood Basalts (CRFB) are different volcanic fi elds and furthermore describes the CBG as ‘basaltic plains volcanism’ (Greeley 1977), where there are numerous overlapping shield volcanoes that result in a lava plateau. Matthews (1988) described the CGB as signifi cantly smaller in scale than the CRFB, and can be characterized by a single lava in some exposures (i.e., many small scale outcrops), or a stacked succession of lavas, typically less than 100 meters thick. Bevier (1982, 1983) and Matthews (1988) used K-Ar (whole rock) geochronology to identify distinctive eruptive pulses of volcanism.  The nature of the bedrock, underlying the CGB is unknown except where exposed in small basement windows. The CGB is typically overlain by thick (>15 m) Pleistocene glacial deposits that are best exposed along valleys and canyons walls such as found at Chasm canyon. 2.1.3 Aerial extent of the CGB  CGB had been considered to have an aerial distribution of ~ 25,000 km2 (Mathews 1988).  Previous work indicated the aerial extent of the CGB map region to be ~55, 000 km2 (Bevier 1981).  The aerial extent has recently been recalculated using new compilations (NTS- map sheets: 92O and 92P) and GIS modeling to indicate a signifi gantly decreased area of ~17,000 km2  (Dohaney 2009).  Variations in the estimated areal extent of the CGB may be explained by several factors.  First, variations in the aerial extent and volume are primarily due to the scale of mapping of the CGB (reconnaissance-scale vs. detailed scale).  Second, the interpretations of different mappers in identifying the geologic boundaries of the CGB may lead to signifi cant variations in the mapped areal extent (pers. 5Figure 2.1: Simplifi ed geological map of the southern Interior Plateau region, including the Chasm study area (outlined). The distribution of the Chilcotin Group basalt is represented in dark grey, and delineates an areal extent of 17, 000 km2 (Dohaney, 2009). 6comm. Dohaney 2009). Moreover, the discrepancies between what defi nes the CGB (e.g. basalts or basalts and underlying sediments etc), and the varying ages of the basalts has created confusion among researchers mapping the CGB lavas. Previously, the total volume of the CGB was reported to be ~ 3,500 km3 (Bevier 1983; Matthews 1988), however the most recent volume estimate is 6, 000 km3 (Dohaney 2009). To date, the vents or volcanic source points of the CGB are unknown.  However plutonic plugs (e.g., Mount Begbie; gabbroic plug closest to study area) are interpreted to be the remnants of the source for at least some of the CGB volcanism (Farquaharson and Stipp 1969; Bevier 1982; Matthews 1988). Complex volcanism is inferred to exist (Matthews, 1988) because of, a) regional evidence of multiple fl ow directions of the lava recorded in the foreset-bedded breccias, indicative of smaller-scale fl ows instead of one large outpour (i.e., fl ood volcanism), and b) the age span of Chilcotin Group basalts is wide-ranging (38.3-1 Ma; Dohaney 2009), which may suggest multiple eruptive centres or long-lived volcanism emanating from one source point. The study site is located within Chasm Provincial Park (NTS 092P/03; Bonaparte Lake).  It is situated on the Interior Plateau, approximately twenty kilometers north of the town of Clinton and seven kilometers east of Highway 97 (Fig. 2.1). The Chasm Provincial Park contains an approximately 8 km long canyon; the canyon is approximately 300 m deep and ranges in width from 500-3000 m (Fig. 2.2). The walls of Chasm canyon expose lavas. The extreme southern end of the canyon exposes the Miocene Deadman Formation underlying the CGB. The Chasm canyon is a notch-like valley, and the shape of the canyon is due to a glacial to post-glacial outburst fl ooding event (Read 1991; Plouffe 2001). The incision of the canyon occurred with the retreat of the glacier during the Fraser glaciation (Fulton 1969, 1975; Plouffe 2001). 7Figure 2.2: Chasm Provincial Park and vicinity geological map (scale: 1:20 000) (Farrell et al. 2010). The map provides the distribution of geological units, location of graphic logs, georeferenced magnetic susceptibility data, geochronology sample locations, and location of mineral deposits. Actual fi gure available at the UBC Library or online at The Geological Survey of Canada (http://geopub.nrcan.gc.ca/index_e.php) 82.1.4 Regional mapping  The most recent geological map covering the Chasm area is the 1: 250, 000 Bonaparte map sheet (NTS map 092P) of Campbell and Tipper (1965). Bedrock exposure is poor but includes rocks ranging in age from late Precambrian to Neogene.  The fi rst general regional stratigraphy, petrological descriptions and K-Ar ages for the CGB derives from Bevier (1982). Bevier’s type-localities for the CGB included Bull Canyon, Dog Creek, Cardiff Mountain and Deadman River. Typical stratigraphic sections of the CGB comprised basaltic lava, pillow lavas, and tephra. Although the lavas could not be traced laterally, correlations between areas were undertaken using similar chemical compositions, magnetic susceptibility, and physical attributes of the lavas.  Bevier also included the Chasm Canyon in her studies, although it was not one of her type sections.  At Chasm canyon, Bevier (1982) defi ned the minimum thickness of the lavas to be 69.1 meters, consisting of at least 11 separate lava units characterized by horizontal vesicle sheets, vertical vesicle chimneys and the presence of zeolites were noted in the amygdales (Bevier 1982; Read 1989). No subaqueous facies were recognized. There have been no isotope age dates available for the Chasm area; however, north of the Provincial Park, at Fifty-Seven Mile, on the east side of the Highway 97. There is one K-Ar age of 9.02 ± 0.4 Ma (Matthews 1988; Fig. 2.2, Table 2). 2.1.5 Landslides  Evans (1983) described three landslide complexes in Chasm canyon (Chasm West Landslide complex, Chasm East Landslide complex, and the North Landslide complex). The North landslide complex is the most recent slope failure and is located near the nick point/apex of the canyon. The East and West complexes are located where the valley widens (Fig. 2.2). Each landslide deposit consists of an upper resistant cap of rock and softer underlying units, constituting a ‘block-type’ landslide (Evans 1983). The underlying softer units for the West Landslide complex were not described, but are inferred to be 9~40 meters autobreccia coherent andesite?fold axis a b c Figure 2.3: a) Small-scale folds in the Cache Creek Group phylite. b) Kamloops Group, part of the Skull Hill formation. c) Bedded volcaniclastic sandstone and breccia, which are a part of the Deadman River formation. d) Angular to subangular clasts belonging to the Skull Hill formation (andesite?) in a breccia bed within the Deadman River formation. e) Imbricated angular clasts in a breccia layer within the Deadman River formation indicating a northwesterly transport direction. View is to the southeast. Pen for scale is 9 cm. 10 clastic units derived from a pillow fragment breccia succession.  The Deadman River Formation sedimentary rocks are inferred to be the ‘softer units’ in the East Landslide Complex. Evans (1983) interpreted that the erosional processes of Chasm creek are not substantitive enough to produce large slope failures.  Instead, Evans (1983) interpreted the landslides are a result of multiple failure events and is on-going to the present-day. The slumped basalt blocks mapped on Fig. 2.2 are rotated blocks associated with these landslide processes. The landslide complexes have not been dated, however fi eld evidence suggests they occurred post-glacially (Evans 1983). Evans (1983) speculated that the fi rst landslides in the canyon occurred approximately 8,200 years ago and began near the completion of the ‘stress-relief phase’, meaning after the canyon had been incised and erosional processes had begun to take affect. Slope failure is an ongoing process in the Chasm canyon, and contributes to the overall weathering and erosional processes taking place in the canyon. The evolution of the canyon landscape, including the landslide events, is important to understand as it provides the context for mapping the rock units. The exposures as a result of the current canyon landscape allow for detailed description and interpretation of the CGB lavas and the interpretation of the paleo-landscape conditions at the time of emplacement of the lavas. 2.2 DETAILED GEOLOGY AT CHASM PROVINCIAL PARK  Detailed fi eld studies in 2006 -2008 focused on CGB rocks that overlie a varied basement sequence of Cache Creek Formation, Kamloops Group and Deadman River Formation rocks (Fig. 2.3). The stratigraphic section, and in particular the CGB units, are exposed in the walls of Chasm Canyon (Fig. 2.4). Four stratigraphic units, the Chilcotin Group, Deadman River Formation, Kamloops Group, and Cache Creek Group, were mapped within the Chasm study area. There are no exposed contacts between the CGB and the underlying basement rocks. 11  1060 m ~750 m 1060 m ~750 m not exposed not exposed multiple coherent basalt lavas pillow fragment breccia topographic bench bedded volcaniclastic sandstone felsic autobreccia flow-foliated felsic lava deformed calcareous black schist Chilcotin Group u/c Kamloops Group u/c Cache Creek Group Generalized Vertical Section ~2000 m till u/c Deadman River FrmKamloops Group Deadman River Formation Chilcotin Group Kamloops Group Chasm Creek Deadman Frm. NW SE Figure 2.4: a) View looking north along Chasm Creek to three of the four rock formations present in the canyon. b) Schematic generalized vertical section summarizing the stratigra- phy present in the Chasm study area. Unconformities are labled u/c. Elevations represent the y-axes. 12 2.2.1 Cache Creek Group  Campbell and Tipper (1965) described the Cache Creek Group in the Chasm as a collection of greenstones, argillites, cherts and limestones. Near the study area, the rocks are typically deformed and sheared.  Brachiopods and fusilinids were used to infer a Permian age for the rocks. Three outcrops of the Permian Cache Creek Group are located along Fifty-Seven Mile Creek (Figs. 3, 4), consisting of strongly folded calcareous phyllites (Fig. 3).  These rocks are locally unconformably overlain by rocks assigned to the Deadman River Formation.  The Chasm Canyon area is considered to be the western extent of the Cache Creek Group (Campbell and Tipper 1965). 2.2.2 Kamloops Group  The Eocene Kamloops Group is subdivided into two formations, the Chu Chua Formation and the Skull Hill Formation (Uglow 1922; Cockfi eld 1948; Mathews and Rouse 1961, 1963). The Chu Chua Formation is a sedimentary succession consisting of conglomerates, arkoses and shales with coal seams. The Skull Hill Formation consists of coarse, unsorted volcanic breccias, and dacite, trachyte, basalt, andesite, and rhyolite lavas and associated fl ow breccias (Campbell and Tipper 1965). Loon Lake, is the type locality for the Skull Hill Formation. Lavas range in colour, and are typically vesicular. The thickness of the lavas can be up to 14 meters, however generally the outcrops are isolated remnants and the geometry of the lavas cannot be determined. The Kamloops Group is undated in the study area. Rocks tentatively assigned to the Skull Hill Formation of the Eocene Kamloops Group are exposed discontinuously along 3 km of Sixty-One Mile Creek and Chasm Creek (Fig. 2.2). The exposed thickness of the Skull Hill Formation in this area ranges from 3-60 m. At the junction of Chasm Creek and the Bonaparte River, the Kamloops Group is unconformably overlain by the Deadman River Formation (Fig. 2.4). Two associated rock 13 units were observed (Fig. 2.3b); the fi rst unit is a red-brown, plagioclase-phyric, coherent andesite with trachytic texture (Fig. 2.3).  Flattened vesicles are aligned parallel to the small (>1 mm) plagioclase phenocrysts. The second unit is a monomict volcanic breccia that conformably overlies unit 1 and consists of clasts of trachyte. Collectively the two units are interpreted as the coherent and autobrecciated components of a single lava. 2.2.3 Deadman River Formation The Deadman River Formation as defi ned by Campbell and Tipper (1965) and Read (1989) consists of cream-colored to brown tuffs, breccias, diatomites, siltstones, arenites and conglomerates and are interpreted to have been deposited in a fl uvio-lacustrine environment.  The type locality is on the eastern shore of Skookum Lake in the Deadman River Valley. Within Chasm Provincial Park, Campbell and Tipper (1965) identifi ed three ‘possible’ exposures of Deadman River Formation, with the best outcrop located at the junction of Chasm Creek and the Bonaparte River although it is dissimilar to rocks in the type-section (Campbell and Tipper 1965). Sandstones and breccias were mapped by Campbell and Tipper (1965), and interpreted to have been deposited as fl at-lying units. The present bedding dips are attributed to post-depositional slumping, compaction from the overlying CGB basalts, or draping of paleotopography. The thickness of the Deadman River Formation varies considerably from centimeters to a maximum thickness of ~150 meters. The Deadman River Formation (DRF) is undated, however the formation is inferred to be late Miocene based on regional correlations (Matthews and Rouse 1986). The main exposures of the Deadman River Formation occur along Chasm Creek, at the junction of Chasm Creek with the Bonaparte River and north of Rickett’s Ranch (Figs. 2.2 and 2.3). Thin (<5 m thick) limited exposures are structurally above the Cache Creek Group in Fifty-Seven Mile Creek. The cliff forming exposure (Fig. 2.3c) is underlain by cream-colored sandstones and bedded volcanic breccias. Breccia clasts, in a sand-sized matrix, are dominantly angular to subangular and imbricated (Figs. 2.3d and 2.3e). Three 14 distinct clast size populations are present (mean sizes = 39.1 cm, 8.6 cm, and 1.1 cm; Fig 2.3). Clast imbrication indicates a northwesterly transport direction (Fig. 2.3e), and the angularity of the clasts suggests minimal transport from their source. 2.2.4 Chilcotin Group basalt  The Chasm area is host to one of the best-known and thickest exposures of the CGB and for this reason was selected for the current detailed study.  Cliff-forming exposures occur continuously for 8 km along Chasm Creek, but away from the canyon walls exposures are limited (Fig. 2.2). The width of the canyon varies between 500 m and 3000 m. The canyon is approximately 300 m in depth. The Chasm lavas are considered a stacked succession of basalt (Mathews 1988), of variable thickness, however, the total succession is typically less than 100 m, indicative of a relatively minor succession. The CGB lavas dominate the landscape and bedrock geology in the canyon.  In the study area, the CGB is estimated to be approximately 140 m thick. The CGB is divided into seven distinctive volcanic facies, (described in Chapter 3) and include: 1) basaltic pahoehoe lava comprising vesicular/amygdaloidal pahoehoe lobes (vlB), 2) aphyric, columnar-jointed and sheet-like basalt lava (acB), 3) dominantly intact basaltic pillow lava (ipB), 4) fi ne-grained paleosols (P), 5) pillow-fragment breccia (pfB), 6) rare hyaloclastite (hB) and 7) lacustrine sandstone (lsS) (Figs. 3.1 and 3.2). 15 CHAPTER 3 CHILCOTIN VOLCANIC STRATIGRAPHY  In this chapter, the key physical volcanological characteristics of the CGB at Chasm are introduced, including: i) a general fi eld description; ii) facies analysis; and iii) delineation of seven discrete facies. Recent research on the CGB has resulted in a signifi cant database of information such as magnetic susceptibility, porosity, density, and conductivity (Dohaney 2009; Andrews 2008; Farrell et al. 2008; Farrell et al. 2007). Facies analysis is an effective method in understanding volcanic stratigraphy (McPhie and Allen 1992; Jerram 2002), and has been used in this research to complement the existing CGB database in order to understand the volcanism in the Chasm canyon Historically, facies analysis is used in sedimentary basin analysis where the assigned facies are directly linked to a depositional environment. This is the routinely used method in sequence stratigraphy (Walker 1984; Miall 2000). There are key differences to the analysis for volcanic stratigraphy, such as a de-emphasis of the depositional setting, and a greater attention to emplacement processes (McPhie 1992, 1993; McPhie 1993). Facies and facies associations are used for understanding the style of eruptive, transport, and explacement processes and proximity to source which collectively make up the volcanic facies architecture of a given area. The defi ned facies include: 1) basaltic pahoehoe lava comprising vesicular/ amgdaloidal pahoehoe lobes (vlB); 2) aphyric columnar-jointed and sheet-like basalt lava (acB); 3) fi ne-grained red coloured paleosols (P); 4) intact pillow lava (ipB); 5) pillow- fragment breccia (pfB); 6) hyaloclastite (hB); and 7) lacustrine sandstone facies (lsS). Within the established facies framework, next the magnetic susceptibility, chemistry and geochronology of the basalt facies are reported and interpreted. The volcanic facies architecture and evolution of the stratigraphy at Chasm is presented in Chapter 5. 16 3.1 FACIES ANALYSIS  In this section, facies analysis methods as described by Cas and Wright (1995) are applied to Chasm sections. The principal goal of facies analysis is to understand the emplacement events at Chasm canyon, and provide evidence for the location for one or multiple eruptive centres. 3.1.1 Introduction  The principal goal of facies analysis is to identify features that allow for interpretation of eruption style, transport, and depositional processes, depositional environments, proximity to vent and timing with respect to major eruptions. The defi nition of facies used for this study is a grouping of rocks, which are interpreted to have formed (i.e., ‘emplaced’ etc., for volcanic rocks) under similar conditions (Miall 2000). Volcanic stratigraphy, facies analysis and architecture are used in relatively young volcanic successions such as Large Igneous Provinces (LIPS) (Mangan 1986; Self et al. 1996; Self et al. 1997; Hooper 1997; Jerram et al. 1999; Jerram 2002; Jerram and Widdowson, 2004; Bondre et al. 2004; Passey and Bell 2007; Elliot and Fleming 2008), and ancient volcanic successions (Cas et al.1989; McPhie and Allen 1992; Paulick and McPhie 1999; Simpson and McPhie 2000; Moore et al. 2000). To clarify, a fl ood basalt is a subcategory of a LIPS, which consist of thick basaltic lavas with an areal extent greater than 130,000 km2 and volume greater than 80,000 km3 (Tyrell, 1937; Jerram and Widdowson, 2004). For defi nitive purposes, LIPS can either be extrusive or intrusive, mafi c to silicic in composition, and continental or oceanic (Jerram and Widdowson, 2004). Jerram (2002) emphasized the need of defi ning facies in order to understand fl ood basalt architecture. He hypothesizes whether or not a repeatable sequence can be observed in emplacement scenarios between different fl ood basalts. The CGB is signifi cantly smaller in size when compared to a fl ood basalt province (e.g., CBG covers 17,000 km2 with a volume of 6,000 km3 in south-central British Columbia (Dohaney 2009)), 17 however the physical volcanology can be comparable in many instances. In particular, the Chasm Canyon, is approximately 8 km in length, ranging from 500 to 3000 m in width, and 300 m deep, hosting a diverse suite of facies symbolic of a range of emplacement events and processes, which will be discussed towards the end of this chapter. 3.1.2 Methodology  The methodology used in this study can be broken into six stages, each of which are described below. Stage 1: Geological Map 1: 20 000 scale  A detailed geological map of the Chasm Canyon at a 1: 20 000 scale was prepared (Fig. 2.2; Farrell et al. 2010). Detailed fi eld studies in 2006-2008 focused on the CGB, which overlie a varied basement sequence of Cache Creek Formation, Kamloops Group, and Deadman River Formation rocks (Fig. 2.4). The CGB are exposed in the walls of the Chasm Creek canyon. Mapping provides the framework for the study. At this scale, the canyon was traversed on foot, mapping by hand using a printed digital base map from Terrain Resource Information Management Program (TRIM). Global Positioning System (GPS) data was received using a PDA (Personal Digital Assistant) supplied by the Geological Survey of Canada. The PDA uses the Ganfeld operating system, which digitally stores all stations, samples, fi eld photographs, and fi eld notes, all of which are geo-referenced simultaneously. There are no roads into Chasm Canyon; however, there are two tracks that permit access. The fi rst access route is from the northern end of the canyon beginning at the Chasm Provincial Park Lookout site, using a track that runs parallel to the eastern canyon wall. The alternative is using a private track, owned by Mr. John Grawhler, which allows for a south- west starting point for traversing (Fig. 2.2).  Stages 1 through 3 occur simultaneously. 18 Stage 2: Structure at Chasm  There are no observed faults in the Chasm canyon. Post-depositional slumping and landslides are observed in places along the canyon walls. They have displaced stratigarphic packages downslope, therefore the slumped blocks founded in the canyon (not on cliffs) are not in-situ (Evans 1983). The only geological instability in the canyon is due to landslides, beginning in 8,200 B.P. and there is continued slip in the present time (Evans 1983). The CGB lavas are sub-horizontal (dip <3°),  and from the Chasm Lookout, the lavas dip to the NE towards the head of the canyon. Approximately, 1 km downstream from the head of the canyon, is a lava package that thickens to the NW, has a wedge-like morphology and is interpreted to be in-situ. Structural data of the CGB also includes bedding orientations from pillow lobes, and bedding measurements in the Deadman River Formation (Fig. 2.2 and Appendix D).  Stage 3: Identifying Facies  Deatiled graphic logging as outlined in McPhie et al. (1993) was undertaken along the canyon walls to produce two main composite graphic logs. The composite graphic log along the eastern wall, covers a lateral distance of approximately 950 m (Fig. 3.1) and  the composite graphic log for the western wall of the canyon, covers a lateral distance of approximately 1060 m (Fig. 3.2). The extent of each of the graphic log can be seen on the map (Fig. 2.2). A combination of both symbology (McPhie et al. 1993) and line drawing was used to illustrate the textures and structure present in the cliff outcrops. The majority of the legend associated with the logs was created specifi cally for the features found at Chasm, aiming for accuracy and precision.  Sampling was conducted simultaneously with graphic logging as well as from additional exposures within the canyon, from outcrops along Highway 97 and from basement exposures. In the East and West composite graphic logs, all coherent lavas were sampled. Clastic rocks were sampled with discretion such as pillows, pillow rinds, the 19 Chasm East Composite Log 10 20 30 70 80 90 100 110 till S-69 S-70 S-71 P4 ?  4 5 0 m KEY lava boundary internal boundary (flow lobe) vesicle amygdales vesicle chimney clastic dike columnar jointing pipe vesicle/amygdale paleosols S-x stations with detailed paleosol profile aphyric basalt pahoehoe lobes vesicle sheets a b c d La va  N u m b er 11.6 6.37 26.0 5.2 6.3 2.5 4.2 13.0 3.0 11.6 5.2 4.2 3.07 5.7 7.7 6.0 5.0 5.5 M ag n et ic Su sc ep ti b ili ty Pa le o so l I D Fa ci es vlB vlB vlB/ acB vlB acB acB vlB acB vlB acB/vlB vlB b a P P P5 P P P P P P Fa ci es A ss o ci at io n AER. SUB AER. SUB SUBAER. SUBAER. SUBAER. SUBAER. SUBAER. SUBAER. SUBAER. SUBAER. AER. SUB AER. SUB AER. SUB AER. SUB AER. SUB AER. SUB AER. SUB SUBAER. A g e 9.44 ± 0.24 9.07 ± 0.26 10.00 ± 0.48 9.65 ± 0.40 9.86 ± 0.30 Fig. 3.1: Composite graphic log for eastern wall of the Chasm canyon. Lateral distance covered is approximately 950 m. Representative fi eld photographs of major units, includ- ing: a) oblique view of representative section (~30 m in height), b) amygdaloidal pahoehoe lobes (vlB), c) clastic dike in top lava (acB) and below paleosol (P), d) paleosol (P) with basaltic core stones (~30 cm long rock hammer for scale). Photograph courtesy of Paul Sanborn. Magnetic susceptibility values in 10-3 SI units. 20 Figure 3.2: Composite graphic log for western wall of the Chasm canyon. Lateral dis- tance covered is approximately 1060 m. The horizontal axis on the graphic log represents the average grain size. Coherent units are illustrated by symbols only and are drawn to the maximum grain size as outlined in McPhie et al (1993). The grain size for units containing variably sized pillow-fragments in a fi ner-grained matrix was calculated using the average size of the smallest pillow fragments. Intact pillow lobes and larger pillow fragments (> 64 mm) are shown schematically and protrude outside the log where they are abundant within a unit.  Representative fi eld photographs of major units: a) Typical exposure of western log section. Person for scale (~170 cm), b) Upper lava (acB) with vesicle chimneys underlain by pillow lava (ipB) with dipping pillows to the SE. Hammer for scale ~40 cm, c) Pillow lava with prismatic jointing and tiny normal joints. Hammer for scale is ~40 cm, d) Pil- low fragment and associated breccia (pfB). Pencil is 14.5 cm long, e) Smaller-sized pillow fragments and breccia (pfB). Pencil is 14.5cm, f) Large pipe amygdales and pahoehoe ropes (vlB), g) Vesicle sheets. Hammer for scale ~40 cm. h) Large Pahoehoe rope (vlB), i) Cross- section through amygdaloidal lobes (vlB). Pencil is 14.5cm. Actual fi gure available at UBC Library. 21 interstitial material between the pillow fragments, and the matrix of the unit. Observations were made with a hand-lens, and discrete protocol (Cas et al. 2008) followed for coherent and clastic rocks. An abbreviated outline of the method is listed below: Coherent rocks (lavas, intrusions) Porphyritic or aphyric/aphanitic1) If porphyritic: note a) crystals (phenocrysts or xenocrysts), b) groundmass, c) 2) xenoliths If aphyric/aphanitic: note a) xenoliths (cognate or exotic), b) groundmass (uniform, 3) clastogenic, segregationary or vesicular/amygdaloidal) For porphyritic and aphyric: determine a) textures, b) contacts, c) geometry 4) (outcrop-scale), and d) colour Clastic rocks (fragmental) Clasts/fragments or interstitial medium1) Clasts/fragments (free crystals, juvenile clasts, lithic clasts)2) Interstitial medium (clastic matrix, primary cement, alteration minerals)3) Geometry, shape, texture, composition4) All samples are found in the regional CGB database (Dohaney 2009), along with stratigraphic reference, and any analyses undertaken on the samples (geochronology, geochemistry, or any physical property measurements. Detailed observations resulted in the indentifi cation of 7 facies (Table 3.1), which are described in section 3.2. Petrography  Petrographic analysis was undertaken on eighteen coherent rock samples in the eastern composite log, and vicinity. In addition, paleosol samples, from stations 069, 070, and 071, were analysed.  Paleosols are discussed in detail in Chapter 4. 22 Stage 4: Age relationships of the facies  Geochronological sampling was focused on the Eastern Composite Log and highway locations north of the Chasm canyon (Table 3.4).  Other areas of the canyon were also sampled (Fig. 2.2) and are stratigraphically referenced by using cross-sectional mapping, which is discussed in Chapter 5 (Figs. 5.2, 5.3, 5.4). The goal of the geochrono- stratigraphy is to understand the age relationships between the facies in the Eastern Composite log, and the overall age relationships in the entire canyon, which contributes to the emplacement model discussed in Chapter 5. Stage 5:  Facies Associations  The grouping of facies together into facies associations is based on any of the following components: a) the geometry or thickness of the facies; b) lateral continuity and shape of the rock units; c) rock types; or d) sedimentary structures (McPhie 1992). For Chasm, the facies associations allow for the interpretation of the lavas, where the rock types (coherent and clastic) and the environment of fi nal deposition as well as emplacement style are considered. The facies associations are Chilcotin Group-Subaerial (Mcb1) or Chilcotin Group-undivided sub-aqueous and subaerial (Mcb2) (Table 3.2). This distinction is emphasized by colour on the map (Fig. 2.2), where the south-west exposure of the CGB in the canyon to be Mcb2 is shown in light blue and the Mcb1 in green. Refer to Table 3.1, for the descriptive data on the individual facies. Stage 6: Facies Architecture  The fi nal step in facies analysis at Chasm is determining the facies architecture, which is discussed in Chapter 5. At Chasm, mapped cross-sections of the length of the canyon walls were drafted, followed by mapping on these sections using a modifi ed (volcanology focused) method of Architectural Element Analysis (AEA) outlined in Miall 23 (2000). Sequence stratigraphy was not attempted for this study due to accessibility of the vertical cliffs. The data obtained from the facies analysis yields the framework for a descriptive emplacement model, with preliminary interpretations regarding the eruptive centre(s). 3.2 FACIES DESCRIPTIONS  Coherent and clastic facies were mapped at Chasm. The three coherent facies are vesicular basaltic pahoehoe lobe facies (vlB), aphyric columnar-jointed basalt facies (acB), and intact pillow lava facies (ipB). The four clastic facies are fi ne-grained paleosol facies (P), pillow-fragment breccia facies (pfB), hyaloclastite facies (hB) and lacustrine sandstone facies (lsS). Refer to graphic logs (Fig. 3.1 and 3.2) for photographs of facies and the facies sequence for each log. Table 3.1 summarizes the facies. 3.2.1 Coherent facies Vesicular basaltic pahoehoe lobe facies (vlB)  The dominant facies is ‘vlB,’ and  consists of aphyric, vesicular (and/or amygdaloidal) pahoehoe lobe lavas (Fig. 3.2, photo i). Lavas are poorly (20-40%) vesicular. Vesicles are randomly distributed and pipe vesicles (average height of 10 cm) commonly occur at lobe contacts and help to differentiate them. Vesicles are  <1 mm in size and amygdaloidal with infi llings of zeolites, specifi cally phillipsite-K and chabazite-Ca (Appendix E).   Pahoehoe ropes and wrinkled textures are common.  Colours of vlB lavas range from dark grey (fresh) to maroon (weathered). Single pahoehoe lobes range from 6 cm-3 meters across and overlap one another resulting in lava units approximately 2-10 m thick. The lobe shapes vary signifi cantly, ranging from bulbous ellipses to elongated thin fl ow lobes. Typically, the contacts between the vlB and other facies are concordant and sharp or irregular.  24 Table 3.1: Volcanic and sedimentary facies of the Chilcotin Group in the Chasm study area Facies Code Facies Characteristics Thickness Coherent units vlB Vesicular basaltic pahoehoe lobe dark grey to maroon, lobate structures, pipe vesicles (avg. height 10cm) are common, pahoehoe ropes and wrinkles noted Vesicles/Amygdales: spherical, 20%, < 1-2 mm Contacts: concordant, sharp or irregular individual emplacement units 2-10m thick single pahoehoe lobes 6cm-3m acB Aphyric columnar-jointed basalt dark grey, tan or maroon, commonly amygdaloidal and/or vesicular. Amygdales: spherical, 3-40%, < 1 mm Phenocrysts: olivine microphenocrysts Contacts: concordant and sharp individual emplacement units 5-20m   thick ipB Intact pillow basalt dark grey, prismatically jointed, tiny normal joints around periphery of pillow; pillows packed together with little or no interstitial material Amygdales: spherical, < 15% Contacts: chilled fi ne-grained black rim (1-3cm thick) average pillow size 70cm Clastic units hB Hyaloclastite monomitic basalt breccia, weakly vesicular; jigsaw-fi t texture Clasts: ~ 3-10mm angular to subangular fragments Matrix: sand-sized comprised of fi ne basalt fragments Contacts: irregular ~ 2m thick pfB Pillow fragment breccia orange, massive, lensodial, pillow fragments, intact basalt pillows Clasts: ~ 1-20 mm, angular to subangular, pillow fragments Matrix: angular, glassy basalt fragments, 1-20 mm Pillows: Average dimension 0.5 m, irregularly shaped, prismatically-jointed with tiny normal joints around the periphery of pillow Contacts: irregular ~ 5-30 m for each lens P Fine-grained paleosol orange/red, locally vesicular/ amgydalodial in C and R horizons, numerous basalt cobble-sized clasts set into the orange material Horizons: typically 1-5 separate horizons from 1-40 cm each, generally abrupt and irregular boundaries between horizons. Bedforms: can be thinly laminated, however bedding is not always present Contacts: gradational, irregular, forming sediment infi lled cracks ~ 0.5-1.5m for each paleosol lsS Lacustrine Sandstone medium-grained buff coloured sandstone Contacts: not laterally continuous / localized outcrop ~ 15-30cm thick  Table 3.1: Volcanic and Sedimentary facies of the Chilcotin Group in the Chasm study area. 25 Aphyric columnar-jointed basalt facies (acB)  The ‘acB’ facies comprises massive, sheet-like lavas, with moderate to well- developed columnar joints (Fig. 3.1; photo c). Units are aphyric with sparse olivine microphenocrysts.  Vesicle chimneys (1.5 – 5 m) (Fig. 3.2; photo g) and horizontal vesicle sheets (1-3 cm width, length varies) are a key feature of ‘acB.’ Vesicularity ranges typically from 30% (poorly vesicular) at the base of the lava, <5% (very poorly vesicular) at the middle, and 30% at the upper portion of the lava. Colour of the acB lavas ranges from dark grey (fresh) to maroon (weathered).  Individual emplacement units are ~1-10m thick. Columnar joints vary in width (from ~30-60 cm) and preserved chisel marks are rare. Spheroidal weathering locally masks the columnar jointing. The contacts are concordant and sharp for the acB facies. Intact pillow lava facies (ipB)  Dark grey, intact pillow lavas are common at the base of the sub-aqueous sequences Fig. 3.2; photo c). The average pillow size is 70 cm, and they have quenched black glassy rims (1-3 cm thick). Locally, pillow sag structures are observed. Prismatic jointing is common at the centre of the pillow, whereas tiny normal joints are commonly preserved adjacent to the black glassy rims. Pillows are packed together with little to no interstitial material. Intact pillows dip at about 37 degrees based on the orientation of their larger plunging ‘head’ and a narrower ‘tail’ (Jones and Nelson 1970). 3.2.2 Clastic facies Fine-grained paleosol facies (P)  This facies consists of red to buff-coloured paleosols that occur between lavas on both the eastern and western walls of the canyon (Fig. 3.1; photo d). Three paleosol sites were analysed, using soil science methodology, on the eastern canyon wall (Fig. 2.2).  Four to fi ve horizons or zones were identifi ed at each site. Blocky soil structure is rare in the fi eld, though additional structures can be identifi ed in thin section. Possible sedimentary 26 structure such as root casts or clastic dikes, of identical composition as the paleosols commonly occur at the basal paleosol-lava contact (Fig. 3.1, photo c), and are described in Chapter 4. A generalized horizon description at one of these sites would include top to base: 1) a upper red fi ne-grained paleosol material (2.5 YR 6/8) with an abrupt, irregular boundary that is platy due to weathering; 2) very pale brown (10 YR 8/4) and increasingly well-lithifi ed paleosol rock; 3) a lowermost horizon of highly amygdaloidal, weathered basalt, identical in colour (10 Yr 8/4 ‘very pale brown’ and 10 Yr 4/1 ‘dark grey’)  to the surrounding  lava in the Chasm, and defi nes the lower limit of the  paleosol.   Each horizon consists of weathered basalt fragments, which include highly amygdaloidal varieties and less common dense basalt fragments (up to 10 cm in size).  Lower contacts of the paleosol are typically undulating, irregular and gradational to the next horizon. The paleosols (P facies) are further discussed and interpreted in Chapter 4. Pillow-fragment breccia facies (pfB)  This facies is unstratifi ed and massive (~5-30 m thick) and includes angular to blocky pillow fragments  (Fig. 3.2; photos d and e). The morphology of this facies is lensoidal in shape. This facies is monomictic, however different degrees of palagonitization of the basaltic fragments are observed, colouration ranging from dark grey fragments with a orange rim, to smaller fragments completely converted to palagonite, which are orange. The clasts range in size (from approximately 3 mm - 20 cm) and shape (sub-angular, blocky, elongate, ragged to curvi-planar) (Fig. 3.2; photo e). The margins on some of the pillow fragments are fi ne-grained with a black glassy rim.  Secondary clay minerals commonly infi ll voids in the breccia. There are two types of secondary zeolite and clay mineralization observed in this facies, one is an dull red chalcedony-like material, which is shown to be analcime (associated with zeolites), and zeolite (phillipsite-K) (Appendix E). Montmorillonite (smectite) is also present, in addtion to plagioclase (albite) and quartz. The second material is chalky and white analcime (associated with zeolites) and zeolite (wairakite) (Appendix 27 E). Montmorillonite is also present, and calcite, clinochore, plagioclase, K-feldspar, and quartz. Therefore, the secondary mineralization of this facies is dominated by zeolites and clays. Both alteration assemblages occur within the interstitial clastic matrix between pillow fragments. Hyaloclastite facies (hB)  The facies is rare and associated with pillow lava (Fig. 3.2; refer to 72 m stratigraphic position). Monomictic basalt breccia consisting of angular to sub-angular fragments, which range in size from ~3 mm-10 mm and are weakly vesicular.  The matrix is sand-sized and consists of fi ne-grained basalt fragments.  Locally jigsaw-fi t textures are preserved indicating in-situ fragmentation and no transport.  More commonly, clasts are rotated relative to one another and randomly distributed indicating transport post brecciation. Lacustrine sandstone facies ( lsS)  This facies is 15 cm thick and not laterally continuous. A lens of medium-grained buff coloured quartz sandstone, with minor feldspars and mica, is found locally at the base of a sub-aqueous sequence  (facies vlB; Fig 3.2 and 3.3). The upper and lower contacts are not observed in detail, on account of inaccessibility. K. Simpson is photographed at the contact for scale (Fig. 3.3), however the cliff remained too dangerous to carefully observe the entire unit. The mapped extent of  this unit is shown entirely within the photo, which may be a function of accessibility. No ripple marks or other sedimentary structures were visible. The grainsize is coarse, and the shape of the grains are subangular to subrounded. 3.2.3 Mineralogy  Field observations of the CGB at Chasm range from aphyric to olivine-phyric. Coherent samples from the eastern composite log section were prepared into thin sections in addition to stations near the apex of the canyon. All thin sections have a stratigraphic context and fi eld description to accompany the petrographic notes (Fig. 3.5). To summarize 10 thin sections were studied in detail (eastern composite log samples), olivine phenocrysts 28 pilllow pile amygdaloidal basalt lsS facies Figure 3.3 Figure 3.3: Lacustrine sandstone facies (lsS) 29 ol ol ol ol a b c d Fig. 3.4: Petrographic textures at Chasm highlighting the younger lavas. A) and B) are sample GA-CH06-40, from the Chasm lookout near the apex of the canyon. C) and D) are sample RE-CH08-4, which is the topmost lava in the eastern stratigraphic log. A) Typical view of olivine phenocrysts and plagioclase in the groundmass. Scale is 0.10 mm; B) Oliv- ine and plagioclase laths. Scale is 0.1 mm; C) Brown coloration of iddingsite surrounding olivine crystals in a dominantly plagioclase groundmass with interstitial glass. Scale is 0.30 mm; D) Olivine partially chemically dissolved with iddingsite rim, surrounded by plagio- clase laths. Scale is 0.10 mm. 30 Chasm East Composite Log 10 20 30 70 80 90 100 110 till S-69 S-70 S-71 P4 ?  4 5 0 m a b c d La va  N u m b er Fa ci es vlB vlB vlB/ acB vlB acB acB vlB acB vlB acB/vlB vlB b P P5 P P P P P P Petrographic Study %  v es ic u la ri ty an d  v es ic le  s iz e m o d al  a b u n d an ce o f o liv in e &  s iz e ra n g e Note: Average length of plagioclase laths = 0.58mm  1%  n/a  15%  0.11 -> 0.55mm  1%  0.35 -> 0.73mm  15%  0.18 -> 1.10mm  5%  20%  0.19 -> 0.59mm  0.15 -> 1.43mm  3%  5%  0.39 -> 1.23mm  0.21 -> 4.06mm  5%  30%  0.30 -> 0.78mm  0.10 -> 2.04mm 1% n/a 20%0.84->4.51  3-5%  15%  0.35 -> 3.23mm  0.32 -> 1.39mm  3-5%  30%  0.11 -> 0.23mm  0.26 -> 0.60mm  0.33 -> 0.36mm  0.30 -> 3.56mm 3- 5% 3o %  3%  25%  0.23 -> 0.44mm  0.16 -> 1.21mm a1 a2 b1 b2 c1 c2 d1 d2 e1 e2 f1 f2 g1 g2 h1 h2 i1 i2 j1 j2 a b c d e f g h i j Fig 3.5: Petrographic statigraphic log (modifi cation of the eastern composite log). The following samples were used: a1& a2) RE-CH08-4: olivine phenocrysts and in the ground- mass; b1 & b2) RE-CH06-21; c1 & c2) RE-CH06-3; d1 & d2) RE-CH06-30: ellipsoidal amygdale; e1 & e2) RE-CH06-17; f1 & f2) RE-CH08-2; g1 and g2) RE-CH06-18: irregular and jagged amygdale and olivine phenocryst; h1 & h2) RE-CH06-16: cluster of olivine phenocrysts and bladed oxides visible; i1 & i2) RE-CH06-4; j1 & j2) RE-CH08-1: altered skeletal olivine phenocryst. The general trend of alteration shows an increase with depth. The scale on all photomicrographs is 1 mm. 31 are common and olivine in the groundmass, which is typical in an alkali olivine porphyritic basalt. Red-brown iddingsite is visible around and inside a portion of the olivine crystals (skeletal olivines), as an alteration product of the olivine crystal. Commonly, the olivines are zoned. Other minerals in the groundmass include plagioclase (average length of laths 0.58 mm), clinopyroxenes, augite, bladed oxides, and interstitial glass. The dominant texture is where the plagiolase laths commonly exhibit dikytaxitic texture. Other textures include ophitic and poikilitic textures.  Accessory minerals are K-feldspar and nepheline in the groundmass. The modal abundance of olivine crystals varies between samples, ranging from 5 to 30%; the average modal abundance is 20.5% (Fig. 3.4). The degree of weathering varies between samples, with the freshest samples located at the stratigraphic top of the canyon. Samples range from non-vesicular, vesicular and/or amygdaloidal. The average abundance of vesicles is 3%, with the average size of the vesicles ranging from 0.28-0.95 mm. The shape of the vesicles range from ellipsoidal to irregular and jagged. All samples are similar in mineralogy but there are grain size and minor textural differences between lavas (Fig. 3.4). Petrography  Petrographic observations demonstrated minor variability between samples, however no major distinctions are detected with the comparison of facies-type (Fig. 3.5). The basaltic subaerial facies (vlB and acB) are similiar in detail, however, the vesicularity is greater in vlB facies.  Mineralogy is consistent at Chasm, including the one phenocryst- type (olivine) identifi ed in the CGB rocks. Differences in grain-size are observed in the groundmass, which are interpreted to be a result of different rates of post-emplacement cooling of the lava. Olivine phenocryst size is unchanged with stratigraphic height. Olivine in the groundmass more often retain their euhedral shape, compared with the phenocrysts, which appear to be more susceptible to weathering and alteration. The second difference is the degree of weathering in the samples, where the transformation of the olivine crystals into iddingsite is evidence for the alteration of the original basalt mineralogy. The general 32 trend of weathering and alteration shows an increase with depth stratigraphically. Units in the ipB, pfB, or hB facies were not analyzed petrographically. 33 Table 3.2: Facies associations within the Chilco- tin Group in the Chasm study area. MAJOR FACIES ASSOCIATIONS   Subaqueous fac ies   Subaerial  facies  Int act  pillo w brecci a (ipB) Interpretati on : This facies  is found  at  the  base of  subaqueous success ions , inferred  that  gravity moved  these  intact bodies  downs lope  to the  base of  the  tempo ra ry Chasm  Lak e. Vesicul ar basaltic p ahoehoe  lobe  (vl B) Interpretati on : emp laced  on a shall ow  slope , with the  sm all est ‘toes ’ at the  fron t of the  flow . An atom ising across  the  la ndsc ape . Pillo w fr agm ent  brecci a (pfB) Interpretati on : The d isagg regati on  of  the  pillows  is interpreted  to occ ur  with movem ent, as the lava spall s into the  tempo rar y lak e. T he p illow  bod ies hit one o the r,  and  the  imp act, creates  the sharp pillow  fragmen ts. Movemen t was limited , as the  fragmen ts ar e no t rounded . Aphyric  col um nar-jointe d basalt facies  (acB) Interpretati on : emp laced  by inflati on  (SW ELL  hypo thes is; Self et al , 1998),  whe re initiall y thin pahoehoe  lava is then  inflat ed  with a new p ulse of  la va,  prod ucing  a massive  non-ves icular  interior (coo ls mo re slow ly) resulti ng  in co lumn ar  joints. Hya locl astite  (hB) Interpretati on : Formed  by  quench  fragm entati on , a non -exp los ive  fracturi ng  and  subsequent break up of b asalt  lava. Fine -gr aine d paleosol  (P) Interpretati on : rep resen ts periods  of  qui esc ence  in the  emplacem ent of  the  lavas to all ow  for so il accumulati on and  developm ent. Soil result s  in the  we athe ring  of  the  basalti c paren t material  and  aeo lia n depos its. Lacustrine S andst one  (lsS) Interpretati on : sands tone grai ns  ar e depos ited  into the  tempo rar y Chasm  La ke, and  accumulat e at t he  base of  the  lak e.  34 3.3 FACIES ASSOCIATIONS & INTERPRETATIONS  Facies associations in the CGB in the Chasm canyon include facies vlB, acB, and P, which are interpreted to have been emplaced subaerially, and facies ipB, pfB, hB, and lsS, which are interpreted to have been emplaced subaqueously (Table 3.2). The facies associations lead to division of the CGB at Chasm into two broad associations (Mcb1 and Mcb2) (Fig. 2.2), wherein Mcb1 comprises the subaerial facies, whereas Mcb2 represents interstratifi ed subaqueous and subaerial facies. Descriptions as well as spatial and temporal relationships of these facies support subaerial and subaqueous interpretations. The sub- aqueous Chasm succession was associated with a temporary lake (i.e. Chasm Lake), which is discussed further in Chapter 5. Further associations are justifi ed based on comparing the facies geometry of the lavas, such as the sequence vlB, acB, vlb is a common occurrence at Chasm. Lastly, the petrography, magnetic susceptibility and geochronology are interpreted based on the facies and facies associations. 3.3.1 Facies Associations Unit Mcb1  Miocene Chilcotin basalt- sub-aerial facies association  This association consists of sub-aerial basaltic lavas and paleosol horizons and includes: 1) basaltic pahoehoe lava comprising vesicular/amygdaloidal pahoehoe lobes (facies vlB); 2) aphyric columnar-jointed and sheet-like basalt lava (facies acB); and 3) fi ne-grained, red-coloured paleosols (facies P).  From a distance, the sub-aerial lava appears to be thick, ‘sheet-like’ units with sparse lobate shapes and moderately developed columnar-joints (facies acB). However, in detail many of the lavas consist of small pahoehoe lobes (facies vlB). Pahoehoe lavas (vlB facies) are interpreted to have been emplaced on a shallow slope. The smallest lobes (‘toes’) are located at the fl ow front, which may refl ect a discontinuous, or slower emplacement with anastomosing pahoehoe lobes. The ‘acB’ facies was emplaced by infl ation  (SWELL hypothesis; Self et al. 1998), producing more massive, 35 sheet-like fl ows indicating a more rapid emplacement. In Hawaii, Hon et al. (1994) observed that slopes must be no greater than 2° to form the sheet-like fl ows; if the slope increases than channelized fl ows will result. Hawaiian fi eld data has documented infl ation process, illustrating a 10-50 cm thick pahoehoe lobe can be infl ated to 4 m (Hon et al. 1994). The presence of ropes imply deformation to the skin of the lava; the skin of the pahoehoe lava is fl exible and when lava moves over topography disturbance in the skin results (Fink and Fletcher 1978). In modeling the emplacement of the CGB lavas into Chasm canyon, infl ation processes commonly invert the surface topography, therefore the paleo-highs in the topography are subsequently termed ‘infl ation pits’ and the paleo-lows are then ‘tumuli’ (Self et al. 1998). Passey and Bell (2007) state that the differences between sheet-like lavas and pahoehoe lobes (compound lavas) is related to the supply rates during emplacement. No a’a pahoehoe lava is observed at Chasm. The presence of paleosols (P facies) suggests many hiatuses in volcanism during emplacement of the lavas in the Chasm area, and are classifi ed and interpreted in Chapter 4. Disconformities mark all contacts between the overlying lava (typically acB) and the P facies. With the interstratifi ed paleosols, commonly the upper contacts of the lavas are paleosol horizons, implying discrete fl ow fi elds in Chasm. This is further discussed in Chapter 4. Unit Mcb2  Miocene Chilcotin basalt- undivided sub-aqueous and sub-aerial facies association  Within the Chasm study area, an important transition occurs between subaqueously- deposited clastic rocks and subaerially-emplaced lavas. The Mcb2 facies association is best developed in the southern portion of the western canyon wall and comprises alternating sub-aqueous and sub-aerial lavas.  Subaerial lavas make up 60% of the sequence. Subaerial facies of the Mcb2 include subaerial lavas from the vlB and acB facies described above. 36 The Mcb2 also includes the dominant intact pillow lava (facies ipB) and pillow-fragment breccia (facies pfB) facies and rare hyaloclastite (facies hB) and lacustrine sandstone (facies lsS) units. The subaerial fl at lying lavas are correlated over 8 km, the interstratifi ed subaqueous and subaerial sequence is a minor component in the Chasm Chasm, only exposed in the southwestern section. The ipB facies represents subaqueous lavas fl owing downslope, and accumulating into a pillow pile. The ipB facies is a dominately ‘close-packed pillow lava’ (Carlisle, 1963), wherein the intact basaltic pillows are molded into each other. Corrugation, a wrinkle pattern on the outer skin of individual pillows (Yamagishi 1987), is a common surface structure. Tensional cracks are prevalent at Chasm (see West graphic log; Fig. 3.2) and form deep grooves into the pillow, and are formed due to another pulse of the molten lava from the interior of the pillow, cracking the solidifi ed exterior crust (Yamagishi 1973, 1983), after the breakout/growth of a new pillow lobe. Pillows with pronounced tensional cracks are observed at the base, middle and top of section.  Single and multiple rinds are observed in the pillows, the latter indicative of more than one surge of the molten interior of the pillow lava as this process breaks the skin of the pillow in the formation an isolated pillow (Yamagishi 1987; McPhie et al. 1993). The pfB facies is interpreted to have formed by disaggregation of pillow lava as pillow breakouts occur from the pillow fronts to form new pillows. The transport of the pillows downslope, the mechanical impact and abrasion of one pillow upon another, and angle of depositional slope all infl uence the abundance of pillow fragments compared to intact pillows. Quench fragmentation also likely contributes fragments to this facies. The hB facies is rare in the Chasm succession and is interpreted to have formed by quench fragmentation (McPhie et al. 1993). Collectively, the pillow lava, pillow-fragment breccia, and hyaloclastite facies are interpreted to have formed a lava-delta sequence as a result of subaqueous emplacement of basalt lavas (Jones and Nelson 1970). The lsS is interpreted to have been deposited into the temporary Chasm Lake, and represent the base 37 East Composite Log Magnetic Susceptibilty 0 20 40 60 80 100 120 2 7 12 17 22 27 Magnetic Susceptibilty (10^-3 SI) West Composite Log Magnetic Susceptibility 0 20 40 60 80 100 120 140 D ep th  (m ) (m) D ep th  (m ) FACIES: = vlB = acB = vlB = acB = acB/vlB FACIES: = acB/vlB = vlB/acB/vlb/acB/vlB = vlB/acB/vlB INT ERS TRA TIFI ED CLA STIC  UN IT INTERSTRATIFIED CLASTIC UNIT INT ERS TRA TIFI ED CLA STIC  UN IT Figure 3.6: Magnetic susceptibility plots of eastern (upper) and western (lower) composite log sections. Identical shapes represent a single lava unit. If there is no symbol, 1 measure- ment was recorded for that lava unit. If there are two symbols for the same unit it implies the upper and lower facies stratigraphically. Note the scale difference between two plots. Refer to Figures 3.1 and 3.3 for corresponding graphic logs. 38 Distribution of Chasm Magnetic Susceptibility -5 0 5 10 15 20 25 30 1 3 5 7 9 11 13 15 17 19 21 23 25 27 29 31 33 35 37 39 41 43 45 47 49 51 53 55 57 Total Samples M ag ne tic  S us ce pt ib ili ty  (1 0^  -3  S I) Figure 3.7: Histogram of the magnetic susceptibility values for Chasm. The average M.S. value at Chasm is 4.5 39 Field # Magnetic Susceptibility 1 UTM Easting (NAD83) UTM Northing (NAD83) Measure ment Type2 (n) Unit3 Location 06REF020q 11.6 609005 5671220 Field (10) Chilcotin Group Eastern Log 06REF020p 6.37 609005 5671220 Field (10) Chilcotin Group Eastern Log 06REF020o 3.07 609005 5671220 Field (10) Chilcotin Group Eastern Log 06REF020n 26 609005 5671220 Field (10) Chilcotin Group Eastern Log 06REF020m 5.24 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020l 6.3 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020k 2.52 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020j 4.15 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020i 5.99 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020h 7.62 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020g 5.68 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020f 12.9 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020e 3 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020d 11.6 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020c 5.18 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020b 5.45 609006 5671220 Field (10) Chilcotin Group Eastern Log 06REF020a 4.97 609006 5671220 Field (10) Chilcotin Group Eastern Log RE-CH08-1 4.2 609093 5671017 Lab (5) Chilcotin Group Eastern Log 07REF143-2A 0.86 607617 5669526 Lab (3) Chilcotin Group Eastern Wall 07REF143-2B 1.32 607617 5669526 Lab (3) Chilcotin Group Eastern Wall 07REF143-1A 3.11 607617 5669526 Lab (3) Chilcotin Group Eastern Wall 07REF143-1B 2.33 607617 5669526 Lab (3) Chilcotin Group Eastern Wall RE-CH06-04 1.75 608609 5671734 Lab (3) Chilcotin Group Eastern Wall RE-CH06-12 3.61 609057 5671112 Lab (3) Chilcotin Group Eastern Wall RE-CH06-16 0.289 609057 5671112 Lab (3) Chilcotin Group Eastern Wall 08REF037 5.06 607514 5669891 Field (10) Chilcotin Group Western Log 08REF034 4.23 607675 5669360 Field (10) Chilcotin Group Western Log 08REF033 3.41 607692 5669236 Field (10) Chilcotin Group Western Log 08REF011c 3.05 607682 5668454 Field (10) Chilcotin Group Western Log 08REF011b 2.77 607682 5668454 Field (10) Chilcotin Group Western Log 08REF011a 4.49 607682 5668454 Field (10) Chilcotin Group Western Log 08REF010b 1.82 607643 5668338 Field (10) Chilcotin Group Western Log 08REF010a 2.2 607643 5668338 Field (10) Chilcotin Group Western Log 08REF038 5.5 607347 5668138 Field (10) Chilcotin Group Western Wall 08REF039 7.73 607422 5668199 Field (10) Chilcotin Group Western Wall 08REF040 9.69 607509 5668283 Field (10) Chilcotin Group Western Wall 08REF077 4.21 607438 5670071 Field (10) Chilcotin Group Western Wall 08REF078 2.79 607431 5670121 Field (10) Chilcotin Group Western Wall 08REF079 2.44 607434 5670258 Field (10) Chilcotin Group Western Wall 06REF027 2.29 607730 5668821 Field (10) Chilcotin Group Western Wall 06REF027 0.78 607730 5668821 Field (10) Chilcotin Group (pillow) Western Wall 06REF027 2.34 607730 5668821 Field (10) Chilcotin Group Western Wall 06REF027 1.14 607730 5668821 Field (10) Chilcotin Group Western Wall 06REF027 1.38 607730 5668821 Field (10) Chilcotin Group Western Wall 06REF027 0.72 607730 5668821 Field (10) Chilcotin Group (pillow) Western Wall 07REF161 1.63 607304 5671207 Field (5) Chilcotin Group Western Wall 07REF162 7.11 607313 5671433 Field (5) Chilcotin Group Western Wall 07REF162 6.12 607313 5671433 Field (5) Chilcotin Group Western Wall 07REF162 9.59 607313 5671433 Field (5) Chilcotin Group Western Wall 07REF174 3.45 608321 5670361 Field (5) Chilcotin Group Western Wall 07REF-186 0.15 606782 5666970 Lab (3) Deadman Frm 07REF195 0.3 608019 5667749 Lab (3) Deadman Frm 07REF177 1.27 608447 5669850 Lab (3) Skull Hill Frm 07REF137-1 4.44 608262 5668917 Lab (3) Skull Hill Frm 07REF137-3 7.78 608262 5668917 Lab (3) Skull Hill Frm 07REF137-2 -0.9 608262 5668917 Lab (3) Skull Hill Frm 07REF176 6.1 608457 5669916 Lab (3) Skull Hill Frm 07REF-184 0.13 606735 5666878 Lab (3) Cache Creek Group CHASM MAGNETIC SUSCEPTIBILITY MEASUREMENTS 3  Chilcotin Group Basalt; Deaman Formation Volcaniclastic sandstone; Skull Hill Formation Volcanics. 1  Magnetic Suceptibility data is recorded in 10 -3   SI units 2  Measurements taken with KT-9 Kappameter; Lab measurements on core Table 3.3: Magnetic Susceptibility data table, specifi c to Chasm. 40 of the lake, (see Chapter 5; Fig. 3.3). 3.3.2 Discussion Magnetic Susceptibility  The average magnetic susceptibility (MS) values for Chasm lavas is 4.5 10-3 SI units.  MS values are plotted for the eastern and western composite log sections (Fig. 3.6), and vary between facies. In the eastern log area,  the vlB facies values are often similar indicating that the overlapping pahoehoe lobed are indistinguishable based on MS. The acB facies in the East Log area, has two values plotting near 12, and one value near 3. The top and base of the lava have similar values, whereas the centre results in a dramatically lower value. The Western Log MS plot  differs from the eastern plot due to the interstratifi ed clastic units, and because each lava measured contains 2 or more facies. Overall, there is no signifi cant MS value variability for the entire western plot (range: 1.5-5.5 10-3 SI units; average value= 3.4 10-3 SI units) compared with the eastern plot range (range: 2-27 10-3 SI units; average value= 7.3 10-3 SI units). To summarize, the range of MS values as shown in Figure 3.7 for Chasm lavas overlap therefore the MS data are not useful for discriminating between fl ow fi elds or facies at Chasm, however there is potential for characterization of individual facies with strategic MS sampling. 3.3.3 Geochronology  The 40Ar/39Ar system was used to investigate the chrono-stratigraphy in Chasm Canyon, aiming to test correlations amoung lavas in a few areas of the canyon. At Chasm, extensive dating of 12 samples from the canyon was carried out, aiming to constrain the emplacement events for the basalts at Chasm and surrounding vicinity (Figs. 3.8, 3.9, 3.10, 3.11, 3.12, and 3.13). There are no ages in the literature specifi cally from Chasm Canyon. Matthews (1988) sampled CGB basalt from 57 Mile Creek, north of the Chasm, and 41 obtained a K-Ar age of 9.2 ± 0.4 Ma. The regional CGB ages are located in Appendix C, and ages specifi cally from Chasm area are located in Table 3.4. Sample preparation methodology can be found in Appendix B. The ages were derived following careful analytical checks including: 1) the plateau shape; 2) observing whether all steps are within the 2 sigma error range; 3) the MSWD (mean-square weighted deviation) number should be close to 1, this provides information on the goodness of fi t parameter (McDougall and Harrison 1999); and 4) if there are any additional notes from the analyst.  Geochronology samples are listed in Table 3.4, with sample number, age, geographical location in the canyon, and the corresponding lava number (see also Fig. 2.2). The 12 new Chasm whole-rock 40Ar/39Ar ages range from 10.00 ± 0.48 Ma to 8.72 ± 0.37 Ma (Fig. 3.14 and Table 3.4). These samples overlap in 2σ, but reveal a complex chronostratigraphy, discussed below.  Refer to Appendix C for CGB regional plots, and the Chasm specifi c plots are located in Figures 3.8 through 3.13. The errors overlap within a 2σ error, except for one sample (RE-CH08-1b), and the entire Chasm suite and related outcrops on the Highway 97 are seen on Fig. 3.10.  All new ages are plotted on the map (Fig. 2.2), except for sample (RE-CH08-1b), which does not plot within the 2σ-error age range. To summarize, the youngest lavas (Lava 1 etc.) are only exposed in the northern section of the canyon, whereas the older lavas are exposed at the base of the canyon due to dissection.  It is not clear what caused this anomalous result (8.59± 0.72 Ma; plot in Appendix C), since it is a younger age compared to analysis RE-CH08-1a which yields 10.00 ± 0.48 Ma; however the analytical source of the error is unclear, since both ages were conducted using two aliquots of the same sample. Stratigraphic constraints indicate 10.00 ± 0.48 Ma (RE-CH08-1a) is likely to be the better age. The degree of weathering of the basalts should not create discrepancy within the geochronology. 42 8.89 ± 0.42 Ma 10 5 0 5 10 15 20 0 10 20 30 40 50 60 70 80 90 100 Cumulative 39Ar Released (%) 08REF-003-A01 Ar-Ages in Ma WEIGHTED PLATEAU 8.89 ± 0.42 TOTAL FUSION 2.66 ± 2.08 NORMAL ISOCHRON 10.01 ± 1.74 INVERSE ISOCHRON 10.06 ± 1.70 MSWD 0.70 Sample Info WR UBC Janet Gabites IRR  =  UBC can52 J  =  0.0037440 ± 0.0000187 A) Ag e (M a) 8.18 ± 0.74 Ma 10 5 0 5 10 15 20 0 10 20 30 40 50 60 70 80 90 100 Cumulative 39Ar Released (%) 08REF-003-A01 b Ar-Ages in Ma WEIGHTED PLATEAU 8.18 ± 0.74 TOTAL FUSION 2.05 ± 3.00 NORMAL ISOCHRON 10.27 ± 5.89 INVERSE ISOCHRON 10.32 ± 5.74 MSWD 0.28 Sample Info WR UBC Janet Gabites IRR  =  UBC can52 J  =  0.0037440 ± 0.0000187 B) Ag e (M a) Figure 3.8: Representative geochronology age plots for Chasm. A) Sample (RE-CH08-91 ) with a plateau age = 8.89 ± 0.42 Ma. B) Sample (RE-CH08-92) with a plateau age = 8.18 ± 0.74 Ma. 43 9.44 ± 0.24 Ma 10 5 0 5 10 15 20 0 10 20 30 40 50 60 70 80 90 100 Cumulative 39Ar Released (%) RE-CH08-04 Ar-Ages in Ma WEIGHTED PLATEAU 9.44 ± 0.24 TOTAL FUSION 7.05 ± 1.18 NORMAL ISOCHRON 9.35 ± 0.30 INVERSE ISOCHRON 9.35 ± 0.30 MSWD 0.22 Sample Info WR UBC Janet Gabites IRR  =  UBC can52 J  =  0.0037360 ± 0.0000187 C) 0 4 8 12 16 20 0 20 40 60 80 100 Cumulative 39Ar QuickTime™ and a  decompressor are needed to see this picture. Plateau age = 9.07±0.26 Ma (2σ, including J-error of .5%) MSWD = 0.67, probability=0.67 Includes 94.9% of the 39Ar Plateau steps are filled, rejected steps are open box heights are 2σ RE-CH06-4 Whole Rock D) Ag e (M a) Ag e (M a) Figure 3.9: Representative geochronology age plots for Chasm continued. C) Sample (RE- CH08-42) with a plateau age = 9.44 ± 0.24 Ma. D) Sample (RE-CH06-4) with a plateau age = 9.07 ± 0.26 Ma. 44 0 4 8 12 16 20 0 20 40 60 80 100 Cumulative 39Ar QuickTime™ and a  decompressor are needed to see this picture. Plateau age = 9.86±0.30 Ma (2σ, including J-error of .5%) MSWD = 0.81, probability=0.58 Includes 100% of the 39Ar Plateau steps are filled, rejected steps are open box heights are 2σ RE-CH06-18 Whole RockE) 0 4 8 12 16 20 0 20 40 60 80 100 Cumulative 39Ar QuickTime™ and a  decompressor are needed to see this picture. Plateau age = 9.58±0.40 M (2σ, including J-error of .5%) MSWD = 1.5, probability=0.17 Includes 99.7% of the 39Ar Plateau steps are filled, rejected steps are open box heights are 2σ RE-CH06-12 Whole RockF) Ag e (M a) Ag e (M a) Figure 3.10: Representative geochronology age plots for Chasm continued. E) Sample (RE-CH06-18) with a plateau age = 9.86 ± 0.3 Ma. F) Sample (RE-CH06-12) with a pla- teau age = 9.65 ± 0.4 Ma. 45 10.00 ± 0.48 Ma 10 5 0 5 10 15 20 0 10 20 30 40 50 60 70 80 90 100 Cumulative 39Ar Released (%) RE-CH08-1 WR Ar-Ages in Ma WEIGHTED PLATEAU 10.00 ± 0.48 TOTAL FUSION 4.58 ± 1.60 NORMAL ISOCHRON 10.43 ± 0.55 INVERSE ISOCHRON 10.55 ± 0.52 MSWD 1.58 Sample Info WR UBC Janet Gabites IRR  =  UBC can52 J  =  0.0037400 ± 0.0000187 G) H) 0 4 8 12 16 20 0 20 40 60 80 100 Cumulative 39Ar QuickTime™ and a  decompressor are needed to see this picture. Plateau age = 9.83±0.31 Ma (2σ, including J-error of .5%) MSWD = 0.94, probability=0.48 Includes 98.9% of the 39Ar Plateau steps are filled, rejected steps are open box heights are 2σ RE-CH06-92 Whole Rock Ag e (M a) Ag e (M a) Figure 3.11: Representative geochronology age plots for Chasm continued. G) Sample (RE-CH08-1) with a plateau age = 10.00 ± 0.48 Ma. H) Sample (RE-CH06-92) with a pla- teau age = 9.83± 0.32 Ma. 46 I) 8.26 ± 0.91 Ma 20 15 10 5 0 5 10 15 20 0 10 20 30 40 50 60 70 80 90 100 Cumulative 39Ar Released (%) RE-HY06-24 Ar-Ages in Ma WEIGHTED PLATEAU 8.26 ± 0.91 TOTAL FUSION 2.04 ± 2.54 NORMAL ISOCHRON 9.06 ± 2.34 INVERSE ISOCHRON 9.06 ± 2.32 MSWD 0.22 Sample Info WR UBC Janet Gabites IRR  =  UBC can52 J  =  0.0037251 ± 0.0000186 J) 9.19 ± 0.41 Ma 20 15 10 5 0 5 10 15 20 0 10 20 30 40 50 60 70 80 90 100 Cumulative 39Ar Released (%) RE-HY06-24 Ar-Ages in Ma WEIGHTED PLATEAU 9.19 ± 0.41 TOTAL FUSION 5.67 ± 1.58 NORMAL ISOCHRON 9.42 ± 0.56 INVERSE ISOCHRON 9.45 ± 0.55 MSWD 0.60 Sample Info WR UBC Janet Gabites IRR  =  UBC can52 J  =  0.0037251 ± 0.0000186 Ag e (M a) Ag e (M a) Figure 3.12: Representative geochronology age plots for Chasm continued. I) Sample (RE- HY06-241) with a plateau age = 8.26 ± 0.91 Ma. J) Sample (RE-HY06-242) with a plateau age = 9.19 ± 0.41 Ma. 47 K) 8.29 ± 0.97 Ma 20 15 10 5 0 5 10 15 20 0 10 20 30 40 50 60 70 80 90 100 Cumulative 39Ar Released (%)  RE-HY-06-29 Ar-Ages in Ma WEIGHTED PLATEAU 8.29 ± 0.97 TOTAL FUSION 0.91 ± 2.74 NORMAL ISOCHRON 9.55 ± 0.95 INVERSE ISOCHRON 9.58 ± 0.95 MSWD 2.31 Sample Info WR UBC Janet Gabites IRR  =  UBC can52 J  =  0.0035197 ± 0.0000176 L) 9.04 ± 0.41 Ma 20 15 10 5 0 5 10 15 20 0 10 20 30 40 50 60 70 80 90 100 Cumulative 39Ar Released (%) RE-HY06-29 Ar-Ages in Ma WEIGHTED PLATEAU 9.04 ± 0.41 TOTAL FUSION 6.17 ± 1.59 NORMAL ISOCHRON 9.31 ± 0.83 INVERSE ISOCHRON 9.32 ± 0.83 MSWD 0.40 Sample Info WR UBC Janet Gabites IRR  =  UBC can52 J  =  0.0035197 ± 0.0000176 Ag e (M a) Ag e (M a) Figure 3.13: Representative geochronology age plots for Chasm continued. K) Sample (RE-HY06-291) with a plateau age = 8.29 ± 0.97 Ma. L) Sample (RE-HY06-292) with a plateau age = 9.04 ± 0.41 Ma. 48 Sample Numbera AGE (Ma) System UTM Easting (NAD83) UTM Northing (NAD83) GEOGRAPHICAL LOCATION Lava Numberb RE-CH08-9 c1  8.89 ± 0.42 Ar-Ar 606393 5675485 Eastern Chasm canyon wall 1 RE-CH08-9 c2 8.18 ±  0.74 Ar-Ar 606393 5675485 Eastern Chasm canyon wall 1 RE-CH08-4 c 9.44 ± 0.24 Ar-Ar 608769 5671521 Eastern Chasm composite log 4 RE-CH06-4 d 9.07 ± 0.26 Ar-Ar 608609 5671734 Eastern Chasm composite log 5 RE-CH06-18 d 9.86 ± 0.3 Ar-Ar 609005 5671220 Eastern Chasm composite log Refer to Figure 3.1 RE-CH06-12 d 9.65 ± 0.4 Ar-Ar 609057 5671112 Eastern Chasm composite log Refer to Figure 3.1 RE-CH08-1 c 10.00 ± 0.48 Ar-Ar 609093 5671017 Eastern Chasm composite log Refer to Figure 3.1 RE-CH06-92 d 9.83 ± 0.32 Ar-Ar 607729 5668821 Western Chasm canyon wall no stratigraphic reference RE-HY06-24 c1 8.26 ± 0.91 Ar-Ar 603381 5671458 57 Mile, West Side of Highway 97 RE-HY06-24 c2 9.19 ± 0.41 Ar-Ar 603381 5671458 57 Mile, West Side of Highway 97 57 Mile Creek e 9.2  ± 0.4 D K-Ar 604277 5670184 57 Mile, East Side of Highway 97 RE-HY06-29 c1  8.29 ± 0.97 Ar-Ar 605595 5678011 63 Mile, West Side of Highway 97 RE-HY06-29 c2 9.04 ± 0.41 Ar-Ar 605595 5678011 63 Mile, West Side of Highway 97 d UBC; T. Ullrich, analyst GEOCHRONOLOGY OF CHILCOTIN GROUP BASALTS: CHASM CANYON AREA c UBC; J. Gabites, analyst e Matthews, 1988. a All samples are whole rocks. b Number assigned to individual lavas that can be traced laterally along the canyon, see Figures 3.1, 5.2, 5.3, and 5.4 Table 3.4: Geochronology of Chasm canyon. 49  The new whole rock ages provide the duration of volcanism at Chasm (Fig. 10; Table 3.4). The youngest lava was analyzed twice, and yielded ages 8.89 ± 0.42 Ma and 8.18 ±0.74 Ma (ages overlap at a 2σ level). The duration of volcanism calculated using the two different measured ages for the youngest lava are 1.11 ±0.64 Ma and 1.82 ±0.88 Ma. Using the weighted average for the youngest lava, the calculation yielded a duration of volcanism of 1.28 ± 0.61 Ma, which is the preferred estimate for the duration of volcanism at the Chasm (2σ internal error, refer to summary geochronology plot in Fig. 3.10, and Table 3.4). The addition in quadrature method was used to average the errors for the duration of volcanism calculation. This method is important for statistically calculating the correct error between two ages. This method as follows is: if ‘s’ is the probable value for the sum (or difference) of the two measurements ‘x’ and ‘y’ and if dx and dy are the probable uncertainties in ‘x’ and ‘y’ then the most probable error in ‘s’ (‘ds’) equals the square root of the sum of the squares ( ds = sqrt (sumsq (dx, dy) ).  The implication of the age results constraining the soil development for the paleosols is covered in Chapter 4 and discussion of the emplacement chrono-stratigraphy is found in Chapter 5, where the lava source direction and eruptive centre (s) are interpreted. 50 7 8 9 10 11 box heights are 2σ A G E (M a) 7 8 9 10 11 box heights are 2σ RE-H Y06-29  (1) RE-H Y06-29  (2) RE-H Y06-24  (1) RE-H Y06-24  (2) RE-CH 08-9 (1) RE-CH 08-9 (2) RE-CH 08-4 RE-CH 06-4 RE-CH 06-18 RE-CH 06-12 RE-CH 08-1 7 8 9 10 11 Plot of 40Ar/39Ar ages  for Chasm and related CGB outcrops OLD YOUNG CHASM SAMPLES Figure 3.14: Plot of 40Ar/39Ar ages for Chasm and related CGB outcrops 51 CHAPTER 4 PALEOSOL CLASSIFICATION 4.1  INTRODUCTION  Paleosols are ancient soils preserved in the geologic stratigraphic record. They are a common occurrence in basaltic successions and interesting to volcanologists because each sequence represents a volcanic hiatus. Paleosols are useful in volcanology where they bracket lava fl ows (Smith 1990), and they preserve soil-forming processes.  The Chasm canyon is the only known CGB exposure to exhibit distinctive red paleosols (Farrell et al. 2007).  The paleosols contain physical and chemical information useful in reconstructing paleoclimates, e.g., the type of ecological environment responsible for producing the soil, the mean annual temperature, and mean annual rainfall. However, such analysis requires multivariate datasets including that from chemical data, thin section analyses, and comparative case studies, to be able to accurately interpret attributes of the paleoclimate.  This chapter provides an overview of paleosols and the usefulness of paleosols in volcanology.  Fieldwork and thin-section analyses from CGB yields a “Brunisolic soil” classifi cation for the Chasm paleosol sample suite, a soil type, which may derive from a forest-type environment (Schaetzl and Anderson 2005). Field observations defi ne the paleosol horizons and horizon boundaries. Laboratory study of micromorphological features illustrates the microstratigraphic relationships in the soil profi les.  Combining these observations leads to a classifi cation of the soil. Chasm paleosols differ from most Canadian soils because of the parent material.  The paleosols exhibit two dominant parent materials, mafi c basalt and felsic tephra. These are qualitatively described below and shown in the horizonization of the soil sites. Chasm paleosols are compared with the Miocene Porcupine basalt paleosols at the Yukon-Alaska border (Smith 1994) and the coeval Columbia River fl ood basalt paleosols (Sheldon 2003). Preliminary climatic interpretations such as types of vegetation, tree growth, and the soil development of the Chasm paleosols are discussed.  Though preliminary climatic interpretations will be covered in this chapter, a complete paleoclimatic reconstruction is not 52 a part of this study. 4.1.1 Paleosol overview  Paleosols have been documented in many of the major continental fl ood basalt successions and igneous provinces, such as the Deccan Traps, the North Atlantic Large Igneous Province (prominent in the Faroe Islands), Karoo basin and the Columbia River Flood basalts (Smith 1990; Sheldon 2003; Sayyed and Hundekari 2006; Passey and Bell 2007; Keller et al. 2008;). For continental fl ood basalts, the paleosols are commonly termed “red boles”, “red beds”, “baked zones” and “red earth.” However the genetic term is paleosol and the red coloration is described by Munsell colors (Munsell 1994). Hawaii is a modern analogue for basaltic paleosols because they derive from the same parental material (Vitousek et al. 1997; Sheldon 2006). However the soil processes in Hawaii relate to its tropical and humid climates and are strongly dissimilar to the paleo-environmental conditions in interior British Columbia during Miocene time.  For the purposes of this study, soil is defi ned as the accumulated material on an earth surface that is altered via a combination of physical, chemical and/or biological processes (Retallack 2001). The classifi cation of paleosols is challenging, likely due to the additional complexity of the buried soils, compared with modern fresh soils, and application of the conventional soil terminology presents a challenge in the combination of soil science and volcanology analysis required to understand the Chasm paleosols. This chapter aims to develop terminology and to classify the paleosols at Chasm. Paleosols, literally ‘ancient soil,’ are distinguished from sediment (Retallack 2001) by evidence of roots or root casts, soil structure, and presence of soil horizons (colour variations). In contrast, a saprolite is simply a decomposing rock that progressively grades downward into coherent solid bedrock.  Saprolite retains the fabric or appearance of a rock, but can be altered drastically. Regolith is a broader term, encompassing any material which ‘blankets’ the bedrock (i.e. tephra, glacial deposits, loess, organic matter, alluvium, colluvium, and soil) 53 (Anand and Butt 1988). Paleosols are often subdivided into horizons; fi eld classifi cation of horizons is subjective as the actual horizons may be diffi cult to defi ne due to compaction, weathering, and erosion. A signifi cant amount of alteration can occur post-burial, which masks the original properties of the soil. It is simpler to recognize horizon boundaries in modern soils, where the layers have not been greatly disturbed or obliterated.  The analyses of horizons in the Chasm paleosols will be described later in this chapter.  However, there are many cases in which paleosol sites will not have all three factors necessary for paleosol classifcation.  In this case, chemical data must be obtained, and the weathering of specifi c elements will be useful in whether or not the material is a paleosol.  In addition, study of the micromorphology of soil peds may also used in combination with the chemistry to classify the paleosol. Paleosols are divided into one of four classes (Schaetzl and Anderson 2005): 1) relict paleosols; 2) vetusol paleosols; 3) buried paleosols (the common type in volcanic sucecessions); and 4) isolated paleosols. Relict paleosols are found at the modern day surface and have characteristics indicative of past environments. Vetusols can be buried or at the surface, and the climate at the time of burial is similar to the present-day climate. Isolated paleosols are a sub-category of ‘buried paleosols.’ Buried paleosols occur interstratifi ed between lavas, and are often baked by an overlying lava fl ow and/or tephra layer. In non-volcanological scenarios, the buried paleosols are overlain by loess, till or alluvium. The rate of burial, gradual or immediate, has direct implications for the amount of erosion. 4.2  PALEOSOL PROFILES AT CHASM  In this section, I defi ne the Master horizons at each profi le site (Stn. 069, 070, 071), describe the colour and thickness of each horizon, and characterize the contacts between the horizon (i.e., horizon boundaries). The sites were chosen in the Chasm eastern composite 54 log section (Fig. 3.1), based on accessibility and exposure needed for detailed soil profi ling. Micromorphology is a thin-section method used whereby textural and fabric analyses are carried out, and results determined, which subsequently classify the Chasm paleosols. The term ‘texture’ differs between the fi elds of soil science and volcanology. For this chapter only, the term ‘texture’ is specifi c to the soil science defi nition, which means proportions of different particle sizes of sand, silt and clay. The particle sizes are measured using the diameter of grain, instead of the entire grain used by geologists. 4.2.1 Field methods  Fieldwork focusing on the paleosols was carried out over two days under the guidance of soil scientists Paul Sanborn (Univ. of Northern British Columbia) and Scott Smith (Soil Classifi cation Working Group 1998).  The methods used in observation and sampling were conducted in accordance with standard soil science practices, and comprise the abbreviated following steps (the description criteria is obtained from ‘Expert Committee on Soil Survey’ (1983), whereas the soil horizon nomenclature is from the ‘Soil Classifi cation Working Group’ (1998)): 1) choose profi le sites 2) draw soil profi le 3) defi ne horizons 4) defi ne color and thickness of each horizon with descending depth 5) identify and characterize the contact boundaries between horizons 6) record any root traces, preserved soil structures, or any other features present.  I chose stations 069 through 071 as profi le sites, based on the stratigraphic context with the overlaying lava and accessibility of the paleosol.  Detailed soil profi les were drawn (Figs. 4.5 and 4.6) in an approximate 2 m x 1 m format at three sites in the Chasm within the main eastern composite section (Figs. 2.2; Fig. 3.2).  At each site, I used oriented and grab (unoriented) samples and samples of adjacent volcanic tephra (Tables 4.1-4.3, Figs.4.5- 55 a) c) b) CUBIC STRUCTURE N E GRADATIONAL BOUNDARY BETWEEN PALEOSOL AND UNDERLYING BASALT AAMYGDALOIDAL BASALT Figure 4.1: Field photographs of paleosols exposed at Station 68; a) Nature of contact between paleosol and the underlying basalt. Hammer for scale is 30 cm, b) Detailed view of the amygdaloidal basalt showing the diffuse boundary between the paleosol and the basalt. Scale card is 7 cm, c) Soil structures are found at Chasm. Scale card is 7 cm. 56 WAVY AND SHARP CONTACT BOUNDARY a) b) c) d) AMYGDALOIDAL BASALT VESICULAR BASALT Figure 4.2: Field photographs of paleosol Station 69. This station is mapped in the East- ern composite log (Fig. 3.1) a) Boundary between paleosol contact and underlying basalt. Note the wavy boundary at this scale., b) Detailed view of the vesicular basalt, undulating paleosol and underlying amygdaloidal basalt emphasizing the wavy paleosol boundary, c) Detailed view of underlying amygdaloidal basalt, which is overlain by the wavy and sharp paleosol boundary, d) View of wavy and sharp contact boundary between overlying basalt and paleosol. 57 a) b) basaltic core stones Figure 4.3: Field photographs at Station 70. a) Basaltic core stones are common, in the Chasm paleosols, and set into the uppermost paleosol horizon (Bmb), b) Detailed view of core stones. Hammer for scale is 30 cm. The core stones are weathered, rounded to sub- rounded, vesicular basalt. 58 a) c) b) Possible tephra layer possible tephra layer core stones vesicle trains Figure 4.4: Field photographs of paleosol at Station 71. a) View of the abrupt, smooth boundary of the paleosol. In addition, horizontal vesicle trains are observed in the overly- ing basalt. b) Note the core stones in horizon, IIBmb1, and overlying tephra layer, horizon Bmb. c) Detailed view of tephra layer. 59 Paleosol Profile: Station 069 Bmb base not drawn 2m 0m OVERLYING LAVA Horizons: Notes: 10- 20 cm depth  II C1 PIPE VESICLES 30-40% BASALT FLOAT FRAGMENTS TRANSITIONAL ZONE  > 90% WEATHERED BASALT WEATHERED BASALT  II C2 R 2.5 YR 5/8 2.5 YR 6/6 0- 15 cm thick 2.5 YR 6/82.5 YR 4/4 20- 40 cm depth 40- 60+ cm depth 2.5 YR 4/2 2.5 YR 4/8 7.5 YR 6/3 Munsell Soil Color: Figure 4.5 Figure 4.5: Paleosol profi le at Station 069, Eastern Composite Log Section (Fig. 3.1). This profi le is the typical paleosol found at Chasm. There is no O, A, or E horizon in this section. Horizon Bmb, means ‘B Horizon, ‘Bm’ is the subcategory delineating that the material has been altered from what the original material was to start with, and lowercase ‘b’ indicates that the paleosol is a buried paleosol. Roman numerals that are the same, in this case in the C Horizon, specifi es that the material is the same, however the numbers 1 and 2 indicate that there are differences between the 2 layers, which separates them into 2 horizons (i.e. contact boundary, coloration, or other features). A C-horizon is weathered basalt; in this case, that has a hardness < 3 on the Mohs Hardness scale.  The R horizon is unweathered or less weathered basalt, the only difference in the overlying lava in Stn 069, is that the R hori- zon is amygdaloidal. Note the Munsell colors combine hue, value, and chroma to defi ne the soil color, which enables a standard for comparison of soil colors down the profi le. 60 base not drawn  II Bmb1  II Bmb2  III C Paleosol Profile: Station 071  R  Bmb Horizons: 2 cm thick 2 - 15 cm depth 15- 30 cm depth 30- 110+ cm depth } TEPHRA FINE LAMINATIONS CORE STONES WEATHERED BASALT OVERLYING LAVA 1.5m 0m Notes: 7.5 YR 6/4 2.5 Y 6/6 2.5 YR 6/8 10 YR 8/4 10 YR 6/3 2.5 YR 6/6 2.5 Y 6/6 10 YR 8/410 YR 4/1 Munsell Soil Color: Figure 4.6 Figure 4.6: Paleosol profi le at Station 071, in the Eastern Composite Log Section (Fig. 3.1) There is no O, A, or E horizon in this section (or in any section in Chasm) Horizon Bmb, means ‘B Horizon, ‘Bm’ is the subcategory delineating that the material has been altered from what the original material was to start with, and lowercase ‘b’ indicates that the pa- leosol is a buried paleosol. Bmb in this profi le is a tephra layer. Roman numerals that are the same, in this case in the IIBmb1 and IIBmb2 Horizon, specify that the material is the same, however the numbers 1 and 2 indicate that there are differences between the 2 layers, which separates them into 2 horizons (i.e. in this profi le the 1st horizon has fi ne laminations whereas the 2nd horizon below has core stones). The C horizon is weathered basalt that has a hardness < 3 on the Mohs Hardness scale; it does not resemble the fi ne grained paleosol material of the overlying horizons, Roman numeral III denotes the different material.  The R horizon is unweathered or less weathered basalt lava. Note the Munsell colors combine hue, value, and chroma to defi ne the soil color, which enables a standard for comparison of soil colors down the profi le. 61 Station: 069   Location: Chasm Provincial Park; eastern wall composite log section  Paleosol ID: P4 (between lava 4 and 5)  Parent Material: Basalt (Miocene) & aeolian deposits including tephra  Soil Classification: Brunisol   1 d indicates a dry sample Horizon (Sample) Depth (cm) Munsell Color Description  Bmb (RE-CH07-37) (RE-CH07-41) 0-15 Red (2.5 YR 5/8 d 1) Red (2.5 YR 6/6d) very fine; grains: subrounded to rounded; 30-40% basalt float fragments; lower boundary broken ; friable IIC1 (RE-CH07-38) (RE-CH07-42) 10-25 Red (2.5 YR 6/8d) Dusky Red (2.5 YR 4/4d) fine; grains: subangular to subrounded; transitional zone from fine grained paleosol to weathered basalt. > 90% weathered basalt; friable IIC2 (RE-CH07-39) (RE-CH07-43) 25-50 Dusky Red (2.5 YR 4/2d) Dark Red (2.5 YR 4/8d) fine; grains: subangular to subrounded; > 90% weathered basalt R (RE-CH07-40) (RE-CH07-44) 40- 60+ Light Brown (7.5 YR 6/3d) unweathered or less weathered basalt lava Table 4.1:  Paleosol samples from Station 069. This table accompanies Figure 4.5. In Bmb horizon a broken boundary means that the horizon is not laterally continuous, some parts of the horizon may be disjointed or disconnected (Soil Survey Staff, 1993). 62 Station: 070   Location: Chasm Provincial Park; eastern wall composite log section  Paleosol ID: (see Fig. 5)  Parent Material: Basalt (Miocene) & aeolian deposits including tephra  Soil Classification: Brunisol   1 d indicates a dry sample Horizon (Sample) Depth (cm) Munsell Color Description  Bmb (RE-CH07-45) (RE-CH07-49) 0-15 Red (2.5 YR 6/6d) Red (2.5 YR 5/6d) very fine; grains: subangular to subrounded; clear wavy boundary; core stones & basalt fragments common; friable IIC1 (RE-CH07-46) (RE-CH07-50) 15-30 Red (2.5 YR 6/6d) Weak red (2.5 YR 5/3d) very fine; grains: rounded; core stones (cobble-sized); clear and broken lower boundary; weathered basalt; friable IIC2 (RE-CH07-47) (RE-CH07-51) 30-75 Dusky red (2.5 YR 4/3d) fine; grains: subangular to subrounded; weathered basalt; friable IIC3 (RE-CH07-48) (RE-CH07-52) 75- 150+ Greyish brown (10 YR 5/2d) Weathered basalt; no “R” horizon present, since lower boundary is covered with taluvium Table 4.2: Paleosol samples from Station 070. There is not a profi le fi gure for this section, however it resembles Figure 4.5, which is the typical Chasm profi le. In Horizon Bmb, the ‘clear’ boundary relates to the sharpness of the contact, which implies the thickness of the boundary to be 2-5 cm (Soil Survey Staff, 1993). The ‘wavy’ contact refers to the lateral continuity meaning that the crests and troughs of the contacts undulations are wider than they are deep. 63 Station: 071   Location: Chasm Provincial Park; eastern wall composite log section  Paleosol ID: (see fig. 5)  Parent Material: Basalt (Miocene) & aeolian deposits including tephra  Soil Classification: Brunisol  Horizon (Sample) Depth (cm) Munsell Color Description  Bmb (RE-CH07-53) 0-2 Light brown (7.5 YR 6/4d) Olive yellow (2.5 Y 6/6d) tephra layer; very fine; grains: subangular to subrounded; laterally continuous for 7 m; retains uniform thickness; very fine gr., subangular to subrounded; possible platy structure; abrupt, smooth boundary IIBmb1 (RE-CH07-54) (RE-CH07-58) 2-15 Red (2.5 YR 6/8d) very fine; grains: subangular to subrounded; abrupt; irregular boundary; very fine grained; subangular to subrounded; platy due to present-day weathering IIBmb2 (RE-CH07-55) (RE-CH07-59) 2-15 Very pale brown (10 YR 8/4d) fine; strong; grains: subangular; medium platy; platy units aligned parallel to the face of exposure (due to present-day weathering), > 10% core stones (cobble-sized) gradational contact; IIIC (RE-CH07-56) (RE-CH07-60) 15-30 Pale brown (10 YR 6/3d) Transistion zone to weathered basalt; gradual; wavy boundary R (RE-CH07-57) (RE-CH07-61)  30- 110+ Olive yellow (2.5 Y 6/6d) Dark grey (10 YR 4/1d) Very pale brown (10 YR 8/4d) Coherent basalt Table 4.3: Paleosol samples from Station 071. This table accompanies Figure 4.6. Horizon Bmb is an abrupt, smooth boundary. 64 4.6) to defi ne horizon boundaries, establish the relative thickness of each horizon, describe the contact areas between horizons, and describe textures.  Below, I review each step in the method and subsequently describe the results from each Chasm sampling/profi le site. Horizons are categorized into broader ‘Major mineral horizons’ and subordinate categories, denoted by a lowercased letter following the Master horizon (e.g., Xx), which adds pedogenic (soil-forming processes) information to the Master horizon (Retallack 2001). The major horizons relevant to this study are: (A, Ae, B, C, R): 1) ‘A’ horizon (i.e., in Canadian soils either ‘Ah’ grassland soil with organic matter and roots or ‘Ae’ forest soils, which show the removal of clay and intensive weathering of primary minerals) 2) ‘Ae’ horizon (i.e., usually lighter in color, characterized by less organic matter, clays and iron and aluminum oxides) 3) ‘B’ horizon (i.e., the descriptive feature is the horizon does not resemble the rock structure, common ped structures can be present including granular, blocky or prismatic. 4) ‘C; horizon (i.e., more weathered than bedrock, characterized by a hardness of 3 on the Mohs Hardnes scale) 5) ‘R’ horizon (i.e., coherent bedrock).  Organic horizons (> 17% organic carbon) may or may not survive burial, and are often absent in paleosols. Different types of organic horizons are recognized depending on whether the original setting was either well-drained or subject to prolonged wet conditions. Soils that do not have all of these Master horizons can still be considered complete profi les, since diverse climates yield different soil profi les (Retallack 2001). In soil science methodology, a section is logged downward from the initial horizon. Colour is categorized by using the Munsell Soil Color Chart (1994), and is commonly the fi rst criterion used to assess the soil.  The Munsell chart combines hue, value and chroma to develop a comprehensive range of colors to describe soils; the chart serves as a standard to relate color changes in the horizons.  Importantly, colour distinctions serve as a method to differentiate between horizons. 65  For example for a reddish brown soil labelled 5 YR 4/3, the hue is 5YR, value is 4, and chroma is 3.  With depth, elements are leached out and the coloration changes.  For basaltic weathering, nearly all of Ca and Na, but less than half of Fe, K, and Al are leached out the rock (Bain et al. 1980).  Ca and Na do not affect colour, soil colours usually are affected by the amount of organic matter present, redox (e.g., redding when soils oxidize), and addition of materials that coat primary grains. Textural analysis: micromorphology  Micromorphology refers to microscopic observations, usually in thin sections. Micromorphology methods are useful in that they help identify fabrics and composition of soils, which may be used to distinguish one soil from another (Stoops 2003). Micromorphology is also used in conjunction with modeling to reconstruct climate.  There are both qualitative and quantitative methods are that being developed (Kemp 1999; Sheldon 2003). Specifi c paleoclimatic information can be discerned only after an extensive study including the chemical weathering of the basalt and tephra deposits, microstructures, and other fi eld features such as roots (Sheldon 2003). For a complete reconstruction, researchers have mostly used comparative biological data such as organic matter, fossil organisms or fl ora, to reconstruct paleo-climates.  As no organic matter, roots, fossils, or fl ora have been observed at Chasm to date,  a complete investigation was not attempted as part of this study. However, micromorphologies can be used to make preliminary climate interpretations (Kemp 1999; Kemp and Zarate 2000).  In the macroscopic study of soil horizons at Chasm, there is insuffi cient fi eld data to completely characterize the paleosols (e.g., the absence of roots or traces of roots in the profi les).  Here, micromorphology methods are used to test whether the material in-between the Chasm basalts interpreted as lava fl ows are in fact paleosols. Methodology: ‘fabric’ studies    The study of micromorphology is divided into two parts, fabric studies and compositional studies (Stoops 2003).  In this study, I use fabric studies to evaluate the 66 micromorphologies of the Chasm suite of paleosols.  The test of whether inter-fl ow layers are paleosols involved a micromorphological analysis of each horizon at all three sampling locations.  Fabric studies describe the different elements of the soil fabric. Bullock et al. (1985) defi ne soil fabric as a comprehensive organization of the soil, not only an emphasis on the large grains, but the entire arrangement in the sample.  Spatial relationships, frequency of elements, size, and shapes of features are all indicative of the processes that formed and weathered the soil. The fi eld of fabric studies within micromorphology is complex and detail- specifi c, and hosts a variety of terms to describe all relevant features in the profi le.  Soil science methods were followed for sampling and the preparation of thin sections, for optimal preservation of the microstratigraphy (Kemp 1999). Paleosols were sampled with known orientation and stratigraphic context in the soil profi le. Each sample was taken from the middle of the defi ned horizon (Figs. 4.5 and 4.6) (Stoops 2003).  A metal frame was inserted into the soil to keep the samples secure, oriented and the microstructures undisturbed. The microstratigraphic relationships are extremely fragile, and the paleosol material friable, especially the upper horizons. To preserve such fragile textures, the samples were impregnated with resin, and cut into lantern-sized thin sections at standard thin section thicknesses.    A total of sixteen Chasm samples were analyzed in the micromorphological study. The thin section analyses were carried out in the laboratory facilities at the University of Northern British Columbia. Components for the Chasm paleosols (Stations 069, 070, 071) are described using the Stoops (2003) reference collection of photographs illustrating the fabric complexities of paleosols (Table 4.4) For comparative purposes, slides from the stations were photographed at the same magnifi cation (5x) to compare the types and relative abundances of the microstructures in each profi le. 67 MICROMORPHOLOGY DATA Sample No. Horizon Summary of Observations: Station 069 RE-CH07-37 Bmb  ~5% of quartz; Fe clay coating fragments; distinctive Mn rim around qtz crystal; granular clusters of Fe; accomodating planes; nodule of Mn with a hypo-coating of Fe; infilling of an Fe channel RE-CH07-38 IIC1 similar to weathered basalt; basaltic clasts are vesicular; Fe clay coating fragments; Mn coating around the rim of the amygdules. RE-CH07-39 IIC2 no soil textures preserved; weathered basalt RE-CH07-40 R no soil textures preserved; weathered basalt Station 070 RE-CH07-45 Bmb Fe nodules (honey brown colour); laminations in Fe channel; Fe papules detached from original coating Station 071 RE-CH07-54 IIBmb1 platy structure; appears to have an alignment of clay coatings/nodules; ribbon-like (infilled channel) of the manganese coating; fragments of coatings observed; zonation in coating, light to dark honey brown colouration visible RE-CH07-55 IIBmb2 platy strcuture; high % of quartz (~20%); sub-angular basalt fragments; olivine microphenocrysts; fragments of nodules and coatings; clusters of fe coating fragments; coating (rim) surrounding basalt clasts; fine laminations seen; example of micro-platy fabric RE-CH07-56 IIIC Fe coating fragments; Mn rims around vesicles in basalt clasts; accomodating planes; absence of quartz; showing typical weathered basalt (olivine, plag etc.) RE-CH07-57 R no soil textures preserved; weathered basalt Table 4.4: Micromorphological data 68 4.2.2 Horizon defi nition  Horizons identifi cation is key to analyzing modern soil profi les and paleosols. A horizon is a soil layer that is approximately parallel to the ground, and distinguished from overlying and underlying layers by physical, biological and chemical factors (Chesworth, 2008). The Canadian soil classifi cation scheme (http://sis.agr.gc.ca/cansis/taxa/cssc3/chpt2. html), to defi ne the soil horizons in the Chasm profi les. Using this scheme, I have defi ned soil horizons from all 3 sampling locations at Chasm (Figs. 4.5 and Fig. 4.6).  At Chasm, because the O, A and E horizons are missing, the B-horizon is the initial horizon. 4.2.3 Colour and thickness of horizons    Colours for the paleosols observed at all 3 sampling locations are shown in Figures 4.5 and 4.6.  In general, B-horizons range from red to purple; usually two different colors are described for this horizon.  In all three Chasm stations, at least 1 Bmb horizon is described (Figs. 4.5, 4.6; Tables 4.1-4.3).  The lowercase ‘m’ denotes that it is either has ped structures (i.e., an aggregate of grains that are separated from the adjacent ped based on a zone of weakness) or is colored appropriately for a B Horizon.  The lowercase ‘b’ signifi es that the soil is a buried soil. Once that is initially specifi ed, all of the remaining horizons with depth are inferred to be ‘buried’ horizons.  Stations 069, 070, and 071 have single or multiple ‘C’ horizons (Figs. 4.5-4.6; Tables 4.1-4.3). The ‘C’ horizons are challenging to categorize on account of the differentiation between weathered basalt with unweathered basalt lava (‘R’). These have been characterized as weathered basalt, which are distinguishable from the overlying basalt lava (above initial paleosol horizon, on the basis of the relative degree of weathering (Figs. 4.5-4.6; Tables 4.1- 4.3).  This interpretation of ‘C’ rather than ‘R’ is justifi ed for the following reasons: 1) Hardness: ‘C’ horizons have a hardness value of less than 3 of the Mohs scale (i.e., calcite range), and can be sampled with a spade, whereas the underlying basalt lava that is less weathered and must be sampled with a rock hammer or a sledgehammer. 69 2) Fractures: There are numerous fractures in the Chasm ‘C’ horizons. The fractures are highly amygdaloidal, and coloration has a reddish hue compared to the grey-brown of the ‘R’ horizon. 3) Features: Rounded to sub-rounded basaltic core stones are common and are interpreted as basaltic fragments that have been ripped up from the underlying lava. Station 071 includes a tephra layer, which is the initial horizon, and then below it fi ne laminations are present, though larger-scale bedding is absent (Fig. 4.6; Table 4.3).  The ‘R’ horizon represents coherent rock, which must have hardness greater than 3 on the Mohs scale. The Chasm basalt is signifi cantly harder than the 3 threshold, on account of the minerals olivine, pyroxene, and oxides, which all have a hardness greater than 6. These horizons are all varying percentages of vesicularity, however the vesicles have been in-fi lled (amygdales). There are less fractures in this fi nal horizon, the basalt is cemented together, and no longer brittle. The coloration of this horizon is typically vastly different from the initial horizon (Figs. 4.5 and 4.6); there are no longer any 2.5 YR hues.  Providing that the initial materials were the same, and similar environments prevailed, older soils will have thicker A and B-horizons. The thickness of the horizons is relevant in describing soils; commonly B-horizons are <2 m (Retallack 2001), and the Chasm paleosols fi t within this range. Each Chasm horizon ranges in thickness between 1- 40 cm. The total thickness of the paleosols range from <0.5-3 m. Soil profi les (Fig. 4.5 and 4.6) graphically show the thickness variations between stations 069 and 071. 4.2.4 Horizon boundaries  The nature of the contacts between the horizons is important, for these soil boundaries help interpretation of the soil-forming processes. The horizon boundary is always referring to the lower boundary. There are two broad categories within horizon boundaries: boundary sharpness and boundary lateral continuity (Retallack 2001). 70  Generally, the uppermost horizon has a sharp boundary, whereas the successive lower horizons have gradational contacts (Retallack 2001).  All three of the study locations exhibit a relatively sharp boundary, which underlie the initial paleosol horizon (Tables 4.1-4.3).  Laterally contacts are typically undulating, irregular or broken and the paleosols commonly infi ll cracks within underlying lava units (Figs. 4.5 and 4.6).  Texture (grain- size) follows the trend of fi ner grained at the initial horizon and coarser with depth. Two soil profi les (Figs. 4.5 and Fig 4.6) have been drawn to show the different types of profi les at Chasm, Station 69 is a typical profi le, whereas Station 71 is a volcanic ash-rich paleosol.  Clastic dikes are a recurrent large-scale feature associated with the paleosols (Fig. 3.5c). The dikes are observed as vertical cracks that are in-fi lled with paleosol material. The dikes do not represent discrete features in time and space; rather, the dikes are commonly laterally connected with a paleosol horizon.  Based on larger-scaled mapping, the Chasm paleosols are pockets which are commonly deeper than wide, and may be considered ‘irregular’ (e.g., Fig. 3.2.c).  The pockets are approximately 1.5 to 5 m depth, however this is variable in the expanse of the canyon. The average depth of the pocket (clastic dike) is 2.2 m.  The three Chasm paleosol sites appear laterally uniform. However, additional fi eldwork across the entire Chasm canyon reveals more complexity.  When mapping the paleosols laterally, it is common for a paleosol to truncate (Figs. 5.2, 5.3 and 5.4), terminate, or show discontinuity at either the present day surface or mid-section.  Moreover, paleosols appear locally ‘welded’, meaning there is a visible but blurred boundary where two separate paleosol profi les (older and younger soil profi les) are mixed together.  Larger scale mapping of the paleosols reveals more lateral irregularities, and will be further discussed in Chapter 5. 71 SA M PL E RE -C H 07 -5 4 SA M PL E RE -C H 07 -4 5 SA M PL E RE -C H 07 -5 5 SA M PL E RE -C H 07 -3 7 accommodating planes infilled vesicle basalt clast Fe nodule Figure 4.7: Summarizing the key soil micromorphology present in the Chasm paleosols. Four oriented thin sections showing the micromorphological diversity at Chasm. Sample RE-CH07-54 (stn. 071 / horizon IIBmb1) shows accommodating planes that are sub- parallel to the underlying basalt; RE-CH07-55 (stn. 71 / horizon IIBmb2) is an example of a corestone (vesicular basalt) set into the fi ner-grained matrix of the palesol; RE-CH07-37 (stn. 069 / horizon Bmb) is a mixture of rod-like, globular, and blocky particles; RE-CH07- 47 (stn. 70 / horizon Bmb) shows a poorly sorted sample, with Fe, Mn and clay coatings present. 72 Figure 4.8: Clay coating (Cl c) with fi ne laminations visible. Sample RE-CH07-54. 73 A B C D ac co m od at in g pl an e Fe Fe Figure 4.9: Micromorphology thin section plate at Station 69. All sections are taken from oriented samples. A is the Bmb horizon, B is the IIC1 Horizon, C is the IIC2 Horizon, and D is the R horizon; samples taken top to bottom in section profi le. All photomicrographs at 5x magnifi cation. A) A vertical accommodating plane (Sample: RE-CH07-37-A); B) Small Fe and Mn nodules make up the reddish brown and back globulars (Sample: RE-CH07-38- -B); C) Weathered basalt with two prominent Fe coatings (Sample: RE-CH07-39-C), D) Weathered basalt, regolith, where the fabric of the basalt is present (Sample: RE-CH07-40- -D). 74 A B C D amygdale Mn coating amygdale Figure 4.10 Figure 4.10: Micromorphology thin section plate at Station 70. All sections are taken from oriented samples. A is the Bmb horizon, B is the IIC1 Horizon, C is the IIC2 Horizon, and D is the IIC3 Horizon; samples taken top to bottom in section profi le. All photomicrographs at 5x magnifi cation. A) Shows a sub-rounded Mn coating (Sample: RE-CH07-45-A); B) Shows amygdale with a well-defi ned rim of Fe (Samples: RE-CH07-46-B); C) Weathered basalt with amygdale rimmed with an Fe coating (Sample: RE-CH07-47-C); D) Weathered basalt with amygdale (Samples: RE-CH07-48-D). 75 A B C accomodating planes Fe channels bl Figure 4.11 Figure 4.11: Micromorphology thin section plate at Station 71. All sections taken from oriented samples. A is the IIBmb1 horizon, B is the IIBmb2 Horizon, C is the IIIC Horizon; samples taken top to bottom in section profi le. All photomicrographs at 5x magnifi cation. A) Shows two accommodating planes sub-parallel to the horizon. Inside the dashed line is an example of blocky structure (Sample: RE-CH07-54-A); B) Two Fe channels are visible in this section. Darker sub-rounded particles are Mn coatings (Sample: RE-CH07-55-B); C) Predominately weathered basalt with Fe coatings surrounding many of the grains (Sample: RE-CH07-56-C). 76 4.2.5 Results  In this section, I will describe the aggregation, voids, microstructure, and pedofeatures of the horizons at Chasm (Stoops 2003).  All of these terms will be defi ned, and described based on the fi ndings within the Chasm paleosols. Aggregation of Chasm paleosols  Aggregation is how the soil partings create void spaces (i.e., peds); and are broken along areas of weakness in the ped (Stoops 2003). There can be granular peds, which are oval shaped and non-porous, or blocky peds (similar to larger-scaled blocky structure observed in the fi eld (Stn. 068; Fig. 4.11a). These blocky peds are typical found lower in the soil profi le in the B Horizon. This is observed at the horizon at station 068. The blocky peds are glued together by coatings that derive from the overlying horizon. These coatings are visible in thin sections (Fe and Mn) and fi lls in the voids in the pore spaces (Fig. 4.10a). At Chasm, angular to subangular blocky peds have been observed in thin-section (Fig. 4.11a), seen with angular edges of the blocks. Granular aggregates are more common and are common in the uppermost horizons (Figs. 4.9c, 4.9d, 4.11a and 4.11b).  There are numerous ways that a soil can form differently shaped aggregates, from processes associated with amount of organic material, any microbial activity, freeze / thaw cycles and texture (grain-size). When the profi le is devoid of aggregates, the horizon is deemed ‘massive.’ Observed soil peds at Chasm, expose a soil-forming process, confi rming the classifi cation of a paleosol. Voids  The voids observed in the Chasm samples, part of the fabric of the paleosol, yielded interesting features such as channels, vughs, and planes. Channels are ‘tubular smooth voids’ (Stoops 2003), and are commonly seen as channel fragments in the Chasm specimens (Fig. 4.8; Sample RE-CH07-37). These channels form shapes such as arches or cylinders, which help to discriminate channels from aggregates. Vesicles are seen where there are basaltic 77 clasts set into the paleosol matrix (Fig. 4.8; Sample RE-CH07-55). Typically, only there is only a 5% modal abundance of these basalt clasts, however when the abundance is higher the classifi cation of a vesicular microstructure can be applied (Table 4.4).  X-ray diffraction methods helped identify the secondary mineralization infi lling the vesicles as the zeolites chabazite-Ca and phillipsite (Appendix E). This occurred after burial, zeolites are unusual in soils, except where salinity is present. Microstructure  There are two kinds of microstructures in the peds of Chasm: fractures and crumb microstructures.  Fractures in the soil are highlighted by a series/sequence of planes.  If the observed planes can be hypothetically reassembled (puzzle-like), the planes are said to ‘accommodate’ one another.  Accommodating planes are technically described as ‘elongated poroids’ (Stoops 2003) that have one or more sharp edges as the plane terminates in the section. These planes can form with the shrinking and swelling of clays in the horizons (usually the horizon with the highest clay content (Bt) horizons, however in our case, Bm horizons). Accommodating planes are typical in the Chasm suite (Fig. 4.8; Sample RE-CH07-54; Fig. 4.9a, Fig. 4.11aa). These planes are only identifi ed in the initial horizon for each station.  Crumb microstructure is also recognized (Fig. 4.8; Sample RE-CH07-45). It comprises largely rounded aggregates, which lack accommodation structures, and locally some particles merge themselves together to form a rounded aggregate (Stoops 2003). Pedofeatures  In paleosols, the most commonly documented micromorphological feature is clay coatings (pedofeatures; Kemp 1999). Iron and manganese coatings are observed in paleosols at every station in the Chasm suite, however clay coatings are less common. At Chasm, there are Fe and Mn coatings, where a rim is observed around the surface of the void (Stoops 78 2003). Clay coatings are birefringent under cross-polars and form through translocation of clay particles downward through the profi le. Laminations are rare, but occur inside the clay coatings (Fig. 4.8: Station 71, Sample RE-CH07-54). Clay coatings are relict of soil processes, specifi cally the translocation of clay, forest settings need more water than grassland environments, clay coatings are suggestive a forest setting, however more work is necessary for a comprehensive classifi cation. Parent Material  The Chasm paleosol suite comprises a complex mix of two distinctive parent materials, mafi c basalt and felsic tephra. Basaltic parent materials generally yield a higher clay content (Wilson 2006); clay minerals such as montmorillonite (smectite) become present in the post- burial alteration process. XRD analyses of sample RE-CH07-58 (Station 071; horizon IIBmb1) indicated dominant peaks of analcime (associated with zeolites), plagioclase, quartz, and zeolites (chabazite-Ca, phillipsite-K and tridymite). Smectite (montmorillonite), K-feldspar, muscovite, and grunerite are present in smaller proportions (Appendix E). With the higher clay content, this implies larger water retention, and studies have shown that basaltic soils hold 40% water content, compared to 17% for granitic soils (Olowolafe 2002), however water retention varies with the age of the soil. Water retention can expedite weathering of the basaltic minerals into soil. The parent material controls grain-size, and a basaltic parent will yield a fi ner-grained soil, opposed to a granitic parent (Wilson 2006). Basaltic weathering studies have measured the different rates of breakdown of the specifi c oxides, emphasizing the stages of weathering, which produce clay minerals (Bain et al. 1980; Eggleton et al. 1987; Wilson 2006).  The felsic ash component was identifi ed in the fi eld, incorporated into the soil profi le, and confi rmed as tephra in the laboratory using immersions oils, as a preliminary means of classifying the material. The ash component is found in all horizons down to  the ‘C’ horizon of most Chasm profi les, and is inferred to the present in all P facies (refer to Chapter 3). The 79 Chasm paleosols are unique when compared to other Canadian soils due to the mixed nature of these parent materials. The smaller tephra fraction elicits a more complex classifi cation and climatic interpretation. The Canadian soil classifi cation does not have a separate classifi cation for ash rich soils, however the US soil classifi cation uses the term Andisols to name these soils. The US soil classifi cation equivalent for a Brunisol is an Inceptisol.  Compositionally, the paleosols are predominately made up of weathered basalt (consistent mineralogy), however there are some non-basaltic minerals, such as quartz, which are interpreted to be introduced into the paleosols from a foreign location by wind or water. Chasm paleosols were chemically analyzed using citrate-dithonthinite-bicarbonate (CDB) extraction of Fe oxides.  CDB extacts crystalline Fe oxides and hydroxides (hematite, goethite), non-crystalline Fe (ferrihydrite), and Fe (organically complexed). The paleosol chemistry is described in section 4.35. 4.3  DISCUSSION Horizon types, thicknesses, contacts, and textures in Chasm paleosols aid in interpreting the length of time between lava fl ows, soil maturity and paleo-climate. 4.3.1 Duration of hiatuses between lava fl ow fi elds The nature and the thicknesses of each horizon indicate the duration of time between lavas, however warmer climates accumulate soil faster and post-burial compaction with the overlying lava affects preserved thickness. The Chasm paleosols did not had adequate time to develop the soil before burial from the next lava fl ow. Age dates for lavas enclosing two paleosols provide minimum and maximum estimates for paleosol development for uppermost and lowest paleosols in the East Log section (Fig. 4.12). Development of the lowest exposed paleosol, occurred before the overlying lava (Sample: RE-CH06-12) dated at 9.65 ± 0.40 Ma and after an underlying lava (Sample RE-CH08-1), dated at 10.00 ± 0.48 Ma. The duration ranges between 0.35 m.y. and, 1.23 m.y. (Fig. 4.12). 80 Duration of Hiatuses between Lava Flow Fields Total Time for each soil to form 8.6 8.8 9 9.2 9.4 9.6 9.8 10 10.2 10.4 10.6 total time for each soil to form S tr a ti g ra p h y Total time for each soil to form 10 20 30 70 80 90 100 110 till S-69 S-70 S-71 0 m A A A A} } (in My) minimum= 0 My preferred= 0.13 My minimum= 0.35 My maximum= 1.23 My Chasm East Log L4 L5 p4 Figure 4.12: Stratigraphic  context for Ar/Ar dates for basalt fl ows (A), which bracket the uppermost and lowest paleosols from the eastern composite stratigraphic log section. Results suggest the paleosols vary in the length of time it takes for each to accumulate, as the minimum value for the lowest paleosol is indicative of a formation period twice as long (270, 000 yrs) as the uppermost paleosol (130, 000 yrs). 81 In the case of formation of paleosol 4, involve dates on the uppermost lavas in the eastern stratigraphic log. The uppermost lava (Sample: RE-CH08-4) yielded an older age of 9.44 ± 0.24 Ma than the lower lava (Sample: RE-CH06-4) dated at 9.07 ± 0.26 Ma. The dates overlap in 2σ-error. The minimum duration of hiatus between the two fl ow fi elds is 0 m.y. (since the older age is the uppermost lava) and the maximum is 0.13 m.y., deduced from the overlap of two errors on the ages, denoted with a dashed line on Figure 4.12. By age dating the bracketing fl ow fi elds for two paleosols, results suggest the paleosols vary in the length of time it takes for each to accumulate. Interpreting the minimum values of each, the stratigraphic lowest paleosol (350,000), potentially took more than twice as long to accumulate the soil opposed to p4, the uppermost paleosol (130, 000 yr or less). Our preferred duration time for the soil to form using this method is 0.13 m.y.  Because of the short time inferred, the textures present in Chasm paleosols are not mature soils and duration of emplacement of the 10 fl ow fi elds in the canyon, 1.28 ± 0.61 m.y., that for the soil development would be signifi cantly less, perhaps in the range of 500-10,000 years (pers. comm. P. Sanborn) and due to the textures present in the Chasm paleosols, which are not mature soils. Horizon contacts indicate that diffuse boundaries in the lower horizons of each of the 3 sites may be genetically related, since they are similar in composition and textural components. The term diffuse implies that the thickness of the contact is  > 15 cm (Retallack 2001). A long period of soil formation would promote horizons that are signifi cantly different from each other, whereas at Chasm (Fig. 4.5 and 4.6), the horizons within a single sampling locality are generally similar to each other (minor differences denoted by numbers 1, 2 etc). Therefore these contacts require only a relatively short length of time to develop, based on the multitude of similarities horizon to horizon. Nazko cinder cone’s 7,000 BP deposits, located west of Quesnel, B.C., have been classifi ed as Orthic Eutric Brunisols (Sanborn 2010, in prep). Surveys of three sites (BC07-09, BC07-07, BC06-01) portray similar fi eld characteristics in terms of horizon characteristics to Chasm, which indicate an immature soil. At Nazko, these sites show minor distinctions between horizons. 82 Horizon features indicate lack of preservation of structures due to post-burial breakdown, and the age of the paleosols. Blocky structure was observed at station 068, and the rest have been obliterated due to long time burial (~9 M.y.).  4.3.2 Soil maturity  Horizons indicate a lack of soil maturity, since major horizons are similar to each other, whereas a mature soil would show vastly different horizons.  The Nazko soils, a more recent basaltic soil, with a parent material produced from Nazko Cone (deposits ~ 7,000 yrs BP; Souther and Clague 1987; Sanborn 2010 in prep), show similarities to the Chasm profi les. This young basaltic soil comprises an ‘O’ horizon, followed by a ‘B’ horizon, in this case horizons ‘A’ or ‘E’ do not exist. Because these are young soils therefore it is unlikely that they would have eroded away this rapidly, therefore it is concluded these horizons never existed, and by analogy, one possibility is that a similar profi le may have existed at Chasm.  The Brunisolic environment for Chasm in the Miocene may be indicative of a forest environment, where originally the Chasm paleosols may have had an Ae horizon, which would be dark in color, rich in organic matter.  Organic matter is not preserved in the Chasm paleosols, due to the emplacement of the capping lava, which would have burnt off the ‘O’ horizon, and any debris would not be preserved for ~ 9 Ma. The organic material, in an ‘Ae’ horizon, naturally decomposes with microbial activity, and therefore would be unlikely to be preserved at Chasm. Without fossil fl ora or organic matter, it is diffi cult to reconstruct the Miocene environmental habitat at the Chasm in the absence of fossil fl ora or organic matter, therefore this is a preliminary interpretation.  Horizon contacts indicate a lack of roots or root traces, which confi rms an immature soil. One possibility of the origin of the clastic dikes, which are commonly joined to paleosol horizon boundary, could be a result of large roots (i.e., presently root casts) that had been growing into the weathered basalt. The preliminary interpretation is an immature soil, 83 however these dikes may have reused the root casts. These large cracks are suggestive of root development and have been observed in saprolites (pers. comm. P. Sanborn 2009).  The dikes range in length, preserving the depth of the trace of the root. This depth distribution is observed at Nazko (~1.5 m depth), however these roots are considered taproots with small diameters, much larger root diameters would be necessary at Chasm to create these clastic dikes (Fig. 3.1; photo c). If the annual mean temperature (MAT) were warmer in the Miocene, then root development would increase with the warmer soil temperatures. This observation supports a milder MAT for the Miocene.  4.3.3 Paleoclimate Several factors suggest paleosols in Chasm are Brunisols including absent horizons (O, A, E), and a shortened time for soil development due to the capping basaltic lava. A Brunisol is a young soil, which lacks soil horizon development and is suggestive of a forest environment for the Chasm during the Miocene. The Chasm paleosols are classifi ed as Brunisols, by the Canadian soils classifi cation scheme (Soil Classifi cation Working Group 1998). For comparative purposes, the US classifi cation scheme would yield the classifi cation of an Inceptisol. The Brunisolic soil order is further organized into the ‘4 Great Groups,’ however these categories refer to modern soils and Chasm paleosols cannot be classifi ed further, because of the post-burial alteration processes.  Horizon  t extures may be suggestive of a forest environment, further micromorphological is necessary for a complete classifi cation. The formation of Brunisolic soils can occur in an array of climates, ranging from tundra environment to a mixed forest (Soil Classifi cation Working Group, 1998). The environmental scenarios include the following: sub-boreal forest, mixed forest, shrubs, grass, heath and tundra. Preliminary paleoclimatic interpretations for the Chasm would be mixed forest or shrubs. 84 4.3.4 Comparative studies  The purpose of describing the paleo-climates deduced at other locations (i.e., Porcupine Basalts and the Columbia River Flood basalts), is to compare the MAT values from each study, where the Chasm site fi ts geographically in-between these two cases. The two MAT’s provide Miocene climate information north (Porcupine basalts; MAT 9°C; Smith 1994) and south (CRFB; MAT 12°C; Sheldon 2003) of the Chasm. Note that without organic material or fossil fl ora the goal of reconstructing a MAP (Mean Annual Precipitation) and MAT are not feasible (Sheldon 2002). There are not any organic matter nor fossil fl ora preserved at Chasm, however these case studies provide an MAT range for the Miocene Chasm climate. Porcupine Basalts, Yukon-Alaska border A comparison of paleosols of the Porcupine River (Smith et al. 1994) from northeastern Alaska to the Chasm paleosols shows the scenarios are not identical, although methodology, parent material and mapping are comparable. The Porcupine River basalts are geochronologically well constrained with Ar-Ar isotopes with ages spanning between 14.4 and 16.8 Ma (Plumley et al. 1989; Kunk et al. 1994). The site comprises approximately 25 basaltic lavas with interstratifi ed paleosols. The Porcupine River paleosols differ from the Chasm paleosols for they have components such as wood peat and organic materials. A combined interpretation, using the paleosols and the biological diversity in the sediments (i.e., palynology and fossils) is able to reconstruct the climate for the Miocene at the NE Alaska and Yukon border. Smith et al. (1994) provide the fi rst paleoclimate reconstruction for the Miocene in this region. With each mapped paleosol profi le, the horizons, fossil fl ora, palynological data and chemistry generate a pedoenvironmental interpretation such as ‘swamp forest,’ or regions that rich in elements to promote plant growth. Palynological data yields a climate with a MAT of 9°C, wet summers with milder winters (Wolfe 1978), and the cumulative paleosol results are in agreement with this climate interpretation. 85 Columbia River Flood Basalt, Oregon USA  In Oregon, Sheldon (2003) qualitatively and quantitatively delivers a paleoclimatic reconstruction of the Columbia River Flood basalt (CRFB) paleosols. Specifi cally, the Picture Gorge Subgroup is the focus of the study, which accumulated soil in the middle Miocene. The degree of chemical weathering in CRFB paleosols in the Bt (clay-rich) and Bw (Bm in Canadian soil classifi cation) horizons provides data he uses to calculate mean annual preciptation (MAP). The MAT is derived from comparative modeling with modern soils (Sheldon, 2002). These two calculations, MAP and MAT, are based on data from three samples in the Bt horizon. The Miocene climate determined was a MAP of ~ 750 mm with a MAT of 12°C, Sheldon’s results are in agreement with the fossil fl ora (Mascall fl ora). 4.3.5 Soil geochemistry  The objective in paleosol chemical analysis is two-fold, fi rst it gleans the necessary evidence to consitutue as soil formation in regards to the Chasm paleosols, and secondly, it provides evidence for more than one parent material, a non-basaltic component, which can be observed chemically by the ratios of immobile elements (Table 4.6). The Chasm paleosol data is subsequently compared to Nazko cinder cone Brunisolic soil profi le chemistry (Sanborn, 2010, in prep), which hosts weathered basalt as one of the parent materials, as is the case at Chasm. In the fi eld paleosols were tested for calcium carbonate, however concluded that the effervescent calcium carbonate on the surface of the paleosol results from the percolation of groundwater. In the chemical data, I test the hypothesis of how much organic C remains in the paleosols, as previously discussed all organic matter appears to have decomposed, however this is tested with calculating the amount of inorganic C from total C and CaCO3. The inorganic C results are equal to or greater when compared to total C, therefore the amount of C is attributable to CaCO3 accounts for all C in the sample. An additional check is observing the N% data, which is basically zero, highlighting the fact that all organic materials have N 86 Chasm Station 069 % ppm Sample No. Horizon SiO2      Al2O3      CaO MgO Na2O  K2O   Fe2O3    MnO TiO2      P2O5    Cr2O3   SrO BaO LOI Sum Rb Sr Y Zr Nb Ba RE-CH07-41 Bmb      48.1 16.6 4.45 3.74 5.52 0.79 8.29 0.12 1.06 0.15 0.02 0.03 0.05 10.3 99.22 14.7 248 16.1 159 9 495 RE-CH07-42 IIC1      45.4 14 8.02 6.12 2.83 0.4 11.4 0.14 1.57 0.3 0.04 0.05 0.02 8.55 98.84 4.6 374 22.8 114 10.3 234 RE-CH07-43 IIC2      44.9 13.3 9.5 6.13 2.57 0.23 12.85 0.15 1.74 0.46 0.05 0.05 0.01 7.59 99.53 2.6 441 21.9 108 10.9 127 RE-CH07-44 R 45.3 13.5 8.17 7.57 2.6 0.46 12.15 0.17 1.59 0.23 0.04 0.05 0.02 7.85 99.70 8.6 375 19.6 98 10.1 175 Chasm Station 070 % ppm Sample No. Horizon SiO2      Al2O3      CaO MgO Na2O  K2O   Fe2O3    MnO TiO2      P2O5    Cr2O3   SrO BaO LOI Sum Rb Sr Y Zr Nb Ba RE-CH07-49 Bmb 51.5 17.4 3.32 2.74 3.36 1.15 6.65 0.14 0.85 0.12 0.01 0.04 0.08 11.7 99.06 29.9 287 18.8 179 9.4 693 RE-CH07-50 IIC1      44.7 15.15 7.67 5.24 2.74 0.64 10.4 0.15 1.34 0.19 0.03 0.05 0.04 10.8 99.14 20.9 383 24.4 125 9.8 396 RE-CH07-51 IIC2  45.8 13.9 8.7 6.47 2.72 0.37 12.35 0.17 1.63 0.26 0.04 0.05 0.02 7.74 100.20 7 394 20.2 96 10.4 222 RE-CH07-52 IIC3    46.2 13.5 8.34 7.35 2.69 0.42 12.15 0.16 1.6 0.24 0.04 0.04 0.02 7.66 100.41 9.5 363 19.4 99 10.4 176 Chasm Station 071 % ppm Sample No. Horizon SiO2      Al2O3      CaO MgO Na2O  K2O   Fe2O3    MnO TiO2      P2O5    Cr2O3   SrO BaO LOI Sum Rb Sr Y Zr Nb Ba RE-CH07-53 Bmb    43.8 11.95 11.75 6.81 2.52 0.44 11.9 0.22 1.76 0.3 0.05 0.04 0.02 8.27 99.83 9.5 289 22.8 120 14.3 174 RE-CH07-58 IIBmb1  51.5 19.5 3.14 1.88 5.46 1.54 5.69 0.11 0.69 0.05 0.01 0.04 0.12 10.1 99.83 33.1 329 16.1 203 13.3 1055 RE-CH07-59 IIBmb2 51.1 19.15 3.17 1.52 5.42 1.52 4.8 0.12 0.61 0.04 0.01 0.04 0.12 11.75 99.37 41.4 335 18 164 12.6 1100 RE-CH07-60 IIIC 43.1 12.8 8.24 7.34 2.13 0.44 11.3 0.14 1.56 0.3 0.05 0.04 0.03 11.75 99.22 7.6 347 21.7 109 15.4 298 RE-CH07-61 R   45.1 12.95 7.17 9.1 2.57 0.76 12.05 0.16 1.66 0.31 0.05 0.04 0.02 8.06 100.00 8.8 366 18 111 16.4 213 Fe Fraction, Ratios pH and Carbon Fraction, and N total Chasm Station 069 Sample No. Fet Fed Fed / Fet SiO2 / Al2O3 CaO/ TiO2 Na2 O/ TiO2 TiO2 / Zr pH (H2O 1:1) Ct CaCO3 Inorganic C Nt RE-CH07-41 5.8 1.983 0.342 2.898 4.198 5.208 66.67 9.01 0.211 2.83 0.34 0.007 RE-CH07-42 7.97 2.683 0.3366 3.243 5.108 1.803 137.7 9.54 0.158 2.027 0.24 0.004 RE-CH07-43 8.99 2.018 0.2245 3.376 5.46 1.477 161.1 9.66 0.182 2.191 0.26 0.005 RE-CH07-44 8.5 1.652 0.194 3.356 5.138 1.635 162.2 9.8 0.103 1.721 0.21 0.002 Chasm Station 070 Sample No. Fet Fed Fed / Fet SiO2 / Al2O3 CaO/ TiO2 Na2 O/ TiO2 TiO2 / Zr pH (H2O 1:1) Ct CaCO3 Inorganic C Nt RE-CH07-49 4.65 1.486 0.3196 2.96 3.906 3.953 47.49 8.76 0.266 2.827 0.34 0.013 RE-CH07-50 7.27 2.250 0.3095 2.95 5.724 2.045 107.2 9.71 0.375 3.47 0.42 0.005 RE-CH07-51 8.64 2.389 0.2765 3.295 5.337 1.669 169.8 9.17 0.135 1.916 0.23 0.009 RE-CH07-52 8.5 1.430 0.1683 3.422 5.213 1.681 161.6 9.85 0.113 2.075 0.25 0.004 Chasm Station 071 Sample No. Fet Fed Fed / Fet SiO2 / Al2O3 CaO/ TiO2 Na2 O/ TiO2 TiO2 / Zr pH (H2O 1:1) Ct CaCO3 Inorganic C Nt RE-CH07-53 8.32 0.803 0.097 3.665 6.676 1.432 146.7 8.25 0.804 4.881 0.58 0.031 RE-CH07-58 3.98 1.092 0.274 2.641 4.551 7.913 33.99 8.64 0.152 2.468 0.29 0.006 RE-CH07-59 3.36 0.727 0.216 2.668 5.197 8.885 37.2 9.22 0.193 2.553 0.3 0.004 RE-CH07-60 7.9 1.148 0.145 3.367 5.282 1.365 143.1 9.56 0.366 2.983 0.36 0.003 RE-CH07-61 8.43 1.812 0.215 3.483 4.319 1.548 149.5 9.8 0.12 2.068 0.25 0.004 Table 4.5: Paleosol chemistry 87 in it, therefore it is the second line of evidence that no organic material has survived the ~9 m.y. burial.  Basalts typically have higher calcium content, therefore it is not surprising that the pH data is alkaline. This data does not record information about the soils prior to burial, however shows that the succession was infused with calcium carbonate percolating by means of water down the rock/soil face. The Nazko data shows a comparable pH value, however does contain organic C, highest value in the fi rst horizon (~ 50%), which comprises a typical forest fl oor such as L= fresh leaf litter, F= fermentation (moderate degree of decomposition), and H= hummus (unrecognizable organic matter) (LFH) (Sanborn 2010 in prep). To assess the degree of weathering of the Chasm paleosols, I compare the elemental chemical analyses (majors and relevant traces) to the citrate-dithinite-bicarbonate Fe data. The citrate-dithionite-bicarbonate method is specifi cally designed to extract Fe oxides, and records the total amount of Fe present in the sample. The CDB method extracts Al, Mn, and Si, however is not specifi c to any form of these elements, therefore is not discussed in this study. The Fe indicates degree of weathering and includes crystalline Fe oxides and hydroxides (hematite, goethite), non-crystalline forms of Fe such as ferrihydrite, and Fe, which is organically complexed. Goethite is most common, and commonly hematite is produced in warmer climates within soil profi les. The Fe data confi rms that the Chasm paleosols are soils. First, I observe the dithionite Fe is considerably less than the total Fe, and secondly, the Fed and Fet ratio tends to increase towards the top of the soil (1 st horizon). These results are to be expected with soils, since the most intense weathering affects the surface and subsequently diminishes with depth, which is observed in station 069 and station 070. This is the best evidence to confi rm that the Chasm paleosols are soils. The outlier station is station 071, which is the station where thin, however laterally continuous, tephra horizon is observed (RE-CH07-53). This sample must be regarded as complex, and consisting of a completely different parent material, while interpreting majors, traces and ratios. Sample RE-CH07-58 remains as representative of the fi rst ‘soil’ horizon at station 071. Using the SiO2, Al2O3, CaO and MgO major element data (Table 4.5), can grossly 88 indicate the presence of 1 or 2 parent materials. The SiO2 data yields the highest weight % in the 1st horizons (B horizons), confi rming different parent materials in the profi le. The Al2O3 data yields the highest weight % in the 1 st horizons (B horizons) and clay minerals (phyllosilicates) have a higher Al content, indicating the most intensely weathered horizon being the 1st, providing more evidence that Chasm paleosols are soils.  In the cases of major elements CaO and MgO, the 1st horizon is half as much as the underlying horizons, implying 2 different parent materials since basalt is rich in Ca and Mg content, whereas other sediments (aeolian deposits etc) are not.  The SiO2/A l2O3 ratios are comparable between Chasm’s Brunisolic paleosols and Nazko’s Brunisolic soils, but both sites exhibit a decreasing value with depth (Sanborn 2010 in prep). CaO/TiO2 and Na2O/TiO2 ratios increase with depth. Both Chasm and Nazko locales show a range in values of TiO2/Zr ratio, where Chasm’s values range between 37.2-162.2 differing from Nazko’s range of 39.1-78.9 (Sanborn 2010 in prep). These higher values indicate multiple parent materials present, whereas consistent data near 20 wt % would be typical of 1 parent material.  To summarize, the paleosols, interstratifi ed with basaltic lavas at Chasm, are soils because of their morphology and chemical composition. 4. 4  FUTURE WORK  A reconstruction of the paleoclimate using microstratigraphic relationships, and depth trends of the micromorphological features (Kemp 1999), may render substantive climate information with Chasm’s complexity of missing information such a organic material, comparative fossil fl ora, etc. Micromorphologists, such as Kemp and Zarate (2000), observe micro-laminated clay coatings, and disturbance in the coatings and are able to draw conclusions on transport, the processes used to produce the coating. Kemp et al. (2000) have developed semi-quantitative methods, such as organizing the varying abundances of micro- materials, placing them in a context of space and time (microstratigraphy) and applying a ‘depth function.’ This method in conjunction with additional fi eldwork and chemistry would 89 yield a more comprehensive data suite for making paleoclimatic interpretations.  The second goal would be to determine to what proportion the Chasm Brunisolic soil has andic properties. An Andisol is a soil classifi cation in the US soil classifi cation scheme, which is generally refers to ‘volcanic ash soil.’ Additional chemistry is necessary for an accurate classifi cation as an Andisol, which are the following: 1) ammonium oxalate- extractable Al, Fe, and Si; 2) phosphate retention; 3) bulk density; and 4) a determination of the volcanic glass content. Interpretation of laboratory work must consider the context that alteration occurs in the burial process of the paleosols, and Chasm paleosols have been buried since the Miocene. The chemical interpretation must be tailored to paleosols and comparative to other Andisols of similar age. 90 CHAPTER 5 VOLCANIC FACIES ARCHITECTURE 5.1 INTRODUCTION  Architectural Element Analysis (AEA) helps describe and interpret sequences of lavas and series of events. The facies architecture in the canyon was deduced from a combination of three approaches:1) cross-sections, which map the CGB cliff exposures using photomosaics, 2) identifi cation of the lava succession and their internal facies, and 3) mapping the spatial distribution of paleosols. The volcanic succession exposed in Chasm canyon comprises seven discrete facies and facies associations. The sequence of Chilcotin basalt lavas are numbererd sequentially from the youngest, uppermost lava (Lava 1, L1) situated in the norther region of the Chasm canyon to the oldest dissected unit (Lava 10, L10) at the base of the canyon. Well-developed paleosols are preserved between some lavas; these paleosols are mapped and correlated laterally throughout Chasm canyon up to distances of 8 km. Paleosol 1 (p1) is the youngest paleosol observed and the oldest paleosol exposed is Paleosol 10 (p10). The volcanic facies architecture of Chasm canyon is subsequently classifi ed, interpreted and compared with other relevant igneous provinces.  The concept of facies architecture and the method Architectural Element Analysis (AEA) originate in sedimentology where it is used to target exploration initiatives in sedimentary basins (i.e., coal, petroleum, placer minerals, and epigenetic ore deposits; (Miall 2000). The overall objective of AEA is to identify and describe individual facies and understand their origins. The architectural elements defi ned for Chasm incorporate two additional objectives: 1) the environment where the eruption(s) are occurring; and 2) the environment of fi nal deposition (McPhie and Allen 1992). Volcanic facies architecture has been applied to Large Igneous Provinces (LIPS) (e.g., Mangan 1986; Self et al. 1996; Self et al. 1997; Hooper 1997; Jerram et al. 1999; Jerram 2002; Jerram and Widdowson, 2004; Bondre et al. 2004; Passey & Bell 2007; Elliot and Fleming 2008;) and ancient volcanic successions (marine and subaerial) (Cas et 91 al. 1989; McPhie and Allen 1992; Paulick and McPhie 1999; Simpson and McPhie 2000; Moore at al. 2000). The volcanic architecture can provide insight on volcanic style, eruptive volume, duration, and periodicity of the succession (Jerram  2004). 5.1.1 Methodology A modifi ed version of the sedimentological AEA, developed by Miall (1985) has been utilized here to defi ne the volcanic facies architecture. The AEA method at Chasm identifi es four architectural elements as defi ned by Allen (1983) to include descriptions of: 1) the upper and lower bounding surface, 2) the geometry of the unit, 3) the scale of the unit, and 4) the internal geometry (e.g., facies) (Miall 1985; Miall 2000; Gilley 2003).  Miall (1985) specifi es the importance of the outcrop quality, noting the outcrop lateral size must be at a minimum of 30 m in order to see the geometry of the units(specifi c to sedimentology) , and there is no maximum lateral extent given, however the lateral range is typically less than 2 km. Continuous exposure is critical for this method; therefore a study area with minor structural disturbance is ideal. Chasm canyon meets the minimum criterion and represents a suitable study area for the AEA method, though Chasm’s lateral extent is considerably larger than traditionally selected sites. The modifi ed method of AEA used at Chasm is found in Appendix A. The western canyon walls were mapped using two photomosaics: i) Lookout Panorama (Fig. 5.2), and ii) Liden Panorama (Fig. 5.3). The Lookout Panorama extends along the western canyon wall from the head of the canyon, at the Chasm Provincial Park lookout site. The Liden Panorama extends from a midpoint in the western walls to a point near Liden Pond. Beyond the most southerly point in the mosaic, the valley widens and the walls curve to the SW and SE respectively out of the plane of the mosaic. For specifi c lateral extents of the mosaics, refer to Figure 5.1. The walls range in height from approximately 10 to 120 meters, and consist of subhorizontal basalt lavas that are commonly interstratifi ed by red paleosols. 92 !!!!!!!! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !!!!!!!!!!!!!!! !!!!!!!! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !!!!!!!!!!!!!!! !!!!!!!! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !!!!!!!!!!!!!!! ! ! ! ! ! ! ! !!!!!!!!!!!!!!!!! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !!!!!!!!!!!!!!!!! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! 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N . 74 73 72 71 70 69 68 67 56 66 00 0m . N . 56 76 000m .N . 75 74 73 72 71 70 69 68 5667 000m .N . 612000m. E.111009080706605000m. E. 613000m. E.12111009080705 606000m. E. 51°14' 75 26' 24' 66 CHASM PROVINCIAL PARK 51°08' 51°08' 10' 10' 51°14' 51°14' 121°30' 121°30' 25' 25' 121°23' 121°23' Eastern panoram a Lookout panoram a Liden panoram a Southern N orthern Figure 5.1: Inset Map showing the lateral extents of the cross sections modifi ed from pub- lish map (2010; Fig. 2.2). A 1: 50 000 scale map is shown. Extents are approximate. 93 Figure 5.2: Lookout Panorama, view to the west. Photomosaic illustrating the stratigraphic relationships on the western wall of the Chasm canyon, beginning at the head of the canyon near the Provincial Park Lookout. The approximate length of this section is 4.5 km. There is no vertical exaggeration. There is some exaggeration inevitably introduced in the produc- tion of the photomosaic as a consequence of the location that the panoramic photograph was made with a conventional camera. The walls range in height from approximately 40 to 120 meters and expose subhorizontal basalt lavas that are underlain by red paleosols. Lavas and paleosols vary in thickness and internal texture. The sequence dips gently to the north, where the youngest lava (Lava 1) on this canyon wall is exposed. Moving south along the canyon exposes older lavas. Circles areas are reference points between the image and the line drawing. Brown line is the top surface of the section. A, B, C, D, E on the photomo- saic correspond with A, B, C, D, E on the line-diagram. Note: Projections may or may not line up due to perspective differences in this panorama. Actual fi gure available at the UBC Library. 94 Figure 5.3: Liden Panorama, view to the southwest. Photomosaic illustrating the strati- graphic relationships on the western wall of the Chasm canyon, terminating near Liden Pond. The approximate length of this section is 3 km. This panorama has been spliced into two panoramas (southern and northern) due to perspective. The northern panorama is en- larged 66 times the size of the southern panorama, using the ‘C’ control point as reference. Letters B and C are control points across the two panoramas. Lava 2 is circled highlighting an identifi able feature in the exposed lavas. The abbreviation ‘R.C.’ indicates the southern- most exposure of the red colouration of the paleosols. There is no vertical exaggeration. There is some exaggeration inevitably introduced in the production of the photomosaic as a consequence of the location that the panoramic photograph was made with a conventional camera.  The walls range in height from approximately 40 to 120 meters and expose sub- horizontal basalt lavas that are underlain by red paleosols. The view ends at the northern end of the “west composite graphic log” (Figure 3.2). Lavas and paleosols vary in thickness and internal texture. Moving south along the canyon exposes older lavas. Circles areas are reference points between the image and the line drawing. Lava 3/4 and paleosol 4 have been correlated across an area of no exposure. The strati- graphic correlation is made on the basis of colour and texture of the paleosol horizon, the blocky to massive character of the columnar-jointed lava, and the clear association of the Lava 3/4 to paleosol 4, where there is exposure. A, B, C, D on the photomosaic correspond with A, B, C, D on the line-diagram. Actual fi gure available at the UBC Library. 95 Figure 5.4: Eastern Panorama, view to the east. Photomosaic illustrating the stratigraphic relationships on the eastern wall of the Chasm canyon. The approximate length of this section is 4 km. There is no vertical exaggeration. There is some exaggeration inevitably introduced in the production of the photomosaic as a consequence of the location that the panoramic photograph was made with a conventional camera.  The walls range in height from approximately 40 to 120 meters and expose subhorizontal basalt lavas that are under- lain by red paleosols. The view begins at the head of the canyon, which is visible from the Chasm Provincial Park lookout site, and ends at a location of the northern end of the “East composite graphic log” (Figure 3.1). Lavas and paleosols vary in thickness and internal texture. The sequence dips gently to the north, where the youngest lava (Lava 1) on this canyon wall is exposed. Moving south along the canyon exposes older lavas. Circles areas are reference points between the image and the line drawing. Brown line is the top surface of the section. A, B, C on the photomosaic correspond with A, B, C on the line-diagram. Actual fi gure available at the UBC Library. 96 The southernmost point on the Liden panorama includes part of the subaqueous succession, and overlaps with a portion of the western composite graphic log (Fig. 3.2). There is nearly continuous exposure except in the area ~ 4.5 km southward away from the head of the canyon, on the western wall. Lavas and paleosols vary in geometry, thickness and internal lobe textures. The western sequence dips gently to the north, where Lava 2 is the uppermost lava, however the azimuth. To the south, the sequence dips due to the presence of a paleodepression where Lava 1 is fi rst exposed within this depression on the western canyon walls (Figs. 5.2 and 5.3). About ~ 2.5 km to the south away from the head of the canyon, the oldest lavas occur at the base of the exposed sequence (Lava 10). The Eastern Panaorama is a photomosaic  (Fig. 5.4), which includes the stratigraphic relationships on the eastern wall of the Chasm canyon.  The walls range in height from approximately 40 to 120 meters and are underlain by intercalated subhorizontal basalt lavas and red paleosols. The mosaic comprises a 4 km extent of the canyon (Fig. 5.4) starting at the head of the canyon, visible from the Chasm Provincial Park lookout site, to the location of the northern end of the composite graphic log (Fig. 3.3), the extent is shown on Figure 5.4. The lavas and paleosols are continuously exposed and vary in thickness, geometry and internal texture within the lobes (see section 5.2). The sequence dips gently to the north, where the uppermost lava (Lava 1) occurs. Lavas are seen farther south within the canyon walls and at the ~2.5 km point in the mosaic the oldest lava (Lava 10) is observed in the sequence. The generalized stratigraphy at Chasm is summarized in Figure 5.5. Following the basalt terminology of Self et al. (1997). a lava fl ow is the product of a single outpouring of lava, and comprises many fl ow lobes. A fl ow lobe is one succinct package of lava, which is distinguished by a chilled margin around the outer rim of the lobe. A sheet lobe shows the complexity involved in discerning the fl ow lobe and the lava fl ow; it is observed as a sheet-like or tabular single lobe, as no chilled margins or smaller lobes are visible. A compound lobe is the combination of two or more fl ow lobes, which 97 BNE L1 L2 L3 L4 L5 L6 L7 L8 L9 L10 TABULAR-CLASSIC TABULAR-CLASSIC TABULAR-CLASSIC COMPOUND-BRAIDED TRANSITIONAL MIXED TRANSITIONAL MIXED FORESET-BEDDED COMPOUND-BRAIDED TRANSITIONAL MIXED TRANSITIONAL MIXED COMPOUND-BRAIDED Figure 5.5: Generalized schematic Chasm canyon stratigraphic log illustrating volcanic fa- cies architecture. Four architectural elements are represented: 1) Tabular-classic, 2) Com- pound-braided, 3) Foreset-bedded, and 4) Transitional-mixed. The transitional-mixed type is the dominant volcanic facies architecture at Chasm. ‘BNE’ refers to ‘base not exposed’. 98 A C D B Figure 5.6: Field photographs illustrating volcanic facies architecture. A) Tabular-classic (L1, L2, L3). Trees for scale range from 3-6 m, B) Foreset-bedded. Hammer for scale is 30 cm, C) Compound-braided (L9). Trees for scale range from 3-6 m. Average lobe is 3 m in height, and D) Transitional-mixed (L5). Trees for scale range from 3-6 m. 99 NWSW Figure 5.7: A photomosaic of a section of the western wall to Chasm canyon illustrating the irregular, non-linear geometry of the canyon wall; locally the wall forms concave out- ward embayments that result from a post-glacial outburst fl ooding event. The glacial deluge exhumed the canyon in likely a matter of hours (pers. comm. J.K. Russell, 2009). This is a mosaic comprised of 4 photographs, which is part of the larger profi le of Fig. 5.2 100 can be any shape or size (Walker 1972). A fl ow fi eld is one or more lavas resulting from a single eruption or pulse of volcanism (Pinkerton and Sparks 1976; Kilburn and Lopes 1991; Mattox et al. 1993). The lavas provide the geometry of the fl ow fi elds, distinctively marked by the presence of the red paleosols (Figs. 5.1, 5.2 and 5.3). Details such as lobe boundaries, paleosols, jointing patterns, evidence of structural disturbance (i.e., landslides) are obvious in the lateral profi les. The photomosaics provide a unique opportunity to map the lateral variability of the paleosols over the length of the canyon. The total number of fl ow fi elds in the canyon are marked by the paleosols, because they represent distinct hiatuses in the volcanism. Without the paleosols, identifi cation of individual lava fl ow fi elds would be less precise due to the diffi culty in delineating the lobe boundaries in the photomosaics (Fig. 5.6). Typically paleosols are assessed laterally within a 1-2 m extent, therefore a 5 to 8 km mapped cross section is unusual, highlighting ample lateral variability (Fig. 5.7). At Chasm, the paleosols have been classifi ed as truncated paleosols, merged paleosols (this study), or a combination of both. Truncated paleosols terminate or are discontinuous in the lateral profi le due to erosion or as a result of the lava morphology (i.e., abut against a fl ow lobe boundary). Merged paleosols refers to locales where the boundary between upper and lower  paleosols cannot be distinguished and the soil profi les are merged together (Schaetzl and Anderson 2005). Symbols for these elements are labeled on the mosaics. Due to the complex lateral behaviour of the paleosols (Fig. 5.7), a descriptive model was established to ensure consistency in the mapping and accurate classifi cation of lavas and paleosols. The model is straightforward, using the geologic principle of superposition, and is abbreviated in the following list: 101 Descriptive model for lateral mapping of paleosols 1) The modern soil horizon is p0, and the descending sequence continues as paleosols (p1, p2, p3…pn) 2) A paleosol, higher in the stratigraphic profi le, must be younger than a lower stratigraphic paleosol. 3) Identify continuous, truncated paleosols vs. merged paleosols. 4) In the circumstance of complex paleosols (Fig. 5.6), note the areas where paleosols merge (i.e., merged) and consider the upper bounding surface younger, with the lower bounding surface as an older paleosol.  Refer to Figure 5.6 (section B) for one explanation of how these vertical paleosols could have formed. 5) Discontinuous paleosols are treated as follows: they are always overlain by younger lava and underlain by older lava. This applies even where the paleosol has only a few meters of strike length  and cannot be laterally connected with an adjacent paleosol (Figs. 5.8 and 5.9). 5.1.2 Volcanic facies architecture Facies architecture is reliant on the geometry and lateral variability of the lavas. Multiple facies can be observed in one architectural element. Each architectural element is coded (i.e., TC= tabular-classic) after Jerram (2002) to provide a volcanological terminology used specifi cally in volcanic facies architecture (also referred to as ‘stacking patterns’) to specifi cally target the processes pronounced at the study area. A number of researchers, working on igneous provinces or continental fl ood basalts, have used these types defi ned by Jerram (2002) (Passey and Bell 2007; Elliot and Fleming 2008). Modifi cations to the architectural-types have been applied, specifi cally thickness. The following descriptions are tailored to be Chasm-specifi c. The facies architecture is shown schematically in Figure 5.7, and in the mosaic fi gures (5.2, 5.3, and 5.4). The architectural elements described by Jerram (2002) are listed below: 102    1) Truncated paleosols (     ) = paleosols that are terminated or discontinuous.    2) Merged paleosols (     ) = a blurred boundary. Younger and older periods of the soil  profile are merged together.  Figure 5.8: Detailed view of interpreted line-diagram of a section of the eastern wall illus- trating the stratigraphic complexity of the paleosols.  Truncated and merged paleosols are illustrated in the fi gure. Scale is approximately 10 m. 103 L5L4 L4 L5 Figure 5.9: Paleosol truncates against local paleo-topographic high formed by pre-existing lobe of lava. Scale is approximately 5 m for this schematic diagram. 104 Facies Architecture TC= Tabular-classic facies architecture: (i.e. thick fl ows (~50 m thick) with massive core and vesicular tops and bases. Columnar-joints ranging from poorly developed to well-developed. CB= Compound-braided facies architecture: thin anastomizing pahoehoe lava fl ows, with the maximum thickness of each lobe at 3 m. Subsequent lavas can in-fi ll the ‘accomodation space’ located in between the fl ow lobes (eg., crevices). TR= Transitional mixed facies architecture (TC + CB):  tabular-clasic and compound-braided architecture are observed in the same fl ow fi eld. The tabular- classic sheet lobes may fi ll-in depressions resulting from CB-type, creating a relatively planar surface  (Jerram 2002). This is equivalent to the element ‘Combination’ of Jerram (2002) and ‘mixed sheet fl ows and compound fl ows’ (Passey and Bell 2007). FB= Foreset-bedded facies architecture: This represents lava fl owing into lakes or seawater. A delta accumulates at the margin of a lake and can be observed as building bars across the embayment (Reading and Collinson 1996). In volcanology, these bars are the foreset-beds. The foreset-beds are created when lava fl ows down steep, high angled slopes, which produce a pahoehoe basaltic lava-fed delta (Skilling 2002). FB is equivalent to Jerram’s (2002) ‘Dipping hyaloclastite.’ The foresets ranging from a few to tens of thousands of meters thick in fl ood basalts. 5.1.3 Stratigraphic Analysis of Chasm Lavas Ten discrete paleosols and lava fl ow fi elds were identifi ed in the canyon, correlated in the western and eastern walls, and the laterally variability of each fl ow fi eld determined. Field descriptions and hand samples were cross-correlated in the canyon for Lava 1 and Lava 2, older lavas proved more diffi cult with this method, and reliance on lobe geometry and thickness of the lava were used for correlation. An objective in tracing the lateral extent of the profi les was to correlate them with the eastern and western composite log extents, 105 in which the small-scale physical volcanological features within each fl ow fi eld and facies classifi cation were determined. West Mosaic Liden overlaps with the western composite log, and East Mosaic overlaps with the eastern composite log. A composite log resulted, which illustrates the generalized ‘Chasm stratigraphy’ for the canyon lava succession (Fig. 5.5). The east and west canyon walls mirror each other for approximately 2 km from the apex except for Lava 1 which is not present of the western wall. The thickness of the lavas changes laterally, but the internal geometry (e.g., facies)  is consistent. Generally, the colour and degree of weathering is identical for both sides of the canyon. Where accessible, the walls were checked and correlated across the canyon with hand samples. The internal geometry (facies) have been determined for each lava fl ow fi eld at Chasm (Fig. 5.5). Uppermost lavas, L1, L2, and L3, are classifi ed as ‘aphyric columnar- jointed facies’ (acB). L4 is ‘vesicular basaltic pahoehoe lobe facies’ (vlB), whereas L5 and L6 are a combination of acB and vlB facies. L7 and L10 are characterized as vlB facies, where an increase in fl ow lobe size is observed. Lastly, L8 and L9 are recognized as the combination of acB and vlB facies, which is the most prevalent fl ow fi eld facies at Chasm. Chasm canyon descriptions: 4 architectural elements  The volcanic facies architecture is summarized in the schematic composite section (Fig. 5.5) and the four architectural elements are individually illustrated in Figure 5.6. Tabular-classic facies architecture This element is recognized at Chasm by a fl at upper bounding surface, a lack of recognizable lobes, but not thickness. It is stratigraphically uppermost in the top three fl ow fi elds in the canyon. The thickness of these TC-type fl ow fi elds ranges between ~2 to 10 meters. Paleosols are observed between fl ow fi elds. The ‘aphyric columnar-jointed’ facies (acB) comprises this architectural element. The columnar-joints are moderate to well- developed columns, and colouration of the two fl ow fi elds that makes up this type, appear 106 to be less oxidized ranging from dark grey to dark brown. These fl ow fi elds have a massive, non-vesicular interiors, with highly vesiculated lava tops and bases. Vesicle sheets and chimneys (cylinders) are visible in the massive interiors of these sheet-like fl ow fi elds. Compound-braided facies architecture  The CB element is characterized by overlapping pahoehoe fl ow lobes. The CB- type is medial and basal in the three fl ow fi elds in the Chasm canyon stratigraphy. The geometry is lobate, and the thickness of the fl ow lobes ranges from 10 cm to 2 m. The fl ow fi eld thickness varies signifi cantly ~8-15 m, and represents the thickest architectural type in the canyon. The quantity and size of fl ow lobes in any fl ow fi eld varies. Paleosols are interstratifi ed between the fl ow fi elds. The ‘vesicular basaltic pahoehoe lobe’ (vlB) facies is the constituent of this architectural-type. There is an absence of columnar-joints. Flow lobes are 2-40% vesicular and pipe vesicles or pipe amygdales are observed along the lobe boundaries, classifying these features as p-type pahoehoe (Self et al. 1998) at Chasm. Transitional mixed facies architecture  This TR-type, a mix of non-lobate TC-type with the CB-type, is the dominant architectural element of the Chasm canyon, where multiple fl ow lobes are observed in a single fl ow fi eld. There is not a consistent observed trend of one type morphologically changing into the other, therefore the architectural element is defi ned as a mixed sequence, whereby the oscillation between the elements may occur multiple times over the length of the canyon. One architectural element can consist of 1 or multiple facies, and in this case both acB and vlB are observed in the TR-type. Stratigraphically, the TR-type occurs in four of the middle fl ow fi elds in the canyon walls. Commonly, paleosols bracket the fl ow fi elds. The thickness range for this architectural-type is ~0.5 m to 8 m. Foreset-bedded facies architecture  FB-type architecture is observed in the southwest section of the western canyon wall. Four discrete subaqueous units are exposed, each exhibiting classic foreset-bedding. Upper and lower bounding surfaces of these units are sharp with the interstratifi ed subaerial 107 lavas (Fig. 3.2). The following facies are observed: ‘intact-pillow basalt’ (ipB), ‘pillow- fragment breccia’ (pfB), ‘hyaloclastite’ (hB), and ‘lacustrine sandstone’ (lsS). The FB-type element occurs in the middle of the succession, however it is restricted to the southern most western wall. The thickness of the forest-bedded units varies throughout section, from ~8 to 22 m. The subaqueous to subaerial succession is classifi ed as a Gilbert-type basaltic lava- fed deltaic sequence (Skilling 2002) is summarized below and illustrated in Figures 5.8 and 5.9. Delta set-1 is the oldest sequence exposed. Delta set-1 represents the basal delta unit observed at Chasm and is 12 m thick. The unit comprises foreset-beds that dip about 40° to the south (estimate from two planar pillow measurements). The dominant facies is intact pillow basalt facies (ipB), with minor pillow- fragment breccia (pfB) facies. A pillow pile is located at the base of this unit. The foresets are abruptly truncated at the base of approximately 12 meters of overlying subhorizontal coherent basalt (vlB and acB facies), which constitutes the topset. The bottomset is not exposed in the section. This Delta-set 1 is interpreted to refl ect lava fl owing south into the initial standing body of water. Delta set-2a has a thickness of 7.5 m. Five planar pillow measurements (volcanic layering) record an average dip of 34° to the south. The foresets are dipping approximately to the southwest, and a pillow pile is observed at the base of the unit. The dominant facies represented is intact pillow basalt facies (ipB), with minor pillow-fragment breccia facies (pfB). The average size of the intact pillows in this section is 0.67 m.  The basal contact of the topset, approximately 10 m of basalt (vlB, acB, vlB facies sequence), abruptly truncates the Delta set-2a. 108 ~ 10 meters ~  3  m transition zone SUB-AQUEOUS SUB-AERIAL facies: intact pillow basalt (ipB)            pillow fragment breccia (pfB) facies: paleosol (P) Lava 4 Paleosol 4 for ese t-b ed de d S N Figure 5.10: Schematic diagram illustrating the transition from the intact pillow basalt (ipB) and pillow fragment breccia (pfB) facies transitioning into the paleosol (P) facies. Note the paleosol facies consists of vesicular basaltic core stones. The interpretation is that ipB and pfB were emplaced into a temporary lake, deep enough to accommodate foreset beds (> 10 m minimum depth, Pedersen 1998). 109 SCHEMATIC CROSS-SECTION OF WESTERN COMPOSITE LOG AREA KEY sub-aerial lava sub-aqeuous lava intermittent drainage (stream/creek) paleosol el ev at io n ~1020m ~900m el ev at io n ~1020m ~900m lateral distance ~ 1.5 km A) B)  CROSS-SECTIONAL VIEW  ILLUSTRATING THE CHASM LAKE sandstone lens present day vegetation (bunch grass) Rise 1 Rise 4 Rise 3 Rise 2 lateral distance ~ 1.5 km Lake water rises: STN 10 STN 26 STN 27 STN 29 STN 34 STN 35 STN 36 STN 37 Paleosol 4 Lava 4 STN 10 STN 34 STN 36 STN 37  8 0 m Figure 5.11: Schematic representation of stratigraphic relationships in a portion of western canyon wall. A) Stratigraphic relationships in transition zone from subaerial (right) to sub- aqueous (left) facies. Station numbers correspond to numbers on western composite graphic log (Figure 3.2). B) Interpretation cross-section of exposed stratigraphic units illustrating the extent of a temporary lake formed by rapid emplacement of Chasm lavas. The maxi- mum water depth is inferred to be ~80m, based on the height of the foreset beds in pillow breccia deposits (Pedersen, 1998). 110 Delta set-2b contains the thickest subaqueous sequence observed at Chasm at~25 m thick. Delta set-2a and 2b are part of the same sequence, but are separate by an interval of no exposure between them (Fig. 5.10). The foreset beds are dipping approximately 34° to the southwest. Intact pillows basalt (ipB) facies is observed and clusters of intact pillows are mapped in the set, less dominant pillow-fragment breccia (pfB) represents the remainder of inter-pillow space. Both the largest pillows and the hyaloclastite facies (hB) are confi ned to the base of the section, and the hyaloclastite is a rare occurrence at Chasm. The overlying subaerial lava sharply truncates the Delta set-2b, and is approximately 9 m thick.  Delta set- 2ab is interpreted to represent the second water rise of the temporary Chasm Lake. Delta set-3 is 16 m thick with foreset-beds dipping approximately 36° to the southwest. The base of the unit is a localized lens of coarse-grained quartz-sandstone overlain by packed pillow lava, deposited in a pillow pile. The overlying subaerial lava is 8m thick and truncates the set, visible as a sharp, planar contact. Along its northern extent, the Delta set-3 includes a record of the subaqueous to subaerial transition.  An important shift is observed as Delta set-3 transitions laterally into Paleosol 4 (Fig. 5.8). This is interpreted to represent the shoreline of the temporary Chasm Lake, where the overlying Lava 4 supplied the lava lobes, which subsequently fl owed down and south westwards, driven by gravity, illustrated by the driving ‘nose’ and ‘tail’ of the lobe (Jones & Nelson, 1970).  Delta set- 3 is interpreted as the record of the third water rise of the Chasm Lake. Delta set-4 is the fi nal set of the delta progradation. This set is truncated by the uppermost subaerial lava unit (~5 m? thick). Delta set 4 is crudely estimated to range between 5 and 8 m. This set is inaccessible, due to exposure height in the cliff, and no pillow structure data were obtained. Through lateral profi le mapping, Delta set-4 is interpreted as the fourth water rise of the temporary lake, and suggests correlation with Paleosol 3, a post- subaqueous to subaerial transition (Fig. 5.2). 111  5.2 VOLCANIC INTERPRETATION  The Chasm canyon sequence provides the record of: 1) the architecture of volcanic facies and facies associations, 2) a mappable transition from subaqueous interstratifi ed coherent and volcaniclastic deposits to subaerial lavas and paleosols, 3) the variation visible in the laterally-continuous paleosols and the implied paleotopograhic landscape, and 4) the directions of transport and deposition. 5.2.1 Subaqueous to subaerial succession  There is an important transition within the Chasm study area, between subaqueously deposited clastic rocks and subaerially emplaced lava fl ows. On the basis of facies associations, the hypothesis is that the source vent(s) was subaerial and that the subaqueous deposits formed when subaerial lava fl owed into a standing body of water. Temporary lakes, affi liated with basaltic systems, are not an uncommon occurrence such as the Laki basaltic deposits in Iceland, which are very similar to the Chasm sequence (pers. comm. T. Thordarson 2007), and these types of deposits were fi rst described in Antarctica by Jones and Nelson (1970), with subsequent studies in Greenland (Pedersen 1973; Clarke and Pedersen 1976; and Pedersen et al. 1998) and further Antarctic reviews by Porebski and Gradzinski (1990). Englacial and subglacial basaltic pahoehoe lava-fed deltas, host similar products to Chasm, and are described by Smellie (2001, 2005) and Skilling (2002). Upon closer examination of the subaqueous – subaerial succession (Figs. 3.2, 5.8 and 5.9), the interstratifi ed subaerial lava fl ows, not sills, due to fi eld observed textures of pahoehoe ropes and wrinkles, and an absence of black, glassy chilled margins. Using the schematic cross-section of these units as a reference (Fig. 5.9), the basal exposure is subaqueous, indicating that the body of water existed prior to the emplacement of the oldest exposed lava in the sequence. It is possible that earlier lavas dammed a stream (Jones and Nelson 1970), which created the temporary ‘Chasm Lake,’ however, neither older coherent lava fl ows nor the basal contact with the pre-volcanic landscape are exposed. Therefore 112 the formation of ‘Chasm Lake’ may or may not be the result of the CGB volcanism in the Neogene; lakes do occur in volcanic environments without direct association to a volcanic process (White and Riggs, 2001). Field observations and the cross-sectional view (Fig. 5.9) support the hypothesis of Chasm Lake originating prior to volcanism in a paleodepression. Chasm Lake is interpreted as terrestrial in origin based upon the lacustrine lava- fed delta sequence, and siliciclastic deposits, and defi ned as the lsS facies (described in Chapter 3). No ripples, laminations or any other sedimentary structures are observed in this localized quartz sandstone lens. Therefore, the present interpretation for the coarse grained deposit is a channelized fl ow in the lake or the shoreline of the lake. With this coarse- grained steep delta, the shoreline would have little sediment transport, and ripples or gravel lags can be a by-product (Orton and Reading, 1993); however, these are not observed at Chasm, perhaps due to cliff inaccessibility for sampling and describing the width of the quartz-sandstone lens.  Grains are subangular to subrounded, indicating some transport, however the unit is massive, therefore could have been transported all at once in a fl ooding event. Lakes are affi liated with a low-energy environment. Peperite was not observed at the contact with the quartz-sandstone lens. The upper and lower contacts of this material were not accessible to retrieve any further information. The Chasm deltaic sequence is analogous to the sedimentary coarse-grained Gilbert- type deltas. A Gilbert-type delta is defi ned as a three-part stacked sequence including a topset, dipping foreset, and bottomset (Postma 1990; van der Straaten 1990). The sequence may or may not comprise a topset. The term ‘topset’ may be interchangeable with ‘bottomset’ of the next deltaic sequence pending the sequence continues.  Each stacked sequence is a ‘set’, for example ‘delta set-1…delta set-n,’ according to the protocol outlined in van der Straaten (1990).  113 A basaltic lava-fed deltaic sequence must incorporate the components listed below: 1) A basal unit comprised of course-grained breccia, which is foreset-bedded typically at 30,° however can exhibit dips greater than 40°. 2) Basaltic lava caps the clastic sequence; the contact between the units is sharp and abrupt and defi ned as the passage zone (Jones and Nelson 1970; Skilling 2002). These lavas are often referred to as ‘drowned lavas’ (Pedersen 1998). The top surfaces of the coherent interstratifi ed lavas show sharp contacts, which are depositional features.  The height of the foresets relative to the basement rocks permit an estimate of the total water depth; an 80 m accumulation described in the Chasm section. For the formation of foresets to occur, there is a required water depth of ~10 m (Skilling 2002). In circumstances where the water depth is shallower, a broad inclined delta front is deposited caused by the underlying friction of the basal sediment, which produces a gently dipping slope, opposed to the steeply dipping foresets, and is defi ned as a Hjulström-type delta (Skilling 2002). There are no known basaltic lava-fed Hjulström-type deltas (Skilling 2002).  The geometry of Chasm Lake cannot be determined nor a plan-view map due to an absence of bounding points on the opposing canyon wall. Paleosols are not part of the delta sequence, they are part of the laterally equivalent subaerial succession. The transition, from foreset-bedded pillow-breccia to the subaerial lava (i.e. paleosol), is illustrated in Figure 5.8. Heading northwest up-section, the canyon walls comprise exclusively subaerial lava fl ow fi elds (vlB and acB facies) (Fig 5.3). 5.2.2 Lateral mapping of the paleosols  A key relationship is observed between the paleosols and the underlying lava fl ow fi eld morphology (i.e., architecture), whereby there is a direct correlation between the thickness of the paleosol and the underlying lava fl ow fi eld architectural type (Fig. 5.10). Tabular-classic facies architecture produces an upper surface, which is sheet-like 114 Lava 1 p1 p8 crevice L3 L4 architecture tabular-classic tabular-classic tabular-classic compound-braided p1 p2 p3 p4 paleosol N S Figure 5.12: A fi eld photograph and interpreted line diagram showing relationship between paleosol thickness and lava architecture. P3 paleosol is particularly thick and this is a refl ec- tion of the nature of the surface of the underlying lava (L4). Lava 4 is Transitional-mixed architecture, opposed to the tabular-classic type of L1, L2, and L3, whereby the lobate geometry promotes crevices, which subsequently stimulates soil development. The crev- ice highlighted in photograph results from intersection of two pahoehoe fl ow lobes. This crevice contains the thickest paleosol in the Chasm sequence. This photo is a section of the Eastern panorama (Figure 5.4). The lavas are approximately 45 m thick. 115 and homogeneous. The weathering of the basalt is fairly uniform over the surface. At Chasm, the paleosols overlying a TC-type architectural component, shows an evenly distributed, relatively thinner paleosol (~0.3 m to 0.5 thickness) (Figs. 5.2, 5.3 and 5.4) due to a homogenous surface for soil development.  The CB-type and TR-type architectural elements have a heterogeneous, irregular upper surfaces and abundant crevices (not cracks), which allow for an increase in soil development and vegetation situated in these paleotopographic depressions. The CB and TR-types display a paleosol thickness ranging from approximately 0.5 to 2 m (Fig. 5.10). Pahoehoe lava fl ow surfaces have been known to yield more vegetation, compared to a’a fl ow surfaces (Vaughan and McDaniel 2009). The crevices in between the pahoehoe lobes create very favourable environment for soil development, acting like a catchment system where tephra, other aeolian deposits and water accumulate in the crevice. There are no a’a fl ow fi elds observed at Chasm. Cracks, not crevices, are prominent in a’a fl ows, whereby the water is not retained, but instead percolates through the rock sequence, and soil development is hindered and delayed (Vaughan and McDaniel 2009). The Chasm paleosols are tephra-rich paleosols, where the tephra acted as a catalyst promoting soil development. The tephra is inferred to be distal from its source, supplied from felsic volcanism, composed of felsic glasses and hydrous micro-phenocrysts, opposed to a product CGB Chasm’s eruptive centre(s). The source of the felsic volcanism is unknown. Distal tephra is more fi ne-grained and retains water, like silt, which aids the weathering and erosion of the underlying basalt and supports soil development and plant growth (Ugolini and Dahlgren 2002). While plants and small shrubs localize in the crevices, litter is collected beneath the vegetation, stimulating more plant growth, and larger shrubbery and trees. Proximal tephra may not promote as much soil development as distal tephra due to increased porosity, therefore limiting water retention (pers. comm. P. Sanborn 2010). The tephra contributes to recognizing the lateral continuity of the lavas independent of the architectural-type of the underlying lava fl ow fi eld. Truncated, welded, and other 116 paleosol complexities are observed, however lateral profi le mapping of the paleosols extends over distances of 5 to 8 km (east and western walls, respectively) in the canyon providing precise correlations within the main composite graphic logs (Fig 5.7 and 5.10). Each of the paleosols represents a preservation of a paleotopographic surface. The uppermost topographic surface (depicted with a brown line; Figs. 5.1-5.3), is underneath the current vegetation (P0). This surface is p0, which is the modern soil surface and modern topographic profi le. 5.2.3 Locating eruptive centre(s)  Source vents for the lavas at Chasm Provincial Park have not been identifi ed. Infl ated pahoehoe lavas are thought to be capable of fl owing for tens of kilometers during emplacement, and it is possible that the source vents were a considerable distance away (Self et al. 1998). The absence of proximal features such as spatter deposits (i.e., formed from spatter cones on the boundary of the fi ssure (Greeley 1977)), volcanic bombs (i.e., ejecta from a shield volcano (Greeley 1977)), or volcanic edifi ces is consistent with the Chasm fl ows being distal from their sources. A series of enigmatic gabbroic plugs have been identifi ed approximately 30 km to the north as possible lava sources (e.g. Mount Begbie; Farquharson and Stipp 1969; Bevier 1983; Matthews 1989). The paleosols imply a periodic emplacement of the Chasm lavas (Andrews and Russell 2008). The lavas are suggestive of low mean effusion rates (Andrews and Russell 2008). This geochronological study tested this hypothesis, yielding a result of a complex chrono-stratigraphy, as discussed in Chapter 3. A slight younging trend in age dates occurs to the north on Highway 99, towards Mount Begbie, however a minima age of the uppermost lava in the canyon (L1: 08REF003A01; run B) is 7.44 Ma, and the Mount Begbie sample (JD-MB07-01; run B) results in a minima of 7.77 Ma; the geochronological data does not provide a clear correlation or trace to specifi c eruptive centre(s).  The lateral mapping of the lavas, which delineate the lava sequence at Chasm, 117 N Bon apa rte R iver Ch as m Cr ee k CHASM CANYON Basaltic “Plains-Style” Emplacement Scenario N Bon apa rte R iver Ch as m Cr ee k CHASM CANYON Basaltic “Plains-Style” Emplacement Scenario A) B) pre-Chasm river shield volcano fissure vent flow fields Figure 5.13: A) Emplacement model for Chasm Canyon showing a modern trace of the Chasm canyon and associated drainages, denoted by gray dotted lines. This fi gure illus- trates multiple source vents including coalescing shield volcanoes and fl ank fi ssures. A pre- Chasm river was dammed by a fl ow fi eld, creating the temporary Chasm Lake. Note differ- ent fl ow fi elds, representing distinct volcanic pulses, yielding a complex geochronological history. The model is schematic and the entire lava succession is not represented. B) Chasm canyon exhumed by a glacial deluge, with the CGB lavas outskirting the canyon walls. The modern trace of the canyon and present-day Chasm Creek and Bonaparte River are noted in bold. Blue box shows the approximate location of facies association, Mcb2, which repre- sents interstratifi ed subaqueous and subaerial facies. 118 provide further insight on direction of fl ow, and eruptive centre(s) (Fig. 5.11). There is a general northerly fl ow direction, with a localized northwesterly fl ow direction where the paleo-depression is located on the western wall, approximately 4.5 km south from the head of the canyon. The Chasm dominant architectural-type is ‘Transitional mixed’ facies architecture, which favors the Plains-style of volcanism (Greeley 1977), therefore one eruptive centre is not the likely source for the entire sequence. The duration of volcanism is calculated as 1.28 ± 0.61 Ma, and architectural assessment is indicative of shield volcano and small fi ssure, point source, eruptions with a northerly transport direction.  This is discussed further in the next section. 5.2.4 Emplacement model at Chasm canyon  The emplacement of the CGB lavas within Chasm Provincial Park can be explained in this descriptive volcanological model, which encompasses geological mapping, facies associations, geochronology, and architectural element analysis (AEA). Facies architecture, when combined with vertical graphic logs, provides insight on the lateral variability of the facies and paleosols representing the complex age relationships between fl ow fi elds. These changes and complex age relationships have been recorded in other volcanic and sedimentary regimes, and are a factor in assessing the three- dimensional emplacement history (Cas and Wright 1990; Miall 2000).  Chasm canyon extends approximately 8 km to the south and ranging between 500-3000m wide, and 300 m deep. The dominant facies architecture is ‘Transitional mixed’ (TR), characterized by the changeover between the TC and CB architectural-types (or vice a versa), which suggests basaltic ‘plains-type’ volcanism (Greeley 1976, 1977, 1982) also observed at the Snake River Plain, Idaho, and in Iceland (Rossi and Gudmundsson, 1996).  Bevier (1982) classifi ed the regional CGB as a product of plains-style volcanism, however, detailed stratigraphy and geological mapping were not a part of her study. Recent detailed physical volcanology at Chasm, which dissects and interprets the architectural complexity, supports 11 9Relevant Volcanic Provinces Summary of Characteristics: Chilcotin Group Basalt Type: Medium-sized igneous province (CGB) Aerial extent: 17,000km2 (total CGB) Architecture: Chasm canyon = 1) Tabular-Classic (~2-10m thick), 2) Compound-braided (~10cm-2m), 3) Transitional-mixed (~0.5-8m thick), 4) Foreset-bedded (~ 10m avg.) Paleosols often observed between lava flow fields. Age: 38.3-1Ma (Chasm: 9Ma) Columbia River Basalt Type: Continental flood basalt (CRBG) (CRFB) Aerial extent: 160,000km2 Architecture: Compound pahoehoe lavas inflated by SWELL hypothesis and dominantly fissure-fed. Sheet lobes range from 20-50m thick. Paleosols often observed between flow fields observed. Age: 16Ma Faroe Islands Basalt Group Type: Continental flood basalt (North Atlantic Igneous Province; NAIP) (FIBG) Aerial extent: 1,300,000km2 Total stratigraphic thickness: ~ 6.6km (7 formations: Faroe Islands Basalt Group; FIBG) Architecture: 1) Tabular-Classic for the Beinisvør  Fm. (~300m thick), 2) Compound-braided for the Malinstindur Fm. (~30m thick), and 3) A ‘mixture of simple and compound flows’ for the Enni Fm. (~70m thick). Paleosols often observed between flow fields. Age: 62-54Ma Snake River Plain Type: “Plains” Volcanism (intermediary scale between shield volcano output and flood basalts (SRP) Aeiral extent: 49, 200km2 Total stratigraphic thickness: ranging between 300-1500m Architecture: Mixture of sheet lobes and compound flows resulting from coalescing shield volcanoes and flank fissure systems. Lava thickness ranges from 3-18m. Shield height ranges from 16-30km. Paleosols often observed between flow fields. Age: 17-6Ma Data Sourced from:  Dohaney, 2009; Farrell et al., 2007; Self et al., 1996; Passey & Bell, 2007; Greeley, 1977; Hooper, 2000 ; White,2006 Table 5.1: Architectural-type Comparison to relevant volcanic provinces 120 the previous classifi cation. Refer to Table 5.1, a table of comparative provinces. Continental fl ood basalts differ from the Chasm area in that the TC- type is generally signifi cantly thicker than the CB-type. Greeley (1976) defi ned the basaltic plains-style volcanism as a combination of coalescing broad shield volcanoes and smaller fi ssures with intermediary scale lava fl ow thicknesses between a fl ood basalt and hawaiian-type eruption (i.e., ~ 10 m/ fl ow fi eld). The coalescing of the shield volcanoes, often termed ‘low shields,’ creates a plateau landscape (Greeley, 1976, 1977). At Chasm, the youngest lavas are located on the eastern canyon wall situated adjacent to the apex of the canyon, however are immediately absent on the western walls mirroring the east wall exposure. Lateral cross-sectional mapping (AEA) provides an explanation, whereby identifying a large paleodepression (~500 m)  The paleodepression heads south along the western canyon wall (Figs. 5.2 and 5.3). The western wall exposure of the youngest lavas suggests an onlapping of the lavas at this topographic low-point. In addition to AEA, fi eld descriptions and samples were used to confi rm these youngest fl ows. Pahoehoe basaltic fl ows succumb to barriers, with heights as little as 30 cm, can redirect the fl ow and continue, gravity-controlled, towards the paleotopographic low areas (Hon et al. 1994). Either the fl ow was redirected to this paleodepression at Chasm, from the main vent, or a smaller fi ssure, point-source, supplied the lava. Small fi ssure systems have been recorded on Mauna Loa, Hawaii and King’s Bowl, Idaho (Greeley 1977). Illustrated by the western composite log section, there is a sub-aqueous to subaerial succession where an existent lake, was subsequently lava-fed creating a delta lake over a period of time. The eruptive style of volcanism at Chasm is refl ected in the defi ned facies architectural-type. The sequence from the exposed base (L10) of the canyon to the uppermost fl ow fi eld (L1) consists of the following facies architecture (Fig. 5.5): 121 CB(L10) ->TR(L9)->TR(L8)->CB(L7) ->TR(L6) ->TR(L5) ->( +/- FB) ->CB(L4)  ->TC(L3) ->TC(L2)->TC(L1) Tabular-classic interpretation  A tabular-classic facies architecture comprises the stratigraphic upper three fl ow fi elds (L1 through L3), and is interpreted to have been emplaced by subaerial effusive basaltic lavas, with a more continuous, steady supply rate of lava, which is likely to have infl ated the lobe (i.e., SWELL hypothesis; Self et al., 1998). After the lobe is infl ated, lobe boundaries are indistinguishable, and the fl ow fi eld resembles a sheet-like fl ow with characteristic poorly to moderately columnar-joints. There is no colonnade and entablature sequence observed at Chasm. Sheet lobes are inferred to have been emplaced from a fi ssure vent, however at Chasm, there is no indication of proximity to the source vent. Compound-braided interpretation  Interspersed within the sequence compound-braided facies are found (L10, L7 and L4). Compound-braided facies architecture suggests effusive basaltic volcanism, represented by pahoehoe non-channelized fl ows. CB-type architecture is likely emplaced from a low shield volcano where anatomising, branching lobes occur. A pahoehoe lobe, likely initially 10-50 cm thick, can infl ate to a size of 4 m as calculated by Kileauea fi eld observations by Hon et al (1994).  There is a relationship between the size of the individual lobes and the supply rate of the incoming lava (Hon et al. 1994). Pahoehoe toes are at the fl ow front in the CB-type, and with a low dip, the toes are predicted to have equant toe widths opposed to elongated toes found with emplacement on steeper surfaces (Crown and Baloga; 1999).  There are no observed spatter or bombs, indicating Chasm to be distal to the eruptive centre(s). Transitional mixed interpretation  Transitional mixed facies architecture is a mixture of TC- and CB-architectural types, and the morphology of the fl ow fi elds suggests a bimodal emplacement. The TR- 122 type represents the quintessential Snake River Plain type volcanism, interpreted to have erupted from coalescing low shield volcanoes, emplacing the CB-type, in addition to fi ssure eruptions (often on the fl anks of the shields), which emplaces the TC-type that subsequently fi lls in the topographic irregularities (i.e., plateau landscape) (Greeley 1976, 1977, 1982; Jerram 2002; Passey and Bell 2007). Another hypothesis for this changeover between architectural types in a single fl ow fi eld, could be a result of infl ation. Jerram (2002) interprets the shift as a beginning with CB-type, and through continual supply of lava, and infl ation the TC-type is formed. At Chasm, the changeover between types can occur in both directions within one fl ow fi eld, illustrated in Figures 5.1 through 5.3. Foreset-bedded interpretation  Foreset-bedded facies architecture is spatially positioned on the southern end of the western canyon wall. FB-type indicates subaqueous lavas representing the relict bars of the delta sequence. A subaerial vent is interpreted to have supplied the lava of the pillow lavas. Further discussion and interpretations regarding the temporary Chasm Lake are found in section 5.2.1 of this chapter.  The sequence of L10 to L1 is indicative of evolution of the volcanic history through time (Fig. 5.11). It is observed that there are changes in the eruptive style, which suggests a progression of volcanism that may indicate different eruption rates. Roughly, the same phenocrysts are present in the Chasm succession as well as a fairly static landscape during emplacement, therefore the changes observed in the architecture refl ects different fl uxes of magma.The viscosity of the magma could change the style of the fl ow fi eld. These observations imply a similar cooing history for each of the 10 fl ow fi elds. The tabular- classic architectural type has been inferred to be a product of a continuous supply of lava, whereas the compound-braided type can indicate early stages of the eruption where there may be intermittent breaks in the supply of lava (Jerram, 2002). The presence of CB-type at the base of the sequence (L10) suggests the early stages of the eruption from low-angle shield volcanoes (perhaps coalescing), prominent with pahoehoe lobes. The next two 123 episodes of volcanism are observed as the TR-type, a mixture of TC and CB, emulating the ‘Plains-style’ of volcanism, which may indicate an irregular supply of lava or sources from multiple sources, such as a shield volcano and a fl ank fi ssure. The uppermost lavas are classifi ed as TC-type, which implies a constant supply of lava for the fi nal 3 volcanic episodes, capping the emplacement history of Chasm.  There are no fi eld observations to suggest proximity to a vent in the volcanic sequence. The Chilcotin Group basalts at Chasm are laterally confi ned to a broad valley between basement highs to the east and west. The lavas are inferred to fi ll and bury a long-lived paleochannel, which cuts into the early Miocene Deadman Formation, which itself fi lled a paleochannel cut into the pre-Miocene basement rocks (Farrell et al., 2007). This suggests that there is a persistent drainage system in Chasm Provincial Park area that has been able to re-establish itself several times in the past 15My. 5.3 IMPLICATIONS FOR REGIONAL CHILCOTIN GROUP  This section provides insight on the relevance of the Chasm detailed physical volcanology in relation to the regional CGB, which spans the interior of British Columbia from Kamloops to Prince George totaling 17,000km3 (Dohaney, 2009). A suggested fi eld- based approach is presented for future needs of mapping and interpreting CGB exposures. This is useful and can be modifi ed for detailed mapping, reconnaissance-scale mapping, and mineral exploration potentials.  Implications derived from the volcanic facies architecture can be applied regionally to see if there is a regional correlation of the CGB. The mapping of Chasm study area is consistent with the Andrews and Russell model (2008), which states that the thickest successions of the CGB such as Chasm, Dog Creek and Bull Canyon are situated in ‘paleo- lows’ (Matthews 1989) and the areas between these thick successions can be considered ‘paleo-highs’ with basalt thicknesses ranging between 0- 30 meters. The areas surrounding the Chasm canyon can be considered a ‘paleo-high’, where the thickness of the basalt 124 rapidly diminishes. The possibility of multiple source vents must be examined in future studies, and whether the lava was sourced from a low-angle shield volcano or a fi ssure. Attention to lavas and volcanic textures is imperative, as proximity to the vent can be determined if spatter or bombs are observed. Distal fl ows may be suggestive of infl ated pahoehoe. 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Geology, 13: 499-502  135 APPENDIX A FIELD METHODOLOGY The modifi ed method of AEA used at Chasm is abbreviated in the following list: Field Method Step 1: Assess study area, and choose outcrop suitable for AEA Step 2: Plan traverses. Develop a photographic method to execute the lateral mapping of the canyon. Step 3: Traverse the canyon, and use a digital camera to photographs the opposing walls of the canyon using the photographic method. Step 4: Stitch the digital photos together in a graphics program (i.e., Adobe Illustrator). Note: Autostitch (Brown and Lowe 2007) or camera photo stitching program cannot be used, if the curves/ undulations in the canyon are observed. These programs cannot normalize the curves. If you have a small lateral extent (500 m-1 km), autostitch is the preferred method. Step 5: Print using fi eld printer, and attach overlays (vellum) on top of the mosaic. Step 6: Map directly onto the overlays, noting the external geometry (i.e., sheet, lens, lobate, wedge, scoop, or u-shaped). Describe the contact boundaries of the fl ow lobes and the fl ow fi eld. Post-fi eld analysis Step 7: Assimilate all photos into two lateral profi les, one for each wall of the canyon. Step 8: Finalize the mosaics in graphics program, and scan the overlays, then digitize the mapping linework and produce the working draft of the lateral profi le. Step 9: Print the mosaics and linework, and identify the succession of lava fl ows (youngest to oldest), and paleosols for the canyon. Step 10: Correlate the lava and paleosols with the graphic logs ensuring a context of space and time. 136 Step 11: Defi ne the architectural elements. Note these elements may comprise multiple facies. Laterally variability must be incorporated into the assessment and classifi cation of the architectural elements.  The photographing method is specifi c to Chasm due to the signifi cant number of undulations of the canyon walls; four type panorama sequences are taken at each station. Additional sketches and notes are made at each station, for systematic purposes since the length of the canyon walls yields three long lateral profi les, where the collation of photographs can prove complex in certain junctures. Magnetic susceptibility  Magnetic susceptibility (MS) measurements were taken using a KT-9 Kappameter during fi eld seasons from 2006 through 2008 (Figs. 2.2, 3.6, 3.7; Table 3.3) in Chasm. The objective was to compare values between different lavas in our stratigraphic sections, and/or identify an overarching trend in the Chasm canyon. Fifty-eight measurements were recorded from the Chasm study area, and the measurement type is either a fi eld measurement or a laboratory measurement, where samples uncut or cored were tested with the hand-held KT-9 Kappameter. The number of measurements at each fi eld station was typically 10 (minimum of 3 measurements are required at each station), which have subsequently been averaged into the recorded MS value. Data is recorded in 10-3 SI units (Table 3.3). For CGB paleomagnetism data, including the Chasm study area, refer to Enkin et al. (2008). Structural measurements:  Structural data of the CGB comprises planar pillow measurements (volcanic layering)  (Appendix D; Fig. 2.2). Planar measurements of the Deadman Formation bedding is recorded (Appendix D; Fig. 2.2). The structure data is plotted on the Chasm Map (Fig. 2.2). 137 A scheme was developed to address the level of certainty for the structure data in the study area, which is outlined below. Measurements assigned a 1 or 2 level are plotted on the Chasm Map (Fig. 2.2) and used for interpretation. Recordings of a 3 or 4 level are discarded. Level of certainty for the structure data 3D pillow / highest1.  level of certainty Estimating plane2. Crude estimate of plane3. Uncertain4. Chasm Samples: All CGB samples are in the regional CGB Database (Dohaney et al. 2010) 138 APPENDIX B AR40/AR39 SAMPLE PREPARATION Sample Preparation  The geochronological data set for the Chasm Provincial Park and immediately adjacent areas is extensive for a canyon of this size. Typically only the lowest and highest lava would be sampled, therefore giving a result of the duration of volcanism for the lavas exposed inside the canyon. The rationale in deciding which basalts to date was based on 3 factors: 1) volcanic stratigraphy (the length of time for the eastern log succession to have been emplaced); 2) constraint of the duration of soil development using the lavas immediately above and below a paleosol; and 3) the aim of determining the duration of volcanism for Chasm Canyon. Two different batches of geochronological samples were prepared for the CGB (Chasm specifi c and regional) and are separated into categories of 2007 and 2009. Forty- one samples in total (Chasm and regional) were analysed for Ar40/Ar39. The analyst for the 2007 ages was T. Ullrich and for 2009 ages J. Gabites. All samples were analyzed at Pacifi c Centre for Isotopic and Geochemical Research at UBC). The methodology for the sample preparation for both sample sets is identical. First, the basalt samples are cut using a standard rock saw into approximately 8 x 8 x 8 cm sized sections, which are then crushed to gravel size using a Rhino Jaw Crusher. A 10 g split of the crushed basalt sample is then subjected to leaching, to clean the samples before picking the freshest gravel-sized basalt fragments. The sample is rinsed multiple times in deionized water until the water runs clear with the decanting. Approximately 10 ml of 5% nitric acid is then added to the sample and allowed to saturate for fi ve minutes. Deionized water (~150 ml) is added, and the samples are placed in an ultrasonic bath for 5 minutes, and then drained onto fi lter paper. Once the samples have dried, the individual grains are picked using a binocular microscope, with the freshest basalt grains selected. Grains are picked that are representative of the whole rock 139 basalt samples, and 10-15 grains of basalt were selected for each sample. This fi nal picking step is critical for locations where a high degree of alteration has taken place, such as at Chasm, and only the freshest grains were selected for analysis. In many cases, the grains are highly oxidized, with a range of colours red to orange, microvesicular with infi lled vesicles, and brittle, following this observation these grains are discarded. As mentioned previously, two separate batches of whole rock CGB were submitted and these batches are distinguished by the year (i.e., 2007 or 2009 ages). An ideal plateau would have contiguous steps within the 2 sigma error, use 50- 100% of the 39Ar gas, have a MSWD value near 1, and a low error value. The plateau shown on the plots (Figs. 3.8-3.13; and in Appendix C) show the width of each square (step) as the amount of gas released and the height of each square as the error associated with the specifi c step. The statistical error resides in each individual heating step, therefore the fi nal plateau age combines the error of each step. Error increases based on the stability of the mass spectrometer, the J factor (irradiation parameter), and the accuracy and precision blanks used. As shown on the table, samples analysed by T. Ullrich were analysed once, therefore recorded a single age result, whereas the samples analysed by J. Gabites each sample was analysed twice, therefore, there are two ages recorded for each sample. When two ages resulted from the same sample number, the addition in quadrature statistical method was used to provide a 2σ weighted average for the error (internal error) using Isoplot. 140 APPENDIX C REGIONAL GEOCHRONOLOGICAL DATA: see included cd 14 1 Sample Numberb AGE (Ma) System UTM Easting (NAD83) UTM Northing (NAD83)  LOCATION Context Analytical Notes RE-AF06-53 9.0 ± 1.4 Ar-Ar 487708 5764223 Anahim Flats Lava 1: basal lava RE-AR06-8 9.64 ± 0.35 Ar-Ar 641623 5649526 Arrowstone Hills Top lava RE-AR06-10 11.04 ± 0.14 Ar-Ar 642074 5648949 Arrowstone Hills Basal lava RE-AR06-13 DISCARDED Ar-Ar 642116 5649056 Arrowstone Hills Middle lava excessive amts of excess Ar gas-NO DATE RE-BC-214E* 5.32  ± 0.80 Ar-Ar 474286 5771309 Bull Canyon Middle lava forced plateau; 61.6% of 39Ar; steps 7-10 RE-CD06-66* 6.21  ± 0.30 Ar-Ar 446246 5704620 Cardiff Mountain Basal lava: BC telephone forced plateau; 82.7% of 39Ar; steps 1-5 RE-CD06-74 DISCARDED Ar-Ar 446451 5704530 Cardiff Mountain Middle lava: colonnade humped plateau; possibility a result of 39Ar recoil in sample RE-CH06-4 9.07 ± 0.26 Ar-Ar 608609 5671735 Chasm East Composite Log Lava 9 RE-CH06-12* 9.65± 0.40 Ar-Ar 609057 5671112 Chasm East Composite Log Lava 2 poor isochron (low initial 40/36); 70.9% of 39Ar; steps 5-9 RE-CH06-18 9.86 ± 0.30 Ar-Ar 609006 5671220 Chasm East Composite Log Lava 6 RE-CH06-92 9.83 ± 0.31 Ar-Ar 607730 5668821 Western Chasm wall No strat. Reference RE-DC06-32* 1.162 ± 0.057 Ar-Ar 555488 5716721 Dog Creek Top lava forced plateau; 91.3% of 39/Ar; steps 3-8 RE-DC06-36* 2.89 ± 0.42 Ar-Ar 555012 5716235 Dog Creek Middle lava forced plateau; re-test; 60.1% of 39/Ar; steps 7-9 RE-DM06-2 1* 17.33 ± 0.28 Ar-Ar 647894 5667970 Deadman Falls Basal lava RE-DM06-2 2* 17.43 ± 0.16 Ar-Ar 647894 5667970 Deadman Falls Basal lava RE-HA06-45 DISCARDED Ar-Ar 492172 5756349 Hanceville Top lava saddle shaped plateau; possibly a result of excessive amts of Ar gas RE-SK06-60 2.78 ± 0.21 Ar-Ar 481886 5771101 Stum Road Basal lava analyst's notes: very low atmos. for high steps RE-SK06-64 2.17 ± 0.26 Ar-Ar 481886 5771101 Stum Road Top lava RE-VK06-79 8.24 ± 0.58 Ar-Ar 444047 5710329 Vedan Lake Lava 1: basal lava RE-VK06-86 7.27 ± 0.35 Ar-Ar 444200 5710432 Vedan Lake Lava 17: middle lava 98.9% of 39Ar; steps 2-8 RE-VK06-89 6.61 ± 0.36 Ar-Ar 444254 5710436 Vedan Lake Lava 24: top lava a UBC, T. Ullrich, analyst. Unpublished preliminary results. b All samples are whole rocks. GEOCHRONOLOGY OF CHILCOTIN GROUP BASALTS: REGIONALa * Forced Age plateau: not complete step spectrum (1-9). At least 3 steps are used, and at 50-100% of the gas for these samples. Ta bl e C 1:  R eg io na l g eo ch ro no lo gy 142 APPENDIX D Structure Data 143 Chasm Structure Measurements for Map STATION EASTING NORTHING STRIKE DIP NOTES* PLANAR PILLOW MEASUREMENTS (VOLCANIC LAYERING) 08REF34 607675 5669360 56 30 Certainty 2 08REF34 607675 5669360 62 30 Certainty 2 08REF34 607675 5669360 40 34 Certainty 2 08REF34 607675 5669360 32 40 Certainty 2 REF34_AVG 607675 5669360 48 34 AVG 08REF079 607434 5670258 90 45 Certainty 2 08REF079 607434 5670258 92 32 Certainty 2 REF079_AVG 607434 5670258 91 39 AVG 08REF006 607788 5669179 29 35 Certainty 2 08REF006 607788 5669179 61 29 Certainty 2 08REF006 607788 5669179 27 51 Certainty 2 08REF006 607788 5669179 26 36 Certainty 2 08REF006 607788 5669179 40 30 Certainty 2 REF006_AVG 607788 5669179 37 36 AVG 08REF005 607769 5669348 52 38 Certainty 2 08REF005 607769 5669348 53 48 Certainty 2 REF005_AVG 607769 5669348 53 43 AVG 08REF010 607682 5668454 127 35 Certainty 2- 08REF010 607682 5668454 98 36 Certainty 2- 08REF010 607682 5668454 105 36 Certainty 2- 08REF010 607682 5668454 134 28 Certainty 2- REF010_AVG 607682 5668454 116 34 AVG * Level of Certainty 1= 3D pillow or highest level of certainty 2= Estimating plane 3= Crude estimate of plane 4= Uncertain PLANAR BEDDING MEASUREMENTS STATION EASTING NORTHING STRIKE DIP NOTES 08REF023 608188 5667679 154 13 Certainty 1 08REF025 608205 5667984 217 20 Certainty 1 08REF025 608205 5667984 218 30 Certainty 1 Table D1: Chasm structure measurements for map 144 APPENDIX E XRD RESULTS: MATERIAL INFILLING THE VESICLES AT CHASM Analyses run by Jenny Lai (UBC) EXPERIMENTAL METHOD The fi ve samples were ground into fi ne powder with a corundum mortar and smeared on to a glass slide with ethanol. Step-scan X-ray powder-diffraction data were collected over a range 3-80°2θ with CoKa radiation on a Bruker D8 Focus Bragg-Brentano diffractometer equipped with an Fe monochromator foil, 0.6 mm (0.3°) divergence slit, incident- and diffracted-beam Soller slits and a LynxEye detector. The long fi ne-focus Co X-ray tube was operated at 35 kV and 40 mA, using a take-off angle of 6°. RESULTS Mineral identifi cation was done using the International Centre for Diffraction Database PDF-4 and Search-Match software by Siemens (Bruker). The results are shown in Table 1. The X-ray diffractograms are shown in Figures 1 – 5. The presence of montmorillonite in samples 08REF030A01, RE-CH07-53, and RE-CH07-58 is confi rmed by glycolation.  The fi t of the montmorillonite pattern varies between samples due to different amounts of hydration within each sample. 145 Summary of Results: XRD qualitative results from Jenny Lai (UBC) Mineralization in the Pillow Breccia West Chasm Composite Stratigraphic Log- all samples have a stratigraphic reference 1) 08REF030A02 Possible zeolites found in the matrix clastic material found at contact between WL2 and WC2 Rationale= confi rm the zeolite composition, with additional classifying of the type of zeolite. Result: Yes, these are zeolites. Specifi cally, chabazite-Ca and Phillipsite-K, both in the Zeolite Group. 2) 08REF034A01 Possible chalcedony. Sampled from WC3 Rationale = confi rm the mineral composition, and classify the material Result: Major peak of analcime (associated with zeolites), and zeolite (phillipsite-K). Montmorillonite (Smectite Gr.) present, in addtion to plagioclase (albite) and Qtz. 3) 08REF030A01 chalky material interstitial with pillows in WC2. Rationale= classify this material, what kind of secondary mineralization is this? Result: Major peak of analcime (assoc. with zeolites), and zeolite (wairakite). Montmorillonite (Smectite Gr.) present, calcite, clinochore, plag., k-feldspar, and qtz. XRD of complete soil profi le: Station 071 (all samples have stratigraphic reference: refer to soil profi le & table for this stn) 4) RE-CH07-53 Tephra layer Rationale: identify and classify the different minerals in this 1st horizon (Bmb) Result: Zeolite (chabazite-Ca), Smectite (Montmorillonite), Plag., Cpx., Clinochore, Gypsum, Calcite. Plagioclase and cpx are the dominant peaks, also montmorillonite. 5) RE-CH07-58 Clastic fi nely laminated paleosol Rationale: identify and classify the different minerals in this 2nd horizon (IIBmb1) Result: Major peaks = analcime (assoc. w/ zeolites), plag and quartz- which makes sense. Zeolites (chabazite-Ca, phillipsite-K and tridymite) are also present. Smectite Gr. montmorillonite is present. K-feldspar, muscovite, and grunerite. 14 6 q y Mineral Ideal Formula 08REF030A02 08REF034A01 08REF030A01 RE-CH07-53 RE-CH07-58 Chabazite-Ca (Ca,K2,Na2)2(Al2Si4O12)2.12H2O X   X X Phillipsite-K (K2)0.48Ca0.52Al2Si4O12.xH2O X X   X Analcime NaAlSi2O6.H2O  X X  X Wairakite CaAl2Si4O12.2H2O   X Plagioclase NaAlSi3O8 – CaAl2Si2O8  X X X X K-Feldspar KAlSi3O8   X  X Quartz SiO2  X X  X Calcite CaCO3   X X Clinochlore (Mg,Fe2+)5Al(Si3Al)O10(OH)8   X X Gypsum CaSO4.2H2O    X Augite (Ca,Na)(Mg,Fe,Al,Ti)(Si,Al)2O6    X Muscovite KAl2(AlSi3O10)(OH)2     X Tridymite SiO2     X Montmorillonite (Na,Ca)0.3(Al,Mg)2Si4O10(OH)2.nH2O  X X X X Grunerite Fe2+7Si8O22(OH)2     X Ta bl e E 1:  R es ul ts  o f qu al it at iv e an al ys is 147 0 0 -0 1 6 - 0 7 1 5 ( I) - P h illip s ite - K s y n - (K 2 )0 4 8 C a 0 5 2 A l2 S i4 O 1 2 ·x H 2 O 0 0 -0 3 4 - 0 1 3 7 ( *) - C h a b a z ite - C a - C a 2 A l4 S i8 O 2 4 ·1 2 H 2 O 1 0 8 R E F0 3 0 A 0 2 N E W D 8 - File : 1 0 8 R E F0 3 0 A 0 2 N E W D 8 ra w 0 1 0 0 0 2 0 0 0 3 0 0 0 4 0 0 0 5 0 0 0 6 0 0 0 7 0 0 0 8 0 0 0 9 0 0 0 1 0 0 0 0 1 1 0 0 0 1 2 0 0 0 1 3 0 0 0 1 4 0 0 0 1 5 0 0 0 2-Theta - S cale 3 1 0 2 0 3 0 4 0 5 0 6 0 7 0 Figure E1: X-ray diffractogram of sample 08REF03A02 148 0 0 -0 0 2 - 0 0 3 7 (D ) - M o n tm o r illo n ite - A lS i2 O 6 ( O H ) 2 0 0 -0 1 6 - 0 7 1 5 ( I) - P h illip s ite - K , s y n - (K 2 ) 0 .4 8 C a 0 .5 2 A l2 S i4 O 1 2 ·x H 2 O 0 1 -0 7 3 - 6 6 1 8 (A ) - Q u a r tz lo w s y n - S iO 2 0 1 -0 8 3 - 1 4 6 6 ( *) - A lb ite lo w - N a 0 9 8 6 ( A l1 0 0 5 S i2 9 9 5 O 8 ) 0 1 -0 7 1 - 0 8 1 1 ( I) - A n a lc im e - N a ( A lS i2 O 6 ) (H 2 O ) 2 0 8 R E F 0 3 4 A 0 1 D 8 - F ile : 2 0 8 R E F 0 3 4 A 0 1 D 8 r a w 0 1 0 0 0 2 0 0 0 3 0 0 0 4 0 0 0 5 0 0 0 6 0 0 0 7 0 0 0 8 0 0 0 9 0 0 0 1 0 0 0 0 1 1 0 0 0 1 2 0 0 0 1 3 0 0 0 1 4 0 0 0 1 5 0 0 0 1 6 0 0 0 1 7 0 0 0 1 8 0 0 0 1 9 0 0 0 2 0 0 0 0 2 1 0 0 0 2 2 0 0 0 2 3 0 0 0 2 4 0 0 0 2 5 0 0 0 2 6 0 0 0 2 7 0 0 0 2 8 0 0 0 2-Theta - S cale 3 1 0 2 0 3 0 4 0 5 0 6 0 7 0 Figure E2: X-ray difractogram of sample 08REF034A01 149 0 0 -0 0 2 - 0 0 3 7 (D ) - M o n tm o r illo n ite - A lS i2 O 6 ( O H ) 2 0 0 -0 1 6 - 0 7 1 5 ( I) - P h illip s ite - K , s y n - (K 2 ) 0 .4 8 C a 0 .5 2 A l2 S i4 O 1 2 ·x H 2 O 0 1 -0 7 3 - 6 6 1 8 (A ) - Q u a r tz lo w s y n - S iO 2 0 1 -0 8 3 - 1 4 6 6 ( *) - A lb ite lo w - N a 0 9 8 6 ( A l1 0 0 5 S i2 9 9 5 O 8 ) 0 1 -0 7 1 - 0 8 1 1 ( I) - A n a lc im e - N a ( A lS i2 O 6 ) (H 2 O ) 2 0 8 R E F 0 3 4 A 0 1 D 8 - F ile : 2 0 8 R E F 0 3 4 A 0 1 D 8 r a w 0 1 0 0 0 2 0 0 0 3 0 0 0 4 0 0 0 5 0 0 0 6 0 0 0 7 0 0 0 8 0 0 0 9 0 0 0 1 0 0 0 0 1 1 0 0 0 1 2 0 0 0 1 3 0 0 0 1 4 0 0 0 1 5 0 0 0 1 6 0 0 0 1 7 0 0 0 1 8 0 0 0 1 9 0 0 0 2 0 0 0 0 2 1 0 0 0 2 2 0 0 0 2 3 0 0 0 2 4 0 0 0 2 5 0 0 0 2 6 0 0 0 2 7 0 0 0 2 8 0 0 0 2-Theta - S cale 3 1 0 2 0 3 0 4 0 5 0 6 0 7 0 Figure E3: X-ray diffractogram of sample 08REF030A01 150 0 0 -0 0 5 -0 5 8 6 ( * ) - C a lc ite , s y n - C a C O 3 0 1 -0 7 6 -1 7 4 6 (N ) - G y p s u m - C a S O 4 ( H 2 O ) 2 0 0 -0 1 9 -0 2 0 8 (A ) - C h a b a z ite - C a 2 A l4 S i8 O 2 4 ·1 2 H 2 O 0 1 -0 8 7 -2 4 9 6 ( * ) - C lin o c h lo r e ( IIb - 4 ) - M g 4 8 8 2 Fe 0 2 2 A l1 8 8 1 S i2 9 6 O 1 0 (O H ) 8 0 1 -0 7 6 - 0 9 2 6 ( *) - A lb ite , c a lc ia n - (N a 0 .7 5 C a 0 .2 5 ) (A l1 .2 6 S i2 .7 4 O 8 ) 0 0 -0 0 3 - 0 0 1 4 (D ) - M o n tm o r illo n ite - M g O ·A l2 O 3 ·5 S iO 2 ·x H 2 O 0 1 -0 7 6 - 0 5 4 4 ( *) - A u g ite - C a 0 6 1 M g 0 7 6 Fe 0 4 9 ( S iO 3 )2 4 R E - C H 0 7 - 5 3 D 8 - File : 4 R E - C H 0 7 - 5 3 D 8 r a w 0 1 0 0 0 2 0 0 0 3 0 0 0 4 0 0 0 2-Theta - S cale 3 1 0 2 0 3 0 4 0 5 0 6 0 7 0 Figure E4: X-ray diffractogram of sample RE-CH07-53 151 0 1 -0 8 6 -0 6 8 1 ( * ) - Tr id ym ite s yn - S iO 2 0 0 -0 1 7 -0 7 4 5 (D ) - G r u n e r ite - ( Fe +2 M g ) 7 S i8 O 2 2 ( O H ) 2 0 1 -0 7 2 -4 6 3 4 (N ) - P h illip s ite - M g 1 5 2 N a 0 8 8 K 0 2 2 (A l4 5 S i1 1 5 O 3 2 ) (H 2 O )1 0 9 6 0 1 -0 7 3 -4 0 3 1 (N ) - C h a b a z ite - (N H 4 )3 2 4 C a 0 2 5 A l3 6 0 S i8 4 0 O 2 4 (H 2 O )1 2 6 0 1 -0 8 9 -5 4 0 1 (N ) - M u s c o v ite 2 M 1 - K A l2 2 0 (S i3 A l)0 9 7 5 O 1 0 ( ( O H ) 1 7 2 O 0 2 8 ) 0 0 -0 5 8 - 2 0 1 0 (N ) - M o n tm o r illo n ite - N a 0 .3 ( A l,M g )2 S i4 O 1 0 (O H ) 2 ·x H 2 O 0 0 -0 4 6 - 1 0 4 5 ( *) - Q u a r tz s yn - S iO 2 0 1 -0 8 6 - 0 4 3 7 ( *) - O r th o c la s e - ( K 0 9 4 N a 0 0 6 ) (A lS i3 O 8 ) 0 1 -0 7 6 - 0 9 2 6 ( *) - A lb ite c a lc ia n - (N a 0 7 5 C a 0 2 5 ) (A l1 2 6 S i2 7 4 O 8 ) 0 0 -0 4 1 - 1 4 7 8 ( *) - A n a lc im e -C - N a ( S i2 A l)O 6 ·H 2 O 5 R E - C H 0 7 - 5 8 D 8 - File : 5 R E - C H 0 7 - 5 8 D 8 r a w 0 1 0 0 0 2 0 0 0 3 0 0 0 4 0 0 0 5 0 0 0 6 0 0 0 7 0 0 0 2-Theta - S cale 3 1 0 2 0 3 0 4 0 5 0 6 0 7 0 Figure E5: X-ray difractogram of sample RE-CH07-58


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