@prefix vivo: . @prefix edm: . @prefix ns0: . @prefix dcterms: . @prefix skos: . vivo:departmentOrSchool "Science, Faculty of"@en, "Earth, Ocean and Atmospheric Sciences, Department of"@en ; edm:dataProvider "DSpace"@en ; ns0:degreeCampus "UBCV"@en ; dcterms:creator "Palsgrove, Regan Jane"@en ; dcterms:issued "2010-12-02T21:35:30Z"@en, "1990"@en ; vivo:relatedDegree "Master of Science - MSc"@en ; ns0:degreeGrantor "University of British Columbia"@en ; dcterms:description """The Albian Lower Skeena Group in the Telkwa coalfield comprises more than 500 metres of conglomerate, sandstone, siltstone, mudstone and coal deposited during two regressive/transgressive cycles. The stratigraphic sequence is divisible into four lithostratigraphic units. The basal unit, Unit I, may be more than 100 metres thick and comprises conglomerate, sandstone, mudstone, coal, and seat earth. Conglomerate and sandstone are composed dominantly of chert and volcanic rock fragments, and mudstones are kaolinitic. Unit I was deposited in a fluvial environment on an eroded volcanic basement. Gravel and sand were deposited in braided channels and bars, and mudstone accumulated in floodplains. Coal formed in poorly drained, peat-forming backswamps. In the northern part of the study area, coal seams thin and split, a result of periodic flooding of peat swamps with sediment-laden water from nearby streams. Deposition of Unit I ended with a marine transgression and deposition of Unit II. Unit II consists of up to 140 metres of silty mudstone, bioturbated or cross-bedded, chert and muscovite-rich sandstone, and rare thin coaly mudstones deposited in a deltaic/shallow marine environment. Sand was deposited in distributary channels and mouth-bars, mud accumulated in bays, and thin discontinuous peat beds accumulated in local salt marshes. There is structural evidence for the presence of an unconformity within Unit II, but palynological and paleontological data suggest that the strata are all similarly aged. Unit III averages 90 metres thick, and comprises bioturbated or rippled, chert and muscovite-rich sandstone, siltstone, carbonaceous mudstone and thick, laterally extensive coal seams deposited in a variety of low-energy, paralic environments. Sand and mud were deposited and biogenically reworked in tidal flats, and siltstone accumulated in a restricted, nearshore marine environment in the eastern edge of the study area. Peat accumulated in freshwater coastal marshes which periodically prograded over tidal flats. All but the lowermost coal seams pinch out eastward into restricted, nearshore marine sediments, and the ash content of the coal increases toward the margin of the seam. Locally, the sulphur content of the coal is high, reflecting occasional inundation of the fresh-water swamps by brackish water. High sulphur coal contains relatively more pyritic sulphur and less organic sulphur, compared to low-sulphur coal. Unit IV is at least 150 metres thick and is composed of chloritic, green sandstone overlain by silty mudstone, deposited in a marine environment. The basal sandstone is a transgressive lag deposit, and silty mudstone, the predominant lithofacies, was deposited in a nearshore, shallow marine environment. The provenance of the sediments in the Telkwa coalfield changes from the base to the top of the stratigraphic section. Conglomerate and sandstone of Unit I contain an abundance of volcanic clasts and grains, locally derived from underlying and surrounding volcanic rocks of the Jurassic Hazelton Group, which were uplifted as part of the Skeena Arch and subsequently eroded and reworked. Sandstones of Units II, III and IV, which contain much less volcanic-derived material and an abundance of mica flakes, were derived from high-grade metamorphic rocks in the Omineca Belt. Chert grains are abundant throughout, reflecting continued clastic influx from the Pinchi Belt-Columbian Orogen."""@en ; edm:aggregatedCHO "https://circle.library.ubc.ca/rest/handle/2429/30267?expand=metadata"@en ; skos:note "STRATIGRAPHY, SEDIMENTOLOGY AND COAL QUALITY OF THE LOWER SKEENA GROUP, TELKWA COALFIELD, CENTRAL BRITISH COLUMBIA (93L/11) By REGAN JANE PALS GROVE B.Sc. University of Calgary 1988 A THESIS SUBMITTED IN PARTIAL FULFILLMENT OF THE REQUIREMENTS OF THE DEGREE OF MASTER OF SCIENCE in THE FACULTY OF GRADUATE STUDIES Department of Geological Sciences We accept this thesis as conforming to the required standard THE UNIVERSITY OF BRITISH COLUMBIA September 1990 (c) Regan Jane Palsgrove In presenting this thesis in partial fulfilment of the requirements for an advanced degree at the University of British Columbia, I agree that the Library shall make it freely available for reference and study. I further agree that permission for extensive copying of this thesis for scholarly purposes may be granted by the head of my department or by his or her representatives. It is understood that copying or publication of this thesis for financial gain shall not be allowed without my written permission. Department The University of British Columbia Vancouver, Canada Date Qdhoki^ 16, 19^0 DE-6 (2788) A B S T R A C T The Albian Lower Skeena Group in the Telkwa coalfield comprises more than 500 metres of conglomerate, sandstone, siltstone, mudstone and coal deposited during two regressive/transgressive cycles. The stratigraphic sequence is divisible into four lithostratigraphic units. The basal unit, Unit I, may be more than 100 metres thick and comprises conglomerate, sandstone, mudstone, coal, and seat earth. Conglomerate and sandstone are composed dominantly of chert and volcanic rock fragments, and mudstones are kaolinitic. Unit I was deposited in a fluvial environment on an eroded volcanic basement. Gravel and sand were deposited in braided channels and bars, and mudstone accumulated in floodplains. Coal formed in poorly drained, peat-forming backswamps. In the northern part of the study area, coal seams thin and split, a result of periodic flooding of peat swamps with sediment-laden water from nearby streams. Deposition of Unit I ended with a marine transgression and deposition of Unit II. Unit II consists of up to 140 metres of silty mudstone, bioturbated or cross-bedded, chert and muscovite-rich sandstone, and rare thin coaly mudstones deposited in a deltaic/shallow marine environment. Sand was deposited in distributary channels and mouth-bars, mud accumulated in bays, and thin discontinuous peat beds accumulated in local salt marshes. There is structural evidence for the presence of an unconformity within Unit II, but palynological and paleontological data suggest that the strata are all similarly aged. Unit III averages 90 metres thick, and comprises bioturbated or rippled, chert and muscovite-rich sandstone, siltstone, carbonaceous mudstone and thick, laterally extensive coal seams deposited in a variety of low-energy, paralic environments. Sand and mud were deposited and biogenically reworked in tidal flats, and siltstone accumulated in a restricted, nearshore marine environment in the eastern edge of the study area. Peat accumulated in freshwater coastal marshes which periodically prograded over tidal flats. All but the lowermost coal seams pinch out eastward into restricted, nearshore marine sediments, and the ash content of the coal increases toward the margin of the seam. Locally, the sulphur content of the coal is high, reflecting occasional inundation of the fresh-water swamps by brackish water. High sulphur coal contains relatively more pyritic sulphur and less organic sulphur, compared to low-sulphur coal. Unit IV is at least 150 metres thick and is composed of chloritic, green sandstone overlain by silty mudstone, deposited in a marine environment. The basal sandstone is a transgressive lag deposit, and silty mudstone, the predominant lithofacies, was deposited in a nearshore, shallow marine environment. The provenance of the sediments in the Telkwa coalfield changes from the base to the top of the stratigraphic section. Conglomerate and sandstone of Unit I contain an abundance of volcanic clasts and grains, locally derived from underlying and surrounding volcanic rocks of the Jurassic Hazelton Group, which were uplifted as part of the Skeena Arch and subsequently eroded and reworked. Sandstones of Units II, III and IV, which contain much less volcanic-derived material and an abundance of mica flakes, were derived from high-grade metamorphic rocks in the Omineca Belt. Chert grains are abundant throughout, reflecting continued clastic influx from the Pinchi Belt-Columbian Orogen. i v T A B L E O F C O N T E N T S TITLE PAGE : i ABSTRACT ii TABLE OF CONTENTS iv LIST OF FIGURES viii LIST OF TABLES x LIST OF PLATES .xi ACKNOWLEDGEMENTS xii INTRODUCTION l STUDY AREA LOCATION l DATA SOURCES 3 METHODS 4 REGIONAL GEOLOGY AND PREVIOUS WORK 7 LOCAL STRATIGRAPHY AND STRUCTURE n SEDIMENTOLOGY OF THE GOATHORN REGION OF THE TELKWA COALFIELD 16 UNIT I SEDIMENTOLOGY 16 GENERAL DESCRIPTION 16 LITHOFACIES DESCRIPTIONS 17 CONGLOMERATE 21 MASSIVE SANDSTONE 21 INTRACLAST-RICH SANDSTONE 23 ARGILLACEOUS SANDSTONE 23 CARBONACEOUS MUDSTONE 23 COAL 25 FIRECLAY 25 MOTTLED CLAYSTONE 27 DEPOSITIONAL ENVIRONMENTS OF LITHOFACIES 27 BRAIDED RIVER 27 FLOODPLAIN 29 DEPOSITIONAL HISTORY OF UNIT I 30 V UNIT II S E D I M E N T O L O G Y 33 GENERAL DESCRIPTION 33 LITHOFACIES DESCRIPTIONS 33 SILTY M U D S T O N E 35 INTERBEDDED SANDSTONE A N D M U D S T O N E 35 M O T T L E D ARGILLACEOUS SANDSTONE 39 CARBONACEOUS M U D S T O N E 39 CROSS-BEDDED SANDSTONE . 41 DEPOSITIONAL ENVIRONMENTS OF LITHOFACIES 41 INTERDISTRIBUTARY BAY 41 COASTAL MARSH 42 BAY FILL 42 DISTRIBUTARY C H A N N E L 43 DEPOSITIONAL HISTORY OF UNIT II 44 U N I T III S E D I M E N T O L O G Y 46 GENERAL DESCRIPTION 46 LITHOFACIES DESCRIPTIONS 46 SILTY M U D S T O N E 46 STRATIFIED SANDSTONE 49 BIOTURBATED SANDSTONE 49 CARBONACEOUS M U D S T O N E 51 LENTICULAR B E D D E D SILTSTONE A N D M U D S T O N E 51 C O A L 53 MASSIVE SANDSTONE 53 DEPOSITIONAL ENVIRONMENTS OF LITHOFACIES 53 RESTRICTED NEARSHORE MARINE 57 INTERTIDAL F L A T 57 UPPER INTERTIDAL FLAT 58 COASTAL SWAMP 59 TIDAL C H A N N E L 60 DEPOSITIONAL HISTORY OF UNIT III 60 U N I T I V S E D I M E N T O L O G Y 66 GENERAL DESCRIPTION 66 LITHOFACIES DESCRIPTIONS 66 G R E E N SANDSTONE 66 SILTY M U D S T O N E 67 v i DEPOSITIONAL ENVIRONMENTS OF LITHOFACIES 67 TRANSGRESSIVE L A G SANDSTONE 67 QUIET N E A R S H O R E M A R I N E 68 DEPOSITIONAL HISTORY OF UNIT IV 68 S T R A T I G R A P H Y A N D S E D I M E N T O L O G Y O F T H E N O R T H T E L K W A R E G I O N O F T H E T E L K W A C O A L F I E L D 70 STRATIGRAPHY 70 DEPOSITIONAL ENVIRONMENTS 72 S A N D S T O N E P E T R O G R A P H Y A N D P R O V E N A N C E 73 P E T R O G R A P H Y 73 UNIT 1 73 UNITS II AND III 75 UNIT IV 75 P R O V E N A N C E 76 R E G I O N A L S I G N I F I C A N C E O F T H E T E L K W A C O A L M E A S U R E S 78 C O A L Q U A L I T Y O F T H E T E L K W A C O A L S E A M S 81 SULPHUR C O N T E N T 8i STRATIGRAPHIC VARIATION IN SULPHUR CONTENT 83 D A T A 83 INTERPRETATION 83 SULPHUR DISTRIBUTION WITHIN INDIVIDUAL SEAMS 85 D A T A .• 85 INTERPRETATION 85 SULPHUR FORMS 88 D A T A 88 INTERPRETATION 89 A S H C O N T E N T 95 STRATIGRAPHIC VARIATION IN ASH CONTENT 95 D A T A 95 INTERPRETATION 95 ASH DISTRIBUTION WITHIN INDIVIDUAL SEAMS 98 D A T A 98 INTERPRETATION 104 C O N C L U S I O N S 105 R E F E R E N C E S 108 v i i APPENDIX ONE: RESULTS OF PALYNOLOGICAL ANALYSES 112 APPENDIX TWO: RESULTS OF PALEONTOLOGICAL ANALYSES 121 APPENDIX THREE: TYPICAL SANDSTONE COMPOSITION OF LOWER SKEENA GROUP 123 APPENDIX FOUR: CLAY MINERALOGY: RESULTS OF X-RAY DIFFRACTION ANALYSES 125 LIST OF FIGURES 1. Location of study area 2 2. Drillhole maps of the Goathorn and North Telkwa regions of the Telkwa coalfield, showing location of cross-sections 5 3. Drillhole maps of the Goathorn and North Telkwa regions of the Telkwa coalfield, showing location of isopach maps and ash and sulphur distribution maps 6 4. Tectonic elements of British Columbia 8 5. Nomenclature for Cretaceous sediments in central British Columbia 1( 6. Cross-section showing offset of Unit 1 1< 7. Representative sections of the Lower Skeena Group in the Goathorn region of the Telkwa coalfield 1' 8. Cross-section of Unit 1 showing palaeotopography of the Jurassic Hazelton Group volcanic basement, and thinning of coal seams over the high IS 9. Fence diagram of Unit I showing lithofacies distribution 1* 10. Isopach map of combined thickness of 3 major coal seams in coal zone 1; seams IB, IC, and ID 2( 11. Depositional environment of Unit 1 3\\ 12. Cross-section through Unit II showing lithofacies distribution 3' 13. Depositional environment of Unit II 4; 14a. Cross-section through Unit III showing lithofacies distribution 4' 14b. Location of cross-section in Figure 15a 4J 14c. Line drawing of outcrop with massive sandstone lithofacies, in roadcut near drillhole 326 5( 15. Shoreline related peat-forming environments 6'. 16. Distribution of coal zones in Unit III 6'. 17. Isopach maps of coal zones 4 and 5 (combined), and of the sandstone immediately underlying the coal zones 6-18. Depositional environment of Unit III 6'. 19. Cross-section of the North Telkwa region of the Telkwa coalfield 1. 20. Range in total sulphur content of each seam in Unit III (raw and washed) 8' 22. Raw total sulphur content of seam 3U relative to the presence or absence of brackish, tidal flat sandstone above it 8( i x 22. Raw total sulphur content of seam 9 relative to the thickness of terrestrial sediments between the seam and marine sediments of Unit IV 87 23. Plot of raw total sulphur content versus washed total sulphur content for coal zone 2 90 24. Plot of raw total sulphur content versus washed total sulphur content for coal zone 3 91 25. Plot of raw total sulphur content versus washed total sulphur content for coal zones 4 and 5 92 26. Plot of raw total sulphur content versus washed total sulphur content for coal zones 6 and 7 93 27. Plot of raw total sulphur content versus washed total sulphur content for coal zones 8, 9, and 10 94 28. Percent ash distribution within coal zone 2 99 29. Percent ash distribution within coal zone 3 100 30. Percent ash distribution within coal zones 4 and 5 101 31. Percent ash distribution within coal zones 6 and 7 102 32. Percent ash distribution within coal zones 8, 9, and 10 103 33. XRD reflections from untreated sample of mottled claystone, compared to XRD reflections from greenolite and quartz 126 34. XRD relections from untreated sample of fireclay, compared to XRD reflections from greenolite and quartz 127 35. X R D reflections from untreated sample of carbonaceous mudstone, compared to XRD reflections from greenolite and quartz 128 36. XRD reflections from untreated sample of mottled claystone, compared to XRD reflections from kaolinite and chlinochore 129 37. XRD relections from untreated sample of fireclay, compared to XRD reflections from kaolinite and chlinochore 130 38. XRD reflections from untreated sample of carbonaceous mudstone, compared to XRD reflections from kaolinite and chlinochore 131 39. XRD reflections from heated sample of mottled claystone 133 40. XRD reflections from heated sample of fireclay 134 41. X R D reflections from heated sample of carbonaceous mudstone 135 X LIST O F T A B L E S Table I. Major compositional differences between sandstones of Units I, II, III and IV 77 Table II. Typical coal quality of coal from the Telkwa coalfield 82 Table UJ. Ash content of seams in Unit III 97 x i LIST OF P L A T E S Plate 1. a) Conglomerate fining-upward sequence, b) Rooted sandstone 22 Plate 2. a) Intraclast-ricb sandstone, b) Intraclast-rich sandstone with large rounded mudclasts. c) Soft sediment deformation, d) Argillaceous sandstone 24 Plate 3. a) Carbonaceous mudstone with plant fossils, b) Seatearth 26 Plate 4. Mottled claystone 28 Plate 5. a) Silty mudstone with Helminthopsis trace fossils, b) Qphiomorpha trace fossil 36 Plate 6. a) Boring bivalves (Teredo) in fossilized wood, b) Interbedded sandstone and mudstone with Planolites and Skolithos trace fossils 37 Plate 7. Calcium carbonate concretions 38 Plate 8. a) Macaronichnus trace fossils, b) Mottled argillaceous sandstone with Rosselia trace fossil, c) Cross-bedded sandstone 40 Plate 9. Wavy-bedded sandstone 50 Plate 10. a) Teichichnus trace fossil in bioturbated sandstone, b) Zoophvcus trace fossil in bioturbated sandstone, c) Syneresis cracks in lenticular-bedded siltstone and mudstone 52 Plate 11. a) Cycad fossil in lenticular-bedded siltstone and mudstone. b) Algal mats in lenticular-bedded siltstone and mudstone 54 Plate 12. Photomicrograph of algal mats 55 Plate 13. a) Hexagonal, monocrystalline, corroded \"volcanic'' quartz grain, b) Volcanic rock fragment 74 x i i A C K N O W L E D G E M E N T S I am indebted to my thesis advisor, Dr. Marc Bustin, for his continued support, advice, and critical reviews. I also wish to think Drs. G. Rouse and W. Barnes, members of my advisory committee, and Drs. R. Johnson and J. Murray, members of my examining committee, for many useful comments. The staff of Crows Nest Resources are thanked for making the project possible by supplying data; Brian McKinstry, of the same company, was especially supportive and helpful. I am grateful to the British Columbia Ministry of Energy, Mines, and Petroleum Resources for financial support. Jim Carlaw provided valuable field assistance, and the Kerr family, of Telkwa, helped at every opportunity during the field season. My good friends Jarand Indrelid, Jonny Hesthammer, Julie Hunt, Michelle Lamberson, Arne Toma, Doni Jacklin, Harrison Cookenboo, Steve Cook, Keith Everard, Susan Taite, Peter Lewis and countless others helped me in every manner throughout the course of this study, and their friendship and kindness will not be forgotten. Lastly, I wish to thank my family and Bruce Ayrton for then-understanding, encouragement and support. i 1 I N T R O D U C T I O N Significant coal resources occur in the Lower Cretaceous Skeena Group near the town of Telkwa in central British Columbia. The coal deposits have been mined on a small scale since the early 1900s, and a major exploration project designed to delineate further exploitable coal reserves was initiated in the 1980s (Handy and Cameron, 1983). Early attempts to resolve the lithostratigraphy and interpret the depositional history of the coal measures were hampered by the lack of natural outcrops and subsurface information. As a result of recent exploration, a large number of drill cores, geophysical logs and coal quality data are now available, facilitating a detailed sedimentological and coal-quality study of the coal measures. The objectives of this study are: 1) to describe and define the stratigraphy and lateral facies changes of the coal measures in the Skeena Group; 2) to interpret the depositional history of coal measures in the Telkwa area; and 3) to relate the coal quality to depositional environment. The results of this study will contribute to the understanding of the regional geology of Cretaceous basins in the Intermontane Belt in central British Columbia, and will aid in the development of a stratigraphic framework for coal exploration in the central Cordillera. In addition, the results will aid in the development of depositional models to predict variations in coal quality in other basins. S T U D Y A R E A L O C A T I O N The Telkwa coalfield is in the Intermontane Belt of west-central British Columbia, approximately 18 kilometres south of Smithers, near the town of Telkwa (Figure 1). The Telkwa River runs through the coalfield, dissecting it into two geographical areas known locally as the North Telkwa and Goathorn regions. The Goathorn region, which has been commercially mined and extensively drilled, is the subject 2 6065500m N • SKEENA GROUP SEDIMENTS (Cretaceous) LXI HAZELTON GROUP VOLCANICS (Jurassic) LX1 INTRUSIVES (Late Cretaceous or Eocene) FAULT (assumed) Figure 1. Location of study area. Boxed areas are locations of drillhole maps in Figure 2. Modified after Maclntyre et al. (1989). 3 of this research. The sedimentology of the North Telkwa region will be discussed briefly and compared to the Goathorn region, as coal seams in the two regions are correlatable. The study area (hereinafter referred to as the \"Telkwa coalfield\") comprises about 24 square kilometres in NTS map sheet 93L/11. The northwest corner of the study area is located at 6 057 000 m N and 619 000 m E, and the southeast corner at 6 051 500m N and 623 000m E. DATA SOURCES From June through August of 1989, 40 cores (totalling approximately 4500 metres) from holes drilled in the Telkwa coalfield by Crowsnest Resources were logged. These cores are presendy stored in and around a coreshack at the old Telkwa mine site. Five additional cores (from holes drilled in late August in the same area by Dr. Alex Matheson for a separate British Columbia Ministry of Energy, Mines, and Petroleum Resources research project) totalling 300 metres were logged in December of 1989. These cores are presently stored at the Geological Survey of Canada Institute of Sedimentary and Petroleum Geology in Calgary. Ten outcrop sections were measured, totalling 100 metres. Drill core and outcrops were sampled for mineralogicaL paleontological and palynological analysis. Palynomorph assemblages were described and dated by Dr. Arthur Sweet, and trigonid macrofossils were dated by Dr. Terry Poulton; both of the Institute of Sedimentary and Petroleum Geology (Sweet, G.S.C. Report AS-90-01), Appendix 1; Poulton, G.S.C. Report J-10-1990-TPP, Appendix 2). Geophysical well logs (gamma-ray/long-spaced density or \"coal lithology\", and gamma-ray/neutron density) from 43 additional holes were examined to supplement the core and outcrop data. Four shallow reflection seismic profiles were obtained from the Coal Mining Research Company. The profdes are confidential but structural interpretations made from these profiles are discussed in this 4 paper. Coal quality data obtained from Crowsnest Resources includes raw and washed total sulphur and ash content of seams in coal zones two through ten, from 125 drillholes. Figures 2 and 3 show the location of drillholes in the study area from which core logs, geophysical logs, and quality data were obtained. The seismic profiles trend north-south and west-east through the middle of the study area. METHODS Detailed stratigraphic columns were drawn for all core and outcrops measured. Drill core was described at a decimetre scale. Sedimentary and biogenic structures, fossil content, color, bedding angles, and grain composition, size, rounding and sorting were described. The original core logs may be obtained from the geology reading room at the University of British Columbia. Using the core logs, nineteen stratigraphic cross-sections were constructed, five of which are presented in this paper. Cross-sections were not extended to the eastern edge of the study area, where the strata are more complexly deformed. Isopachous, iso-sulphur and iso-ash maps were constructed. Thicknesses for coal isopach maps were measured from wire line logs. Coal thicknesses could not be obtained from drill core, as most of the coal in the core had been previously removed for analysis. For sandstone isopach maps, sandstone thicknesses were measured from drill core. Sandstone petrography was determined from examination of nine thin sections and several hand specimens, and clay mineralogy was determined by X-ray diffraction analysis. Details of methods used for X-ray diffraction analysis are given in Appendix IV. Wherever possible, lithological interpretations are based on core logs instead of geophysical logs. Lithological interpretation from 5 NORTH TELKWA REGION in 6059500m N GOATHORN REGION 6051000m N Figure 2. Drillhole maps of the Goathorn and North Telkwa regions of the Telkwa coalfield, showing locations of isopach maps and ash and sulphur distribution maps. Area represented by Figure 2 is shown in Figure 1. Triangles represent drillholes which were core-logged, and asterisks represent holes which were not core-logged, but for which geophysical logs were obtained. Solid circles represent drillholes from which only quality data were obtained. NORTH TELKWA REGION 6059500m N GOATHORN REGION * 429 • . 2 3 421 401 35? 3 M 437 ! A | ( 436 1 430 432 | • A 337 • 1 2S< j 341 i • 340 j . k 433 1 338 * 219 i • j 1 352 320 322 j 402 3 2 3 * 235 i 235 * • 403 3J1 « ' ! 1 405 2 5 5 . | > 22S 4 0 > l 335 J 250 « 6051000m N Figure 3. Drillhole maps of the Goathorn and North Telkwa regions of the Telkwa coalfield, showing locations of cross-sections. Area represented by Figure 3 is shown in Figure 1. Drillhole symbols same as for Figure 2. 7 geophysical logs, aside from the recognition of coal seams, proved difficult due to poor definition of the typically argillaceous and volcanogenic sandstones in the Telkwa coalfield. Unfortunately, most of the core from the lower coal-bearing unit is in poor condition as a result of being stored outside. Therefore, lithological and depositional interpretations of the lower coal-bearing unit are based largely on drill core from nine holes. R E G I O N A L G E O L O G Y A N D P R E V I O U S W O R K The Telkwa coalfield is located on the northern flank of the Skeena arch, near the southern limit of sedimentary rocks in the Bowser Basin. The coal measures are included in the Lower Cretaceous Skeena Group, and are an erosional remnant of a larger Cretaceous basin referred to as the \"Nazko Basin\" by Hunt and Bustin (1990), which overlies the Jurassic Nechako Basin and includes the Methow Basin (Figure 4). The Telkwa coalfield is considered correlative with nearby coal measures at Denys Creek, Chisholm Lake, Zymoetz River, and Roche Deboule (Koo, 1984). In the Telkwa area, the coal-bearing strata are more than 500 metres thick and unconformably overlie Jurassic Hazelton volcanic rocks. The Skeena Group comprises a Lower Cretaceous sedimentary unit and an Upper Cretaceous volcanic unit referred to by Sutherland Brown (1960) as, respectively, the Red Rose and Brian Boru Formations. Tipper (1976) excludes the coal measures in the Telkwa area from the Red Rose Formation, and assigns them to undifferentiated Lower Cretaceous Skeena Group. Tipper (1976) restricts the term \"Red Rose Formation\" to interbedded shale and chert conglomerate. Koo (1984) makes a distinction between \"Red Rose coal measures\" and \"Telkwa coal measures\", and proposes the term \"Early Cretaceous Skeena coal measures\" for all coalfields in the Skeena Arch area Maclntyre et al. (1989) include the Telkwa coal measures in the Red Rose Formation. Figure 4. Tectonic elements of British Columbia. Modified after Gabrielse and Yorath (1989). 9 In this discussion, to avoid confusion, the sediments of the Telkwa coalfield are referred to as Lower Skeena Group. Figure 5 summarizes several published stratigraphic nomenclatures for the Skeena Group. -1 1 — I 1 I I - l 1 —i r-o> 8 a o c ll n cn O cr M n> C « n 2 3. c II 1 8 3 * § 8 ft —. II 5 c o o T O O II 0Q o £L 5 g OB en &> o'o g. f\" n o I* 2. » 3 U O Ct 9? cn Ct ct a r „ 3 » 2 s \" Ct cn ty <~ \" CT\" 3 II K 3 O Q. — OS o S. cr I I SS. B II g- -1 3 II Jurassic Cretaceous H A Z E L T O N G R O U P S K E E N A SERIES I? 5 coat-baaring Crst. sads. H A Z E L T O N G R O U P 1 = H A Z E L T O N G R O U P »5 > ->• CO Z Q CO I m ° o CD i CO H A Z E L T O N G R O U P B O W S E R L A K E G R O U P S K E E N A G R O U P H A Z E L T O N G R O U P B O W S E R L A K E G R O U P RED ROSE FORMATION BRIAN B0RU , g. - & 0 FORMATION Iff j l S K E E N A G R O U P 2 = > 33 < • < CO \"0 cn m 33 o 33 O 33 m o m O co co m o m z H CO o m 33 > CD b CO —I 33 o 33 > TJ O m z o 5 c 33 m oi 11 Deposition of Skeena Group sediments began during the Early Cretaceous, following regional uplift and erosion of the Skeena arch. The sediments of the Skeena Group were transported southwest across the arch from the Pinchi belt and Columbian orogen (Tipper and Richards, 1976). Sediments of the Lower Skeena Group are marine or continental and coal-bearing, and typically contain an abundance of fine-grained detrital muscovite (Leach, 1910; Sutherland Brown, 1960; Tipper and Richards, 1976). LOCAL STRATIGRAPHY AND STRUCTURE The Telkwa coalfield is in fault contact on all sides with the Lower Jurassic Telkwa Formation of the Hazelton Group (Maclntyre et al., 1989). Displacements on the faults are primarily vertical and estimated to be between 50 and 300 metres (Koo, 1983). In addition, several northeast and northwest striking high-angle faults dissect the coalfield. Recently obtained seismic data indicates that the Hazelton Group basement and lowermost coal-bearing strata in the western edge of the study area are offset by a nearly vertical north-south trending fault with an apparent displacement of approximately 80 metres (Figure 6). The upper coal-bearing strata are not cut by this fault, suggesting that an unconformity is present within the section. Minor nearly-vertical faults slightly displace the upper coal-bearing strata. In the southeastern corner of the coalfield, northwest striking lower angle reverse faults are present, and strata in this area are very disrupted. Steep bedding dips locally occur, and strata are repeated in some drill holes. The seismic profiles have poor resolution in the vicinity of these faults, so the dip angles and magnitudes of throw are difficult to ascertain. However, they have an apparent dip of approximately 45° with displacements of 10 to 30 metres. Porphyritic Late Cretaceous and Eocene dykes and sills intrude the coal measures throughout the coalfield, and a large granodiorite and quartz monzonite intrusion is present Figure 6. Cross-section showing offset of Unit I. Coal zone 1 is repeated in drillhole 225. The identical section, restored, is shown in Figure 8. Geophysical logs are gamma-ray and density. Location of cross-section shown in Figure 3. 13 in the North Telkwa region (Koo, 1983). These igneous intrusions locally alter the organic petrology of the coal significantly (Goodarzi and Cameron, 1989). More than 500 metres of Lower Skeena Group strata unconformably overly Hazelton Group volcanic rocks. Plant fossils found in Skeena Group sedimentary rocks in the Telkwa coalfield were dated as Early Cretaceous by Hacquebard et al. (1967). Palynomorph assemblages from the lower and upper coal-bearing units indicate that the strata are Early Albian or possibly Aptian or Barremian in age (Sweet, G.S.C. Report AS-90-01); Appendix 1). The presence of Distaltriangulatisporites sp. in the upper coal-bearing unit may indicate that the age of this unit to medial or late Albian (G. Rouse, pers. comm.). Trigonids from the marine unit between the lower and upper coal-bearing units are Albian or as old as Barremian (Poulton, G.S.C. Report J-10-1990-TPP; Appendix 2). Over most of the study area, the stratigraphic succession is divisible into four informal units based upon gross lithology (Figure 7). Coal occurs in ten \"zones'' (Handy and Cameron, 1983); each zone is named for one or more seams split by a thickness of organic-rich mudstone that is less than or equal to the thickness of the coal seams themselves. An exception is coal zone 1, in which all the laterally correlatable seams are grouped together as one zone, despite the fact that the seams may be separated by as much as 8 metres of carbonaceous mudstone. The four lithological units defined in this study correspond to those defined by Handy and Cameron (1983), and the three lowest units correspond roughly to those recognized by Koo (1983). The lowermost unit (Unit I) unconformably overlies volcanic basement and consists of fine to coarse-grained crossbedded sandstone, conglomerate, siltstone, mudstone and coal (coal zone 1). Conglomerate and sandstone contain an abundance of volcanic rock fragments and chert, and mudstone is kaolinitic (Appendices III and IV). Coal zone 1 contains a highly radioactive interval which is a regional marker on gamma ray logs. Unit II overlies coal zone 1 and consists primarily of monotonous silty mudstone, with occasional siltstone and sandstone 14 o 0 o 03 0 o 0 > h-o = CD 2 < 3 2 UJ UJ CO D C L U 5 -HAZELTON GROUP (Jurassic) WEST -I 400 m bright green sandstone/siltstone (regional marker) coarsening-upward sequence (regional marker) gamma-ray spike (regional marker on well logs) v V v v v v v V v v v v v v v v v v v V EAST vertical scale: 50m V V v v v v COal ( c o a l z o n e s numbered) mudstone siltstone sandstone conglomerate volcanic Figure 7. Representative sections of the Lower Skeena Group in the Goathorn region of the Telkwa coalfield. 15 beds. Sandstone is chert-rich and micaceous (Appendix III). The top of Unit II is defined by a 10 to 15 metre coarsening-upward sequence that serves as a regional marker on geophysical logs. Unit III, which overlies the coarsening-upward sequence, comprises chert-rich, micaceous sandstone, siltstone and mudstone (Appendix III), and up to nine coal zones (coal zones 2 through 10). The uppermost unit, Unit IV, overlies coal zone 10 and is characterized by monotonous silty mudstone similar to that in Unit II. A 2 to 4 metre thick bright green chloritic sandstone or siltstone marks the base of Unit IV and serves as a regional marker in drill core (Appendix III). The stratigraphic succession changes markedly from west to east (Figure 7). In the eastern margin of the study area, Unit III lacks sandstone and contains only the two lowest coal zones (coal zones 2 and 3). 16 SEDIMENTOLOGY OF THE GOATHORN REGION OF THE TELKWA COALFIELD Sedimentary strata of the Telkwa coalfield record a complex depositional history. In this chapter, the lithostratigraphy and depositional history of the Goathorn region are described in detail. U N I T O N E S E D I M E N T O L O G Y G E N E R A L D E S C R I P T I O N : Unit I comprises conglomerate, sandstone, siltstone, mudstone, and coal zone 1 (seams LA to IG) present between the unconformable, weathered contact with volcanic basement and the base of Unit II. Conglomerate and sandstone contain an abundance of volcanic rock fragments and chert grains, and mudstone is kaolinitic (Appendices III and IV). Unit I thickens northward from less than 30 metres to more than 100 metres, reflecting palaeotopographic relief on the volcanic basement (Figure 8). The thickness of Unit I may also be controlled by the depth of erosion during deposition of overlying, transgressive marine deposits of Unit II (Figure 12). In the western part of the study area, Unit I is tectonically thickened as a result of reverse faulting (Figures 5 and 6). The contact between Unit I and basement was observed in well logs from drill holes in the Goathorn region, and in drill core from just outside the study area in the North Telkwa region. Volcanic rocks are bleached from green to brown or maroon near the contact. Strata immediately above the contact consist of mottled claystone, conglomerate, or coarse sandstone. Overall, Unit I fines upward, from primarily conglomerate and sandstone to almost entirely mudstone and coal (Figure 7). The lower half of the unit is composed of fining-upward conglomerate 17 and sandstone sequences up to 10 metres thick. The fining-upward sequences are lenticular or sheet-like and have sharp, erosional bases. Carbonaceous mudstone and thin coaly beds cap the sequences. The upper half of the unit consists primarily of carbonaceous mudstone, seat earth, and 1 to 7 coal seams (1A to IG) in coal zone 1. However, coarser sediments (sandstone and conglomerate) are present within coal zone 1 in the northeastern part of the study area (Figure 9). Drillholes 425 and 354 contain sandstone and conglomerate beds above coal seam 1A (Figure 9). Sandstone and conglomerate is also present above coal seam ID in drillhole 354 and above coal seam IF in drillhole 361 (Figure 9). Coal seams IB, IC and ID are the thickest and most laterally extensive seams in the study area. The combined thickness of these seams averages 6.5 metres and ranges up to 11 metres thick. Generally, coal seams split and thin toward the northwest part of the study area (Figures 9 and 10). Geophysical logs from Unit 1 show a regional, distinctive gamma-ray spike between or within coal seams IB and IC (Figure 8). The source of the peak in gamma-ray intensity was not apparent in the core. LITHOFACIES DESRCIPTIONS: Unit I comprises eight lithofacies that occur regularly. Coarser-grained lithofacies are more abundant at the base of Unit I, and finer-grained facies predominate in the upper part. Detailed facies changes are illustrated in Figure 9. NW STRATIGRAPHIC CROSS-SECTION: UNIT I (PRE-FAULT) DH239 1.6km SE 0.45km 0.15km D H 2 2 3 D H 2 2 5 D H 2 2 5 D H 2 2 7 (BASE) (TOP) volcanic basement V V Figure 8. Cross-section of Unit 1 showing palaeotopography of the Jurassic Hazelton Group volcanic basement, and thinning of coal seams over the high. Identical section, unrestored, is shown in Figure 6. Geophysical logs are gamma-ray and density. Location of cross-section shown in Figure 20 UNIT I: COMBINED COAL ISOPACH COAL SEAMS 1B, 1C, AND 1D 6057000mN ro CO 3 m Figure 10. kopach map of combined thickness of 3 major coal seams in coal zone 1; seams IB, IC, and ID. Thickness in metres. Area represented by map shown in Figure 2. LITHOFACIES A: C O N G L O M E R A T E This lithofacies is composed of poorly to well-sorted clast-supported volcanic rock fragment and chert conglomerate, with local pebbly sandstone interbeds (Plate la). Clasts are granule to pebble-sized, and sub-angular to sub-rounded. It is light green when fresh and reddish-purple when weathered. Individual conglomerate beds form fining-upward sequences up to 4 metres thick. The basal contact is sharp and erosional, whereas the upper contact is gradational or sharp. Internal stratification is generally not well developed, except in moderately to well-sorted beds, in which elongate clasts are commonly imbricated. Mud drapes, pyritized mud clasts and large coal spar are common. This lithofacies is usually interbedded with massive sandstone. LITHOFACIES B: MASSIVE SANDSTONE The massive lithofacies is characterized by up to 4 metres of light to medium grey-green, fine to medium-grained sandstone. Grains are primarily volcanic rock fragments or chert, and are sub-angular to sub-rounded. The lower contact is gradational or sharp and the upper contact is gradational. Usually, the lithofacies fines upward. Horizontal lamination and high-angle planar-cross bedding commonly occurs. Carbonaceous laminae are abundant throughout, and mudstone laminae are common in the upper part of the lithofacies. Granule and pebble-rich beds are common. Near the base of the lithofacies, scour structures filled with mudclasts, coarse sand, granules and coal spar are widespread. Ripples, mud drapes, rootlets and desiccation cracks are occasionally present near the top (Plate lb). Massive sandstone is usually interbedded with conglomerate and carbonaceous mudstone. Plate 1. a) Conglomerate fining-upward sequence. b) Rooted sandstone from upper part of massive sandstone lithofacies. 23 LITHOFACIES C: INTRACLAST-RICH SANDSTONE The distinguishing characteristics of this sandstone is the presence of abundant rounded or angular mudstone clasts, partially replaced by siderite or pyrite, which occur in a poorly sorted matrix of coal spar, mudstone, fine to medium-grained sandstone and granules (Plate 2a). Where mudstone clasts are most abundant, the lithofacies is a matrix-supported intraclast conglomerate (Plate 2b). Lithofacies C averages 3 metres in thickness with sharp upper and lower contacts, and locally, the lithofacies fines upward. Scour structures commonly occur. In the upper part of the lithofacies, sorting improves to moderate, carbonaceous laminae are abundant, and parallel bedding is well developed. Thin (1 centimetre) mudstone beds, typically distorted by soft-sediment deformation, are interbedded throughout the lithofacies (Plate 2c). LITHOFACIES D: ARGILLACEOUS SANDSTONE The argillaceous sandstone lithofacies comprises fine-grained sandstone up to 3 metres thick, with abundant carbonaceous laminae and millimetre to centimetre-scale carbonaceous mudstone beds (Plate 2d). Lower and upper contacts are sharp or gradational. The lithofacies may fine or coarsen upward. Small silt and sand filled scours are common. Soft sediment deformation structures, mudcracks, and rootlets are occasionally present. Well preserved macroscopic plant fossils occur rarely. LITHOFACIES E: CARBONACEOUS MUDSTONE Lithofacies E consists of medium to dark grey, thinly laminated, carbonaceous, kaolinitic mudstone with thin coal stringers (Appendix IV). It is up to 10 metres thick, and Plate 2. a) Intraclast-rich sandstone. b) Intraclast-rich sandstone with abundant large, rounded mudclasts. c) Soft sediment deformation structures from upper part of intraclast-rich sandstone lithofacies. d) Argi l laceous sandstone with abundant carbonaceous laminae. 25 upper and lower contacts are gradational. Rootlets and well-preserved plant fossils are usually present (Plate 3a), and the palynomorph content is dominated by miospores and gymnosperm pollen (Sweet, G.S.C. Report AS-90-01); Appendix 1). Scour horizons and centimetre-scale sandstone beds and scours are common. Pyrite occurs associated with organic debris, or as isolated blebs. Rarely, sand grains are scattered within the mudstone. Carbonaceous mudstone is interbedded with all other lithofacies. LITHOFACIES F: COAL Coal in Unit I is dull, banded, or bright, and frequently contains pyrite as blebs or in cleats. Individual seams are up to 6 metres thick, and coal zones (coal and partings) may exceed 12 metres in thickness. Partings are laterally extensive, thin, tabular, and fine-grained. Rarely, partings are lenticular sandstone bodies. Coal is gradationally underlain by carbonaceous mudstone or fireclay, and is gradationally or sharply overlain by a number of facies. LITHOFACIES G: FIRECLAY Fireclay consists of light pink-grey, very fine-grained, kaolinitic mudstone up to 6 metres thick (Appendix IV). It contains abundant, well preserved (occasionally pyritic) rootlets, large coal spar, and spherical orange siderite nodules (Plate 3b). Fractures are conchoidal and slickensided. This lithofacies may be up to 6 metres thick. The lower and upper contacts are gradational, and the upper contact is usually mottled. In some localities, the lowermost part of this lithofacies consists of up to 30 centimetres of dark grey carbonaceous mudstone with abundant red spherulitic siderite grains. Rarely, the uppermost part of the lithofacies has a pisolitic texture (Plate 3b). In outcrop, fireclay is very resistant. Fireclay overlies any lithofacies, and is usually overlain by carbonaceous mudstone or coal. 26 Plate 3. a) Carbonaceous mudstone with well-preserved plant fossils. b) Seatearth with pisolitic texture near top of sample and roots throughout. 27 LITHOFACIES H: MOTTLED CLAYSTONE This lithofacies has a mottled appearance, and consists of very fine-grained, reddish-purple and light green, kaolinitic mudstone with conchoidal and slickensided fracture surfaces (Appendix IV; Plate 4 ) . The thickness rarely exceeds 2 metres and lower and upper contacts are gradational. Rootlets are locally present, and reddish-colored mottles contain abundant sub-millimetre siderite spherulites. Mottled claystone is interbedded with carbonaceous mudstone, and is only found in the lower third of Unit I. Locally, it directly overlies volcanic basement. DEPOSITIONAL ENVIRONMENTS OF LITHOFACIES: Unit I comprises alluvial sediments derived from, and deposited on, the underlying irregular, eroded, deeply weathered volcanic land surface. Braided river and floodplain facies are recognized. BRAIDED RIVER (LITHOFACIES A, B, C AND D) In the study area, braided river channel deposits are represented by two facies associations. The most common association is composed of cyclic, 0.5 to 1.0 metre beds of conglomerate and massive sandstone. Poorly sorted conglomerates are channel lag deposits, and better sorted, clast-supported, imbricated conglomerate and massive sandstone represent longitudinal bars of braided river systems (Miall, 1977). Cross-bedded sandstone was deposited on the margins and downstream end of bars. Bar tops are represented by beds of rippled sandstone, mud drapes, desiccation cracks and roots. Random lithofacies patterns, such as are present in this lithofacies association, are produced in braided river systems where channels and bars shift rapidly and only fragmented bars and channel fills are preserved. A complex history of erosion and deposition are recorded in the preserved deposits. Plate 4. Mo t t l ed claystone. 29 A second lithofacies association is a vertical fining-upward sequence of conglomerate overlain by cross-bedded sandstone. This association is interpreted to be the deposits of a single channel. The presence of finer sediments at the top is indicative of waning flow. Lithofacies C and D represent higher levels of the braid plain, which were active only during stages of high flood. During high stages, water and sediment spilled out of the main channels and spread over the floodplain. Coarse sediment and large mudclasts in lithofacies C were deposited as bedload in reactivated channels. The presence of fine sediment together with poorly sorted sand, granules, pebbles and mud clasts is indicative of rapid sedimentation. Finer, parallel bedded sandstone and mudstone were deposited during waning flow, and locally, bedding was convoluted during subsequent dewatering. Thinly interbedded sandstone, mudstone, and carbonaceous material in lithofacies D reflect repeated inundation of the floodplain by sediment-laden water. Periods of inactivity in the higher levels of the braid plain are represented by mudcracked and rooted horizons. FLOODPLAIN (LITHOFACIES E, F, G, AND H) Carbonaceous mudstone and thin peat beds accumulated as vertical accretion deposits in low energy floodbasins and backswamps away from active channels. Well-preserved plant fossils together with thinly laminated mudstone reflect slow deposition from suspension in low-energy conditions. The high kaolinite content of samples of the mudstone suggests that leaching occurred to some degree (Appendix IV). Mudstone with interbedded sandstone and scattered sand grains represent parts of the floodplain which were proximal to active channels and frequently received coarser sediment during overbank flooding and wind storms. Kaolinitic, rooted fireclays are seat earths, and represent leaching and soil development on portions of the floodplain characterized by decreased sediment supply and lower water table. Siderite nodules in seat earths precipitated from slightly reducing ground water in saturated soils (Reading, 30 1976; Leckie et al., 1989). The characteristic, slickensided fracture of seat earths in the study area developed as a result of collapse and compaction of roots (Huddle and Patterson, 1961) and peds (Leckie et al., 1989). Mottled claystone also represents soil development, despite a paucity of carbonaceous matter other than occasional rootlets. The kaolinitic composition reflects leaching, and the mottled texture is indicative of poorly drained conditions with a high water table (Leckie et al., 1989). The rarity of carbonaceous matter may be attributable to long-term exposure and oxidation of the organic-rich layer. Seat earths in Unit I are commonly overlain by thick, laterally extensive coal seams. Peat formation reflects a change to more submerged conditions, in which preservation of a thick organic layer was favored. Thicker peat beds were preserved where peat accumulation kept pace with subsidence and water table rise. Laterally extensive, tabular mudstone splits in the coal seams represent periods of increased subsidence and associated increase in terrigenous influx. D E P O S I T I O N A L H I S T O R Y O F U N I T I: An alluvial environment persisted throughout the deposition of Unit I. Deposition began with intense weathering and local soil development on the Jurassic volcanic land surface. With continued weathering of surrounding volcanic rocks, braided rivers spread pebbles, granules and coarse sand derived from the volcanics across the study area. Thick packages of coarse sediment accumulated in a topographic low in the northern part of the study area. Floodplains were developed in the interchannel areas, but preservation of carbonaceous mud and peat was hampered because of frequent erosion by migrating channels. 31 As the topography was levelled (by erosion of highs and deposition in lows), a peat-forming floodplain was established, resulting in the formation of coal zone 1 (Figure 11). Peat formation was interrupted by terrigenous influx during periods of accelerated subsidence. Peat development was also disrupted by periods of decreased subsidence and relative stability, leading to the formation of seat earths. Peat deposition climaxed with the formation of seams IB, IC, and ID, which are thick, laterally extensive seams. In the southern part of the study area, seam IB is missing and seam IC is very thin over a palaeotopographic high on the underlying Jurassic volcanic basement, suggesting that peat marshes over the high were better drained than in other areas (Figures 8 and 11). While peat deposition prevailed in the southwest, clastic deposition continued in the northeast. Coal seams tend to thin and split in a northeastward direction, and more of the partings are composed of sandstone, likely reflecting periodic flooding and erosion of peat proximal to channels. The overall fining upward sequence observed in Unit I (from predominantly coarse-grained deposits at the base to exclusively fine-grained sediments and coal at the top) reflects abandonment of the active braid plain and development of a poorly drained floodplain and backswamp, probably as a result of denudation of the source area and waning of sediment supply without tectonic rejuvenation. A marine transgression halted deposition of Unit I. 32 Figure 11. Depositional environment of the upper strata of Unit I. Peat formed in poorly drained backswamps in a fluvial environment. Clastic deposition continued in the northeastern part of the study area. 33 U N I T T W O S E D I M E N T O L O G Y G E N E R A L D E S C R I P T I O N : Unit II comprises 110 to 140 metres of grey muddy siltstone interbedded with light grey-green beds of chert-rich, micaceous, bioturbated or cross-bedded sandstone. Details of the sandstone petrography of Unit II are presented in Appendix III. The contact between Unit I and II is usually sharp, but is not defined by the presence of a particular marker bed; rather, it is denoted by the occurrence of bioturbated sandstone or siltstone on top of essentially unbioturbated, fluvial deposits of Unit I. The uppermost strata of Unit II comprise a 10 to 15-metre thick, regionally extensive coarsening-upward sequence, abruptly overlain by coal zone 1 of Unit III. The coarsening-upward sequence consists of silty mudstone with an upward increasing abundance of planar, lenticular, and wavy bedded siltstone or fine-grained sandstone. L I T H O F A C I E S DESCRIPTIONS-. Five lithofacies are recognized in Unit II. Lithofacies A through E are scattered laterally and vertically throughout the unit, and lithofacies F is restricted to the western part of the study area. Lithofacies are difficult to correlate laterally, for facies changes are abrupt (as illustrated in Figure 12). Few drill holes penetrated thick sections of Unit II, so no complete section of was core logged. Figure 12. Cross-section through Unit II showing lithofacies distribution. Lithofacies A: silty mudstone. B: interbedded sandstone and mudstone. C: mottled argillaceous sandstone. D: carbonaceous mudstone. E: cross-bedded sandstone. 3 5 LITHOFACIES A: SILTY MUDSTONE Lithofacies A is up to 30 metres thick and is composed dominantly of light grey highly bioturbated silty mudstone. Contacts with underlying and overlying lithofacies are gradational or sharp. The massive, structureless appearance of this lithofacies is a result of extensive biogenic reworking. The only readily identifiable trace fossil in the mudstone is Helminthopsis. which is abundant, especially in siltier layers (Plate 5a). Physical sedimentary structures are rare, consisting of 1 to 4 centimetre thick, wavy or graded beds of very fine-grained sandstone with occasional Planolites burrows. Locally, 3 metre thick beds of very fine-grained, bioturbated (Helminthopsis and rare Ophiomorpha?1 sandstone occur interbedded in the silty mudstone (Plate 5b). Marine fauna in lithofacies A consist of gastropods, inoceramid-like pelecypods, trigonids (Mvophorella?1. scaphopods (Dentalium?! and boring bivalves (Teredo') (Smith, pers. comm., 1990; Poulton, G.S.C. Report J-10-1990-TPP; Appendix 2; Plate 6a). A diverse population of dinoflagellates are present throughout and are locally abundant, whereas terrestrial spores and pollen are rare to abundant (Sweet, G.S.C. Report AS-90-01); Appendix 1). Siderite bands and concretions and pyritized coal spar are common, and carbonaceous laminations are rare. Thin (less than 20 centimetres) limestone beds occur in silty mudstone near the top of Unit II. They comprise microscopic calcium carbonate concretions, partially replaced by chert, in a muddy matrix (Plate 7). Contacts between adjacent concretions are polygonal. LITHOFACIES B: INTERBEDDED SANDSTONE AND MUDSTONE This lithofacies is characterized by moderately bioturbated, thinly interbedded light grey-green to green, fine to medium-grained sandstone and mudstone (Plate 6b). The thickness may exceed 15 metres. The lower contact is frequently sharp, and the upper contact is gradational or Plate 5. a) Siltv mudstone with Helminthopsis trace fossils. Bedding defined by lighter-colored, sil l ier layer. b) Very fine-grained sandstone and well-preserved Oph iomorpha i ? ) trace lossil in silty mudstone lithofacies. 27 Plate 6. a) Bor ing bivalves (Teredo) in fossilized wood from siity mudstone lithofacies. b) Interbedded sandstone and mudstone. with abundant Planolites trace fossils and a Skolithos trace fossil near bottom of photo. Plate 7. Calc ium carbonate concretions partially replaced bv chert. sharp. Generally, the lithofacies coarsens upward, and then abruptly fines to lithofacies A. Fine organic detritus and siderite concretions are abundant. Wavy and parallel bedding is present throughout, and massive sandstone is common in the upper part. Planar cross-beds, graded beds, scour structures and carbonaceous laminations also occur. Bedding is frequently disrupted by Skolithos. Planolites. and Teichichnus trace fossils, especially near the base; and Macaronichnus is locally present in massive sandstone near the top of the lithofacies (Plate 8a). LITHOFACIES C: MOTTLED ARGILLACEOUS SANDSTONE This lithofacies is up to 4 metres thick and comprises poorly sorted, highly bioturbated fine to medium grained argillaceous sandstone (Plate 8b). The sandstone usually has a gradational basal contact and a sharp upper contact. The ichnofossil content includes Rosselia?. and other poorly-defined, large, mud filled and sideritized burrows. Isolated pelecypod shells locally occur. LITHOFACIES D: CARBONACEOUS MUDSTONE Dinoflagellate-bearing, carbonaceous mudstone, up to 3 metres thick, with thin, root-mottled beds and coaly intervals define this lithofacies (Sweet, G.S.C. Report AS-90-01); Appendix 1). Contacts with underlying and overlying lithofacies are gradational. Argillaceous coal seams less than a metre thick are rare. Carbonaceous mudstone is interbedded with all other lithofacies. Plate 20 THICKNESS OF COAL ZONES FOUR AND FIVE THICKNESS IN METRES: H <1 1-2 2-3 3-4 >4 Figure 17. Isopach maps of coal zones 4 and 5 (combined), and of the sandstone immediately underlying the coal zones. Thickness in metres. Boxed area represents same area shown as the 'Goathorn Region' in Figure 2. cn 4^ 65 \\ Figure 18. Depositional environment of Unit III. Restricted nearshore marine, tidal flat, tidal channel, and coastal marsh environments existed. 66 U N I T I V S E D I M E N T O L O G Y G E N E R A L DESCRIPTION: Unit IV abruptly overlies Unit III and consists of a laterally extensive, bright green, chert-rich, chloritic sandstone or siltstone bed at the base, overlain by massive grey silty mudstone similar to that of Unit II. The petrography of the basal sandstone is described in detail in Appendix III. Koo (1983) reports a thickness of 150 metres for Unit IV; only the basal 40 metres were core logged in this study. Quaternary sediments unconformably overlie Unit IV, and in most of the study area, the majority or all of Unit IV has been eroded. LITHOFACIES DESCRIPTIONS: The basal 40 metres of Unit IV comprise two lithofacies; green sandstone and silty mudstone. The sandstone petrography of the basal sandstone is presented in Appendix III. Handy and Cameron (1984) and Koo (1983) examined longer sections of Unit IV and report the presence of additional lithologies. LITHOFACIES A: GREEN SANDSTONE Lithofacies A consists of bright green, chloritic, massive fine-grained sandstone or siltstone. It is 1 to 5 metres thick, and always sharply overlies Unit III. The upper contact is gradational with grey muddy siltstone (lithofacies B). The sandstone is regionally correctable across the study area. Generally, the sandstone appears massive, but in places, it appears mottled by bioturbation. Coal spar, 67 fine organic detritus, and large, poorly defined, pyritic, sand-filled burrows are common. Mudstone rip-up clasts are locally present. LITHOFACIES B: SILTY MUDSTONE This lithofacies comprises structureless (completely bioturbated) silty mudstone with rare 1 to 5 centimetre thick parallel beds of slighdy bioturbated (PjanoHtes?) siltstone or fine sandstone. Helminthopsis trace fossils are abundant, and are particularly apparent in siltier zones. Siderite bands and concretions, pyritized coal spar, and carbonaceous matter commonly occur. Silty mudstone contains rare to common dinoflagellates, and a relatively high abundance of terrestrial spores, pollen, and fusinite (Sweet, G.S.C. Report AS-90-01); Appendix 1). This lithofacies is very similar to silty mudstone in Unit II. DEPOSITIONAL ENVIRONMENTS OF LITHOFACIES: Unit IV was deposited in a marine environment. Following transgression and deposition of a lag sandstone on top of the sediments of Unit IU, a quiet water nearshore marine environment prevailed. TRANSGRESSIVE LAG (Lithofacies A; green sandstone) The sheet-like geometry and erosive basal contact of the green sandstone lithofacies are typical characteristics of transgressive lag deposits. During a marine transgression, sediments of Unit Ill were eroded, reworked, and redeposited over the old coastal plain. The presence of marine silty mudstone (lithofacies B) overlying the sandstone is consistent with a marine transgression. The abundance of chlorite in Unit IV may reflect the change from a terrestrial to a paralic/marine depositional environment. Chlorite is commonly concentrated in lagoonal and nearshore environments where iron-bearing rivers enter the sea, and mixed-layer montmoriilonite/ilhte converts to chlorite (Folk, 1974). Additional chlorite may also have been produced during weathering of the uppermost sediments of Unit III, for chlorite can be formed from weathering of other clay minerals in soils (Curtis, 1984). QUIET NEARSHORE MARINE (Lithofacies B; silty mudstone) Silty mudstone in Unit IV is interpreted to have been deposited in a quiet, nearshore marine environment because of several facts: the combined presence of dinoflagellates and abundant terrestrial spores, pollen, and fusinite, the presence of quiet-water marine ichnofossils, and the fine-grained, completely bioturbated texture of the lithofacies. In Unit IV, delta facies, such as distributary channels, were not recognized, so it is uncertain if silty mudstone in Unit IV was deposited in an interdistributary bay or in another type of low-energy coastal environment. DEPOSITIONAL HISTORY O F UNIT IV: Unit IV was deposited during a marine transgression. During transgression, the uppermost sediments of Unit III were winnowed and reworked by shallow marine wave, current, and tide processes and redeposited as a sheet sandstone. A quiet, nearshore marine environment became 6 9 established. Deposition in this environment was primarily from suspension, but coarser sediment was periodically transported in during storms. Coal seams and dinoflagellate-barren sediments are present in the upper Unit IV (Handy and Cameron, 1984; Koo, 1983), indicating that terrestrial conditions resumed later in the depositional history of Unit IV. STRATIGRAPHY AND SEDIMENTOLOGY OF THE NORTH TELKWA REGION OF THE TELKWA COALFIELD Eight cores from the North Telkwa region were examined, facilitating a comparison of the stratigraphy and sedimentology of the North Telkwa and Goathorn regions. S T R A T I G R A P H Y The lithostratigraphy of the Lower Skeena Group in the North Telkwa region is very similar to that described for the Goathorn region. In the North Telkwa region, the strata overlie volcanic basement and are divisible into the same four units. Unit III and incomplete sections of Units II and IV were penetrated by drillholes in the western part of the study area, and Unit I and thin sections of Unit II were encountered in a few holes drilled into uplifted fault blocks on the eastern perimeter (Figure 19). Three marker beds present in the Goathorn region are also present in the North Telkwa region: the gamma-ray spike in coal zone 1 of Unit I, the coarsening-upward sequence at the top of Unit II, and the green sandstone at the base of Unit IV. Lithofacies present in the Goathorn region also occur in the North Telkwa region. The distribution of the lithofacies is similar, with some exceptions in unit III. Silty mudstone, an important lithofacies in the eastern part of Unit III in the Goathorn region, does not occur in the North Telkwa region (Figures 14a, 14b, and 19). In addition, sandy lithofacies are much less prevalent in the North Telkwa region than in the Goathorn region. In the Goathorn region, Unit III contains two major sandstone beds (above coal zones 3 and 7) and several thinner sandstone beds, whereas in the North Telkwa region, only one thick sandstone bed is present, above coal zones 6 and/or 7 CROSS-SECTION: NORTH TELKWA REGION, TELKWA COALFIELD NW SE DH 811 DH 804 DH 805 DH 814 DH 440 DH 504 DH 218 DH 443 DH 444 1 — 340m — 1 1 500m ' 340m — ' '-150m - 1 ~ 1040m ~ L208m - 1 306m — 1 ' 382m — ' Figure 19. Cross-section of the North Telkwa region of the Telkwa coalfield showing lithofacies distribution. Lithofacies abbreviations same as in text; first digit of abbreviation refers to unit number. Geophysical logs are gamma-ray and density. Coal zones of Unit III and coal seams of Unit I are labelled. Location of cross-section shown in Figure 3. 72 (Figures 14a, 14b, and 19). Consequently, Unit III is thinner in the North Telkwa region, with a maximum thickness of approximately 70 metres as compared to an average of 90 metres in the Goathorn region. In the North Telkwa region, Unit III thickens northwestward, due to the presence of a thick clastic wedge between coal zones 5 and 6 in the western part of the region (Figure 19). Coal zones in the North Telkwa region are correctable with those in the Goathorn region, and the same nomenclature can be used, although seams in the North Telkwa region tend to thicken, thin, split, or pinch out over short distances (Figure 19). The thicknesses of individual seams average 1 to 3 metres, comparable to seam thicknesses recorded in the Goathorn region. Coal zones in the North Telkwa region, particularly coal zone 5, thicken southeastward, and interburden thins. A zone of no coal development, such as is present in the eastern part of the Goathorn region, does not occur in the North Telkwa region. In the North Telkwa region, two additional thick seams are present below coal zone 1 (Figure 19). These may be correlative to a thin, discontinuous, argillaceous coal seam present at approximately the same stratigraphic horizon in the Goathorn region (Figure 8). D E P O S I T I O N A L E N V I R O N M E N T S The depositional environments that prevailed during deposition of the Lower Skeena Group in the Telkwa coalfield were very similar in the Goathorn and North Telkwa regions, although some minor differences existed. Peat deposition in Unit I of the North Telkwa region began earlier than in the Goathorn region, resulting in the development of thick seams below coal zone 1. In Unit III of the North Telkwa region, lagoons did not develop, and sandflats and mudflats were not established until after the deposition of coal zone 6. Deposition occurred primarily in upper intertidal flats and coastal marshes. 73 S A N D S T O N E P E T R O G R A P H Y A N D P R O V E N A N C E PETROGRAPHY Sandstones from throughout the stratigraphic section were sampled, and representative samples from each of the four lithostratigraphic units were examined in thin section. All of the sandstones are litharenites, using the sandstone classification scheme of Folk (1974), but this does not reflect the wide compositional variety of the samples. The results of the thin section analyses are presented in Appendix 3, and are discussed in the following section. U N I T I: The main framework grains are chert (30%), volcanic clasts (20%), and quartz (35%), with lesser amounts of sedimentary rock fragments and feldspar and rare muscovite and chlorite. The matrix is composed of pore-filling carbonate cement, with thin rims of iron oxide around many of the grains. Quartz grains are either monocrystalline or polycrystalline. Monocrystalline quartz has straight extinction and may be hexagonally shaped with corrosion embayments (Plate 13a). Polycrystalline quartz is altered and partially replaced by clay minerals and comprises equidimensional grains with sutured or straight boundaries. Volcanic rock fragments are dark and fine-grained, and commonly contain numerous plagioclase laths (Plate 13b). Felted texture or, less commonly, trachytic texture, usually developed. Sedimentary rock fragments comprise dark brown mudstone and organic i matter. Plagioclase is the dominant feldspar, and potassium feldspar is rarely present. Feldspar is usually heavily altered and partially replaced by calcite or, less commonly, by clay minerals. 74 13. a) Hexagonally shaped, monocrystalline quartz grain with corrosion embayments. indicative of provenance from a volcanic source, b) Volcan ic rock fragment at right, with chert grains and carbonate cement. 75 UNITS II A N D III: The sandstone petrography of Units II and III is very similar and will be described together. Framework grains consist of chert (30%), quartz (25%), sedimentary rock fragments (25%), and chlorite (15%), with minor amounts of muscovite and rare volcanic rock fragments and feldspar. All but the quartz grains are heavily altered. The matrix is composed of organic-rich, brown argillaceous material. Monocrystalline quartz with straight extinction is much more abundant than polycrystalline quartz. Rarely, 'stretched' grains of polycrystalline quartz, composed of sub-parallel elongate crystals, were recognized. Sedimentary rock fragments consist of carbonaceous mudstone and organic matter. Iron-rich chlorite occurs as light-green rounded grains with anomalous blue interference colors and no visible cleavage. It is not apparent if the chlorite is replacing another mineral. U N I T IV: The basal, transgressive lag sandstone of Unit IV is petrographically similar to sandstone in Unit III in all respects except chlorite abundance. In Unit IV, iron-rich chlorite is much more abundant (40%) and is the main framework grain. The chlorite may be a replacement mineral, but it is not apparent what type of grain it is replacing. 76 PROVENANCE An eastern source has been suggested for the Skeena Group, based upon sparse paieocurrent data (Eisbacher, 1981). The composition of sandstone in the Telkwa coal measures is agreeable with an eastern source, and also indicates an additional, local volcanic source for the lowermost sediments. In the Lower Skeena Group at Telkwa, chert and other sedimentary rock fragments are abundant throughout the stratigraphic section (Table I), reflecting continued clastic input from the chert and argillite-rich Cache Creek Group, which was uplifted as part of the Pinchi Belt-Columbian Orogen (Tipper and Richards, 1976). t Unit I, at the base of the Lower Skeena Group, is enriched with dark, fine-grained volcanic rock fragments (Table I). There is also an abundance of \"volcanic\" quartz, a type of quartz consisting of whole or fragmented bipyramidal crystals with corrosion embayments that is an excellent indicator of volcanic provenance (Plate 13a; Folk, 1974). A likely source of the volcanic rock fragments and volcanic quartz in the sediments is the Jurassic Hazelton Group, which the Skeena Group unconformably overlies. Among other lithofacies, the Hazelton Group comprises rhyolitic to basaltic tuffs and flow rocks similar to fragments found in the Skeena Group (Tipper and Richards, 1976). In Units II, III and IV volcanic rock fragments are rare and volcanic quartz is not present, and muscovite is relatively abundant (Table I). Although the thin section analyses indicate an increase in muscovite of only a few percent, the increase is much more apparent in hand specimens. Muscovite is derived chiefly from metamorphic rocks, and is a good indicator of metamorphic provenance. The presence of \"stretched\" quartz is also indicative of a metamorphic source. The source of sediments in Units II and III is probably metamorphic rocks of the Omineca Belt, which underwent considerable uplift (1 to 3 millimetres per year) and erosion during the Upper Jurassic and Lower Cretaceous (Parrish, 1979; Eisbacher, 1981). 77 Units II, III, and IV are enriched with chlorite (Table I), which may reflect increased input from a metamorphic source, for chlorite is a common metamorphic mineral. However, the abundance of chlorite is probably attributable to depositional environment and weathering (see discussion in \"Unit IV Sedimentology'). The presence of chert throughout the stratigraphic section suggests that the Cache Creek assemblage was a continuous source for the Skeena Group. The upward decrease in volcanic rock fragments and volcanic quartz, and increase in muscovite, reflects gradual denudation of the Hazelton Group volcanics accompanied by uplift, erosion, and increased contribution from metamorphic rocks of the Omineca Belt. UNIT: VOLCRFAND VOLC O: MUSCOVITE: CHLORITE: OTHER QUARTZ: CHERT: I II, III IV minor mmor 25% mmor <5% <5% mmor 15% 40% 30% 25% 15% 30% 30% 25% Table I. Major compositional differences between sandstones of Units I, II, III and IV. 78 REGIONAL SIGNIFICANCE OF THE TELKWA COAL MEASURES Strata in the Telkwa coalfield are correctable with other nearby Cretaceous coal measures at Denys Creek, Thautil River, Chisholm Lake, and Zymoetz River (Koo, 1984). The Telkwa coal measures are also correlatable with coal-bearing 'Red Rose Formation' sediments west of the study area in the Roche Deboule Range; members A, B, and C of the Red Rose Formation, as described by Sutherland Brown (1960) (Figure 5), are very similar to Units I, II, and HI of the Telkwa coal measures. It has been proposed that the Telkwa coal measures are correlative with the upper strata of the Groundhog coalfield (Currier Formation) north of the Skeena Arch in the Bowser Basin (Koo, 1984; Richards and Gilchrist, 1979). However, the Currier Formation is wholly Jurassic in age (Cookenboo and Bustin, 1989), whereas the Telkwa coal measures are medial Cretaceous. The Telkwa coal measures are more similar (lithologically, mineralogically, and in terms of age and depositional environment) to the coal-bearing Aptian/Albian McEvoy Formation in the Bowser Basin, one of two formations considered equivalent to the Skeena Group by Cookenboo and Bustin (1989). Cretaceous \"Skeena Group\" sediments have also been described south of the Skeena arch in the Nechako Basin (Tipper and Richards, 1976; Kleinspehn, 1985; Hunt and Bustin, 1990). Apparently, deposition of the Skeena Group occurred in a different basin, termed the \"Nazco Basin\" by Hunt and Bustin (1990), than the Jurassic Bowser Lake Group, for Jurassic sediments were not deposited across the Skeena Arch (Tipper and Richards, 1976). Subsidence of the study area, accompanied by uplift and erosion of source areas, led to accumulation of Albian Lower Skeena Group sediments on middle Jurassic Hazelton Group volcanics in the Telkwa coalfield. Sediments of the Skeena Group record two transgressive events. The transition from Unit I to Unit II marks an abrupt change from a braided fluvial system to a 79 deltaic/near-shore environment, and the transition from Unit III to Unit IV reflects a change from a paralic (coastal plain/tidal flat) environment to a near-shore marine setting. Chert and other sedimentary rock fragments are abundant throughout the Lower Skeena Group in the study area. This reflects continued clastic influx from the eastern Cache Creek Group, which was uplifted as part of the Pinchi Belt-Columbian Orogen (Tipper and Richards, 1976). The basal strata are relatively enriched with texturally and mineralogically immature coarse-grained sediment, with a large proportion of volcanic grains and 'volcanic' quartz, indicative of derivation from local volcanic rocks of the Hazelton Group. The fining-upward trend in Unit I, from conglomerate and sandstone to mudstone and coal, represents a transition to a lower-energy depositional environment, resulting from gradual denudation of the source area. The paucity of volcanic material in units II, IH, and IV, and relative abundance of muscovite, reflects decreased clastic influx from the Hazelton Group and increased influx from a metamorphic source. High-grade metamorphic rocks of the Omineca Belt, east of the study area, were likely the source of muscovite, for the Omineca Belt was undergoing rapid uplift in the medial Cretaceous as a result of the collision between Stikinia (composite terrane I) and the North American craton in the Medial Jurassic (Parrish, 1979; Eisbacher, 1981; Monger et al., 1984). Strata in the study area are disrupted by northwest and northeast striking high-angle reverse faults. Northwest striking faults may be related to regional compression which began in the medial Cretaceous, as a result of accretion of composite terrane II to North America and subsequent uplift of the Coast Plutonic Belt (Eisbacher, 1981; Monger et al, 1984). Northeast striking faults in the study area may be related to emplacement of the Late Cretaceous \"Bulkley Intrusions\" (quartz monzonite and granodiorite plutons) in the Telkwa area (Figure 1); similarly, east and northeast trending folds are common in the southern Bowser Basin, where numerous granitoid stocks were emplaced during the Late Cretaceous (Woodsworth, 1979; Eisbacher, 1981). The 80 presence of a high angle reverse fault, which cuts only the lowermost strata (Unit I) of the Telkwa coal measures, indicates that deformation also occurred in the Albian, and that an unconformity must be present in Unit II. Albian faulting may be related to subsidence and basement faulting of the Skeena Arch; if this is the case, basement-controlled subsidence may have been responsible for at least the earliest transgressive event recorded in the stratigraphic section. A possible location for the unconformity would be at the base of the transgressive marine sediments of Unit II. However, the unconformity was not directly observed, and an appreciable age difference between Units I and III cannot be confirmed with paiynological data (Appendix I). C O A L Q U A L I T Y O F T H E T E L K W A C O A L S E A M S Coal in the Telkwa coalfield ranges in rank from high to medium volatile bituminous, and is suitable for thermal use (Handy and Cameron, 1983). Typical coal quality characteristics for each coal zone are outlined in Table II. For the purposes of this study, detailed coal quality data were obtained for all 20 seams within coal zones 2 through 10 in Unit III. Quality data were not available for the coal zone 1 in Unit I. In the following sections, trends in ash and sulphur distribution within the stratigraphic sequence, and laterally within individual seams, are described and interpreted in terms of the depositional environments of the coal. In addition, the raw and washed sulphur data are compared in order to estimate the relative amounts of pyritic and organic sulphur. SULPHUR CONTENT Research on modern peat-forming environments has proven that the total amount of sulphur found in coal can be incorporated during the peat-forming stage, and that all forms of sulphur found in coal may be found in peat (Casagrande et al, 1977; Cohen et al., 1983; Altschuler et al., 1983; Given and Miller, 1985). It is well established that sulphate in a peat-forming environment is reduced by anaerobic bacteria, releasing H2S, which in turn reacts with iron to form pyrite or with organic matter to form organic sulphur. A part of the organic sulphur is also directly contributed by the plant community, such as in sulphur-bearing amino acids (Nissenbaum and Kaplan, 1972). 82 COAL ZONE: MOIST: % VOL MATT: % ASH: % FIXED C: % CALVAL: kcal/kn 1 1.23 26.1 14.40 58.20 7005 2 1.98 27.1 12.30 57.90 7007 3 1.74 27.4 12.90 58.00 7057 4 1.87 28.0 10.40 59.80 7258 5 2.05 27.7 9.50 60.90 7319 6 2.03 28.4 9.70 53.90 7257 7 1.81 29.0 10.10 59.10 7262 8 2.17 28.4 9.2 60.20 7307 9 1.38 31.9 10.00 56.70 7368 10 1.38 30.8 10.70 57.10 7295 Table II. Typical coal quality of coal from the Telkwa coalfield. All samples washed and air dried. From Smith (1989). 83 STPVATIGRAPHIC VARIATION IN SULPHUR CONTENT: D A T A The range in total sulphur content of each seam, before and after washing, is presented in Figure 20. All seams contain a minimum raw sulphur content of approximately 0.5%, and seams 2E, 8, 9, and 10 contain a minimum of 1 to 2%. The maximum total sulphur content of the seams is more variable, ranging from 2 to 7% (raw) and 1.5 to 3.5% (washed). In general, the lowest sulphur seams are seams 2, 2L, 2M, 3, 4L, 4U, and 5. These seams have raw sulphur contents of 1 to 3%, which may be reduced to 0.5 to 2.5% (washed). Two cycles are apparent in the raw data shown in Figure 20. The maximum total sulphur content of the coal field increases upward from seam 2 to seam 3T, decreases from seam 3T to 4, and then increases again from seam 4 to seams 9 and 10. INTERPRETATION Examination of modern peat deposits provides evidence that higher-sulphur peats are found in brackish environments (i.e. Spackman et al, 1976; Styan and Bustin, 1984). Sedimentological, palynological, and paleontological evidence indicates that paralic and marine conditions persisted thoughout the deposition of the upper coal measures of the Telkwa coalfield. Dinoflagellates, marine fauna, and marine or brackish ichnofacies are present in sediments between all nine coal zones of Unit III, so it is not unusual that many of the seams or parts of the seams in the Telkwa coalfield contain a high amount of sulphur. Marine influence was strongest during the deposition of the sandstones overlying seam 3T, seam 7, and seams 8, 9 or 10 (Unit IV basal sandstone). The sandstones over seams 3T and 7 are thick tidal flat sandstones which have prograded 84 RANGE IN TOTAL SULPHUR CONTENT (RAW AND WASHED): TELKWA COALFIELD % TOTAL SULPHUR Figure 20. Range in total sulphur content of each seam in Unit III (raw and washed). Sulphur content of coal seams in the stratigraphic section increases upward in two trends. Data point were excluded if they were more than 5% higher than the next lowest data value for the same seam. over coastal marshes during marine transgression. The basal sandstone of Unit IV is a marine transgressive lag sandstone. Marine influence was weakest around the time of deposition of coal zones 4 and 5, during which period coastal marsh and upper intertidal flat environments prevailed. Correspondingly, two upward-increasing raw total sulphur trends are recognized in the coalfield (Figure 20). The lower trend reflects steadily increasing marine influence and sulphur enrichment during deposition of coal zones 2 and 3. Following a period of diminished marine influence and little sulphur enrichment during the deposition of coal zones 4 and 5, marine influence and sulphur enrichment began increasing again during deposition of the upper coal seams. The top of the upper trend corresponds with a major marine transgression and deposition of deltaic/shallow marine sediments of Unit IV over the coal measures. S U L P H U R DISTRIBUTION WITHIN INDIVIDUAL SEAMS: D A T A No overall generalizations may be made concerning the spatial distribution of sulphur enrichment in the coalfield. For the most part, the variation in sulphur content of a single seam is independent of the pattern of variation in another seam. The greatest lateral variation in sulphur content occurs in the higher sulphur coal seams, particularly seams 3T, 6U, and 9 (Figure 20). Iso-sulphur maps for seams 3U and 9 are presented in Figures 21 and 22. INTERPRETATION Williams and Keith (1963), Gluskoter and Simon (1968), Home et al. (1978), Hower and Pollack (1988) and others attribute lateral changes in the sulphur content of coal 86 % TOTAL SULPHUR: SEAM 3U coal seam 3U overlain by terrestrial sediments (seam 3T and carbonaceous mudstone) coal seam 3U overlain by brackish, tidal flat sandstone: low-sulphur coal (<1%) medium-sulphur coal (1-2%) high-sulphur coal (>2%) scale: 300m Figure 21. Raw total sulphur content of seam 3U relative to the presence or absence of brackish, tidal flat sandstone directly above the seam. Area represented by map shown in Figure 2. 87 % TOTAL SULPHUR CONTENT: SEAM 9 coal zone nine overlain by marine sandstone of Unit IV coal zone nine overlain by less than 0.8m of terrestrial sediments (coal zone 10 and carbonaceous mudstone) coal zone nine overlain by more than 0.8m of terrestrial sediments (coal zone 10 and carbonaceous mudstone) lowest sulphur coal scale: 200m Figure 2 2 . Raw total sulphur content of seam 9 relative to the thickness of terrestrial sediments between the seam and marine sediments of Unit IV. Area represented by map shown in Figure 2 . 88 seams to the proximity of marine roof rocks, and a similar relationship was observed in the study area. Seams 3U and 9 are variably overlain by terrestrial or marine rocks. Where seam 3U is overlain by carbonaceous mudstone and seam 3T, the sulphur content is low (usually 2% or considerably less), and where it is directly overlain by tidal flat sandstone and mudstone, the sulphur content is higher (2% or greater) (Figure 21). Similarly, where seam 9 is overlain by marine sandstone and mudstone of Unit IV, the sulphur content is very high ( greater than 4%) (Figure 22). The sulphur content of seam 9 decreases regularly as the thickness of terrestrial sediments between the coal and overlying marine sandstone increases. Where the thickness of the intervening terrestrial sediments exceeds 0.8 metres, the sulphur content is usually less than 2%, with a few exceptions near the perimeter of this low-sulphur zone (Figure 22). Sulphur content variation in other seams is less easily explained. Local differences in pH, Eh or salinity in the depositional environment may explain anomalously low-sulphur portions of the seams, all of which formed in a paralic environment with high sulphate availability. S U L P H U R FORMS: D A T A The sulphur content of a coal may be broken down into pyritic sulphur, organic sulphur, sulphate, H2S, and elemental sulphur. Pyritic and organic sulphur are the predominant form of sulphur found in coal (Casagrande, 1987; Given and Miller, 1985). In this study, the relative amounts of pyritic sulphur and organic sulphur are estimated from comparisons of the raw and washed analyses. Washing removes mainly the pyritic component of the total sulphur, leaving primarily organic sulphur with minor amounts of other sulphur forms. Therefore, 89 assuming that pyrite and organic sulphur are the only quantitatively significant forms, the total sulphur content of the coal before washing (\"raw\") is composed of both pyrite and organic sulphur, and after washing (\"washed\") is composed dominantly of organic sulphur. In using this method of estimation, error may arise if some pyrite is left in the coal after washing, in which case the percentage of organic sulphur originally present in the coal will be over-estimated. It has been observed that some finely disseminated framboidal pyrite may remain in the coal even after washing (Carruccio and Geidel, 1979). Regardless of this possible source of error, some valid generalizations may be made concerning the forms of sulphur present within Telkwa coal. Figures 23 to 27 are plots of raw total sulphur content (pyrite and organic sulphur) versus washed total sulphur content (organic sulphur) for all samples from all seams. Any data point that plots below the dashed line is considered invalid due to analytical error, for the total sulphur content of a coal can not increase after washing. Data points that plot on or near the dashed line represent samples in which the sulphur content is the same before and after washing, indicating that all sulphur originally present was organic sulfur. Data points that plot above the line contain relatively more pyritic sulphur. INTERPRETATION It may be observed from Figures 23 to 27 that, in every seam, all the low-sulphur (< 1%) coal samples cluster around the dashed line, yet almost no high-sulphur (> 1%) coal samples plot on it. Progressively higher-sulphur coal samples plot further above the dashed line. The conclusions that can be drawn from these observations are as follows: (1) low-sulphur coals in the Telkwa coalfield are composed almost entirely of organic sulphur, whereas higher sulphur coals contain more pyrite; and (2) the proportion of pyrite increases as the total sulphur content increases. The amount of organic sulphur in the higher-sulphur samples does not remain constant as the total sulphur increases, or else 90 SULPHUR CONTENT OF COAL ZONE 2 03 cz CD •4—• § 4 o k_ zz JZ Q_ ZZi CO 2 3 o • A • * • * A ^ • • A A • 0 • ^ A o/ J_ coal seam 2 • coal seam 2L A coal seam 2M O coal seam 2U * coal seam 2E 1 2 3 4 % total sulphur content (washed) Figure 23. Plot of raw total sulphur content versus washed total sulphur content for coal zone 2. The raw sulphur content represents the total sulphur content (primarily pyritic and organic sulphur), and the washed sulphur content approximates the pyritic sulphur content. 91 SULPHUR CONTENT OF COAL ZONE 3 c CD -C CO 2 3 o o A ° l o 0 & A A O ° ^ /6 * o O A * ^ ' 9 * / 'O coal seam 3 A coal seam 3L o coal seam 3U * coal seam 3T 1 1 2 3 4 % total sulphur content (washed) Figure 24. Plot of raw total sulphur content versus washed total sulphur content for coal zone 3. The raw sulphur content represents the total sulphur content (primarily pyritic and organic sulphur), and the washed sulphur content approximates the pyritic sulphur content. 7 -_ 5 03 SULPHUR CONTENT OF COAL ZONES 4 AND 5 92 c a> § 4 o • 3 CO iS 3 o • • o o o o • • • • A coal seam 4 • coal seam 4L A coal seam 41) o coal seam 5 1 2 3 4 % total sulphur content (washed) Figure 25. Plot of raw total sulphur content versus washed total sulphur content for coal zones 4 and 5. The raw sulphur content represents the total sulphur content (primarily pyritic and organic sulphur), and the washed sulphur content approximates the pyritic sulphur content. 93 SULPHUR CONTENT OF COAL ZONES 6 AND 7 A O o * i ° : o AAo°/ 0 A p - ' O coal seam 6 A coal seam 6L o coal seam 6U * coal seam 7 1 2 3 4 % total sulphur content (washed) Figure 26. Plot of raw total sulphur content versus washed total sulphur content for coal zones 6 and 7. The raw sulphur content represents the total sulphur content (primarily pyritic and organic sulphur), and the washed sulphur content approximates the pyritic sulphur content. TOTAL SULPHUR CONTENT OF COAL ZONES 8, 9, AND 10 O o o * o o o ° o o o , * coal seam 8 ' o coal seam 9 * coal seam 10 0 1 2 3 4 5 % total sulphur content (washed) Figure 27. Plot of raw total sulphur content versus washed total sulphur content for coal zones 8, 9, and 10. The raw sulphur content represents the total sulphur content (primarily pyritic and organic sulphur), and the washed sulphur content approximates the pyritic sulphur content. 95 the data would plot in a vertical line; organic sulphur also increases, but at a lesser rate. These conclusions are in accordance with those of Ruch et al. (1974) and Roberts (1989) regarding Illinois and South African coals, and also with those of Casagrande et al. (1979) and Given and Miller (1985) on modern peats. These workers noted that where total sulphur was low the amount of organic sulphur exceeded pyritic sulphur, and that in higher total sulphur coals, more pyritic sulphur is present than organic sulphur. Although H2S may react with either iron or organic matter to form pyrite or organic sulphur in a sulphate-rich environment (Casagrande, 1979), H2S reacts preferentially with iron (Howarth and Merkle, 1984). A S H C O N T E N T STRATIGRAPHIC V A R I A T I O N IN A S H CONTENT: DATA The range in ash and average ash content for all seams in Unit III is presented in Table III. Generally coal zones 2 and 3 have the highest ash contents, and zones 4, 5, 8, 9, and 10 have the lowest. INTERPRETATION As previously discussed, coal zones 4 and 5 were deposited in a depositional environment which was relatively isolated from infiltration by brackish tidal water, compared to the depositional environments of the other seams. This is evident from the sulphur contents of coal zones 4 and 5, which are the lowest of all the seams in the coalfield. It is also suggested by the lithofacies associated with coal zones 4 and 5, which consist of fine-grained coastal marsh and upper intertidal flat sediments, 96 as opposed to sand- and mud-flat deposits. Correpondingly, the low-ash content of coal zones 4 and 5 is attributable to the relatively low frequency of flooding of the peat swamp with sediment-laden water. COAL SEAM: AVERAGE ASH: RANGE IN ASH: # SAMPLES: % % 10 14.73 7.49-24.28 13 9 15.37 8.67-27.11 12 8 13.86 9.36-28.84 17 7 19.01 10.36-48.34 21 6U 23.86 12.34-40.54 11 6L 14.47 6.25-36.59 12 6 19.78 10.44-34.63 14 5 18.31 11.33-44.72 36 4U 23.30 9.92-37.63 8 4L 12.10 6.71-19.75 7 4 13.00 6.94-23.38 31 3T 25.36 15.58-42.12 16 3U 20.57 8.55-45.78 30 3L 26.81 10.71-46.43 • 26 3 22.95 17.46-40.63 11 2E 30.81 15.19-39.19 25 2U 25.81 14.39-49.61 20 2M 25.01 8.15-41.39 17 2L 23.33 12.21-40.27 12 2 19.27 13.04-40.21 20 Table III. Ash content of seams in Unit III. Samples with ash contents of greater than 50% were excluded. The averages are not necessarily representative, as certain parts of the coalfield were sampled more extensively. In addition, some of the averages were calculated from a small number of data values. The ash content of coal zones 8, 9, and 10 is surprisingly low, considering that these seams were under considerable marine influence and were frequently flooded by brackish, sediment-laden water during deposition. They have the highest sulphur content of all the zones, and marine sediments of Unit IV immediately overlie portions of the seams. In addition, seams in coal zones 9 and 10 are generally less than a metre thick, and thin seams often have relatively higher ash contents. One explanation for the low ash content of these seams is that they originally contained more ash, but some of it was leached out after burial by marine sediments. Kosters and Bailey (1983) note that peats overlain and leached by marine water have lower ash contents. A S H DISTRIBUTION WITHIN INDIVIDUAL SEAMS: D A T A Lateral variation in ash content within a single seam can be considerable, especially in the higher-ash seams (Table III). For example, the ash content of seam 7 ranges from 10 to 48%. Lower-ash seams have less variable ash contents, such as seam 4L, which contains 7 to 20% ash, a range of only 13%. Iso-ash maps for all coal seams in Unit III are shown in Figures 28 to 32. A similar pattern of ash content variation is apparent in all coal zones, except coal zones 4 and 5. Ash content is consistently higher in the east, and is also higher in two west-east trending zones near drillholes 321 and 336. Relatively lower ash coal is found in the northern part of the study area, near drillhole 343, and in the central part of the study area near drillhole 320, between the two high ash zones. ASH DISTRIBUTION: C O A L Z O N E 2 Seam 2L 20 20 •(r 30 •//V 30 40 6051000m N Seam 2M . 20 30 30 30 -s 30 30 '. 40 ' y-50 Figure 28. Percent ash distribution within coal zone 2. Shaded area represents stable position of lagoon during coal deposition (see chapter \"Unit III Sedimentology\" and Figures 14a and 14b for explanation). Bold, outer box represents same area shown as the \"Goathorn region\" in Figure 2. VO A S H DISTRIBUTION: C O A L Z O N E 3 Seam 3L 20 30 20 3 0 // // 9 30 Seam 3U 2 0 1 0 2 0 30, 20 2 0 //SAW. 3 0 2 0 6051000m N Figure 29. Percent ash distribution within coal zone 3. Shaded area represents stable position of restricted nearshore marine environment during coal deposition (see chapter \"Unit III Sedimentology\" and Figures 14a and 14b for explanation). Bold, outer box represents same area shown as the \"Goathorn region\" in Figure 2. ASH DISTRIBUTION: C O A L Z O N E S 4 AND 5 Seam 4 10 to 10 • * 5(OH)4), a clay mineral alternatively considered to be a serpentine (Klein and Hurlbut, 1985), a serpentine-kaolinite (Roberts et al., 1990), a chlorite (Phillips and Griffen, 1981), or a \"septechlorite\" (Deer et al., 1966; Figures 33 to 35). Chemically, it is closely related to chlorite, but it is structurally similar to serpentine (Deer et al., 1966). The reflections of the untreated samples also resemble those of kaolinite and chlinochore (a magnesium chlorite), although not as closely as greenolite (Figures 36 to 38). In particular, a small peak at approximately 6.1°29 may be a chlorite (001) reflection. 126 HABOON i < 5.808 x : 2theta y : 648. Lint*r 2 9 . 9 9 8 > 31-0337 fe.iS'\\Os CoH)M 6recr»alJ+c JT T KG 3 3 - J 161 S i 0 2 Quartz. Syn Figure 33. XRD reflections from untreated sample of mottled claystonc, compared to XRD reflections from grcenolite and quartz. 127 ? 1 WHITE ss: 9.9190 tn! 1.99 CuK 3^ -0337 Fe 3s;o 5 CoH>i Greenolite IT T R& 33- 1161 5 i 0 2 Quartz, syn Figure 34. XRD relections from untreated sample of fireclay, compared to XRD reflections from greenolite and quartz. 128 • ss: 8.01'.''.) t»: 1 j < 5.080 x : 2th«ta y : 785. Li n e a r 29.990> 31-o337 FejSt'OsfoH)^ Greenal'.+e IT T R& 33- II6I S i O i Quartz syn Figure 35. XRD reflections from untreated sample of carbonaceous mudstone, compared to XRD reflections from grccnolite and quartz. 129 MAROON ss: 0.0109 ru: 1.00 CuK*l*2 < 5 . 0 0 8 x : 2 t h e t a u : 6 4 9 . Linear 2 9 . 9 9 0 > Al z S>' 2 0 5 fbH) M Kaolinite. IT Md R 6 29-0853 M g 5 A l ( S i j A I ) Cy> (OM) 8 Clinochore IT M I I b RG Figure 36. X R D reflections from untreated sample of mottled claystone, compared to XRD reflections from kaolinite and chlinochore. 5. 009 x ! 2th#U y : 642. Linear 2 9 . 9 9 0 > Z1-1H88 AlzSij.0 5 Con)^ KaolinlfC IT Md R6 Z1-OB53 M 3 5 A l C 5 i 3 A!> 0,0 (oW)& Clinochore I t H 1 i b Kb Figure 37. XRD relections from untreated sample of fireclay, compared to XRD reflections from kaolinite and chlinochore. ss: 0.01QO t « : 1.00 Ci.iKal*2 'iM ******* < 5.000 x : 2 t h » t » u I 785. L i n » « p 29.990> 21-H88 t\\liS\\zo5(OH?H Kaolirt»+c IT RG z q - 0 8 5 3 M 3 5 A ! C 5 i 3 A I ) 0 | C , (0H)s Clinochore. IT M I l b R& Figure 38. XRD reflections from untreated sample of carbonaceous mudstone, compared to XRD reflections from kaolinite and chlinochore. 132 XRD patterns from the same samples, after heating to 550°C, contain no reflections other than the weak one at approximately 6.1° 28 and the quartz peak (Figures 39 to 41). This reflects destruction of the mineral structure upon heating, which is an excellent indicator of kaolinite (Carrol, 1970). The kaolinite may be chemically similar to greenolite, and contain iron. The presence of iron would explain the dark color of the kaolinite in two of the samples, mottled claystone and carbonaceous mudstone. The lighter sample, fireclay, may contain less iron; correspondingly, the reflections from this sample do not match the greenolite reflection pattern as well as do the other samples (Figure 34). In addition to kaolinite, all samples probably contain some chlorite; this is suggested by the persistence of the 6.1° 29 peak after heating. C3F.Y3 ss: 0.0100 t « : 1.00 CuKal+2 Figure 39. XRD reflections from heated sample of mottled claystone. Background reflections removed. MAROONS s s ! 8 . 0 1 0 0 t » : 1.R8 C u K a l + 2 Figure 40. XRD reflections from heated sample of fireclay. Background reflections removed. re 41. XRD reflections from heated sampte of carbonaceous mudstone. Background reflections removed. "@en ; edm:hasType "Thesis/Dissertation"@en ; edm:isShownAt "10.14288/1.0052686"@en ; dcterms:language "eng"@en ; ns0:degreeDiscipline "Geological Sciences"@en ; edm:provider "Vancouver : University of British Columbia Library"@en ; dcterms:publisher "University of British Columbia"@en ; dcterms:rights "For non-commercial purposes only, such as research, private study and education. Additional conditions apply, see Terms of Use https://open.library.ubc.ca/terms_of_use."@en ; ns0:scholarLevel "Graduate"@en ; dcterms:title "Stratigraphy, sedimentology and coal quality of the Lower Skeena Group, Telkwa Coalfield, Central British Columbia"@en ; dcterms:type "Text"@en ; ns0:identifierURI "http://hdl.handle.net/2429/30267"@en .