Kiessling, Mark 1998 - Department of Geosciences - Idaho State ...

PROVENANCE AND STRATIGRAPHIC CORRELATION OF THE MID-
CRETACEOUS PASAYTEN GROUP, NORTHERN WASHINGTON
AND MANNING PROVINCIAL PARK, BRITISH COLUMBIA
By
Mark A. Kiessling
A thesis submitted in partial fulfillment
of the requirements for the degree of
Master of Science
in
Geology
Idaho State University
1998

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In presenting this thesis in partial fulfillment of the requirements for an advanced
degree at Idaho State University, I agree that the library shall make it freely available for
inspection. I further state that my permission for extensive copying of my thesis for
scholarly purposes may be granted by the Dean of the Graduate School, Dean of Arts and
Sciences, or by the University Librarian. It is understood that any copying or publication
of this thesis for financial gain shall not be allowed without my written permission.
Signature
Date

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To the Graduate Faculty:
The members of the committee appointed to examine the thesis of MARK A.
KIESSLING find it satisfactory and recommend that it be accepted.
______________________________
Dr. Paul Karl Link major advisor
______________________________
Dr. Mike McCurry
______________________________
Dr. David W. Rodgers
______________________________
Dr. J. Brian Mahoney
University of Wisconsin-Eau Claire
______________________________
Dr. Robert J. Fisher
Graduate Faculty Representative

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AKNOWLEDGEMENTS
I would like to thank my advisor Paul K. Link. His generosity and enthusiasm
has made my learning experience here a pleasure. Paul provided multiple critical reviews
of this thesis and much needed support during the low part of the thesis cycle. Paul
taught me a lot about stratigraphy, petrology and plate tectonics. He also made sure that
everything ran smoothly and taught me the value of shmoozing with intent. A special
thanks to J. Brian Mahoney, who guided me to Idaho State University and introduced me
to the North Cascades. Brian suggested the project and set me up in a Cadillac camp. He
provided the field assistants and invaluable field assistance even during logistical
nightmares. I would like to thank Dave Rodgers who provided a critical review of this
thesis. Dave always seemed to have time to listen and has taught me much about
geology, people and life. Ralph Haugerud and Roland Tabor taught me much about
mapping, Cordilleran geology and the Methow terrane. Ralph also suggested
stratigraphic section locations and provided assistance in the field. Many thanks to Mike
McCurry, who sacrificed valuable time to critique and evaluate my geochemical
correlations. Thanks to Scott Hughes, he knows what he has done. Savona and I will
name our first born after you. Thanks to Melissa Neiers who always seemed to straighten
out my administrative problems and made sure that I got paid. Thanks to Connie
Tillotson who provided the Jelly Bellies and fed Einstein. Tim Funderberg and the rest
of the crew in the GIS lab for giving us computers that work, answering annoying
questions and solving what appeared at the time to be earth shattering problems.
Many thanks to all of the members of Bear Bait. Aaron Walczak and Michelle
Haskin were excellent field assistants. They both provided point counts, humor, strong
backs, good conversation and geologic insight. Tom Danielson provided a strong back to
haul zircon and geochem samples. Thanks to Dale Kerner for stud service in Manning
Park. Thanks to Jim Riesterer who entertained discussions on Cordilleran geology and
Idaho Gold.
I would like to thank all the faculty and students in the geology department at
Idaho State University. The geology department supplied the microscopes, thin-sections,
NAA and ICP. Dave Fortsch, Glenn Thackray, Jeff Geslin, and Gary Gianiny all taught
me a lot about geology. A special thanks to Paul Wetmore, the other part of the Biscuit
and Gravy hour. Gravy provided valuable and not so valuable insight, good humor,
apathy and cynicism during my stay in Pocatello. Thanks to Chad Johannsen, Jim
Riesterer, Anni Watkins, Bryan Keizer, Brian Cervi, Brian Richardson, Sandra Jobe,
Nadine McQuarrie, John Glover, Brian Hough, Gus Winterfeld, Ted Reid and everyone
else who brought fear into the eyes of the Pocatello natives.
I would like to express a warm thank you to Jimmy and the gang at Goody’s who
helped the graduate students retain their sanity. Thanks to Gail and the crew of the
College Market who provided the best morning stimulant around.
This study was funded by the National Science Foundation grant EAR-9628515
to J. Brian Mahoney and Sigma Xi. I would like to thank these organizations. Many
thanks to the geology department at the University of Wisconsin-Eau Claire who taught
me the basics and provided the XRF. The Geological survey of Canada provided
logistical support and air photos. I would like to thank Rich Friedman and Mark

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Fanning, who provided whole rock and detrital zircon ages respectively. Many thanks to
B.C. Parks who allowed us to work in Manning Park. Finally, a special thanks to the
people at Manning Park, who provided a place to stay, pleasant company and the Bears
Den.
DEDICATION
I dedicate this thesis to Savona Anderson, whose patience and sacrifices were
much appreciated. Savona provided selfless support, critical reviews of my ideas, superb
companionship and sanity to my stay in Pocatello.
I would also like to dedicate this thesis to my family. LaVonne and Bill Kiessling
who introduced me to the wilderness and have always believed in me. Laura Kiessling
and Ron Raines who have supported me through it all. Bill, Julie, Emily and McKala
Kiessling made my visits home enjoyable. Ruth and the late August Korth taught me the
value of land and indirectly geology. Finally, the late William and Abbey Kiessling
provided support that made this work possible.

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TABLE OF CONTENTS
Copyright Information…………………………..………………………………...i
Title Page………….…………………………..…………...…………………….ii
Signature Sheet………………………………..……………………...…………iii
Acknowledgements…………………………..….……………...……………….iv
Dedication…………………………………..…….……………...………………v
Table of Contents…………………………..………………………………...….vi
Tableof Figures……………...…………………………………………………..ix
Table of Tables……………..………………………………………………….....x
Abstract……………………..………………………………………...…………xi
Chapter One: Introduction………………..……………………………………...1
Location of the study area…...…..…………………………………….....1
Purpose…………………………………………………………...………1
Regional Geology…………………………………………………...……5
The Problem………………………………………………………..….…9
Age of the Pasayten Group…………..………………………………….10
Methods……………………………………………………………..…..11
Chapter 2: Structural Setting of the Methow Terrane………………………….17
ThePasayten Fault……...……………………………………………….17
The Ross Lake Fault……………………………………………...……..19
TheHozameen Fault……………………………………………...……..20
Internal Structure of the Methow terrane………………………...……..20
Mid-Cretaceous contractional structures………………………..21
LateCretaceous transpressional structures…...…………………23
Eocene() transtensional structures………………..……………23
Structure of Manning Park………………..…………………………….24
Compressional structures……………………………………….24
Strike-slip structures………………………………………….....25
Chapter 3: Stratigraphy of the Pasayten Group in Manning Park…………...…27
Previous stratigraphic framework………. ……………………………..27
Lithofacies………...…………………………………………………….30
Graded sandstone and mudstone facies………………...…....….31
Cross-stratified sandstone facies……………………………..…34
Channelized sandstone facies……………………………...……36
Rippled siltstone…………………………………...…………....38
Inverse graded channel fill………………………………..….…40
Tuffaceous pebbly mudstone……………………………………42
Stratigraphy…………………………………………………………..…44
Winthrop Formation……………………………………………………..45
Big Buck member………………………………………..46
Contact relations…………………………………………47
Lithology…………………………………………………48
Clast Count data………………………………………….48
Lateral and vertical variations……………………………49

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Paleocurrents……………………………………………..51
Depositional environment………………………………..53
Ventura Member of the Midnight Peak Formation……..………54
Contact relations…………………………………………55
Lithology…………………………………………………55
Clast Counts..…………………………………………….56
Lateral and Vertical Variations…………………………..57
Paleocurrents……………………………………………..57
Depositional environment…………………………….….59
Lone Man Ridge sandstone………………………………………60
Contact relations…………………………………………61
Lithology…………………………………………………61
Clast Count data………………………………………….63
Lateral and vertical variations……………………………63
Paleocurrents……………………………………………..65
Depositional environment………………………………..65
Chapter 4: Provenance of the Pasayten Group in Manning Provincial Park.....67
Introduction………………..……………………………………………67
Winthrop Formation……………………………………………..68
Petrology …...………………………...……………………….68
Zircons………….…………...…………………………………..73
Provenance Interpretation.……………...…………...………..73
Ventura Member of the Midnight Peak Formation………………..……75
Petrology……...……..……………………...…………………..76
Detrital zircons…………………………………...……………..77
Provenance Interpretation.……………………………......…….77
Lone Man Ridge sandstone…………………………………..…………81
Petrology……………………………………..…………………81
Provenance Interpretation.…………...………………………....82
Chapter 5: Geochemical Correlation of the Pasayten Group to the
Intermontane Superterrane……………………..……………………………..83
Introduction……..………………………………………………………83
Sampling Uncertainties.…………..…………….……………....84
Sample preparation and analysis……………….……...………..84
Major element analysis………………………….……………....85
Minor and rare earth element analysis………………………..85
Trace and rare earth element analysis…….…………………..86
Results…..……………………………………………………………...87
Major elements………….……...……………………………….87
Minor, trace and rare earth element analysis………………...….87
Interpretation of Results.………………...……………………...92
Chapter 6: Depositional History of the Methow Basin…….………………….98
Introduction…….……….……………………………………………...98
Depositional history…………..………………………………………..98
Pre-Winthrop Deposition…………………………...…………..98
Deposition of the Big Buck member……….………………….100

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Deposition of the Winthrop Formation…………..…….…...…101
Deposition of the Ventura Member …….………….……….....102
Deposition of the Lone Man Ridge sandstone…...………….103
Tectonic Implications…………………………..…………………..104
Conclusions…………………………………………………...……………..106
Suggestions for Future Work……………………………...………………...109
References Cited………………………………………………..……………111
Appendix 1: Stratigraphic Sections.
Appendix 2: Thin-section Data
Plate 1: Map of the Pasayten Group in Manning Park

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TABLE OF FIGURES
Figure 1. Geologic map of Manning Provincial Park and surrounding areas……………2
Figure 2. Simplified geologic map for Manning Park…………………………………...3
Figure 3. Stratigraphic synthesis diagram………………………………………………..4
Figure 4. Minor displacement hypothesis for the evolution of the Canadian Cordillera6
Figure 5. Major displacement hypothesis for the evolution of the Canadian Cordillera…7
Figure 6. Generalized stratigraphic section for the Pasayten Group in the eastern
belt…12
Figure 7. Generalized stratigraphic section for the Pasayten Group in the western belt..13
Figure 8. Map of the major structures surrounding and within the Methow terrane……18
Figure 9. Balanced cross-section of the Methow basin from McGroder (1991)……...22
Figure 10. Photograph of the graded sandstone lithofacies…...…...…………………32
Figure 11. Photograph of the cross-stratified sandstone lithofacies.………...…………35
Figure 12. Photograph of the Channelized sandstone lithofacies..………..……………37
Figure 13. Interpreted fining-upward sequences within the channelized lithofacies…39
Figure 14. Photography of rippled siltstone lithofacies.………...………………………41
Figure 15. Photograph of inverse-graded channel lithofacies...………………………43
Figure 16. Photograph of the tuffaceous mudstone lithofacies……...………………..43
Figure 17. Clast compositions for the Big Buck member of the Winthrop Formation.50
Figure 18. Rose diagrams showing paleocurrents from the Pasayten Group ………...52
Figure 19. Clast composition variation from the western belt to the eastern belt…….58
Figure 20. Photograph of the contact between the Lone Man Ridge sandstone and the
Ventura Member .……………………………………………………………………..62
Figure 21. Typical fining-upward sequence within the Lone Man Ridge sandstone ..…64
Figure 22a. Ternary plots for the Winthrop Formation……………………………….69
Figure 22b. Ternary plots for the Ventura Member of the Midnight Peak Formation….70
Figure 22c. Ternary plots for the Lone Man Ridge sandstone………………………..71
Figure 23. Stratigraphic distribution of selected grain ratios…………………………72
Figure 24. Preliminary whole rock U/Pb date for a plutonic clast ……………………..74
Figure 25. Age distribution of detrital zircons within a sandstone……………………...78
Figure 26. Major element plots of plutonic clasts and plutonic bedrock………………..88
Figure 27. Rare-earth element patterns for the plutonic clasts and the plutonic bedrock.91
Figure 28. Plot of select rare-earth and trace elements against SiO 2 ……………………93
Figure 29. Tectonic discrimination plots for plutonic clasts and plutonic bedrock……..94
Figure 30. Tectonic discrimination plots for both plutonic clasts and plutonic
bedrock...95
Figure 31. Tectonic evolution of the Methow basin………………………………….…99

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TABLE OF TABLES
Table 1. Lists the samples that were used in geochemical analysis…………………..16
Table 2. Pasayten Group lithofacies…………………………………………………..33
Table 3. Mean paleocurrents for the Pasayten Group…………………………………...53
Table 4. Potential source terranes for detrital zircons within the Ventura Member…….80
Table 5. Geochemical data from the Eagle Plutonic Complex and plutonic clasts……..89
Table 6. Elemental characterization and the tectonic location of four types of granites..96

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ABSTRACT
The mid-Cretaceous Pasayten Group in Manning Park and WA is a thick
sequence of feldspathic-, volcanic-, and chert-rich strata that were deposited within the
Methow Basin. These strata are subdivided into: (1) a western belt studied in the
Methow valley, WA consisting of the meandering fluvial Virginian Ridge Formation,
meandering fluvial Winthrop Formation, braided fluvial Ventura Member of the
Midnight Peak Formation and volcanic main body of the Midnight Peak Formation; (2)
an eastern belt exposed in Manning Park, B.C. consisting of the deltaic Big Buck member
of the Winthrop Formation, meandering fluvial main-body of the Winthrop Formation,
braided fluvial Ventura Member of the Midnight Peak Formation and meandering fluvial
Lone Man Ridge sandstone. Strata of the eastern belt are composed of six lithofacies:
graded sandstone and mudstone; cross-stratified sandstone; channelized sandstone;
rippled siltstone; inverse-graded channel fill; and tuffaceous pebbly mudstone.
Paleocurrents, petrology, geochemistry, detrital and whole rock zircon ages were
used to determine the provenance of the Pasayten Group. Paleocurrents and sandstone
petrology show that the Pasayten Group was derived from an eastern plutonic source and
a western volcanic- and chert-rich source. Chert- and volcanic-rich strata are interpreted
to have been derived from the Bridge River terrane and the Midnight Peak arc
respectively. A whole rock U/Pb age (108 +3 / -21 Ma) from a plutonic clast within the Big
Buck member of the Winthrop Formation overlaps with the Falls Lake Plutonic Suite of
the Eagle Plutonic Complex and the Okanogan Range Batholith. Detrital zircons from
the Ventura Member of the Midnight Peak Formation are the exact ages of plutons in the
Intermontane superterrane. Major, minor and trace element data from a small sample

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suite of plutonic clasts within the Big Buck member (n=10) and plutonic bedrock
samples from the Eagle Plutonic Complex (n=5) display no apparent correlation.
A model was developed for the Methow basin during deposition of the Pasayten
Group. During the middle Albian the Methow forearc basin was receiving sediment from
a western chert-rich Bridge River complex and the eastern plutonic- and volcanic-rich
Spences Bridge arc. The late Albian marks a time of erosion along the western margin of
the Methow forearc basin while the Big Buck member on the east received sediment
from the Eagle-Okanogan Complex. During the Cenomanian, uplift of the western
Bridge-River terrane along east-vergent thrusts forms the Methow foreland basin into
which the main body of the Winthrop Formation and Virginian Ridge Formation were
deposited. The Winthrop Formation was derived from the Eagle-Okanogan Complex and
the Midnight Peak arc while the Virginian Ridge Formation was derived from the Bridge
River terrane. The Ventura Member of the Midnight Peak Formation is interpreted to
have been deposited in a foreland basin setting during the Cenomanian to Turonian. This
unit was derived partly from plutonic sources east of the Methow basin and from the
western Midnight Peak Formation and Bridge River terrane. The Turonian Lone Man
Ridge sandstone signifies the introduction of chert-rich strata into the eastern belt and is
inferred to have been derived from the Bridge River terrane and Midnight Peak volcanic
arc.

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CHAPTER 1. INTRODUCTION
LOCATION OF THE STUDY AREA
Mid-Cretaceous strata of the Pasayten Group are exposed in Manning Provincial
Park, B.C. and in the Methow Valley, WA forming a northwest-southeast trending
outcrop belt, extending ~ 200 km from northern, WA to south-central B.C.. This study
focuses on exposures of the Pasayten Group in Manning Provincial Park and to a lesser
extent on exposures within the northern part of the Methow Valley in WA.
Manning Park is located within the North Cascades, adjacent to and north of the
International Border between Hope and Princeton, BC (Figure 1 and 2). Exposures of the
Pasayten Group crop out between the eastern boundary of the Park and the Manning Park
Lodge and extend northward from the International Border to beyond the northern
boundary of the Park.
Outcrops of the Pasayten Group continue south from Manning Park into the
Methow Valley, north-central WA. In Washington, the Pasayten Group outcrop belt
reaches its maximum width of 40 km and continues from the southern border of Manning
Park to south of Twisp, WA.
PURPOSE
The primary purpose of this study is to describe in detail the mid-Cretaceous
Pasayten Group in Manning Park, BC, including its stratigraphy, paleocurrents,
geochemistry of conglomerate clasts, petrology and provenance. This work will build
upon the study by Coates (1974) which was interrupted by Coate’s untimely death and
lacked stratigraphic and petrologic detail.

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Once described, the Pasayten Group is correlated with the regional stratigraphy
established by Haugerud et al. (1996) for the Methow terrane in northern WA (Figure 3).
These stratigraphic relationships are used to develop a tectonic and sedimentary model
for the evolution of the Methow basin preceding and during deposition of the Pasayten
Group.
Recent controversy over the paleogeographic position of the allochthonous
terranes of the Canadian Cordillera (Cowan, 1994; Wynne et al., 1996; Irving et al.,
1995; 1996) has instigated new studies designed to determine the provenance of mid- to
Late Cretaceous strata (Figures 4 and 5)(Mahoney et al., 1996). This study attempts to
shed light on this controversy.
REGIONAL GEOLOGY
The Pasayten Group was deposited in the Methow basin on the Methow terrane (a
tectonostratigraphic terrane with a distinct stratigraphy that cannot be mapped to adjacent
terranes) (Miller et al., 1994 in Haugerud et al., 1994). Methow terrane strata consist
primarily of feldspathic sandstone of the Lower to Upper Cretaceous Jackass Mountain
Group, Harts Pass Formation, and the Upper Cretaceous Pasayten Group (Cole, 1973,
Tennyson, 1974; Coates, 1974; Barksdale, 1975; Monger, 1989b; Kiessling and
Mahoney, 1997) (Figure 3). The Pasayten Group is a nonmarine succession of sandstone
and conglomerate of probable late Albian to Turonian () age, exposed in the footwall of
the east-vergent Chuwanten thrust fault (Figure 2); coeval rocks have not been identified
in the hanging wall in British Columbia (Coates, 1974; Monger, 1989a).

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In Manning Park, the Pasayten Group contains over 2400 m of strata divided into
the Big Buck member of the Winthrop Formation, main body of the Winthrop Formation,
Ventura Member of the Midnight Peak Formation and Lone Man Ridge sandstone
(Figure 3) (Kiessling and Mahoney, 1997). The Winthrop Formation has been traced
across the international border into the Methow Valley of northern Washington where it
interfingers with the underlying Virginian Ridge Formation and with the overlying
Ventura Member of the Midnight Peak Formation (Figure 3) (Barksdale, 1975; Tennyson
and Cole, 1978; Haugerud et al., 1996; Kiessling and Mahoney, 1997). No strata
definitively correlative with the Lone Man Ridge member of the Midnight Peak
Formation have been identified in Washington although highly metamorphosed outcrops
of a chert-bearing unit stratigraphically overlie the Ventura Member just south of the
border (Ralph Haugerud, personal communication, 1997).
The Methow terrane is bounded on the east by the Pasayten fault, which separates
it from Paleozoic and Mesozoic volcanic and plutonic rocks of Quesnellia (Figure 1).
North and east of Manning Park, Quesnellia contains Triassic Nicola Group andesitic
volcanic rocks, Jurassic to Cretaceous plutonic rocks of the Eagle Plutonic Complex and
volcanic rocks of the Cretaceous Spences Bridge Group (Monger, 1989a and b; Monger
and Journeay, 1994). The Methow terrane is bounded on the west by the Hozameen and
Ross Lake faults, separating it from oceanic chert, argillite and volcanic rocks of the
Bridge River terrane (Figure 1) (Monger, 1989a; Monger and Journeay, 1994).
Two superterranes comprise much of the Canadian Cordillera. The Intermontane
superterrane consists of terranes east of the Pasayten fault including Quesnellia (Figures

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1 and 2). This superterrane was amalgamated and then accreted to the western margin of
North America during the Jurassic (Monger et al., 1982). The Insular superterrane
consists of those terranes west of the Pasayten fault including the Bridge River terrane
(Figures 1 and 2). The Methow terrane has been structurally tied to the Insular
superterrane since the Late Cretaceous (91 Ma) based on cross-cutting plutons (Journeay
and Friedman, 1993).
THE PROBLEM
The paleogeographic location of these superterranes has been disputed (Cowan,
1994; Cowan et al., 1997) (Figures 4 and 5). Geologic correlations suggest that the
Insular superterrane was accreted to the margin of North America at its present latitude
by 91 Ma (Monger et al., 1982; Garver, 1989; 1992; Journeay and Friedman, 1993;
Monger and Journeay, 1994; Monger and Price, 1996; Mahoney et al., 1996).
Paleomagnetic data indicate that the Insular and Intermontane superterranes were
accreted to the margin of North America at the latitude of Baja California and northern
California respectively (Irving et al., 1995; Wynne et al., 1996; Irving et al., 1996).
Following accretion these terranes were translated 3000 km and 1100 km northward
between 85 and 70 Ma along a margin-parallel fault zone between the two superterranes
(Cowan, 1994; Mahoney et al., 1996). If the paleomagnetic interpretations are accurate
then clastic sediments deposited on the Insular superterrane before 85 Ma can not have
been derived from Intermontane superterrane. The mid-Cretaceous Pasayten Group in
Manning Park, BC was deposited on the Insular superterrane and is therefore ideally
located to test the large scale translation hypothesis.

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This project is a small part of a larger project supervised by J. Brian Mahoney,
investigating Albian and Cenomanian conglomerates in the southern Canadian
Cordillera.
AGE OF THE PASAYTEN GROUP
The age of the Pasayten Group is poorly constrained. The Pasayten Group is
broadly constrained to be Albian() to Turonian() in age, based on plant assemblages,
underlying marine fauna, and cross-cutting Turonian-Coniacian (ca. 90-88 Ma) dikes
documented in Washington (Haugerud et al., 1996) (Figure 3).
Coates (1970; 1974) suggested an Albian age for strata within Manning Park
based on plant fossil assemblages and the gradational lower contact with Albian Hamitesbearing
strata. Barksdale (1975) suggested a Cenomanian to possibly Turonian age for
the Winthrop Formation in northern Washington based on the occurrence of marine
fossils in the underlying Virginian Ridge Formation. Haugerud et al (1996) interpret the
Winthrop Formation to be older than 97.5 +2 / -3 Ma based on a cross-cutting dike. The
Winthrop Formation must also be younger than 108 +3 / -21 Ma, the age of a plutonic clast
within the Winthrop Formation. The Ventura Member is assumed to be Albian or
Cenomanian in age based on the interfingering relationship with the Albian () Winthrop
Formation (Barksdale, 1975). Haugerud et al. (1996) suggest a Turonian to Coniacian
age for the Midnight Peak Formation based on an 87.0 +/- .4 Ma lava flow within the
Midnight Peak Formation and an 88 Ma cross cutting dike. Coates (1974) suggested an
Albian age for the Lone Man Ridge sandstone based on the Pasayten Group being
internally conformable.

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METHODS
Field work began during the 1996 field season and involved geologic mapping,
sampling of outcrops and construction of stratigraphic sections. Geologic mapping
(1:50,000 scale) was begun and continued through the 1997 field season to document the
geographic distribution and the structural style of deformation within the Pasayten Group
in Manning Provincial Park, British Columbia.
The Pasayten Group in both Manning Park and the Methow Valley was divided
into eastern and western belts based on structural position. Strata within the eastern belt
are located within the footwall of the Chuwanten thrust fault in both the Methow Valley
and in Manning Park (Figures 1 and 6). Strata within the western belt are found in the
hanging wall of the Chuwanten thrust fault in Washington and have been translated
perpendicular to strike as much as 60 km to their present location (McGroder, 1991)
(Figures 1 and 7). Six stratigraphic sections were measured, one in northern Washington,
in the western belt, and five in Manning Park, in the eastern belt, to document vertical
and lateral lithologic variations (Figures 1 and 2). The provenance of the Pasayten Group
was established by integrating the petrology, paleocurrents and the ages of detrital
zircons from known stratigraphic locations.
Clast counts were done in conglomeratic intervals. Clast counts were done by
marking out a 1 m by 1m box and counting all the clasts within.
Hand samples and cobbles (where available) were collected from sandstone and
conglomerate at 50 m intervals for sedimentary petrology investigation. From these
samples, 35 thin sections were stained for k-spar and point-counted (n=500) using the
Gazzi-Dickinson point count method (appendix 2-petrology data). The point count data

14
was analyzed in conjunction with the paleocurrents and pebble counts to determine
patterns of sedimentation, specifically lateral and vertical variations, and possible
provenance sources.
Following Ingersoll (1990), the Methow basin is interpreted to be a 1 st or 2 nd
order basin and therefore point count data were not plotted on Dickinson and Suczek
(1979) provenance diagrams. These diagrams were based on very large sample
populations from very large areas (3 rd order systems of Ingersoll, 1990). Ingersoll (1990)
recognized that local drainages (1 st order basins) may be more influenced by a local
sediment source than a tributary or a big river (2 nd and 3 rd order basins respectively) and
would therefore plot within a different tectonic provenance on Dickinson and Suczek
diagrams. In order to overcome this problem, Ingersoll et al. (1993) defined 3 scales of
petrologic sampling: 3 rd order sampling, big rivers and their deltas and marine
environments; 2 nd order sampling, streams and rivers; and 1 st order sampling, talus piles,
alluvial fans and local drainages. Depositional environment interpretations of the
Pasayten Group suggest that it was deposited in a 1 st order or 2 nd order system. The data
was organized into ratios and these ratios were plotted against their stratigraphic location.
Logs, trough cross-stratification, epsilon and planar cross-stratification, pebble
imbrications and channel axes were used to determine both unidirectional and
bidirectional paleocurrents. Logs and wood with 3:1 long to short axis ratios were
assumed to be parallel with stream-flow and were measured as bidirectional current
indicators (Tucker, 1994). Unidirectional indicators (channel axes, pebble imbrications,
trough, epsilon and planar cross stratification) were measured only when all 3 dimensions

15
were obvious. For imbrication study, only the long axis of each pebble was measured.
Multiple attitudes were taken from each paleocurrent site and averaged together to
establish an average strike and dip for the location. Paleocurrents were rotated back to
paleohorizontal and plotted on rose diagrams using Stereonet 3.5 by Allmendinger
(1992). Standard deviations were determined using circular statistics (Krause and Geijer,
1987).
Detrital zircon samples consisted of ~1 kg of sandstone while whole-rock zircon
samples consisted of >8 cm radius plutonic clasts. Two detrital zircon samples from
sandstone in the Winthrop Formation and the Ventura Member of the Midnight Peak
Formation of the Midnight Peak Formation were analyzed using a SHRIMP (Sensitive
High Resolution Ion Microprobe) by Mark Fanning of the Australian National
University, Canberra, Australia. One conglomerate clast from the Big Buck member of
the Winthrop Formation was analyzed using conventional U/Pb whole rock analysis by
Rich Friedman at the Geochronology Laboratory at the University of British Columbia,
Vancouver, British Columbia. Detrital zircon ages were compared with U-Pb ages for
plutons east of the Pasayten fault within the Intermontane superterrane in an attempt to
fingerprint possible source terranes.
Samples of plutonic bedrock from potential source terranes on the Intermontane
superterrane and plutonic clasts within the Pasayten Group were analyzed to identify
possible geochemical correlations and therefore provenance ties (Table 1). These
samples were analyzed for trace and rare earth elements using neutron activation analysis
at Idaho State University, and major and minor elements using X-ray florescence at the
University of Wisconsin-Eau Claire (Table 1). Plutonic clasts were sampled from the

16
Big Buck member of the Winthrop Formation at the type section on Big Buck Mountain
and on 4 th Brother Mountain. Lithologically distinct (hornblende bearing, biotite and
muscovite bearing, etc.) clasts > 10 cm in diameter were collected. The Eagle Plutonic
Complex was sampled immediately east of the border of Manning Park (Figures 1 and 2).
Variable phases of the pluton were sampled in an east-west transect across the complex at
the Manning Park eastern entrance, north of Hwy. 3, and along Whipsaw Creek road near
Skaist and Kettle Mountains. These samples were collected on the basis of freshness and
any weathered or altered portions were removed in the field.
Table 1-lists the samples that were used in the geochemical analysis. Samples were
compared with potential source terranes to establish possible terrane linkages.
Stratigraphic unit
Sampled
Sample type Compared with Possible
Provenance
Purpose
Winthrop Fm. in
Plutonic clasts
Eagle Plutonic
Spences Bridge
Link Methow
WA and BC
Complex and
Arc
terrane to the
Okanogon
Intermontane
Complex
superterrane
Eagle Plutonic
Biotite, hornblende
Clasts from the Big
N/A
Link Methow
Complex in BC
tonalite; biotite
Buck Member
terrane to the
tonalites, biotite
Intermontane
tonalite gneiss
superterrane

17
CHAPTER 2. STRUCTURAL SETTING OF THE METHOW TERRANE
The Methow terrane is a fault bounded block that contains an internally consistent
stratigraphy which cannot be mapped into adjacent terranes (Monger and Journeay,
1994). The Methow terrane is bounded to the east by Pasayten fault and to the west by
the Ross Lake, Hozameen and Fraser-Straight Creek faults (Monger and Journeay, 1994;
Haugerud et al., 1996) (Figure 8). The displacement history of these faults is not lucid
and has been a topic of much controversy (Irving et al., 1996; Monger and Price, 1996).
THE PASAYTEN FAULT
The Pasayten fault forms the boundary between plutonic and volcanic rocks of
Quesnellia to the east and clastic strata of the Methow terrane to the west (Figure 8).
Rhyolites and andesites of the Cretaceous Spences Bridge Group form the volcanic
carapace to tonalites and granodiorites of the Eagle and Okanogon complexes; these
rocks comprise most of Quesnellia immediately east of the Pasayten fault (Hurlow and
Nelson, 1993; Thorkelson and Rouse, 1989; Grieg, 1992). The remaining Quesnellian
strata consist of foliated volcanics of the Triassic Nicola Group and gneisses of the
Okanogan gneiss and Eagle gneiss.
The Pasayten Fault is documented as primarily a brittle structure but most
workers have also recognized older ductile fabrics (Hurlow, 1989; Grieg, 1992;
Haugerud et al., 1996). LITHOPROBE seismic reflection studies of the fault interpret it
as a steeply east-dipping structure (Cook et al., 1992). Grieg (1992) suggested the
Pasayten fault underwent ductile, sinistral and east-side up reverse movements during the
mid-

19
Cretaceous (110 Ma) based on K-Ar and Rb-Sr cooling dates. He further suggests, based
on stratigraphic offsets, that the Pasayten fault was reactivated as a post-Eocene brittle
structure. Hurlow (1989) and Haugerud et al. (1996) suggest a similar slip history for the
Pasayten fault along its southern extension in Washington. Kinematic studies, based on
stratigraphic offsets along the fault, indicate 10’s of km of displacement but do not
preclude larger displacements of up to 100’s of km (Kleinspehn, 1985; Hurlow, 1993;
Haugerud et al., 1996; Irving et al., 1996).
The Eagle plutonic complex was uplifted prior to the Late Cretaceous. Grieg et
al. (1992) and Grieg (1992) found concordant K-Ar and Rb-Sr muscovite dates of 100
Ma from both the Eagle plutonic complex and the Pasayten fault and interpreted these
ages to indicate the Pasayten fault accommodated uplift of the plutonic complex.
THE ROSS LAKE FAULT
The Ross Lake fault system forms the southwest boundary of the Methow terrane
(Figure 8). The Ross Lake fault separates metamorphosed rocks of the Chelan block
from clastic strata of the Methow terrane (Haugerud et al., 1996). This fault zone has
been interpreted differently by various workers: (1) Davis and others (1978) suggested
the zone was a pre-90 Ma, terrane-bounding strike-slip fault; and (2) Haugerud et al.
(1996) and references therein interpreted the zone to be a major post-orogenic obliqueslip
system. Haugerud et al. (1996) suggest that the Ross Lake fault zone has had at least
six “identities”: (1) an original boundary, either a depositional contact or an accretionary
or transform fault; (2) a NE vergent, mid-Cretaceous thrust placing the Hozameen
allochthon over the Methow terrane; (3) a SW side down, post 90 Ma dip-slip fault

20
responsible for the deep burial of the Chelan block; (4) a Late Cretaceous to early ()
Tertiary dip-slip fault responsible for causing the unroofing of the Chelan block; (5) a
pre-middle Eocene dextral transcurrent fault; and (6) a post 45 Ma belt of dextral strikeslip
faults.
THE HOZAMEEN FAULT
The Hozameen fault bounds the Methow terrane to the west and juxtaposes
oceanic affinity rocks of the Bridge River terrane with clastic rocks of the Methow
terrane (Figure 8) (Journeay and Monger, 1994). To the north the Hozameen fault is a
vertical east-side-down reverse fault while to the south, in Washington, it becomes the
east-directed Jack Mountain thrust fault (Misch, 1966). Based on this geometry,
Kleinspehn (1985) suggests that any recent transcurrent movement along this fault must
be sinistral. Umhoefer and Miller (1996) suggested that the Hozameen fault is the
southern extension of the Yalakom fault based on reconstructions of the Fraser fault
system. Furthermore, they suggest that a Hozameen-Yalakom fault may have
accommodated up to 80 km of dextral movement.
INTERNAL STRUCTURE OF THE METHOW TERRANE
The internal structure of the Methow terrane contains both thrust and transcurrent
faults with fewer normal faults (Figure 8) (Coates, 1974; Barksdale, 1975; Haugerud et
al., 1996). Haugerud et al. (1996) categorized these structures into: (1) mid-Cretaceous
contractional structures; (2) Late Cretaceous transpressional structures; (3) Eocene
transtensional structures.

21
MID-CRETACEOUS CONTRACTIONAL STRUCTURES
The major contractional structures of the Methow terrane include north to
northwest-trending folds and thrust faults (Coates, 1974; Monger, 1989; Haugerud et al.,
1996). The major folds include: (1) the Gibson Pass and Castle Creek synclines in
Manning Park and Washington; (2) the Sweetgrass anticline in Washington; and (3) the
Goat Peak syncline in Washington (Figure 8) (Coates, 1974; Haugerud et al., 1996).
These folds appear to become tighter to the northwest where the basin width thins
(Coates, 1974). Thrust faults in the Methow terrane verge to the east and are part of the
contractional Chuwanten fault system (Figure 9) (Coates, 1974; Haugerud et al., 1996).
The geometry of the Chuwanten and associated faults is similar to the geometry
of classic fold and thrust belts where transport is normal to the strike (McGroder, 1991)
(Figure 8). Haugerud et al. (1996) suggested that initiation of the Chuwanten system was
penecontemporaneous with basin sedimentation, such that thrusting began by 110-105
Ma (the first appearance of sediments derived from the thrust sheets) and continued until
90 Ma (the age of the Rock Creek pluton which intrudes the Chuwanten system).
McGroder (1991) estimated, from balanced cross-sections, ~60 km of east-west
shortening within the Methow basin along the Chuwanten fault system. Based on
McGroder’s shortening estimates and their timing constraints, Haugerud et al. (1996)
estimated shortening rates of 2-2.5 mm/yr.

23
LATE CRETACEOUS OR TERTIARY TRANSPRESSIONAL STRUCTURES
Haugerud et al. (1996) documented northwest-striking transpressional structures
within the Methow valley of Washington. These structures comprise the Slate Creek
fault system which displays west-side up, dextral oblique-slip and minor thrust faulting.
Because this fault system cuts across the Castle Creek syncline in northern Washington,
the structures are interpreted to be younger then the mid-Cretaceous contractional event
(Haugerud et al., 1996). The Slate Creek system is itself cut by the 49 Ma Golden Horn
batholith indicating that this transpression probably occurred between 90 and 49 Ma
(Haugerud et al., 1996). In Manning Park, Coates (1974) documents oblique-slip and
high-angle reverse structures with similar trends but was uncertain about their timing
(these structures may just as easily be included with Eocene transtensional structures).
EOCENE() TRANSTENSIONAL STRUCTURES
Haugerud et al. (1996) documented northwest-striking strike-slip faults and
approximately east-west trending extensional stepovers (Figure 8). The stepovers
consisted of high-angle normal faults and low-angle detachment faults. Stepover-related
faults dip both to the north and south and display a maximum displacement of 5 km
(Haugerud et al., 1996). Coates (1974) found northwest-striking oblique-slip faults and
some local normal-faults in Manning Park but it is unclear whether these structures are
related to transtensional or transpressional events (see above).

24
STRUCTURE OF THE MANNING PARK AREA
Structural features mapped in Manning Park were subdivided into 2 categories:
(1) contractional structures and (2) strike-slip structures. Contractional structures are
well-documented within the Methow basin and are attributed to the Late Cretaceous
accretion of the Insular superterrane to North America along a northeast-vergent thrust
belt (Coates, 1974; Barksdale, 1975; Garver, 1989; McGroder, 1991; Journeay and
Monger, 1994; Monger and Journeay, 1994; Haugerud et al., 1996; Umhoefer and Miller,
1996). Strike-slip structures have also been well documented within the Methow basin
and are associated with Late Cretaceous and Early Tertiary dextral translation (Coates,
1974; Barksdale, 1975; Journeay and Monger, 1994; Monger and Journeay, 1994;
Haugerud et al., 1996). This section focuses on these structures, found between and
including the Chuwanten thrust fault and the Pasayten fault.
COMPRESSIONAL STRUCTURES
Compressional structures within Manning Park consist of post-depositional eastvergent
thrust faults and folds. The Chuwanten thrust fault is the largest of the
compressional faults mapped in Manning Park (Plate 1). In the park, the fault strikes
~135 o , dips ~25 o west and extends from the International Border to the northern
boundary of the park. The Chuwanten thrust fault is composed of a complex system of
southwest dipping splays that place Jurassic rocks (Ladner Group) over the mid()-
Cretaceous Pasayten Group. The fault itself was obscured by cover at all localities
investigated but was its general locations was easily recognized by the juxtaposition of
two very different lithologies.

25
In the footwall of the Chuwanten fault an anticline-syncline pair represent the
only map scale folds in this portion of the park (Plate 1). These Monument Hill folds
extend from south of the border (Ralph Haugerud, personal communication, 1997) to just
north of Monument Creek on the southwestern slopes of Monument Hill. These folds are
upright and open, trend 330 o and plunge 17 o N. They are truncated by the Chuwanten
fault just west of Monument Hill (Plate 1).
Thrust faults and folds in the map area cut and deform Late Cretaceous and older
strata making these structures younger than Cenomanian and probably Turonian (see the
“Age of the Pasayten Group”). This timing relationship suggests that by Turonian time
the Chuwanten thrust fault in Manning Park had ceased movement. This timing is
consistent with a Cordilleran wide compressional event (Journeay and Friedman, 1993;
Umhoefer and Miller, 1996).
STRIKE-SLIP STRUCTURES
The strike-slip structures in Manning Park consist of a young (Tertiary)
generation of transcurrent faults (Plate 1). The Pasayten fault is the largest of these
structures extending from northern Washington through the Park and continuing to the
north. The Pasayten fault separates Lower Cretaceous sandstones of the Jackass
Mountain Group from tonalites and tonalite gniesses of the Jurassic Eagle Plutonic
complex. Numerous smaller transcurrent faults merge into or occur proximal to the
Pasayten fault. These faults comprise 70 o ). These fault zones cut the mid-Cretaceous Pasayten

26
Group and are therefore interpreted to be Late Cretaceous or Tertiary. These smaller
faults are attributed to the most recent movement on the Pasayten fault.

27
CHAPTER 3. STRATIGRAPHY OF THE PASAYTEN GROUP IN EASTERN
MANNING PROVINCIAL PARK, BRITISH COLUMBIA
PREVIOUS STRATIGRAPHIC FRAMEWORK
The Pasayten Group was originally defined in Manning Park for an assemblage of
nonmarine strata exposed in the eastern half of the park (Daly, 1912; Rice, 1947). Coates
(1974) described the Group as a sequence of nonmarine sandstone, conglomerate, and
mudstone of probable Albian age that overlies marine strata of the Jackass Mountain
Group. He divided the group into three subdivisions, comprising about 3300 m of strata:
(1) map-unit 11, dominated by micaceous arkosic sandstone; (2) map-unit 12 (the Red
Bed unit), consisting of distinctly red siltstone, sandstone, and conglomerate; and, (3)
map-unit 13, weakly indurated, poorly sorted sandstone and chert-bearing conglomerate
(Figure 3). He attributed a nonmarine origin to each unit, and hypothesized an eastern
source for map-unit 11 and a western source for map-units 12 and 13, based on outcrops
of the chert-rich Hozameen Group to the west and the Eagle Plutonic complex to the east.
Barksdale (1948; 1975) correlated the Pasayten Group in Manning Park with midto
Upper Cretaceous strata in the Methow Valley of Washington. He subdivided strata in
Washington into, in ascending order, the chert-rich Virginian Ridge Formation, the
arkosic Winthrop Sandstone, and the volcanic Midnight Peak Formation. Barksdale
(1975) recognized the Virginian Ridge Formation was not exposed in Manning Park,
correlated the Winthrop Sandstone with map-unit 11, and correlated the Ventura Member
of the Midnight Peak Formation with map-unit 12. He recognized that there were no
strata in Washington directly correlative with map-unit 13.

28
The Winthrop Formation in WA and unit 11 of the Pasayten Group in BC both
display east to west paleocurrents, and are similar petrographically (Cole, 1973). Cole
(1973) noted strong lithological similarities between the Ventura Member of the
Midnight Peak Formation and the middle member of the Pasayten Group (map-unit 12).
Tennyson (1974) suggested that the upper member of the Pasayten Group (unit 13 of
Coates, 1974) in Manning Park was correlative with the Ventura Member of the
Midnight Peak Formation.
Various other workers in the region have referred to rocks of the Pasayten Group
as “Winthrop facies” (Monger, 1989a), a combination of formation and map-unit
numbers (McGroder, 1991), and as Winthrop Formation (Journeay and Monger, 1994).
Haugerud et al. (1996) further refined Cretaceous stratigraphy in WA. They
defined a north to south facies transition (Figure 3). To the north they recognized eight
lithologic units that stratigraphically up consist of: (1) the marine Albian Dead Lake
unit, lithic sandstone, argillite and pebble conglomerate; (2) Albian () Little Jack unit,
marine shale, siltstone, sandstone and tuffaceous rock; (3) Albian () Jackita Ridge
Formation, marine siltstone, sandstone and chert pebble conglomerate; (4) middle Albian
Harts Pass Formation, marine arkosic sandstones and siltstones; (5) Albian to
Cenomanian Virginian Ridge Formation, fluvial siltstone, sandstone and chert pebble
conglomerate; (6) Albian to Cenomanian Winthrop Formation (including the 3 AM
Mountain Member), fluvial siltstone and arkosic- to volcanic-lithic sandstone and
interbedded lava flows; (7) Ventura Member of the Midnight Peak Formation, terrestrial
sandstone, siltstone, and conglomerate; and (8) Midnight Peak Formation, andesite lava
flows and breccias.

29
South of Winthrop, WA they recognized four lithologic units: (1) the Albian
Patterson Lake unit, marginal marine volcanic and sedimentary conglomerate; (2) Albian
to Cenomanian Virginian Ridge Formation; (3) Albian to Cenomanian Winthrop
Formation; and (4) Turonian Midnight Peak Formation. They agreed with Barksdale’s
(1975) correlation of mid- to Upper Cretaceous strata in the Methow Valley with the
Pasayten Group and defined the Pasayten Group in WA to include: (1) the Virginian
Ridge Formation; (2) Winthrop Formation; (3) Ventura Member of the Midnight Peak
Formation; (4) and Midnight Peak Formation. They also correlated the Harts Pass
Formation to marine turbidites of the Nicomen Ridge sandstone (unit 10) within the
eastern outcrops of the Jackass Mountain Group, Lower Cretaceous marine sandstone
and conglomerate of Coates (1970; 1974) (Figure 3).
The Pasayten Group in Manning Park and northern Washington is subdivided
here into a western and eastern belt. These belts run roughly north-south and are
separated by the Chuwanten thrust fault (figure 1). The western belt is located in the
Methow Valley, WA and stratigraphically up, contains: (1) the Albian () or
Cenomanian () Virginian Ridge Formation (which unconformably overlies the Harts
Pass Formation); (2) the Albian () or Cenomanian () Winthrop Formation; (3) the
Cenomanian () or Turonian () Ventura Member of the Midnight Peak Formation; and
(4) the Turonian () Midnight Peak Formation (Figure 3). This belt extends from
Washington to the 49 o parallel; no equivalent strata to this belt have been mapped in
Manning Park (Haugerud et al., 1996; Coates, 1974). The eastern belt is found in both
northern WA and in Manning Park and contains many of the units found in the western
belt. Stratigraphically upwards the belt contains: (1) the late Albian Big Buck member

30
of the Winthrop Formation (which conformably overlies the Jackass Mountain Group; (2)
the Albian to Cenomanian() Winthrop Formation; (4) the Cenomanian to Turonian ()
Ventura Member of the Midnight Peak Formation; and (5) the Cenomanian to Turonian
() Lone Man Ridge sandstone (Ralph Haugerud et al., 1996; Haugerud, personal.
communication, 1997; Kiessling and Mahoney, 1997; Kiessling et al., 1997) (Figure 3).
The eastern belt represents a facies variation of the western belt within the
Methow basin. Most workers agree that the Winthrop Formation on the west side of the
Methow basin is equivalent to identical trough-cross-stratified sandstone (Winthrop
Formation) on the east side of the basin in Washington and Manning Park (Cole, 1973;
Tennyson, 1974; Barksdale, 1975; Monger and Journeay, 1994; Haugerud et al., 1996;
Kiessling and Mahoney, 1997). Tennyson (1974) documented interfingering between the
Winthrop Formation to the east and the Virginian Ridge Formation to the west suggesting
that these two units are facies equivalents. The Ventura Member, although somewhat
lithologically different in the two belts, is easily recognized by its red color, plagioclaseporphyritic
andesite clasts and stratigraphic position above the Winthrop Formation. In
the east belt the Turonian () Lone Man Ridge sandstone conformably overlies the
Ventura Member of the Midnight Peak Formation and appears to have no correlative
strata within the western belt (Ralph Haugerud, personal communication, 1997).
LITHOFACIES
This section describes the stratigraphy and defines lithofacies for the Pasayten
Group in Manning Park. These are then correlated with the stratigraphy in the Methow
Valley established by Haugerud et al. (1996).

31
Strata within the Pasayten Group were subdivided into 6 lithofacies to facilite
description of the sedimentary succession. Each stratigraphic unit contains one or more
of the following lithofacies: graded sandstone and mudstone; cross-stratified sandstone;
channelized sandstone; rippled siltstone, inverse-graded channel-fill; and tuffaceous
pebbly mudstone (Table 2). The lithofacies were designated based on grain size,
sedimentary structures, and textural maturity. Depositional interpretations from these
lithofacies were used to reconstruct the Methow basin.
GRADED SANDSTONE AND MUDSTONE FACIES
The graded sandstone and mudstone facies comprises most of the strata below
and forms a portion of the base of the Big Buck member of the Winthrop Formation
(Figure 3). This facies is dominated by thick (10 m) successions of laterally continuous,
normally-graded, thin- to medium-bedded (10-15 cm), fine- to medium-grained
sandstone (Figure 10). Sandstone beds may contain cross-stratified and current- and
climbing-rippled tops. The base of these beds is erosive and the lower portions of the
beds may contain mud-chip breccias. Sandstone beds grade from a medium- to coarsegrained
feldspathic arenite to clayey mudstone. Sandstones are interbedded with locally
thick (> 2m) successions of dark-gray mudstone. Indeterminate gastropods and bivalves
are locally abundant within this lithofacies.
The graded sandstone and mudstone facies is interpreted to represent marine
deposition in a prodelta setting. Boggs (1995) interprets sequences of laterally
continuous, normally-graded, planar beds overlain by cross-stratified sandstone beds and

33
Table 2. Pasayten Group lithofacies
Lithofacies Description Interpretation
Graded
sandstone
and
mudstone
Thick successions (>1 m) of medium-bedded (10-15 cm),
normally-graded, gray, subrounded to subangular, moderatelysorted,
medium- to coarse-grained, micaceous sub-feldspathic to
feldspathic arenite. The bases of sandstone beds ubiquitously
load the underlying beds. Cross-stratification and ripple marks
commonly occur at the top of sandstone beds. Sandstone is
commonly interbedded with dark gray laminated siltstone.
Siltstone is locally thick bedded (>2 m) and may display z-folds
and flame structures.
Turbidites in a prodelta
environment.
Crossstratified
sandstone
Medium- to thick-bedded (10-100 cm), gray, planar- and
trough- cross-stratified, moderately- to well-sorted, subangular
to subrounded, medium- to coarse-grained, subfeldspathic and
feldspathic arenite intercalated with locally fossiliferous dark
gray siltstone.
Migrating bars and
channel fill in a
delta-top
environment
Channelized
sandstone
Channelized, medium- to thick-bedded (

34
capped by mudstone as turbidites (Bouma C-E) (Figure 3.28, p. 73). These sequences are
present within the graded sandstone and mudstone lithofacies and are interpreted as
Bouma sequences (C-E). This interpretation is supported by thick sequences of laterally
continuous mudstone that contain marine fauna and display abundant soft-sediment
deformation.
CROSS-STRATIFIED SANDSTONE FACIES
The cross-stratified sandstone facies encompasses most of the Big Buck member
of the Winthrop Formation. This facies consists of medium to thick beds (< 2 m) of gray,
structureless to planar- and trough- cross-stratified sandstone with cosets < 25 cm (Figure
11). Sandstone ranges from medium- to coarse-grained and from feldspathic to
subfeldspathic arenite. Locally the sandstone contains abundant (< 2 cm) plutonic and
vein quartz pebble lags. Sandstone beds pinch laterally (> 5 m) and display sharp
erosive, undulose and locally concave-up bases < 50 cm deep and > 1 m wide. These
bases are commonly marked by abundant rip-up and mega rip-up clasts up to 50 cm and
locally abundant wood fragments (< 5 cm). Ripples commonly cap sandstone beds.
Geometric stacking patterns of sedimentary structures are highly complex. Locally
sandstone beds contain vertical (Skolithos) and horizontal burrows, and indeterminate
gastropods. Sandstone beds contain thick interbeds of laminated to thin-bedded siltstone
that commonly displays soft-sediment deformation. Siltstone beds contain locally
abundant ammonites (Hamites) and indeterminate bivalves. Overall this unit contains
multiple fining-upward sequences that range from 20 cm to 4 meters.

36
The cross-stratified sandstone facies represents distributary mouth-bars in a
subaqueous delta-plain environment. Multiple fining-upward sequences with marine
sediments and structureless sand beds have been interpreted as distributary-bar
deposition (Brown and Richards, 1989; Helland-Hansen et al., 1989). Sandstone beds
display trough-cross-stratification, planar-cross-stratification and asymmetrical ripples
indicating a current-driven environment commonly associated with delta-top settings
(Brown and Richards, 1989; Helland-Hansen et al., 1989). The presence of both
terrestrial flora and marine fauna support a marginal marine interpretation.
CHANNELIZED SANDSTONE
The normally graded channel facies is the most common of the lithofacies and is
dominant within the upper member of the Winthrop Formation and the Lone Man Ridge
sandstone. This facies is also present in the Big Buck member of the Winthrop
Formation and the Ventura Member of the Midnight Peak Formation. The facies is
characterized by sequences of channelized sandstone and conglomerate that fine
vertically (< 5 m) into fine-grained sandstone and siltstone. Channels may be nested or
independent and locally are deeply erosive (Figure 12). Where the base is conglomeratic,
the clasts are usually imbricated and grade vertically depending on the clast size from
cobbles (< 50 cm) to pebbles (< 10 cm) into trough-, planar- and epsilon-cross-stratified
sandstone and finally into siltstone or mudstone (Figure 12). Clasts are sub-rounded and
moderately- to well-sorted. Where the base is sandstone, the sequence is similar, passing
into mudstone or siltstone from coarse-grained, subrounded to subangular, trough-

38
(locally over-steepened) and planar-cross stratified sandstone beds. In some units,
trough- cross-stratified sandstone passes into planar-cross-stratified sandstone and finally
into the rippled siltstone lithofacies. In other units, the trough- cross-stratified sandstone
occurs without the other sedimentary structures. Channels are commonly < 5 m wide.
The base of all the channels is erosive and commonly contains wood fragments.
The channelized sandstone facies was deposited as sinuous- and straight-crested
dunes within channels and point or transverse bars in a fluvial system. Channel
deposition is recognized by concave-up sandstone bases that display locally abundant
insitu wood and logs (Miall, 1996). Channels are locally filled with trough and planar
cross-stratified sandstone characteristic of point and transverse bars (Plint, 1983).
Trough-cross-stratified sandstone indicates sinuous-crested dunes while planar-or
tabular-cross-stratification is commonly caused by straight-crested dunes and lateral
accretion (Plint, 1983; Boggs, 1995; Miall, 1996). Sandstone beds that pass from troughcross-stratified
sandstone into planar-cross-stratified sandstone and finally into the
rippled siltstone lithofacies are interpreted as point bar sequences while sandstone beds
that lack the planar-cross-stratified sandstone beds and the rippled siltstone lithofacies are
intrepreted as transverse bars (Figure 13) (Boggs, 1995; Miall, 1996).
RIPPLED SILTSTONE
The rippled siltstone facies composes the fine-grained strata within the Winthrop
Formation. Medium to thick beds (< 2 m) of climbing-ripple and current-ripplelaminated
siltstone pass up section (< 5 m) into massive fossiliferous siltstone (Figure

40
14). Locally this facies contains trough- cross-stratified very fine-grained sandstone with
cosets < 10 cm. Fossils are ubiquitously carbonized wood and leaves (ferns) with
uncommon vertical and horizontal burrows.
The rippled siltstone facies is interpreted as bar-top and overbank deposits in a
meandering fluvial environment. A bar-top interpretation is suggested by the
stratigraphic location of this lithofacies above the channelized sandstone lithofacies.
Commonly this facies is laterally restricted (10 m). Miall
(1996) interpreted laterally extensive rippled siltstone and fine-grained sandstone as
overbank deposits.
INVERSE-GRADED CHANNEL FILL
The inverse-graded channel fill facies is restricted to and dominates the coarsegrained
strata within the Ventura Member. This facies is dominated by deeply-incised
channelized sandstone and pebbly sandstone that coarsens vertically into poorly-sorted
conglomerate. The sandstone within these channels is commonly green, moderatelysorted,
subangular lithic feldspathic arenite and wacke. Conglomerate contains poorly
sorted, angular, matrix-supported, volcanic and sedimentary, pebble to boulder sized
clasts which appear to lack a preferred orientation (Figure 15). Locally conglomerate
beds contain large, angular blocks of tuffaceous sandstone. Channels are commonly

42
The inverse-graded channel fill facies is non-systematically intercalated with the
channelized sandstone facies. The inverse-graded channel fill facies is interpreted to be
deposited by debris flows in a fluvial environment. The poorly-sorted nature of these
deposits coupled with matrix-supported conglomerates and inverse-graded beds indicate
debris flow deposition (Wells, 1984; Miall, 1996). The local appearance of intercalated
beds of the channelized sandstone facies dictates that the inverse-graded channel fill
lithofacies was deposited within a fluvial environment.
TUFFACEOUS PEBBLY MUDSTONE
The tuffaceous pebbly mudstone facies is present only within the Ventura
Member of the Midnight Peak Formation and is easily recognized in the field by its red
color. This facies is characterized by thick beds (< 1 m) of poorly sorted, red mudstone
interbedded with lesser amounts of green sandstone. Mudstone beds contain local
calcareous nodules, floating clasts (< 6 cm) of volcanic tuff and angular, coarse feldspar
grains (Figure 16). Sandstone beds are thin- to medium-bedded (< 50 cm), parallel- to
cross-laminated, moderately-sorted, medium- to coarse-grained, calcite-cemented,
volcanic lithic arenite. The basal contact of the sand beds is sharp and erosive while the
upper contact may be either gradational into red mudstone or sharp. Sandstone and
mudstone beds are laterally extensive and are truncated by either the channelized
sandstone or the inverse-graded channel fill facies (see above).
The tuffaceous pebbly mudstone facies is interpreted as bioturbated overbank
deposits and channel plugs within a fluvial environment. This study agrees with previous
workers who suggested the lack of internal structures within this facies indicates a

44
reworking of the mudstone due to burrowing (Haugerud et al., 1996). This burrowing
probably causes the floating pebbles and the calcareous concretions. Alternatively this
facies may have been deposited during mudflows. These flows would also display
floating pebbles but would probably lack the concretions (Davis, 1992; Miall, 1996).
The thin- to medium-bedded parallel-laminated sandstone beds are interpreted as
channel-plug deposits when they occur in conjunction with the inverse-graded channel
fill facies (Winston, 1982; Miall, 1982; Miall, 1996) Finally, the parallel-laminated and
cross-stratified sandstones that occur in thick sequences (>2 m) intercalated within the
red mudstone and independent of the other facies are interpreted as high flow-regime
overbank deposits.
STRATIGRAPHY
The stratigraphy of the Pasayten Group in Manning Park has not been described
in detail beyond the original work of Coates (1970, 1974). This study modifies the threefold
subdivision of Coates (1970, 1974) by adding a unit (the Big Buck member)
previously included in the Jackass Mountain Group to the Winthrop Formation (Figure
3). The Pasayten Group is now subdivided into, in ascending order: (1) Big Buck
member of the Winthrop Formation (the Hamites beds in map-unit 10 of Coates, 1974), a
thick (650 m) succession of interbedded feldspathic arenites and mudstones with locally
abundant Hamites; (2) Winthrop Formation (map-unit 11 of Coates, 1974), a thick (>800
m) succession of trough- cross-stratified micaceous feldspathic arenite with interbedded
siltstone; (3) Ventura Member of the Midnight Peak Formation (map-unit 12 of Coates,
1974), a thin (

45
mudstone; and (3) the Lone Man Ridge sandstone (map-unit 13 of Coates, 1974), a
succession of planar- to trough- cross-stratified chert- and volcanic-lithic sandstone with
minor amounts of siltstone and chert-pebble conglomerate (Kiessling and Mahoney,
1997). These units are revised from the previous stratigraphic nomenclature and refined
from the unit descriptions of Coates (1970, 1974) and Kiessling and Mahoney (1997).
WINTHROP FORMATION
The Winthrop Formation is the basal unit of the Pasayten Group in Manning Park,
where it is exposed in a westward dipping monocline in the footwall of the Chuwanten
thrust fault (Plate 1). The Winthrop Formation in Manning Park is approximately 1900
m thick and consists of the basal Big Buck member and the overlying main body. The
Winthrop Formation in Washington contains two members, the Yellow Jacket Member
(which occurs locally throughout the Winthrop Formation) and 3 AM Mountain Member
(Haugerud et al., 1996). The main body of the Winthrop Formation is dominated by
trough- cross-stratified sandstone and interbedded siltstone. Along the eastern margin of
the Methow terrane, in WA, the Winthrop Formation is laterally contiguous to the Big
Buck member of the Winthrop Formation, in Manning Park, and therefore directly
correlative (Ralph Haugerud, personal communication, 1997).
The Winthrop Formation overlies marine rocks of the Albian Jackass Mountain
Group and is overlain by the Ventura Member of the Midnight Peak Formation. The
Winthrop Formation forms prominent ridges characterized by lichen-covered outcrops.
Particularly good exposures occur north of Highway 3 on Spotted Nellie Ridge, west of
the 1 st Brother Mountain and southeast of Nicomen Ridge (plate 1).

46
Big Buck member
The Big Buck member represents ~650 m of strata best exposed at the type
section on an east facing ridge between Big Buck Mountain and 1 st Brother Mountain
(663000E, 5446500N). At this type location, the Big Buck member gradationally
overlies the Jackass Mountain Group and underlies the upper member of the Winthrop
Formation. At any locality, the Big Buck member displays the graded-sandstone and
mudstone, cross-stratified sandstone and channelized-sandstone lithofacies. The marine
graded-sandstone and mudstone lithofacies is locally interbedded with the terrestrial
channelized sandstone lithofacies and intercalated with the cross-stratified sandstone
facies. The graded sandstone and mudstone and cross-stratified sandstone lithofacies
comprise most of the basal part of this unit.
Near the top of the member (at 150 m), the graded sandstone and mudstone
lithofacies is replaced by the channelized sandstone lithofacies. Here the channelized
sandstone facies is interbedded with the cross-stratified sandstone facies.
The channelized sandstone facies commonly contains lenticular (< 10 m) plutonic
and volcanic cobble conglomerates that grade vertically (< 10 m) into feldspathic
sandstones and siltstones. Conglomeratic lenses are commonly nested within discrete
beds that can be traced laterally over 1 km. Clasts within the lenses are moderately
sorted, subrounded, and well-imbricated. Similar stratigraphic architectures can be
found on the 4 th Brother Mountain and along Cable Creek just north of Highway 3 (Plate
1).

47
Contact relations
The conformable nature of the Winthrop Formation and the underlying Jackass
Mountain Group has led to repeated refinements to the definition of the contact between
these two units. Coates (1974) suggested that the lower contact of the Winthrop
Formation be placed above the stratigraphically highest marine fossils of the Jackass
Mountain Group. This contact designation would place marine and marginal marine
rocks into the Jackass Mountain Group and restrict terrestrial strata to the Pasayten
Group (Coates, 1970; 1974). The youngest marine strata recognized by Coates (1974)
are characterized by the locally abundant Albian ammonite Hamites, found within dark
shale intercalated with sandstone. However, fossiliferous strata are only locally present
and do not constitute an easily recognizable lithologic boundary. Kiessling and Mahoney
(1997) defined the base of the Winthrop Formation as the first appearance of troughcross-stratified
sandstone above structureless to planar- cross-stratified sandstone of the
Jackass Mountain Group. This is awkward since it places strata lithologically and
sedimentologically identical to the Winthrop Formation into the Jackass Mountain
Group.
This study further revises this contact to be the top of the last thick (> 6 m)
siltstone succession above which planar- and trough-cross-stratified sandstone of the
Winthrop Formation is predominant and below which normally-graded, parallel-bedded
sandstone of the Jackass Mountain Group dominates. This gradational lower contact is
best exposed west of 1 st Brother Mountain and more poorly exposed on Chuwanten
Mountain and Spotted Nellie Ridge. This designation places approximately 650 meters
of strata that display characteristics of both units into the Big Buck member of the

48
Winthrop Formation. The upper contact of this member is placed at the transition from
dominantly planar- and trough-cross stratified sandstone with plutonic cobble
conglomerates of the Big Buck member to trough- cross-stratified sandstone of the main
body of the Winthrop Formation. This contact is best exposed west of the Heather Trail
on a western ridge between Big Buck Mountain and 1 st Brother Mountain. This new
contact places marginal marine rocks into the Big Buck member of the Winthrop
Formation and restricts fluvial rocks to the main body of the Winthrop Formation.
Lithology
The main body of the Winthrop Formation is lithologically monotonous, and is
dominated by the channelized sandstone and rippled siltstone lithofacies. The
channelized sandstone facies within this unit displays well-developed fining-upward
sequences, 1 to 5 m thick, and less commonly large amalgamated sandstone beds, 3 to 10
m thick, composed of nested channels. Sandstone beds are characterized by ubiquitous
trough-cross-stratification and lesser planar-cross stratification with cosets that are less
then 25 cm. Fining-upward sequences are cyclically stacked and grade from: a) the base
of the channel which locally contains insitu stumps, large logs and oriented wood
fragments; to b) medium- to coarse-grained trough cross-stratified feldspathic sandstone;
and finally into c) the rippled siltstone facies.
Clast count data
In the eastern belt, the Big Buck member of the Winthrop Formation contains
plutonic and volcanic cobble conglomerate. This conglomerate displays slightly-foliated
to non-foliated, subrounded to rounded clasts and is clast- to locally matrix-supported.

49
Clasts included plutonic (35 %) and volcanic (34%) clasts with lesser sedimentary(17%),
meta-volcanic (8%) and plutonic quartz (6%) clasts (one clast count, n = 750) (Figure
17).
Plutonic clasts range from 1-20 cm with the most common clast size from 1-5 cm.
These clasts vary in composition from phaneritic biotite-muscovite to hornblende tonalite
and tonalite gneiss.
Volcanic clasts range from .5-20 cm but are commonly between .5-5 cm. The
volcanic clasts are brown to green, plagioclase porphyritic andesite and dacite. A
subordinate amount of these clasts display a strong foliation and were classified as metavolcanics.
Sedimentary clasts are commonly .5-5 cm but range from .5-20 cm, and are
dominated by argillite and sandstone. Sandstone clasts are commonly micaceous
feldspathic arenites.
The Winthrop Formation in the western belt also displays a channelized volcanic
cobble conglomerate exposed on Sandy Butte, WA. This conglomerate differs from
conglomerates in the Big Buck member in that it contains primarily volcanic clasts,
ranging in composition from dacite to andesite, and lacks the plutonic clasts. The
conglomerate is subrounded to rounded and clast-supported with clasts that range in size
from 1-50 cm.
Lateral and vertical variations
The Winthrop Formation appears to become thicker-bedded but finer-grained
toward the southern margin of Manning Park. The entire formation may be described as
a

51
single fining-upward sequence, although a coarsening-upward succession is locally
evident at the base. In the Three Brothers Mountain area, the Big Buck member of the
Winthrop Formation coarsens upward from interbedded siltstone and sandstone of the
graded sandstone and mudstone facies into the cross-stratified sandstone facies and
finally plutonic and volcanic conglomerate of the channelized sandstone facies. From the
conglomeratic horizons of the Big Buck member, the Winthrop Formation fines upward
into micaceous feldspathic arenites of the main body of the Winthrop Formation. On
Spotted Nellie Ridge, north of Highway 3, at least 1400 m is exposed, with the Big Buck
member containing

53
Table 3. Mean paleocurrents for the Pasayten Group. Standard deviations were
determined using circular statistics after Krause and Geijer (1987).
Units
Winthrop
Formation
Big Buck
member
Number of
measurements
Unidirectional
mean
Number of
measurements
Bidirectional
mean
Number of
measurements
Total mean
112 287 o + /-46 o 164 323 o + /-46 o 276 276 o + /-48 o
66 323 o + /- 18 o N/A N/A 64 323 o + /- 18 o
Main body 46 235 o + /- 51 o 164 323 o + /-46 o 210 279 o + /- 69 o
Ventura
Member of the
Midnight Peak
Formation
Lone Man
Ridge
sandstone
88 88 o + /- 27 o N/A N/A 88 88 o + /- 27 o
198 120 o + /- 53 o 16 78 o + /- 72 O 214 99 o + /- 89 o
Depositional Environment
The base of the Big Buck member consists of the graded sandstone and mudstone,
cross-stratified sandstone, and channelized sandstone lithofacies. These lithofacies are
interpreted to be the major component of the fluvial-dominated delta. The complex
interbedding of both marine and nonmarine strata within these lithofacies, the lateral
discontinuity of the channelized sandstone and cross-stratified sandstone lithofacies and
the overall coarsening-upward succession indicates deltaic deposition (Alexander, 1989;
Pederson, 1989; Walker and James, 1992). A similar coarsening-upward transition from
graded sandstone to channelized sandstone in sediments within western Greenland was
interpreted as a fluvial-dominated deltaic deposit by Pederson (1989). Channelized
sandstone beds that contain locally abundant wood and both trough- and planar-crossstratification
indicate fluvial deposition (Walker and James, 1992). The presence of these
fluvial deposits and the prevalence of planar and trough cross-stratification indicating

54
unidirectional currents suggests that the deltaic complex was dominated by fluvial
processes.
The main body of the Winthrop Formation contains trough- cross-stratified
sandstones of the channelized sandstone facies. This facies is interpreted as point and
hybrid bars within either a sandy meandering (e.g. Wabash River) or a sandy braided
(e.g. Saskatchewan River) fluvial environment (Cant, 1982; Plint, 1983; Miall, 1982;
1996). Both fluvial environments are characterized by abundant trough-crossstratification
and local planar-cross-stratification, however, the meandering fluvial
system is characterized by stratigraphic architectures that display trough crossstratification
overlain by planar cross-stratification (Cant, 1982). This is typical in the
Winthrop Formation. The Winthrop Formation also contains locally thick sequences of
fine-grained “woody” siltstone that caps many of the normally-graded cycles which is
more characteristic of a sandy-meandering than a braided-fluvial environment (Miall,
1996). In summary, the Winthrop Formation marks the transition from a submarine fan
to a fluvial-dominated delta and finally a meandering fluvial system.
VENTURA MEMBER OF THE MIDNIGHT PEAK FORMATION
The Red bed (unit 12) unit of the Pasayten Group (Coates, 1974) in Manning Park
was defined as the Ventura Member of the Midnight Peak Formation by Kiessling and
Mahoney (1997). The prominent red coloration of the unit, its high volcanic clast
content, and its stratigraphic position above the Winthrop Formation support this
definition, although the unit apparently lacks the chert-clast component common in
exposures to the south (in the USA) within the western belt. The Ventura Member

55
weathers recessively, and is poorly exposed except on Spotted Nellie Ridge, Lone Man
Ridge and Monument Hill. In the northern and southern portions of the park, the unit is
truncated by east-vergent splays of the Chuwanten fault (Coates, 1974).
Contact relations
The base of the Ventura Member of the Midnight Peak Formation is defined as
the first appearance of red, volcanic-lithic mudstone overlying trough- cross-stratified
sandstone of the Winthrop Formation. The lower contact is exposed in the footwall of
the Chuwanten thrust about 1 km south of Monument Hill and in discontinuous
exposures on Spotted Nellie Ridge. South of Monument Hill, the contact is transitional
across approximately 50 m, with tan, medium-bedded (

56
channelized sandstone facies.
The channelized sandstone facies is intercalated throughout the Ventura Member
of the Midnight Peak Formation. Channels within this facies are lenticular and grade
from imbricated, pebble- and locally cobble-sized clasts to green planar-and troughcross-stratified
volcanic lithic arenite.
The inverse-graded channel fill facies forms less then 20% of the section and
contains a similar clast assemblage to the channelized sandstone facies except for
boulder-sized clasts (sometimes greater than 50 cm in diameter) of volcanic lithic
sandstone. These boulders are lithologically identical to sandstones within the Ventura
Member of the Midnight Peak Formation.
Lithofacies of the Ventura Member are irregularly interbedded, with sequences of
1-10 m of the tuffaceous pebbly mudstone commonly intercalated with 1-5 m sequences
of either the inverse-graded channel fill or the channelized sandstone facies. This
interbedding results in an outcrop pattern characterized by resistant conglomerate beds
standing in bold relief above recessively weathering red mudstone intervals.
Clast counts
In the eastern belt, the Ventura Member of the Midnight Peak Formation contains
channelized volcanic and sedimentary conglomerate. This conglomerate is dominated by
subrounded, matrix-supported, volcanic (40%) and sedimentary (52%) clasts with lesser
chert, plutonic and plutonic quartz (8%) clasts (Figure 19). Volcanic clasts range from
.5-10 cm with the most common clast size from 1-5 cm. These clasts are ubiquitously
green and brown, plagioclase-porphyritic andesite and dacite. Sedimentary clasts range

57
in size from .5-1 m but are commonly 1-5 cm. These clasts consist of buff to green, lithic
arenite and both green and red silicified siltstone.
The western belt contains channelized volcanic- and chert-pebble conglomerate.
These conglomerates range from subrounded to rounded with matrix-supported clasts.
Conglomerate clast composition varies from chert-rich to chert-poor (60% to 10%) and
from volcanic-poor to volcanic-rich (10% to 40%). Both chert and volcanic clasts range
in size from 1-5 cm. Sandstone, argillite, plutonic and plutonic quartz clasts form a
subordinate component of these conglomerates.
Lateral and vertical variations
The Ventura Member varies from 135 to 477 m thick in Manning Park (eastern
belt). The unit displays two coarsening-upward successions and appears to increase in
thickness but decrease in grain size from south to north. A maximum thickness of 477 m
was measured on Lone Man Ridge, where conglomerate comprises 20%
of the section. It is uncertain if this thickness variation is depositional, or is the result of
structural truncation along splays of the Chuwanten thrust.
Paleocurrents
Paleocurrent measurements from the Ventura Member of the Midnight Peak
Formation indicate east-directed transport (Table 3 and Figure 18). Trough crossstratification
and pebble imbrications (n = 88) were measured from sandstones and
conglomerates respectively. From these measurements, unidirectional paleocurrents
were

59
determined. These paleocurrents show a general east-directed transport that contradicts
Cole’s (1973) results that indicate west directed transport (n = 33).
Cole (1973) measured 33 bidirectional and unidirectional paleocurrent indicators
from the Ventura Member of the Midnight Peak in Washington. Out of these 33
measurements 14 unidirectional measurements indicate west directed paleocurrents while
11 unidirectional measurements indicate east-directed paleocurrents. This study places
more confidence in the east directed measurements based on: (1) less than 50% of the
paleocurrent measured by Cole (1973) suggest east to west transport; (2) the Ventura
Member of the Midnight Peak Formation is more deformed in WA than in Manning Park;
and 83 paleocurrent measurements from this study support east-directed transport.
Furthermore, McGroder (1991; Figure 3, p. 193) suggested east-directed transport for the
Ventura Member of the Midnight Peak Formation in Washington based on unpublished
data by Mohrig.
Depositional Environment
The Ventura Member records a change from a meandering-fluvial environment to
a proximal sediment-choked braided-fluvial system that is commonly inundated by
volcanic-rich debris flows. The Ventura Member is composed of both the tuffaceous
pebbly mudstone and the channelized sandstone facies in relatively equal proportions
with a lesser component of the inverse-graded channel-fill facies. Channelized
sandstones are interpreted as transverse bars filling small channels. The presence of
trough-cross-stratification and gravel- to cobble-lags within these channels supports this
interpretation. These channelized sandstones are interbedded with the tuffaceous-pebbly

60
mudstone facies which represents the overbank deposits. Intercalated within these facies
is the inverse-graded channel-fill facies indicating periodic inundation of the braidedfluvial
environment by debris flows. The lack of lateral continuity of sandstone and
conglomerate beds within either the channelized sandstone or inverse-graded channel fill
facies suggests that channel avulsion or abandonment may have played an important role
in deposition (Miall, 1996).
LONE MAN RIDGE SANDSTONE
The Lone Man Ridge sandstone (Unit 13 of Coates, 1974; and the conglomerate
of Hampton Creek of Kiessling and Mahoney, 1997) forms the uppermost unit of the
Pasayten Group and comprises the youngest strata in Manning Park. Kiessling and
Mahoney (1997) informally designated this unit the conglomerate of Hampton Creek
based on exposures on Lone Man Ridge and Monument Hill. This study maintains an
informal designation for this unit but changes its name to the Lone Man Ridge sandstone
based on: (1) the relative paucity of conglomerate and the dominance of sandstone
within this unit; and (2) the location of the type section.
The Lone Man Ridge sandstone forms the westernmost beds of the west-dipping
monocline in the footwall of the Chuwanten thrust fault. This unit extends from possibly
just south of the international border, where it is highly deformed in the core of a
syncline (Ralph Haugerud, personal communication, 1997), to just west of Three
Brothers Mountain where it is truncated by the Chuwanten fault. The unit is underlain by
the Ventura Member and the upper portion of the unit is truncated by the Chuwanten
fault at all localities (Plate 1). The best exposures of this unit are on Monument Hill,

61
where it forms prominent cliffs, but the section on Lone Man Ridge is thicker and is more
accessible.
Contact relations
The Lone Man Ridge sandstone conformably overlies the Ventura Member. The
lower contact is best exposed on Monument Hill, where green volcanic-lithic sandstone
and red mudstone of the Ventura Member pass gradationally into green to buff volcaniclithic
sandstone and chert-pebble conglomerate of the Lone Man Ridge sandstone. This
lower contact is placed at the first appearance of chert-pebble conglomerate and
approximately coincides with a distinct iron-stained horizon that contains calcareous
concretions (Figure 20). The upper contact of the Lone Man Ridge sandstone is not
exposed due to truncation along the Chuwanten thrust fault.
Lithology
The Lone Man Ridge sandstone contains the channelized sandstone facies. This
facies grades from imbricated chert, volcanic and plutonic pebble-conglomerate to
sandstone and locally to siltstone (Figure 21). Channel bases are erosive and locally
contain oriented wood (< 15 cm). Clast-supported conglomerate commonly grades
normally into matrix-supported conglomerate with both planar- and epsilon-crossbedding.
The sandstone is composed of tan, thin- to medium-bedded, medium- to coarsegrained
volcanic lithic arenite. Isolated chert, volcanic and plutonic pebbles are locally
present. Sandstone beds display trough-cross-stratification near the base and are usually

63
capped by planar-cross-stratification (cosets for both types of stratification ~ 10 to 25
cm). Siltstone beds are dark-gray and display parallel and climbing-ripple laminations,
and abundant wood fragments.
At the type locality on Lone Man Ridge (UTM coordinates, 5441000N,
663500E), the volcanic-lithic sandstone is interbedded with tuffaceous sandstone. Here,
approximately 30 m of red-gray, thin- to medium-bedded tuffaceous sandstone with
circular green devitrification spots are present 280 m above the base of the unit.
Clast counts
The Lone Man Ridge sandstone contains channelized chert-pebble
conglomerates. This conglomerate is dominated by dark-gray, subrounded to rounded,
clast-supported chert (50 %) and volcanic (40%) clasts with lesser (10%) sedimentary,
plutonic and plutonic quartz clasts (Figure 19). All of the clasts range from .5-5 cm with
1-5 cm being the most common pebble size. Chert clasts are commonly black to darkgray,
fractured and veined chert. Volcanic clasts range from green to brown and are
plagioclase porphyritic andesite and dacite.
Lateral and vertical variation
The Lone Man Ridge sandstone displays a single (~300 m) fining-upward
succession throughout the Manning Park area. At the type section, the succession fines
upward from chert-lithic arenite intercalated with lenticular conglomerate to chert-lithic
arenite interbedded with siltstone and minor lenticular conglomerate and tuffaceous

65
sandstone. Similar fining-upward successions occur on Spotted Nellie Ridge and
Monument Hill.
Lateral thickness variations within the Lone Man Ridge sandstone are obscured
due to structural truncation beneath the Chuwanten thrust fault. The maximum thickness
observed is 374 m in the type section; the minimum thickness of 173 m occurs on
Monument Hill (plate 1).
Paleocurrents
Paleocurrents from the Lone Man Ridge sandstone indicate east-directed transport
(Figure 18). Pebble imbrications, planar (epsilon)- cross-stratification and channel axes
were measured (n = 214) to determine both unidirectional and bidirectional currents.
Unidirectional current indicators exhibit a mean current of 120 o (Table 3).
Depositional Environment
The Lone Man Ridge sandstone records a change from the braided system of the
underlying Ventura Member to a meandering fluvial environment. The Lone Man Ridge
sandstone is dominated by the channelized sandstone facies. This facies displays a
gradation from lenticular conglomerates (< 2m) to locally trough-cross-stratified and
epsilon-cross-stratified sandstone and finally to uncommon siltstone. The ubiquitous
epsilon cross-stratification within this facies and the concentration of pebbles in lag
deposits indicates deposition within the point bar characteristic of meandering fluvial
systems (e.g. Endrick, Wabash and Amite Rivers) (Rust, 1982; Plint, 1983). This
depositional system was probably very similar to the Winthrop Formation except that the

66
Lone Man Ridge sandstone lacks the mud fraction and the logs common in the Winthrop
Formation and yields paleocurrents that indicate a southeast transport direction. The
paucity of fine-grained deposits suggests that this may not be a simple meandering
system but a hybrid braided-meandering system (Miall, 1996).

67
CHAPTER 4. PROVENANCE OF THE PASAYTEN GROUP IN MANNING
PROVINCIAL PARK
INTRODUCTION
The provenance of mid-Cretaceous strata of the Methow terrane is critical in
resolving the ongoing debate over large-scale latitudinal displacements of major blocks
of the Canadian Cordillera (Cowan, 1994; Wynne et al., 1996; Irving et al., 1995; 1996;
Monger and Price, 1996). Cole (1973) used stratigraphic, petrologic and paleocurrent
arguments to suggest that Methow basin strata were derived from plutonic rocks east of
the Pasayten fault (on the Intermontane superterrane). Coates (1970; 1974) also inferred
that at least a portion of the Pasayten Group was derived from the east, based on the
presence of plutonic and volcanic conglomerates containing clasts lithologically identical
to rocks east of the Pasayten fault.
Recent geophysical and some geological studies have suggested that right-lateral,
margin-parallel, large-scale translation has occurred between the Methow terrane and the
rocks to the east (the Intermontane superterrane) (Garver and Brandon, 1994; Irving et
al., 1995; 1996; Wynne et al., 1996). Therefore this provenance tie has become crucial in
the debate.
This section provides the first detailed study of provenance of the Pasayten Group
in Manning Park, British Columbia. The section focuses on establishing provenance
links across the Pasayten fault using sedimentary petrology, paleocurrents, clast
compositions and the age of detrital zircons from the Pasayten Group in Manning Park
and northern Washington.

68
WINTHROP FORMATION
PETROLOGY
In the eastern belt, the Winthrop Formation is initially a feldspathic arenite
(Q 40 F 55 L 5 ) that changes vertically to a volcanic-lithic arenite (Q 30 F 30 L 40 ). Argillite
represents the dominant lithic type (Lm 40 Lv 0 Ls 60 ) within the feldspathic arenite near the
base of the section. Near the top of the section, felsic and lathwork volcanics form the
dominant grain type (Lm 20 Lv 79 Ls 1 ). The majority of quartz grain types are
monocrystalline quartz (Q p /Q = .06). The monocrystalline quartz ubiquitously displays
undulose extinction and may contain aligned vacuoles. Plagioclase feldspar comprises
most if not all of the feldspar grains (P/F = .99).
Sandstones in the western belt are lithologically similar to these sandstones
except for a higher volcanic lithic content (n = 5) Q 20 F 70 L 10 and Lm 26 Lv 74 Ls 0 (Figure
22a).
Both east and west belts display an up-section increase in volcanic lithics (Figure
23). The base of the Winthrop Formation is characterized by high feldspar vs.
quartz+lithics. In the western belt, a plot of chert vs. total lithics shows an increase in
chert near the top of the formation (Figure 23).
Muscovite and biotite micas constituted

73
numerous (biotite) muscovite monzogranite stocks, dikes and sills. Plutonic clasts within
the Big Buck member are also muscovite-biotite granodiorites.
ZIRCONS
Whole rock U/Pb geochronology from one plutonic clast taken from the Big Buck
member of the Winthrop Formation reveals a mid-Albian crystallization date (Mahoney,
personal communication, 1998). Age constraints were derived from 3 colinear points
with a lower intercept of 108 +3 / -21 Ma and slightly off concordia between 111-114 Ma
(Figure 24).
The location of these points just below concordia indicates that this sample has
either undergone a thermal event (Faure, 1991) or that it may contain inherited zircons
(Pidgeon and Compston, 1991).
The preliminary whole rock age of 108-114 Ma is in exact agreement with
crystallization ages for the Falls Lake Plutonic Suite (of the Eagle plutonic complex),
(Monzanite age of 110 + /-0.5) (Grieg et al., 1992). This age overlap indicates that clasts
within the Big Buck member of the Winthrop Formation could have been derived from
the Falls Lake Pluton to the northeast.
PROVENANCE INTERPRETATION
The large proportion of granitic-derived sediment, plagioclase, quartz, biotite and
muscovite, and the relative lack of volcanic sand near the base of the Winthrop
Formation is evidence that its basal unit was derived solely from a plutonic terrane. A
volcanic source is indicated by the presence of volcanic conglomerates and volcaniclithic

75
sandstone. The presence of these two lithologies suggest a dissected arc may have
supplied the sediment to the Winthrop Formation. The location of this source terrane was
likely to the east of the Methow basin, supported by the west-directed paleocurrents.
The Big Buck member of the Winthrop Formation contains clasts lithologically
similar to the Falls Lake Plutonic Suite suggesting that the pluton could have been one of
the eastern sources. This interpretation is supported by the whole-rock crystallization age
from the clast that overlaps the age range given for the Falls Lake Plutonic Suite.
Near the top of the Winthrop Formation within the eastern belt and in the western
belt, volcanic lithic fragments in sandstone become more common. These relationships
indicate that a volcanic source was located west of or within the Methow basin during
deposition of the Winthrop Formation. This new source is inferred to be the 3 AM
Volcanics to the west (the 3 AM Volcanics may represent initiation of the Midnight Peak
volcanic arc). This interpretation is supported by interbedding of Winthrop Formation
strata with andesitic and dacitic lava flows of the 3 AM Mountain Member near the
western portion of the basin, on Midnight Peak in the Methow Valley, WA (see chapter
2).
VENTURA MEMBER OF THE MIDNIGHT PEAK FORMATION
The Ventura Member of the Midnight Peak Formation records a braided fluvial
succession that prograded westerly into the Methow basin between late Albian and
possibly early Turonian time.
This unit consists of volcanic, chert- and feldspathic-rich sandstone intercalated
with chert, volcanic and sedimentary pebble to cobble conglomerate. Cole (1973) used

76
west-directed paleocurrents to suggest that this sedimentary unit was derived from the
Okanogan complex to the east. As discussed below, paleocurrents and clast counts from
this study provide evidence that this unit was derived from a volcanic source to the west.
PETROLOGY
Sandstones of the Ventura Member of the Midnight Peak Formation vary from
volcanic lithic arenite in the eastern belt to chert lithic arenite in the western belt. In the
eastern belt, sandstone of the Ventura Member of the Midnight Peak Formation display
compositions of Q 30 F 35 L 35 and Lm 30 Lv 60 Lst 10 (Figure 22b). Volcanic lithics within this
belt are commonly lathwork volcanics while metamorphic lithics are QM aggregates. In
the western belt, sandstones display more sedimentary lithic-rich compositions of
Q 15 F 20 L 55 and Lm 12 Lv 30 Lst 58 (Figure 22b) indicating they are chert-lithic arenites. Chert
forms the majority of the sedimentary lithics with lathwork volcanic grains comprising
most of the volcanics. Monocrystalline quartz dominates quartz grain types in the eastern
belt (Q p /Q = .06) where it ubiquitously displays undulose extinction and may contain
vacuole trains. Polycrystalline quartz or chert forms the majority of quartz grains in the
western belt, (Qp/Q = .65). Plagioclase feldspar comprises nearly all of the feldspar
grains (P/F = .99).
Sandstones from the Ventura Member of the Midnight Peak Formation display a
westward increase in chert. In the eastern belt sandstone is characterized up section by
an increase followed by a decrease in the plagioclase vs plagioclase + quartz (Figure 23).
Quartz in the sandstones tends to decrease up-section while the ratio of volcanic lithics to
total lithics displays a trend similar to that of the plagioclase (Figure 23). In the western

77
belt, sandstones contain a substantial portion of chert. In this belt, the ratio of chert to
total lithics increases from almost zero in the Winthrop Formation to > 50% in the
Ventura Member of the Midnight Peak Formation (Figure 23).
Detrital muscovite formed a small percentage of the grains counted.
DETRITAL ZIRCONS
Detrital zircon ages data from the Ventura Member of the Midnight Peak
Formation were obtained from 50 grains in one sandstone sample. Probability curves
show that most of the grains are bracketed between 80 and 280 Ma with prominent peaks
at 110 Ma, 120 Ma, 150 Ma, 178 Ma, 190 Ma, 207 Ma and 250 Ma, evidence of
derivation from Permian to Cretaceous sources (Figure 25). These curves also display a
smaller peak at ~2580 Ma, evidence of an Archean provenance (Figure 25).
PROVENANCE INTERPRETATION
East-directed paleocurrents (chapter 2), the restriction of chert-rich strata to the
western basin, and the increased size of volcanic-clasts in the western basin provide
evidence that the Ventura Member of the Midnight Peak Formation was derived from
both a western volcanic- and chert-rich source.
The chert-rich strata within the Ventura Member of the Midnight Peak Formation
were probably derived from the Bridge River terrane and possibly from the uplift of the
Virginian Ridge Formation (Haugerud et al., 1996). The lack of chert-pebble
conglomerate clasts within the Ventura Member of the Midnight Peak Formation argues

79
for a “primary” (a source that contains oceanic deposited chert) chert-rich source terrane.
The Hozameen Group of the Bridge River terrane forms the only “primary” chert-rich
source immediately west of the Methow basin. This study agrees with previous workers
(Cole, 1973; Garver, 1989) who have proposed the Bridge River terrane as the primary
chert source for the Ventura Member of the Midnight Peak Formation.
Based on volcanic clasts within the Ventura Member of the Midnight Peak
Formation that are lithologically identical to the Midnight Peak andesite; and (2)
interbedding of the Midnight Peak Formation lava flows with Ventura Member of the
Midnight Peak Formation sediments, the Midnight Peak volcanic arc is interpreted to be
the western volcanic source (Barksdale, 1975; Haugerud et al., 1996).
Detrital zircons in the Ventura Member of the Midnight Peak Formation form a
potential link to the North American margin to the east. Table 4 displays potential source
terranes for the detrital zircons. The entire population of detrital zircons can be matched
to plutons to the east suggesting the Ventura Member could have received sediment from
the Okanogan Range Batholith and/or the Falls Lake Plutonic Suite, the Eagle tonalite,
the Zoa Complex and/or the Eagle gneiss, the Copper Mountain Suite and the Guichon
Suite. These correlations permit a mid- to Upper-Cretaceous link between the Methow
basin and the Intermontane superterrane. It is also possible that similar crystallization
ages may exist for plutons within Mexico and these plutons could have provided
sediment to the Methow basin.
Paleocurrents within the Ventura Member of the Midnight Peak Formation argue
against an eastern source. Large sandstone boulders within the Ventura Member of the

80
Midnight Peak Formation argue for intrabasinal tectonics (see Chapter 2). Haugerud et
al. (1996) and McGroder (1991) have suggested that contraction may have been
Table 4. Potential source terranes for detrital zircons within the Ventura Member of the
Midnight Peak Formation.
Zircon
population from
sandstone
sample
Age of
crystallization for
potential source
Name of potential source
References
110 Ma 107-115 Ma
110 + /- 2 Ma
Okanogan Range Batholith
Falls Lake Plutonic Suite
Hurlow and Nelson,
1993
Grieg et al., 1992
120 Ma 123 + /- 5 Ma Eagle tonalite (Manning Park) Grieg et al., 1992
150 Ma 153 + /- 10 Ma
~156 Ma
148 + /- 4 Ma
Zoa Complex
Eagle Tonalite (Hwy 5 and
Murphy Lakes)
Eagle gneiss
Grieg et al., 1992
178 -198 Ma 170-209 Ma Copper Mountain Suite Woodsworth et al.,
1991
207 Ma 200-210 Ma Guichon Suite Woodsworth et al.,
1991
occurring along the Chuwanten thrust fault causing uplift of the Virginian Ridge and
possibly the Winthrop Formation. Therefore, eastern-sourced detrital zircons could have
been transported from west to east.
Some workers have suggested that the presence of Archean zircons within the
Methow basin (part of the Insular superterrane) restricts deposition of these sediments to
northern latitudes where Archean source terranes crop out (Cowan, 1994; Cowan et al.,
1997; Mahoney et al., 1997; Mustard et al., 1998). The presence of Archean zircons
within Ventura Member of the Midnight Peak Formation sandstone suggests that at least

81
some of the sediment within this unit could have been derived from Archean crust
generally found north of latitude 35 o within North America (Mahoney et al., 1997).
LONE MAN RIDGE SANDSTONE
The Lone Man Ridge sandstone records a Cenomanian to Turonian-age
meandering fluvial sequence that, like the Ventura Member of the Midnight Peak
Formation, was derived from the west. As discussed below, this unit is dominated by
ubiquitous volcanic-lithic arenite intercalated with chert-and volcanic-rich pebble
conglomerate. Coates (1974) inferred the chert-rich Hozameen Group was the primary
source for this unit.
PETROLOGY
The Lone Man Ridge sandstone displays compositions of Q 20 F 40 L 40 and
Lm 10 Lv 70 Lst 20 indicating its a volcanic-lithic arenite (Figure 22c). The majority of
volcanic lithics are felsic with lesser lathwork grains. Sedimentary lithics are
ubiquitously chert (Qp/Q = 50), while metamorphic lithics are meta-chert grains (Qm
aggregates). Monocrystalline quartz comprises a range of quartz grains from Qp/Q = .1
to .7 and are commonly undulose (Qmu/Qm = .7). Plagioclase feldspar comprises most
of the feldspar grains with P/F = .85. This sandstone commonly displays < 2% detrital
mica.
Sandstones from the Lone Man Ridge sandstone display an up section increase in
plagioclase vs quartz + total lithics (Figure 23). They also display the highest chert vs.

82
total lithic ratios (.25) within the eastern belt. The Winthrop Formation and the Ventura
Member of the Midnight Peak Formation display chert ratios of < .01.
PROVENANCE INTERPRETATION
East-directed paleocurrents suggest that the Lone Man Ridge sandstone was
derived from volcanic- and chert-rich source terranes.
Pebble counts in the chert-rich strata within the Lone Man Ridge sandstone
provide evidence it was derived from the Bridge River terrane. Alternatively, the chertrich
component may have been cannibalized from the uplifted chert-rich Virginian Ridge
Formation in the hanging wall of the Chuwanten thrust fault but the lack of chert-pebble
conglomerate clasts within this unit argues against this second hypothesis.
Petrographic study reveals abundant, relatively fresh, felsic and lathwork volcanic
lithics, evidence that during deposition of the Lone Man Ridge sandstone, active
volcanism was occurring proximal to the basin. One airfall tuff is present at the top of
the unit on Lone Man Ridge. The stratigraphic position of this unit directly above the
Ventura Member of the Midnight Peak Formation (Figure 3) and the presence of volcanic
lithics and tuffs suggest that this unit is possibly correlative with the Midnight Peak
Formation. The Midnight Peak arc is a plausible source terrane for the volcanic lithics
within the Lone Man Ridge sandstone.

83
CHAPTER 5. GEOCHEMICAL CORRELATION OF THE PASAYTEN GROUP
TO THE INTERMONTANE SUPERTERRANE
INTRODUCTION
The basal conglomeratic Big Buck member of the Winthrop Formation contains
abundant plutonic and volcanic clasts that appear lithologically identical to bedrock east
of the Pasayten fault. Two source terranes occur east of the Pasayten fault and are
proposed for the volcanic cobbles: the Cretaceous Spences Bridge Group and the
Triassic Nicola Group (Coates, 1970; 1974; Cole, 1973; Tennyson and Cole, 1978;
1987). Only sparse geochemical data exist for the Nicola Group.
This study focuses on comparing the plutonic cobbles of the Big Buck member of
Winthrop Formation to the Eagle Plutonic Complex. The Eagle Plutonic Complex is
composed of 157 Ma to 110 Ma, foliated and nonfoliated, granitic and tonalitic plutons
that intrude the Intermontane superterrane immediately east of the Pasayten fault (Grieg,
1992; Grieg et al., 1992).
Geochemical correlation of plutonic clasts to possible source terranes may
provide a possible link between the Methow terrane, part of the Insular superterrane, and
the Intermontane superterrane. Major and trace element geochemistry was performed on
both the plutonic clasts and lithologically similar rocks in the Eagle Plutonic complex.
The focus of this portion of the study is to use this geochemical data to evaluate the
plausibility of a geochemical correlation between the plutonic clasts and the proposed
source terrane.

84
SAMPLING UNCERTAINTIES
This section addresses the sampling errors that were inherit when sampling the
cobble conglomerate and the pluton for geochemical correlation. Although an attempt
was made to collect lithologically dissimilar clasts, the size of the cobbles dictated the
samples chosen. The clasts contained large phenocrysts of both plagioclase and K-spar
(10 cm diameter) clasts were collected to insure a
representative sample. Most of the larger, fresh clasts that were sampled were quartzrich
and therefore lithologically similar because quartz-deficient clasts tended to be too
small to sample. The size of each clast also restricted the number of samples collected;
most of the clasts present within the conglomerate were

85
into a tungsten-carbide ring mill and powdered to

86
Wisconsin-Eau Claire. Each pressed pellet was formed by mixing 4 grams of sample
with .4 grams of Spectroblend. The mixture was then placed into a die press and hand
pressed into a small, < 3 cm, pellet. Enough boric acid was added to surround the pellet
and fill the die press ~ ¼ full. The die press was then placed into a hydraulic press and
compressed to approximately 21.5 metric tons for 1-1.5 minutes to form a casing for the
pellet.
The pellets were analyzed for V, Co, Cu, Zn, Rb, Sr, Y, Zr, Nb, Ba, and Pb in a
Siemens SRS 3000 X-ray fluorescence spectrometer. Estimated analytical uncertainties
are: 1-5% for V, Co, Rb, Sr, Y, Zr, and Ba; 5-10% for Nb, Cu, and Zn; and 10-15% for
Pb. Actual analytical uncertainties may be ascertained by contacting J. Brian Mahoney at
the University of Wisconsin-Eau Claire.
TRACE AND RARE-EARTH ELEMENT ANALYSIS
Neutron Activation Analysis of powdered samples for rare-earth and trace
element abundances was done at the Laboratory for Environmental Geochemistry at
Idaho State University. Between .6000 and .7000 grams of powdered sample (see sample
preparation) was weighed and encapsulated into a 2/5 dram polyethylene vial. Each vial
was sealed by melting the top and then placed into a 2 dram polyethylene vial which was
also sealed and numbered. The samples and standards (BHVO-1, CRB-1 and 1633-A)
were irradiated for 2 hours in the Oregon State University megawatt TRIGA reactor.
The samples were counted sequentially using Idaho State University’s High
Purity Germanium detector array (HPGe). Three counts of 3,600, 10,000 and 20,000
seconds were performed to establish peak statistics on Sc, Cs, La, Ce, Nd, Sm, Eu, Tb,

87
Yb, Lu, Hf, Th, Rb, and U. Analytical uncertainties (2 sigma, 95% confidence level) for
these elements are: 0.1-1% for Sc, Ce, Sm, and Eu; 2-4% for La, Yb, Lu, Hf, Th; 5-10%
for Tb, 10-15% for Rb, Cs, and Nd; and 20% for U (Scott Hughes, personal comm.,
1998).
RESULTS
MAJOR ELEMENTS
Major element plots, excluding K 2 O, show two distinct clusters, one of plutonic
clasts and the other of the plutonic bedrock. Figure 26 displays the major elements
plotted against silica for each sample (Cox et al., 1979). The plutonic clasts display a
tight cluster of data, with one outlier, while the plutonic bedrock samples display a linear
arrangement (Figure 26). The majority of plutonic clasts display higher percentages of
SiO 2 and lower percentages of the major elements (except for Na 2 O which is
approximately equal to the bedrock samples). Bedrock samples display greater major
element variation in SiO 2 , CaO, MgO, Fe 2 O 3, and P 2 O 5 than do the bedrock samples. For
the remaining major elements, the variation between sample suites is about equal. Table
5 lists the major element data from both the plutonic clasts and the Eagle Plutonic
Complex.
MINOR, TRACE AND RARE-EARTH ELEMENTS
The minor, trace and rare-earth elements were plotted on a rare earth element
diagram (“spider diagram”) and Harker diagrams (with respect to SiO 2 ). Rare-earth
element concentrations are listed in table 5 and the chondrite normalized rare-earth
element patterns are shown in Figure 27. This figure shows that all the plutonic bedrock

92
samples and most of the plutonic clasts (with the exception of samples 55EMK97 and
53JBM97) are enriched in the light rare-earth elements. Overall, the bedrock samples
display more enrichment than the plutonic clasts in all of the rare-earth elements. All of
the samples display an Eu anomaly except for 53BJBM97, 53AJBM97, 23BMK97 and
30MK97. Harker diagrams for these trace and rare-earth elements illustrate a relatively
tight cluster for the plutonic clasts (except for plots B, E and F which may display two
clusters) and ranges for the plutonic bedrock samples, which may reflect linear trends
(Figure 28). Both the clasts and the bedrock display relatively equal amounts of Sr, Zr,
Th, and Y while the plutonic clasts appear to show lower amounts of TiO 2 and greater
amounts of Ba.
Both sample suites were plotted on tectonic discrimination diagrams developed
by Pearce et al. (1984). These diagrams display distinct groupings of the two sample
types (Figure 29). The first plot, Nb vs. Y, displays a dispersion of the clast data and a
cluster of the plutonic bedrock samples around 100 ppm Y and 20 ppm Nb. The second
plot, Y+Nb vs. Rb, displays a slight overlap between the clasts and the pluton (Figures 29
and 30). Figures 30 displays four plots that display distinct grouping into fields. The
plutonic clasts form one group while the plutonic rocks form a second cluster. These
clusters range from some overlap to no overlap of the groupings.
INTERPRETATION OF THE RESULTS
Tectonic field plots and the geochemical data indicate that the sample suites share
a volcanic arc signature. These diagrams display both suites plotting within the volcanic
arc granite field. The geochemical data show that these samples are enriched in K 2 O, Rb,

96
Ba, Th and depleted in Y, Zr, Nb, Yb and Hf which is characterized by a volcanic arc
setting according to Pearce et al. (1984). Elemental characterization and tectonic
location of four different granite types are listed in table 6.
Table 6. Elemental characterization and the tectonic location of four types of granites
(synthesis from Pearce et al., 1984).
Volcanic arc
granite
Within plate
granite
Ocean ridge
granite
Collision granite
Tectonic setting subduction zones Oceanic islands,
attenuated
continental crust,
intra-continental
ring complexes
and grabens
mid-ocean ridges,
backarc basins and
forearc basins
continentcontinent
or
continent-arc
collisions
element
enrichment
K, Rb, Ba, Th and
sometimes in Ce,
Sm
Rb, Th, Y, Yb and
Nb
Th, Nb, Ce and Ba
Rb, Ba, Th and K
element depletion
Nb, Hf, Zr, Y, and
Yb
Ba K 2 O, and Rb Ce, Zr, Hf and Sm
Major, minor, rare-earth and trace element plots for both sample suites display
similar characteristics. Harker diagrams show the samples plotting into separate distinct
fields while rare-earth element diagrams show light rare-earth element enrichment in the
bedrock samples indicating that the sample suites appear geochemically different. Most
of the Harker diagrams show slight overlap between the samples suggesting that the
suites could be related. Therefore, geochemical analysis does not clearly provide a tie
between the Methow basin and the Intermontane superterrane nor does it exclude the
possibility.

97
Sample size and the spatial distribution of sampling affects the ability to use
geochemistry to correlate the plutonic clasts to their source terrane. Both the sample size
of the pluton and the plutonic clasts were low (n

98
CHAPTER 6. DEPOSITIONAL HISTORY OF THE METHOW BASIN
INTRODUCTION
Chapter 3 provides evidence that the Pasayten Group records a synorogenic
succession that reflects deltaic to fluvial deposition in a foreland basin. Chapters 4 and 5
suggest possible source terranes for sediment within the Pasayten Group. This section
integrates detailed stratigraphic relationships with the proposed provenance to reconstruct
the mid-Cretaceous Methow basin.
DEPOSITIONAL HISTORY
PRE-WINTHROP DEPOSITION
Pre-Winthrop deposition is characterized by mid-Albian turbidite deposition of
the Harts Pass Formation and the Jackass Mountain Group in a marine Methow basin
(Coates, 1974; Barksdale, 1975; Tennyson and Cole, 1987; Haugerud et al., 1996).
Based on volcanic and plutonic conglomerates, Tennyson and Cole (1978) interpreted
these units to be deposited in a forearc basin during unroofing of an eastern arc (Figure
31A).
Haugerud et al. (1996) document chert pebbles in the mid-Albian Little Jack unit
and Jackita Ridge Formation that interfinger with the Harts Pass Formation within the
western belt. They attribute these chert-rich strata to uplift of the Bridge River terrane
(McGroder, 1991; Haugerud et al., 1996).
Figure 31A shows a cartoon of the Methow basin during mid-Albian deposition.
In this model the Methow basin is sitting in a fore-arc position in front of the Spences
Bridge arc with a subduction zone outboard of the Bridge-River-Hozameen complex.

100
Both the Spences Bridge arc and the Bridge River-Hozameen complex were supplying
sediment to turbidites within the basin.
During the mid-Albian, the Methow basin may have been translated west as a
coherent block. McGroder (1991) presented a structural model, based on balanced crosssections,
whereby the Methow basin along with the Bridge River terrane begin to move
west along west-verging thrust faults before the mid-Albian (Figure 31a). If the Methow
basin is assumed to be in a fore-arc setting at this time, this underplating was responsible
for uplift of the Bridge River terrane to the west.
DEPOSITION OF THE BIG BUCK MEMBER OF THE WINTHROP
FORMATION
Deposition of the upper Albian Big Buck member of the Winthrop Formation
records the transition from marine to terrestrial deposition within the Methow basin. This
member is found only in the eastern belt. In the western belt an unconformity (locally
angular) occurs at the same stratigraphic level as the Big Buck member of the Winthrop
Formation (Haugerud et al., 1996).
Paleocurrent data suggest that plutonic-derived sediments had an eastern
provenance. Petrologic, detrital and whole rock zircon data suggest the Okanogan Range
Batholith and Eagle Plutonic Complex could have been possible source terranes (Figure
1). Geochemical correlations are inconclusive but argue against the Eagle Plutonic
Complex as a possible source terrane.
Figure 31B is a cartoon for the Late Albian deposition of the Big Buck member.
During this time the Methow basin was receiving plutonic sediment from the Eagle-

101
Okanogan Complex and the denuded Spences Bridge arc to the east. In this model,
deposition within the Methow basin was restricted to the eastern-margin as strata of the
western-belt were uplifted along west-vergent thrust faults. Uplift of the Methow basin
caused cannibalization of the basin supported by sandstone cobbles within the Big Buck
member. This uplift and erosion is inferred to be the result of the collision between the
Methow basin and the Insular superterrane.
DEPOSITION OF THE WINTHROP FORMATION
The Albian to Cenomanian Winthrop Formation is characterized by terrestrial
strata derived from both a plutonic and volcanic source (Figure 31c). In the eastern belt
the Winthrop Formation is dominantly eastern-derived plutonic sand probably shed off
from the Okanogan Range Batholith and the Eagle Plutonic Complex (Cole, 1973;
Kiessling and Mahoney, 1997; Kiessling et al., 1997). In the western belt, the Winthrop
Formation contains more volcanic lithics which may be coming from the west. A
western derivation is supported by interfingering of the 3 AM Mountain Member,
andesite and dacite lava flows, with the Winthrop Formation (Figure 3).
In the western belt, the Winthrop Formation intertongues with the Virginian
Ridge Formation, a chert-rich, meandering-fluvial succession derived from the west
(Cole, 1973; Trexler, 1985; Haugerud et al., 1996). Tennyson (1974) suggested that the
Virginian Ridge Formation was derived from the Hozameen complex of the Bridge River
terrane.
Figure 31C shows a model of Cenomanian deposition within the Methow basin.
Deposition during this time appears to involve both an eastern and western provenance

102
supplying sediment to an underfilled Methow basin (a basin characterized by transverse
drainages that feed a central longitudinal drainage system, Jordan, 1995). The Methow
basin is interpreted to be foreland basin, in general following Haugerud et al. (1996).
Figure 31C shows the Bridge River-Hozameen terrane being uplifted along west-vergent
thrust faults (possibly the Hozameen fault) and providing a western chert-rich source.
The Midnight Peak arc is shown as an intrabasinal arc and may have been the source for
lava flows within the 3 AM Mountain Member of the Winthrop Formation. Figure 31C
suggests that the Chuwanten fault system may have been active as a detachment under
the Methow basin during the Cenomanian however McGroder (1991) suggests the
Chuwanten fault system may have been active as early as the late Albian.
Volcanic lava flows within the Methow basin are uncharacteristic of foreland
basin deposits but may occur when the basin is proximal to an arc. Blasi and Maneassero
(in Jordan, 1995) documented volcanic-rich strata within the Andean Bermejo foreland
basin, adjacent to the Andean arc. The presence of volcanics within the Methow basin
suggests that subduction must have been occurring outboard of the Methow terrane
during deposition of the Winthrop Formation (Figure 31C).
DEPOSITION OF THE VENTURA MEMBER OF THE MIDNIGHT PEAK
FORMATION
Cenomanian to Turonian strata of the Ventura Member of the Midnight Peak
Formation were deposited in a terrestrial environment. The provenance of these
sediments is interpreted to have been the Midnight Peak volcanic arc and the Bridge
River terrane. The Ventura Member of the Midnight Peak Formation, in both the western

103
belt and eastern belt, records braided fluvial deposition and periodic volcanic-rich debrisflows.
The member appears to thicken to the southwest where it is interbedded with
andesitic lava and ash flows of the Midnight Peak volcanics. To the west the Ventura
Member of the Midnight Peak Formation is much more chert-rich (Cole, 1973; Ralph
Haugerud, personal communication, 1997).
Figure 31D shows a cartoon of the Methow basin during deposition of the
Ventura Member of the Midnight Peak Formation. In this model, the Ventura Member
forms a predominantly westerly-derived sheet of volcanic and chert-rich strata that
extended across the Methow basin. Figure 31D shows the Methow basin as an overfilled
foreland basin (characterized by transverse drainages that deposit sediment derived from
the thrust sheet across the entire basin, Jordan, 1995) that was receiving sediment from
the western Midnight Peak arc and Bridge River-Hozameen terrane. The Midnight Peak
arc was active during this period and is shown in this model as an intrabasinal arc. The
Chuwanten fault system was active during this time (McGroder, 1991; Haugerud et al.,
1996) and was probably causing uplift within the basin. This interpretation is supported
by large sandstone boulders, lithologically identical to Ventura Member sandstones
within this unit. Uplift of the western portion of the basin may have been responsible for
recycling previously deposited detrital zircons, sourced from plutons to the east.
DEPOSITION OF THE LONE MAN RIDGE SANDSTONE
The Turonian Lone Man Ridge sandstone represents meandering fluvial
deposition within the Methow basin. The Lone Man Ridge sandstone appears to be
restricted to the eastern outcrop belt where it represents the initial appearance of chert.

104
Figure 31E shows a model for the Methow basin during the Turonian. In this
model, the Bridge River-Hozameen terrane was being uplifted along east-vergent thrust
faults and was supplying chert-rich sediments to the basin. Uplift of the Virginian Ridge
Formation by the Chuwanten fault system also may have supplied chert-rich sediment to
the Methow basin. This uplift would have caused an eastward shift in the basin
depocenter which is supported by the restriction of the Lone Man Ridge sandstone to the
eastern belt. Because the Lone Man Ridge sandstone was derived from the west and
deposited along the eastern margin, the Methow basin is interpreted to be overfilled. A
volcanic ash bed within this unit indicates active volcanism interpreted here to be the
Midnight Peak arc.
TECTONIC IMPLICATIONS
The petrology, paleocurrents and the detrital zircons from the Pasayten Group
permit an eastern derivation of plutonic sands from the Eagle Plutonic Complex and
possibly the Okanogan complex. It seems highly probable that the Winthrop Formation
was derived from the Eagle Plutonic Complex based on: (1) lithologically identical
clasts to rocks across the superterrane boundary; (2) a dated clast with a whole rock date
that is exactly the same age as the Falls Lake Plutonic suite located east of the
superterrane boundary; and (3) paleocurrents indicating an eastward source for the
conglomerate.
The Ventura Member of the Midnight Peak Formation also provides a potential
tie to northern North America during the Late Cretaceous. Detrital zircons within this
unit can be matched to plutons east of the superterrane boundary. Furthermore, Archean

105
zircons within this unit likely were derived from northern (above 40 o N latitude) North
America, the only recognized source of Archean crust in North America.

106
CONCLUSIONS
This purpose of this study was to describe the Pasayten Group in Manning
Provincial Park and correlate it with the Pasayten Group in northern WA. The
conclusions of this study are listed below:
1. The Pasayten Group can be divided into an eastern belt and western belt based on
lithologic differences and geographic location.
2. Structures within Manning Park consist of a series of thrust faults which form the
Late Cretaceous Chuwanten fault and strike-slip faults which are attributed to Late
Cretaceous or Tertiary strike-slip movement along the Pasayten Fault.
3. The Pasayten Group in Manning Park can be subdivided into four units: the Big
Buck member of the Winthrop Formation, the main body of the Winthrop Formation, the
Ventura Member of the Midnight Peak Formation, and the Lone Man Ridge sandstone.
4. Strata with the four divisions of the Pasayten Group consist of six lithofacies: (a)
graded sandstone and mudstone lithofacies; (b) cross-stratified sandstone lithofacies; (c)
channelized sandstone lithofacies; (d) rippled siltstone lithofacies; (e) inverse-graded
channel fill lithofacies; and (f) tuffaceous pebbly mudstone lithofacies.
5. The six lithofacies are interpreted, respectively, as: (a) turbidites in a prodelta
setting; (b) migrating bars and channel fill in a delta-top environment; (c) bar sequences
and channel fill in either a braided or meandering fluvial system; (d) point bar-top
deposits in a meandering fluvial system; (e) debris flows and reworked debris flows in a
volcaniclastic apron; (f) bioturbated overbank and channel fill deposits in a braided
fluvial system.

107
6. The Pasayten Group in Manning Park is internally conformable and conformably
overlies the Jackass Mountain Group.
7. The Pasayten Group records a transition from the marine setting of the Jackass
Mountain Group, to the deltaic Big Buck member of the Winthrop Formation, to the
meandering fluvial main body of the Winthrop Formation, to the braided fluvial Ventura
Member of the Midnight Peak Formation and finally the meandering fluvial Lone Man
Ridge sandstone.
8. Paleocurrent and petrologic data indicate that the Pasayten Group received
sediment from eastern plutonic and western chert- and volcanic-rich source terranes.
9. The Bridge River terrane may represent the chert-rich western source while the
Midnight Peak volcanic arc may represent the western volcanic-rich source terrane.
9. Detrital zircon ages from a sandstone sample and a whole rock age from a
plutonic clast can be correlated to plutons on the Intermontane superterrane suggesting
that it may have been supplying sediment to the Methow basin.
10. Geochemical data from plutonic clasts within the Winthrop Formation and the
Eagle plutonic complex indicate a volcanic arc affinity.
11. Geochemical data from plutonic clasts within the Winthrop Formation and from
the Eagle plutonic complex group into separate fields with minimal overlap. These data
do not clearly suggest that these clasts were derived from the Eagle Plutonic Complex
nor do the data preclude it.
12. The Late Cretaceous Pasayten Group is thought to have been deposited initially in
a fore-arc basin and finally in a foreland basin that was receiving chert-rich sediment

108
from the east-verging Bridge River allochthon. During the final stages of deposition, the
Pasayten Group records a western, intrabasinal volcanic source.

109
SUGGESTIONS FOR FUTURE WORK
This study has focused on the provenance and stratigraphy of the Pasayten Group
but a number of questions remain regarding both the Pasayten Group and the Methow
terrane.
1. Detailed mapping of the Pasayten Group north of Manning Park needs to be
conducted. This would help to define the lateral extent of and facies changes within the
Pasayten Group.
2. The detailed stratigraphy of the Jackass Mountain Group needs to be completed
and correlated with units in WA. Isotopic studies (εNd) need to be done on fine-grained
sediments to better determine the provenance of the Pasayten Group. Isotopic studies
could be used to fingerprint plutons and test whether the plutons inferred by this study,
were supplying sediment to the Methow basin.
3. Major, minor, trace and rare-earth element geochemistry needs to be done on
more plutonic clasts within the Pasayten Group, plutonic clasts within the underlying
Jackass Mountain Group, the Falls Lake Plutonic Suite and the Okanogon complex. The
results should be compared to determine if the clasts are geochemically similar to the
proposed plutons.
4. Major, minor, trace, rare-earth element and isotope geochemistry are needed from
plutons from north-western Mexico. This data should be compared to the geochemistry
of fine-grained strata and plutonic clasts within the Pasayten Group and the Jackass
Mountain Group.

110
5. Isotopic ages are needed for plutons in north-western Mexico. These ages could
be compared to detrital zircons from sandstone within the Pasayten Group to better
discriminate possible source terranes.
6. More geochemistry needs to be done on the Triassic Nicola Group and volcanic
clasts within the Pasayten Group and Jackass Mountain Group. This data should be
compared to data from the Spences Bridge Group to determine if the volcanic clasts
could have been derived from either volcanic source terrane.

111
REFERENCES CITED
Alexander, J., 1989, Delta or coastal plain With an example of the controversy from the
Middle Jurassic of Yorkshire, in Whateley, M. K. G. and Pickering, K.T., ed.,
Deltas: sites and traps for fossil fuels: Geological Society Special Publications:
Oxford, Blackwell Scientific Publications, p. 11-20.
Allmendinger, R., 1992, Stereonet 3.5.
Barksdale, J. D., 1948, Stratigraphy in the Methow quadrangle, Washington:: Northwest
Science, v. 22, no. 4, p. 164-176.
Barksdale, J. D., 1975, Geology of the Methow Valley, Okanogan County, Washington,
Washington Division of Geology and Earth Resources Bulletin 68, 72 p.
Best, M. C., 1995, Igneous and Metamorphic Petrology: New York, W. H Freeman and
Company, 630 p.
Boggs, S. J., 1995, Principles of Sedimentology and Stratigraphy, New Jersey, Prentice
Hall, 774 p.
Brown, S. and Richards, P.C., 1989, Facies and development of the Middle Jurassic
Brent Delta near the northern limit of its progradation, North Sea, in Whateley,
M. K. G. and Pickering, K.T., ed., Deltas: Sites and Traps for Fossil Fuels:
Geological Society Special Publications: Oxford, Blackwell Scientific
Publications, p. 253-268.
Cant, D. J., 1982, Development of a facies model for sandy braided river sedimentation:
comparison of the south Saskatchewan River and the Battery Point Formation, in
Miall, A. D., ed., Fluvial Sedimentology: Exploring For Energy: Calgary, Alberta,
Canada, Canadian Society of Petroleum Geologists Memoir 5, p. 627-638.
Coates, J. A., 1970, Stratigraphy and structure of Manning Park area, Cascade
Mountains, British Columbia: Geological Association of Canada, Special Paper
number 6, p.149-154.
Coates, J. A., 1974, Geology of the Manning Park area, British Columbia, Geological
Survey of Canada Bulletin 238, 177 p.
Cole, M. R., 1973, Petrology and dispersal patterns of Jurassic and Cretaceous
sedimentary rocks in the Methow River area, North Cascades, Washington,
Unpublished Ph.D. thesis, 110 p.
Cook, F.A., Varsek, J.L., Clowes, R.M., Kanasewich, E.R., Spencer, C.S., Parrish, R.R.,
Brown, R.L., Carr, S.D., Johnson, B.J., and Price, R.A., 1992, Lithoprobe crustal

112
reflection cross-section of the southern Canadian Cordillera, 1, Foreland thrust
and fold belt to Fraser River Fault: Tectonics, v. 11, p. 12-35.
Cowan, D. S., 1994, Alternative hypotheses for the Mid-Cretaceous paleogeography of
the Western Cordillera: GSA Today, v. 4, no. 7, p. 181-186.
Cowan, D. Brandon, M., and Garver, J; 1997, Geological tests of hypotheses for large
coastwise displacements: a critique illustrated by the Baja British Columbia
controversy, American Journal of Science, v. 297, no. 2, p. 117-173.
Cox, K. G., Bell, J.D. and Pankhurst, R.J., 1979, The Interpretation of Igneous Rocks:
London, George Allen & Unwin, 450 p.
Daly, R. A., 1912, Geology of the North American Cordillera at the forty-ninth parallel:
Geological Survey of Canada, Memoir 38.
Daly, R. A., 1912, Geology of the North American Cordillera near the forty-ninth
parallel: Geological Survey of Canada.
Davis, R. A. Jr, 1992, Depositional Systems: an introduction to sedimentology and
stratigraphy: Englewood Cliffs, New Jersey, Prentice Hall, 604 p.
Davis, G. A., Monger, J.W.H., and Burchfiel, B.C., 1978, Mesozoic construction of the
Cordilleran "Collage", central British Columbia to central California, in Howell,
D. G. and. McDougall, K.A., ed., Mesozoic paleogeography of the western
United States, Pacific Section, Society of Economic Paleontologists and
Mineralogists, Symposium 2, p. 1-32.
Dickinson, W.R. and Suczek, 1979, Plate tectonics and sandstone compositions:
American Association of Petroleum Geologists Bulletin, v. 63, p. 2164-2182.
Faure, G., 1991, Principles and Applications of Inorganic Geochemistry: Englewood
Cliffs, Macmillan Publishing Company, 626 p.
Garver, J. I., 1989, Basin evolution and source terranes of Albian-Cenomanian rocks in
the Tyaughton basin, southern British Columbia: implications for mid-Cretaceous
tectonics in the Canadian Cordillera, Unpublished Ph.D. thesis, 227 p.
Garver, J. I., 1992, Provenance of Abian-Cenomanian rocks of the Methow and
Tyaughton basins, southern British Columbia: a mid-Cretaceous link between
North America and Insular terranes: Canadian Journal of Earth Sciences, v. 29, p.
1274-1295.
Garver, J.I. and Brandon, M.T., Fission-track ages of detrital zircons from Cretaceous
strata, southern British Columbia: Implications for the Baja BC hypothesis:
Tectonics, v. 13, p. 401-420.

113
Greig, C. J., 1992, Jurassic and Cretaceous plutonic and structural styles of the Eagle
Plutonic Complex, southwestern British Columbia, and their regional
significance: Canadian Journal of Earth Sciences, v. 29, p. 793-811.
Greig, C. J., Armstrong, R.L., Harakel, J.E., Runkle, D., and van der Heyden, P., 1992,
Geochronometry of the Eagle Plutonic Complex and the Coquihalla area,
southwestern British Columbia: Canadian Journal of Earth Sciences, v. 29, p.
812-829.
Haugerud, R. A., Brown, Edwin D., Tabor, Roland W., Kriens, Bryan J., and McGroder,
Michael F., 1994, Chapter 2E: Late Cretaceous and early Tertiary orogeny in the
North Cascades, in Swanson, D. A. a. H., R.A., ed., Geologic field trips in the
Pacific Northwest: 1994 Geological Society of America Annual Meeting: Seattle,
Wa, p. 2E1-2E51.
Haugerud, R. H., Mahoney, J. B., and Dragovich, J.D., 1996, Geology of the Methow
Block: Northwest Geological Society Fall Field Trip; Unpublished Field Guide,
September 5-8, 1996, p. 38.
Helland-Hansen, W., Steel, R., Nakayama, K., and Kendall, C. G. St. C., 1989, Review
and computer modelling of the Brent Group stratigraphy, in Whateley, M. K. G.
and Pickering, K. T., ed., Deltas: Sites and Traps for Fossil Fuels: Geological
Society Special Publications, Oxford, Blackwell Scientific Publications, p. 237-
252.
Hurlow, H. A., 1993, Mid-Cretaceous strike-slip and contractional fault zones in the
western Intermontane terrane, Washington, and their relation to the North
Cascades-Southeastern Coast Belt orogen: Tectonics, v. 12, no. 5, p. 1240-1257.
Hurlow, H. A., and Nelson, B.K., 1993, U-Pb zircon and monazite ages for the Okanogan
Range batholith, Washington: Implications for the magmatic and tectonic
evolution of the southern Canadian and northern United States Cordillera:
Geological Society of America Bulletin, v. 105, p. 231-240.
Ingersoll, R. V., 1990, Actualistic sandstone petrofacies: Discriminating modern and
ancient source rocks: Geology, v. 18, p. 733-736.
Ingersoll, R.V., Kretchmer, A.G., and Valles, P.K., 1993, The effect of sampling scale on
actualistic sandstone petrofacies: Sedimentology, v. 40, p. 937-953.
Irving, E., Thorkelson, D.J., Wheadon, P.M., and Enkin, R.J., 1995, Paleomagnetism of
the Spences Bridge Group and northward displacement of the Intermontane Belt,
British Columbia: A second look: Journal Geophysical Research, v. vol. 100, no.
B4, p. 6057-6071.

114
Irving, E., Wynne, P.J., Thorkelson, D.J., and Schiarizza, P., 1996, Large (1000-4000)
northward movements of tectonic domains in the northern Cordillera, 83-45 Ma:
Journal of Geophysical Research, v. 101, no. B8, p. 17,901-17,916.
Jordan, T., 1995, Retroarc Foreland and Related basins, in Busby, C. J. and Ingersoll,
R.V., ed., Tectonics of Sedimentary Basins: Cambridge, Massachusetts,
Blackwell Science, Inc, p. 331-363.
Journeay, J. M., and Friedman, R.M., 1993, The Coast Belt Thrust System: Evidence of
Late Cretaceous shortening in southwest British Columbia: Tectonics, v. no. 3, p.
756-775.
Journeay, J. M., and Monger, J.W.H., 1994, Geology and crustal structure of the southern
Coast and Intermontane belts, southern Canadian Cordillera, British Columbia:
Geological Survey of Canada Open File 2490.
Kiessling, M. A., and Mahoney J.B., 1997, Revised Stratigraphy of the Pasayten Group,
Manning Provincial Park, British Columbia: in Current Research 1997-A;
Geological Survey of Canada, p. 151-158.
Kiessling, M. A., Mahoney, J. B., and Link, P. K., 1997, Evolution of the Methow terrane
in the Late Cretaceous: stratigraphy and petrology of the Pasayten Group,
southern Methow terrane, B.C.: Geological Society of America Abstracts with
Programs v. 29, no. 6, Annual Meeting, Salt Lake City, UT, p. A278.
Kleinspehn, K. L., 1985, Cretaceous sedimentation and tectonics, Tyaughton-Methow
Basin, southwestern British Columbia: Canadian Journal of Earth Sciences, v. 22,
p. 154-174.
Krause, R., G. F., and Geijer, T. A. M., 1987, An improved method for calculating the
standard deviation and variance of paleocurrent data: Journal of Sedimentary
Petrology, v. 57, no. No. 4, p. 779-780.
Mahoney, J. B., Monger, J.W.H., and Hickson, C.J., 1996, Albian-Cenomanian
conglomerates along the Intermontane/Insular superterrane boundary, Canadian
Cordillera, British Columbia: a critical test for large-scale terrane translation:
Current Research 1996-A; Geological Survey of Canada, p. 101-109.
Mahoney, J., Mustard, P.S., Haggert, J.W., Friedman, R.M., Fanning, M. and McNicoll,
V.J., 1997, Archean zircons in Upper Cretaceous sediments of the Canadian
Cordillera: HOW MANY ARE ENOUGH: Geological Society of America
Abstracts with Programs, v. 29, no. 6, Annual meeting, Salt Lake City, UT, p.
A278.

115
McGroder, M. F., 1991, Reconciliation of two-sided thrusting, burial metamorphism, and
diachronous uplift in the Cascades of Washington and British Columbia:
Geological Society of America Bulletin, v. 103, p. 189-209.
Miall, A. D., 1982, Lithofacies types and vertical profile models in braided river deposits:
a summary, in Miall, A. D., ed., Fluvial Sedimentology: Calgary, Alberta,
Canadian Society of Petroleum Geologists Memoir 5, p. 597-605.
Miall, A. D., 1996, The Geology of Fluvial Deposits: sedimentary facies, basin analysis,
and petroleum geology: New York, Springer, p. 131-245.
Miller, R. B. Haugerud, R.A., Smith, F.; and Nicholson, L., 1994, Tectonostratigraphic
framework of the northeastern Cascades, in Lasmanis, R., and Cheney, E.S., ed.,
Regional Geology of Washington State: Washington Division of Geology and
Earth Resources Bulletin 80, p. 73-92.
Misch, P., 1966, Tectonic evolution of the northern Cascades of Washington-A westcordilleran
case history: in Gunning, H.C., ed., A symposium on the tectonic
history and mineral deposits of the western Cordillera in British Columbia and
neighboring parts of the United States, Vancouver, 1964: Canadian Institute of
Mining and Metallurgy Special Volume 8, p. 101-148, 1 plate.
Monger, J. W. H., 1989a, Geology, Hope, British Columbia: Geological Survey of
Canada Map 41-1989, sheet 1, scale 1:250,000.
Monger, J. W. H., 1989b, Overview of Cordilleran geology, in Ricketts, B.D., ed.,
Western Canada Sedimentary Basins, Canadian Society of Petroleum Geologists,
p. 9-32.
Monger, J. H. W., Price, R.A., and Templeman-Kluit, D.J., 1982, Tectonic accretion and
the origin of the two major metamorphic and plutonic welts in the Canadian
Cordillera: Geology, v. 10, p. 70-75.
Monger, J. W. H., and Journeay, J.M., 1994, Guide to the geology and tectonic evolution
of the southern Coast Mountains: Geological Survey of Canada, Open File 2490.
Monger, J. W. H., and Price, R.A., 1996, Paleomagnetism of the Upper Cretaceous strata
of Mount Tatlow: evidence for 3000 km of northward displacement of the eastern
Coast Belt, British Columbia and on Paleomagnetism of the Spences Bridge
Group and northward displacement of the Intermontane Belt, British Columbia; a
second look; discussion and reply, Journal of Geophysical Research, v. 101, no. 6,
p. 13793-13803.
Mustard, P. S., Mahoney, J.B., Haggart, J.W., Friedman, R.M., Fanning, M., and
McNicoll, V.J., 1998, Archean zircons in upper Cretaceous sediments of the
western Canadian Cordillera-does the "Baja B.C." hypothesis fail a "crucial

116
test", in Geological Society of America-Cordilleran Tectonics, Vancouver, B.C.:
in Cook, F. and Erdmer, P., compilers, Slave-Northern Cordillera Lithospheric
Evolution (SNORCLE) Transect and Cordilleran Tectonics Workshop Meeting
(March 6-8), Simon Fraser University, Lithoprobe Report No. 64, 331 p.
Pearce, J. A., Nigel, B. W., and Tindle, A. G., 1984, Trace element discrimination
diagrams for the tectonic interpretation of granitic rocks: Journal of Petrology, v.
25, no. Part 4, p. 956-983.
Pederson, G. K., 1989, A fluvial-dominated lacustrine delta in a volcanic province, W
Greenland, in Whateley, M. K. G. and Pickering, K.T., ed., Deltas: Sites and
Traps for Fossil Fuels: Geological Society Special Publications: Oxford,
Blackwell Scientific Publications. p. 139-146.
Pidgeon, R. T. and Compston, W., 1992, A SHRIMP ion microprobe study of inherited
and magmatic zircons from four Scottish Caledonian granites, in Brown, P.E. and
Chappell, B.W., eds., The Second Hutton Symposium on the Origin of Granites
and Related Rocks, Geological Society of America Special Paper, 272, p.
Plint, A. G., 1983, Sandy fluvial point-bar sediments from the Middle Eocene of Dorset,
England, in Collinson, J. D. and Lewin, J., ed., Modern and Ancient Fluvial
Systems: Special Publication Number 6 of the International Association of
Sedimentologists: Oxford, Blackwell Scientific Publications, p. 355-369.
Rice, H. M. A., 1947, Geology and mineral deposits of the Princeton map-area, British
Columbia, Geological Survey of Canada, Memoir 243, 136 p.
Rust, B. R., 1982, Depositional Models for Braided Alluvium, in Miall, A. D., ed.,
Fluvial Sedimentology: Exploring For Energy: Calgary, Alberta, Canada,
Canadian Society of Petroleum Geologists Memoir 5, p. 627-638.
Tennyson, M. E., 1974, Stratigraphy, structure, and tectonic setting of Jurassic and
Cretaceous sedimentary rocks in the west-central Methow-Pasayten area,
northeastern Cascade Range, Washington and British Columbia: unpublished
Ph.D. thesis, 112 p.
Tennyson, M. E., and Cole, M.R., 1978, Tectonic significance of upper Mesozoic
Methow-Pasayten sequence, northeastern Cascade Range, Washington and British
Columbia: in Howell, D.G., and McDougall, K.A., eds., Mesozoic
paleogeography of the western United States, Pacific Section, Society of
Economic Paleontologists and Mineralogists, Pacific Coast Paleogeography
Symposium 2, p. 499-508.
Tennyson, M. E., and Cole, M.R., 1987, Upper Mesozoic Methow -Pasayten sequence,
northeastern Cascade Range, Washington and British Columbia: Washington
Division of Geology and Earth Resources Bulletin, v. 77, p. 73-84.

117
Thorkelson, D. J., and Rouse, G.E., 1989, Revised stratigraphic nomenclature and age
determinations for mid-Cretaceous volcanic rocks in southwestern British
Columbia: Canadian Journal of Earth Sciences, v. 26, p. 2016-2031.
Trexler, J. H., 1985, Sedimentology and Stratigraphy of the Cretaceous Virginian Ridge
Formation, Methow Basin, Washington: Canadian Journal of Earth Science, v. 22,
p. 1274-1285.
Tucker, M., 1994, The Field Description of Sedimentary Rocks, Geological Society of
London Handbook: Chichester, New York, Birsbane, Toronto, Singapore, John
Wiley & Sons, 111 p.
Umhoefer, P. J., and Miller, R. B., 1996, Mid-Cretaceous thrusting in the southern Coast
Belt, British Columbia and Washington, after strike-slip fault reconstruction:
Tectonics, v. 15, no. No. 2, p. 545-565.
Walker, R. G. and Cant, D. J., 1992, Sandy Fluvial Systems, in Walker, R. G., ed., Facies
Models: Geoscience Canadian Reprint Series 1, p. 71-89.
Ward, P.D., Hurtado, J.M., Kirschvink, J.L. and Verosub, K.,1997, Measurements of the
Cretaceous paleolatitude of Vancouver Island: consistent with the Baja-British
Columbia hypothesis, Science, v. 277, p. 1648-1645.
Wells, N. A., 1984, Sheet debris flow and sheetflood conglomerates in Cretaceous coolmaritime
alluvial fans, south Oriney Islands, Antartctica, in Koster, E. H. and S.,
R. J., ed., Sedimentology of Gravels and Conglomerates: Calgary, Alberta,
Canadian Society of Petroleum Geologists, p. 133-147.
Winston, D., 1982, Fluvial systems of the Precambrian Belt Supergroup, Montana and
Idaho, U.S.A., in Miall, A. D., ed., Fluvial Sedimentology: Exploring for Energy:
Calgary, Canada, Canadian Society of Petroleum Geologists Memoir 5, p. 343-
361.
Woodsworth, G. J., Anderson, R.G., and Armstrong, R.L., 1991, Plutonic regimes: in
Chapter 15 of Geology of the Cordilleran Orogen in Canada, Decade of North
American Geology, Gabrielse, H. and Yorath, C.J., eds.; Geological Survey of
Canada, Geology of Canada, v. no. 4, p. 491-531.

Wynne, P. J., Irving, E., Maxson, J.A., and Kleinsphen, K.L., 1996, Paleomagnetism of
the Upper Cretaceous strata of Mount Tatlow: evidence for 3000 km of northward
displacement of the eastern Coast Belt, British Columbia: Journal of Geophysical
Research, v. v. 100, no. B4, p. 6073-6091.
118

APPENDIX 1. DESCRIPTION OF MEASURED SECTIONS
Locations of measured sections in UTM:
1. Sandy Butte, WA, 688600, 538100
2. Monument hill, B.C., 667500, 5433000
3. Lone Man Ridge, B.C., 663900, 5442100
4. Big Buck Mountain, B.C., 663800, 5446600
5. 3 Brothers Mountain, B.C., 661000, 5448500

DESCRIPTION OF MEASURED SECTIONS
SANDY BUTTE MEASURED SECTION, SANDY BUTTE, WA.
Unit Description
Mostly covered. Coarse-grained arenite and fine
wacke and mudstone. Dark-gray, calcite-cemented,
thick-bedded, moderately-sorted, angular, volcaniclithic
arenite interbedded with red, thin-bedded,
moderately sorted, subangular lithic wacke and
mudstone.
Thickness (m)
Unit Cumulative
27 2512
Top of the Winthrop Formation.
Coarse- to fine-grained lithic feldspathic arenite and
siltstone. Tan, silica-cemented, thick-bedded (1 m), well-sorted, subangular,
micaceous-feldspathic arenite that grades normally
into dark-gray, thick-bedded (

Fine- to coarse-grained sandstone and siltstone. Buff
to tan, thick-bedded, well-sorted, subangular to
subrounded, biotite lithic feldspathic arenite that
grades normally into dark-gray, siltstone. Sandstone
beds display erosional bases and trough-crossstratification.
These beds commonly grade normally
into climbing-ripple laminated siltstone with local
plant leaves. Locally these beds appear massive but
contain interbeds of siltstone ripup clasts and wood
lag deposits. Sample 96MK090.
Cobble to boulder conglomerate. Brown, massive to
thick-bedded, moderately- to poorly-sorted,
subrounded, clast-supported, conglomerate.
Conglomerate is lenticular (20 m. wide and 58
meters tall) and grades normally from boulder to
pebble. The base of the conglomerate is erosional
and displays insitu stumps. Clasts are ubiquitously
volcanic and lesser plutonic and sandstone.
96MK089.
Medium- to fine-grained sandstone. Tan to buff,
thin-bedded, well-sorted, subangular, micaceous
feldspathic arenite. Sandstone displays common
trough- and planar cross-stratified beds with local
parallel laminations near the base of beds.
Commonly cross-stratified sandstone beds overlie
trough-cross stratified sandstone beds. The base of
sandstone beds is erosive and locally contains load
casts. Plutonic lag deposits are uncommon.
Climbing-ripple laminated mudstone and siltstone
occurs at the top of beds. Samples 96MK079 to
96MK083.
Mudstone. Dark-gray, thin-bedded, mudstone.
Medium- to coarse grained sandstone. Tan, thickbedded,
poorly-sorted, subangular, chert-lithic
feldspathic arenite interbedded with dark-gray, thickbedded,
well-sorted, subangular, micaceous
132 1647
58 1515
212 1457
33 1245
20 1212

feldspathic arenite. Chert-lithic sandstone beds
display local chert pebble lags.
Covered. Soil composed of black siltstone chips
82 1182
Medium- to fine-grained sandstone. Green, thickbedded,
well-sorted, subangular, micaceousfeldspathic
arenite interbedded with green (patchy
weathering), thin-bedded, well sorted, subangular,
micaceous chert-lithic arenite. Sandstone beds grade
normally into dark-gray siltstone with abundant leaf
fossils. Sandstone beds display erosional bases,
ubiquitous planar-cross-stratification and local
trough-cross-stratification. Samples 96MK078 and
96MK095.
125 1100
Top of the Virginian Ridge Formation.
Poor exposure. Slope is covered with dark-gray,
mudstone with a pencil cleavage.
261 975
Medium-grained sandstone. Gray, thin-bedded,
well-sorted, subangular, micaceous chert-lithic
arenite with thin (

siltstone. Conglomerate beds display erosional bases
and commonly load into the underlying siltstone
beds. Sandstone beds display planar-crossstratification
which commonly overlies trough-crossstratification.
Fine-grained siltstone and mudstone. Dark-gray,
parallel laminated (

MONUMENT HILL, MANNING PARK, B.C.
Unit Description
Medium- to coarse-grained sandstone and pebble
conglomerate. Tan, thin- to medium-bedded (

lenticular (

LONE MAN RIDGE MEASURED SECTION, MANNING PARK, B.C.
Unit Description
Medium-grained sandstone and pebble conglomerate.
Tan, medium- to thin-bedded, moderately sorted,
subrounded to subangular, chert-volcanic-lithic
conglomerate. Conglomerate occurs at the base of
fining upward sequences (1-10 m). Conglomerate
beds fine into tan, medium-bedded, well-sorted,
subangular, chert-lithic arenite. Sandstone beds
display trough-cross-stratification overlain by planarcross-stratification.
The sandstone beds commonly
display chert pebble lags on foresets. Thin-beds of
dark-gray siltstone are intercalated within the
sandstone beds. Sample 96MK067.
Fine-grained tuff. Red to purple, laminated,
devitrified, ash-fall tuff. Devitrification spots
commonly weather gray-green. Sample 96MK066
Coarse-grained to pebbly sandstones fine upwards
into medium-grained sandstones. The base of these
fining upwards sequences is usually marked by a
horizon of rip-up clasts and wood fragments.
Sandstone beds display planar-cross-stratification
with pebble lags on the foresets. Sample 96MK065.
Pebble conglomerate and medium- to coarse-grained
sandstone. Tan, thick- to medium-bedded,
moderately sorted, subangular to subrounded, clastsupported,
chert-lithic conglomerate. Conglomerates
contain imbricated clasts and are lenticular (

Top of Ventura Member of the Midnight Peak
Formation.
Coarse- to fine-grained sandstone with pebble to
cobble conglomerate and mudstone. Red, mediumto
thick-bedded (

BIG BUCK MOUNTAIN MEASURED SECTION, MANNING PARK, B.C.
Unit Description
Unit
Thickness (m)
Cumulative
Coarse- to fine-grained sandstone and siltstone. Tan,
medium-bedded, moderately-sorted, subangular to
subrounded, micaceous feldspathic arenite.
Sandstone beds display erosive bases and troughcross-stratification
(cosets

Top of Big Buck member of the Winthrop
Formation.
Coarse-grained, gray sandstone. Massive sandstone
beds appear structureless except for parallel and
planar-cross-beds from 676-688 meters. Sandstone
beds grade normally into dark-gray, parallel
laminated siltstone. Locally siltstone laminae are
obscured by abundant bioturbation. A horizon of
dark-gray siltstone rip-up clasts (

Siltstone. Thickly-laminated to thinly-bedded
siltstone. Siltstone beds display planar-crossstratification,
asymmetric-ripples, vertical and
horizontal burrows. Siltstone beds cap finingupward
sequences from medium to coarse-grained,
trough-cross-stratified sandstone (cosets

to subrounded, micaceous feldspathic arenite.
Sandstone beds display erosive bases with dark-gray
siltstone rip-up clasts and local coarse-grained lag
deposits. These beds form the base of fining-upward
sequences (5-10 m) and grade into rippled sandstone
overlain by dark-gray bioturbated siltstone.

THIRD BROTHER MOUNTAIN MEASURED SECTION, MANNING PARK,
B.C.
Thickness (m)
Unit Cumulative
Unit Description
Fine-grained sandstone. Tan, thin-bedded (20 cm),
moderately-sorted, subangular to subrounded,
micaceous feldspathic arenite. Sandstone beds
display trough-cross-stratification (cosets

normally-graded. These beds commonly display an
asymmetrical-rippled top and grade into dark-gray
laminated siltstone. Siltstone displays flamestructures
and z-folds. Two indeterminate bivalves
were found within the sandstone beds. Sample
96MK126.

Sample Unit UTM-North UTM-East Qpt Qp Qmu Qm P K Lvv Lvf Lvm Lvl Lmv Lmp Lmqt Lma Lsa Lsc M D C Total
96MK032 KPW 5439500 668600 0 10 N/A 178 182 182 0 15 0 25 3 0 0 30 2 0 49 0 0 500
96MK035-1 KPW 5439000 667500 0 16 N/A 180 247 20 0 2 0 3 0 0 1 10 0 0 21 0 0 500
96MK042 KPMv 5331100 664900 0 3 68 64 272 6 2 19 7 15 16 1 0 5 8 0 8 5 1 500
96MK053 KPMv 5437850 665050 3 8 122 9 306 1 0 18 0 6 0 0 6 6 1 0 10 4 0 500
96MK061 KPMl 5441600 663600 1 124 55 11 108 12 2 123 2 37 0 0 1 20 0 0 4 0 0 500
96MK067 KPMl 5441500 663600 0 32 N/A 125 172 28 1 39 12 28 0 1 6 37 10 0 7 2 0 500
96MK069 KPVs 5373700 700200 3 144 85 4 106 1 5 83 1 10 2 0 5 34 13 0 3 1 0 500
96MK070 KPVs 5374600 699300 0 100 52 10 182 5 0 69 4 8 6 0 3 46 7 0 6 2 0 500
96MK076 KPvs 5381200 688700 1 256 64 0 25 1 0 63 2 8 0 0 10 56 12 0 2 0 0 500
96MK078 KPW 5382050 689400 0 8 N/A 52 267 24 0 18 10 77 0 1 0 1 4 0 35 1 0 500
96MK079 KPW 5382200 690100 2 5 N/A 79 270 9 3 24 12 73 0 0 0 4 0 0 17 2 0 500
96MK081-2 KPW 5382200 690250 0 6 N/A 65 302 6 0 17 15 54 0 1 0 4 3 0 24 3 0 500
96MK097 KPMv 5392200 682150 0 204 66 14 78 4 0 42 2 24 1 0 8 50 6 0 1 0 0 500
96MK100 KPMv 5392900 682050 0 107 58 11 147 11 0 71 1 49 3 0 2 25 11 0 3 1 0 500
96MK101 KPMv 5392450 682050 1 308 27 4 33 4 0 46 4 41 1 0 0 12 18 0 1 0 0 500
96MK106-2 KPVs N/A N/A 2 8 104 19 215 0 0 20 0 0 4 0 13 8 0 0 7 0 0 500
96MK108 KPW N/A N/A 0 3 78 28 364 1 0 12 0 1 2 0 1 1 4 0 10 1 0 500
96MK111 KPW N/A N/A 1 9 N/A 116 334 15 0 0 0 0 1 0 0 1 3 0 17 2 1 500
96MK112 KPMv 5433250 667550 1 4 86 6 321 4 0 34 9 3 1 0 4 9 4 0 4 10 0 500
96MK114-1 KPMv 5433500 667550 0 0 28 2 152 4 11 54 30 190 3 0 2 4 0 0 20 0 0 500
96MK116-1 KPMl 5433600 668350 0 9 129 13 312 1 0 26 0 3 0 0 0 2 1 0 4 0 0 500
96MK117-1 KPMl 5433700 668300 0 7 140 11 299 1 1 23 1 1 1 0 1 10 0 0 4 0 0 500
96MK126 KPW 5448500 660900 2 3 158 12 304 0 0 4 0 0 3 0 0 7 0 0 6 1 0 500
96MK133 KPW 5437900 666025 11 6 N/A 133 113 14 0 25 47 76 0 4 7 21 0 0 43 0 0 500
96MK134 KPMv 5438000 665900 1 13 N/A 99 138 7 0 79 11 51 5 2 2 80 6 0 4 0 2 500
96MK135 KPMv 5437850 665850 0 12 N/A 140 226 5 0 54 4 25 1 1 5 9 1 0 15 2 0 500
96MK141 KPW 5431500 668950 0 11 N/A 159 223 1 0 9 0 50 2 0 3 16 0 0 26 0 0 500
96MK142-1 KPMv 5432100 668350 3 3 126 20 286 2 0 32 0 0 1 0 0 16 0 0 10 1 0 500
96MK145 KPW 5447000 662500 0 1 130 18 321 0 0 10 0 0 0 0 0 4 0 0 16 0 0 500
96MK147 KPW 5446950 662600 1 8 N/A 207 231 21 0 1 0 0 3 0 3 3 1 0 16 5 0 500
96MK153 KPMv 5433825 667800 2 7 N/A 108 337 2 0 17 3 3 4 0 0 7 0 0 8 2 0 500
96MK154 KPMl 5433825 667800 2 39 N/A 125 231 19 0 39 2 16 5 0 2 13 2 0 3 2 0 500
8PL96 KPWb N/A N/A 2 37 N/A 168 186 0 0 0 0 0 0 0 0 6 9 0 3 0 24 500
9PL96 KPWb N/A N/A 0 18 N/A 240 188 0 0 0 0 0 0 0 0 0 8 0 44 2 0 500
10PL96 KPW N/A N/A 1 11 N/A 202 193 60 0 0 0 0 0 0 0 1 12 0 19 1 0 500
11PL96 KPMl N/A N/A 126 1 N/A 110 95 47 0 46 7 41 0 0 0 12 2 0 8 2 3 500

Sample P/F Qp/ Q %M %D %Lm %Lv %Ls %Qp %Lvm %Lsm %Lm %Lv %Lst %Q %F %Lt %Qt %F %L
96MK032 0.96 0.05 9.8 0 44 53 3 12 51 37 39 47 14 39 42 19 42 42 16
96MK035-1 0.93 0.08 4.2 0 69 31 0 50 16 34 34 16 50 38 56 6 41 46 3
96MK042 0.92 0.09 1.2 4.2 30 59 11 4 78 18 29 57 14 27 57 16 28 57 15
96MK053 0.98 0.02 1.6 1 32 65 3 23 50 27 25 50 25 27 63 10 29 63 8
96MK061 0.9 0.65 0.8 0 11 89 0 40 53 7 7 53 40 13 24 63 39 24 37
96MK067 0.86 0.2 1.4 6.1 33 60 7 19 48 33 27 48 25 25 40 34 32 41 27
96MK069 0.99 0.62 0.6 0.2 27 65 8 49 34 17 14 33 53 18 22 60 48 22 30
96MK070 0.97 0.62 1.2 0.4 38 57 5 41 36 23 23 33 44 13 38 49 33 38 29
96MK076 0.96 0.8 0.4 0 44 48 8 63 18 19 16 18 66 13 5 82 64 5 31
96MK078 0.92 0.13 7 0.4 3 93 4 7 87 6 2 87 11 11 63 26 13 63 24
96MK079 0.97 0.08 3.4 0.58 3 97 0 6 91 3 3 91 6 16 58 26 18 58 24
96MK081-2 0.98 0.08 4.8 0.56 5 91 4 6 86 8 5 86 9 14 65 21 15 65 20
96MK097 0.95 0.72 0.2 0 44 51 5 61 20 19 18 20 62 16 16 68 57 16 27
96MK100 0.93 0.61 0.6 0.2 19 75 6 40 46 14 11 45 44 14 32 54 35 32 33
96MK101 0.89 0.91 0.2 0 11 75 14 72 21 7 3 21 76 6 7 87 68 7 25
96MK106-2 1 0.08 1.4 0 56 44 0 18 44 38 46 36 18 25 64 11 27 64 9
96MK108 0.99 0.03 2 0.2 19 62 19 13 62 25 17 54 29 20 75 5 21 75 4
96MK111 0.96 0.08 3.4 0.5 40 0 60 67 7 26 13 0 87 24 73 3 26 73 1
96MK112 0.99 0.89 0.8 2 22 72 6 7 68 25 20 67 13 19 67 14 20 67 13
96MK114-1 0.97 0 4 0 2 97 0 0 98 2 3 97 0 6 33 61 6 33 61
96MK116-1 0.99 0.06 0.8 0 6 91 4 22 71 7 5 71 24 29 63 8 30 63 7
96MK117-1 0.99 0.04 0.8 0 32 68 0 15 60 25 27 58 15 30 60 10 32 60 8
96MK126 1 0.03 1.2 0.2 71 29 0 26 37 37 53 21 26 34 62 4 35 61 2
96MK133 0.89 0.11 8.6 0 18 82 0 9 75 16 16 75 9 29 28 43 33 28 39
96MK134 0.95 0.12 0.8 0 38 60 2 6 58 36 36 56 8 20 29 51 23 29 48
96MK135 0.98 0.08 3 0.13 16 83 1 11 75 14 14 74 12 29 48 23 21 48 21
96MK141 0.99 0.06 5.2 0 26 74 0 12 67 21 23 65 12 34 47 19 36 47 17
96MK142-1 0.99 0.04 2 0.2 35 65 0 11 60 29 31 58 11 30 59 11 31 59 10
96MK145 1 0.01 3.2 0 29 71 0 7 67 26 27 67 6 31 66 3 31 66 3
96MK147 0.92 0.04 3.2 0.61 82 9 9 45 20 35 45 5 50 43 53 4 45 53 2
96MK153 0.99 0.08 1.6 0.4 32 68 0 21 63 16 26 53 21 22 69 9 24 69 7
96MK154 0.92 0.25 0.6 0.4 25 72 3 34 52 14 17 47 36 25 50 25 34 51 15
8PL96 0.74 0.19 0.6 0 40 0 60 72 0 28 11 0 89 35 53 12 44 53 3
9PL96 0.94 0.07 8.8 0.004 0 0 100 69 0 31 0 0 100 53 41 6 57 41 2
10PL96 0.76 0.06 3.8 0.002 8 0 92 48 0 52 4 0 96 42 53 5 44 52 4
11PL96 0.67 0.54 1.6 0.4 11 87 2 54 40 6 5 40 55 23 29 48 49 29 22